SUMMARY OF SIGNIFICANT RESULTS IN- ?* Mineral resources Water resources engineering geology and hydrology Regional geology > ||j||§j Principles and processes Laboratory and field methods ‘ropographic surveys • and mapping Management, resources ^ on public lands * Investigations in other countries LISTS OF- Investigations in progress Reports published in fiscal year 1964 Cooperating agencies Geological Survey o GEOLOGICAL SURVEY RESEARCH 1964 4 Chapter A - -6 ^ a* & Sr // {- x 64?/ - /9~g earth SCIENCE^ Library OF 17 1964 SCIENCE THi 4 1 * * V % > 4' 4 * 1 f GEOLOGICAL SURVEY RESEARCH 1964 THOMAS B. NOLAN, Director GEOLOGICAL SURVEY PROFESSIONAL PAPER 501 Significant results of investigations for fiscal year 1964, accompanied by short papers in the fields of geology, hydrology, and related sciences. Published separately as Chapters A, B, C, and D UNITED STATES GOVERNMENT PRINTING OFFICE, WASHINGTON: 1964UNITED STATES DEPARTMENT OF THE INTERIOR STEWART L. UDALL, Secretary GEOLOGICAL SURVEY Thomas B. Nolan, DirectorGEOLOGICAL SURVEY RESEARCH 1964 GEOLOGICAL SURVEY PROFESSIONAL PAPER 501-A A summary of recent significant scientific and economic results, accompanied by a list of publications released in fiscal 1964, a list of geologic and hydrologic investigations in progress, and a report on the status of topographic mapping UNITED STATES GOVERNMENT PRINTING OFFICE, WASHINGTON: 1964 A 293UNITED STATES DEPARTMENT OF THE INTERIOR STEWART L. UDALL, Secretary GEOLOGICAL SURVEY Thomas B. Nolan, Director For sale by the Superintendent of Documents, U.S. Government Printing Office Washington, D.C., 20402 - Price $2.75Q£is ?(* v. sol • A-& earth SCIENCES LIBRARY FOREWORD Geological Survey Research 1964 is the fifth annual review of the economic and scientific work of the U.S. Geological Survey. As in previous years the purpose of the volume is to make available promptly to the public the highlights of Survey investigations. This year the volume consists of 4 chapters (A through D) of Professional Paper 501. Chapter A contains a summary of significant results, and the remaining chapters are made up of collections of short technical papers. Many of the results summarized in chapter A are discussed in greater detail in the short papers or in reports listed in “Publications in Fiscal Year 1964,” beginning on page A277. The tables of contents for chapters B through D are listed on pages A271-A275. Next year, the sixth year of publication of this series, Geological Survey Research 1965 will appear as chapters of Professional Paper 525. Numerous Federal, State, county, and municipal agencies listed on pages A221-A225 cooperated financially with the Geological Survey during fiscal 1964 and have contributed significantly to the results reported here. They are identified where appropriate in the short technical papers, but generally are not identified in the brief statements in chapter A. Many individuals on the staff of the Geological Survey have contributed to Geological Survey Research 1964. Reference is made to only a few. George H. Davis was responsible for organizing and assembling chapter A and for critical review of papers in chapters B-D. He was assisted by George Pliair, who was largely responsible for material from the Geologic Division. Marston S. Chase was in charge of production aspects of the series, assisted by Jesse R. Upperco in technical editing, and William H. Elliott in the planning and preparation of illustrations. Thomas B. Nolan, Director. mCONTENTS Foreword---------------------------------------------- Investigations of natural resources___________________ Mineral resources________________________________ Resource compilation_________________________ Heavy metals_________________________________ Iron_____________________________________ Molybdenum_______________________________ Chromium_________________________________ Copper___________________________________ Lead and zinc____________________________ Tin.................._................... Manganese________________________________ Tungsten_________________________________ Mercury__________________________________ Laboratory studies of sulfide-ore minerals. _ Light metals and industrial minerals_________ Phosphate________________________________ Beryllium________________________________ Fluorspar________________________________ Bauxite and clay_________________________ Zeolites_________________________________ Evaporites and brines____________________ Other light metals and industrial minerals.. Radioactive minerals_________________________ Uranium in sandstone_____________________ Uranium and thorium in crystalline rocks.. Minor elements_______________________________ Rare earths and niobium__________________ Selenium and tellurium___________________ Organic fuels________________________________ Coal_____________________________________ Petroleum and natural gas________________ Oil shale________________________________ Water resources__________________________________ Water use____________________________________ Atlantic coast area__________________________ New England______________________________ New York_________________________________ New Jersey_______________________________ Pennsylvania_______________________^_____ Maryland_________________________________ West Virginia____________________________ North Carolina___________________________ Georgia__________________________________ Florida__________________________________ Puerto Rico______________________________ Virgin Islands___________________________ Midcontinent area____________________________ Minnesota________________________________ Investigations of natural resources—Continued Water resources—Continued Midcontinent area—Continued Page Wisconsin_________________________________ A30 Michigan___________________________________ 30 Ohio___________________________________ 31 Indiana____________________________________ 31 Iowa_______________________________________ 31 Missouri___________________________________ 32 Kentucky___________________________________ 32 Tennessee__________________________________ 32 Alabama____________________________________ 33 Mississippi________________________________ 33 Louisiana__________________________________ 33 Interstate investigations__________________ 34 Rocky Mountain area____________________________ 35 Montana____________________________________ 35 North Dakota_______________________________ 35 Wyoming____________________________________ 36 South Dakota_______________________________ 36 Nebraska___________________________________ 37 Utah.................................... 38 Colorado___________________________________ 38 Kansas_____________________________________ 39 Arizona____________________________________ 39 New Mexico_________________________________ 40 Oklahoma_________________________________ 41 Texas------------------------------------ 42 Colorado River basin_______________________ 42 Pacific coast area_____________________________ 43 Alaska_____________________________________ 43 Pacific Northwest__________________________ 44 Nevada_____________________________________ 45 California_________________________________ 46 Hawaii_____________________________________ 47 Saline water resources_________________________ 48 Management of natural resources on the public land. 49 Classification of mineral lands---------------- 49 Waterpower classification---------------------- 49 Supervision of prospecting, development, and recovery of minerals___________________ 50 Geology and hydrology applied to engineering and public health_________________________________ 51 Investigations related to nuclear energy____________ 51 Nevada Test Site studies_______________________ 51 plowshare Program______________________________ 53 vela uniform Program___________________________ 55 Disposal of radioactive wastes_________________ 55 Movement of radioactivity in streams____ 55 Disposal of wastes to the ground___________ 57 Sites for nuclear powerplants------------------ 57 Page III A1 1 1 3 3 3 3 3 4 4 5 5 5 5 6 6 8 10 11 12 12 13 13 13 15 15 15 15 15 15 16 17 19 19 21 21 22 23 24 25 26 26 26 27 28 29 29 30 vVI CONTENTS Geology and hydrology, etc.—Continued Water contamination studies______________________ Detergents and pesticides in water supplies__ Acid mine waters_____________________________ Industrial wastes____________________________ Oil-field brines________:____________________ Salt-water contamination_____________________ Distribution of minor elements as related to public health_______________________________ Engineering geology______________________________ Engineering hydrology---------------------------- Land subsidence------------------------------ Evaporation suppression______________________ Floods_______________________________________ Outstanding floods of 1963-64____________ Flood frequency__________________________ Flood mapping____________________________ Alaskan earthquake_______________________________ Regional geology______________________________________ Maps of large regions____________________________ Coastal plains___________________________________ Atlantic Coastal Plain__:-------------------- Gulf Coastal Plain and Mississippi Embay ment. New England and eastern New York_________________ Maine________________________________________ Massachusetts________________________________ Rhode Island_________________________________ Connecticut__________________________________ Adirondack Mountains_________________________ Appalachian region_______________________________ Stratigraphic studies________________________ Geophysical studies__________________________ Geochemical exploration______________________ Geochronological studies_____________________ Quaternary geology___________________________ Eastern Plateaus_______-___________-_____________ Pennsylvania_________________________________ Kentucky_____________________________________ Shield area and Upper Mississippi Valley_________ Michigan_____________________________________ Iowa_________________________________________ Wisconsin____________________________________ Illinois_______________________*.____________ Minnesota.___________________________________ Interior Highlands and eastern plains____________ Arkansas_____________________________________ Missouri_____________________________________ Texas________________________________________ New Mexico___________________________________ Northern Rocky Mountains and plains______________ Northeastern Washington______________________ Idaho________________________________________ Wyoming______________________________________ Montana______________________________________ North Dakota and South Dakota________________ Southern Rocky Mountains and plains______________ Geology of Precambrian rocks of Colorado_____ Stratigraphic and paleontologic studies______ Geology of volcanic and hypabyssal intrusive rocks________________________________ Quaternary geology___________________________ Geophysical investigations___________________ Colorado Plateau_________________________________ Geophysical studies__________________________ Geological studies___________________________ Regional geology—Continued page Basin and Range region____________________________ A101 Stratigraphy and structural geology___________ 101 Nevada and eastern California____________ 101 Western Arizona and southeastern California______________________________________ 103 Eastern Nevada and Utah_____________________ 104 Eastern Arizona, New Mexico, and western Texas___________________________________ 106 Cenozoic volcanism_____________________________ 106 Cenozoic stratigraphy_________________________ 107 Geochemical exploration__________________________ 108 Columbia Plateau and Snake River Plain_______________ 108 Pacific coast region_________________________________ 110 Washington_______________________________________ 110 Oregon___________________________________________ 111 Coast Ranges and Klamath Mountains of northern California and southern Oregon___________ 111 Southern Cascade Range and Sierra Nevada of California______________________________ 113 Central and southwestern California______________ 114 Alaska_______________________________________________ 115 Northern Alaska__________________________________ 115 West-central Alaska______________________________ 116 Southwestern Alaska______________________________ 117 East-central Alaska______________________________ 117 Southern Alaska__________________________________ 118 Southeastern Alaska______________________________ 119 Puerto Rico__________________________________________ 120 Antarctica___________________________________________ 120 Geologic and hydrologic investigations in other countries. 123 Afghanistan__________________________________________ 123 Brazil_______________________________________________ 123 Chile_______________________________________________ 126 Colombia_____________________________________________ 126 Costa Rica___________________________________________ 126 Indonesia____________________________________________ 127 Korea________________________________________________ 127 Libya________________________________________________ 127 Pakistan____________________________________________ 127 Peru_________________________________________________ 129 Saudi Arabia_________________________________________ 129 Thailand____________________________________________ 129 Investigations of principles and processes---------------- 131 Paleontology_________________________________________ 131 Classic area_____________________________________ 131 Biostratigraphy__________________________________ 133 Evolution________________________________________ 135 Biologic oceanography and paleoecology___________ 137 Marine geology and hydrology_________________________ 138 Atlantic continental shelf and slope_____________ 138 Geologic studies on Guam_________________________ 140 Estuary study in Maryland________________________ 140 Astrogeologic studies-------------------------------- 140 Lunar geologic mapping___________________________ 140 Terrestrial and experimental impact and cratering phenomena___________________________________ 142 Terrestrial craters and structures_______________ 142 Extraterrestrial materials_______________________ 144 Geochemistry and petrography of tektites.. 144 Magnetic susceptibility and electrical resistivity of tektites__________________________ 146 Space-flight studies_____________________________ 147 Page A 57 58 58 59 59 60 61 61 63 63 65 65 65 68 69 69 71 72 73 73 74 75 76 77 79 80 81 81 81 83 84 84 84 84 84 84 86 86 87 87 87 87 88 88 88 88 89 89 89 89 91 92 93 94 94 95 96 98 98 99 99 100CONTENTS VII Page Investigations of principles and processes—Continued Geophysical investigations________________________ A149 Studies of the crust and upper mantle___________ 149 Theoretical and experimental geophysics_________ 151 Solid-state studies_____________________________ 153 Geochemistry, mineralogy, and petrology______________ 154 Field studies in petrology and geochemistry__ 154 Mineralogic studies and crystal chemistry____ 156 Experimental geochemistry_______________________ 159 Geochemical data________________________________ 162 Geochemistry of water___________________________ 163 Studies of atmospheric precipitation________ 164 Studies of springs, streams, and lakes___ 164 Ground-water studies______________________ 164 Chemical equilibrium studies________________ 165 Isotopic studies in hydrology_______________ 166 Investigations at the Hawaiian Volcano Observatory. 166 Isotopic and nuclear studies__________________,___ 167 Geochronology___________________________________ 168 Light stable isot opes_________________________ 170 Natural radioactive disequilibrium studies___ 170 Isotopic tracer studies_________________________ 171 Isotopic studies of crustal evolution___________ 172 Hydraulic and hydrologic studies_____________________ 173 Surface water___________________________________ 173 Ground water____________________________________ 176 Ground-water-surface-water relations____________ 179 Soil moisture and evapotranspiration_____________181 Sedimentation________________________________________ 183 Erosion_________________________________________ 184 Transportation__________________________________ 184 Variability of sediment loads in river___ 185 Deposition______________________________________ 186 Limnology____________________________________________ 188 Geomorphology________________________________________ 191 Plant ecology________________________________________ 191 Glaciology___________________________________________ 193 Permafrost___________________________________________ 194 Page Laboratory and field methods_____________________________ A195 Analytical chemistry_________________________________ 195 Optical spectroscopy_________________________________ 197 X-ray fluorescence analysis___________________... 198 Electron microprobe studies_________________________ 199 Petrographic techniques______________________________ 199 Geochemical and geobotanical exploration........... 200 Analysis of water__________________________________ 201 Hydrologic measurements and instrumentation.----- 202 Topographic surveys and mapping .... —............ 207 Mapping accomplishments______________________________ 207 Mapping in Antarctica________________________________ 215 Research and development_____________________________ 215 Field surveys_________________________________ 217 Photogrammetry___________________________________ 217 Cartography______________________________________ 219 Cooperating agencies for fiscal year 1964-------------- 221 Federal agencies_____________________________________ 221 State, county, and municipal agencies---------------- 221 U.S. Geological Survey offices____________________________ 227 Main centers______________________________________ 227 Public inquiries offices_____________________________ 227 Selected field offices in the United States and Puerto Rico_______________________________________________ 227 Conservation Division____________________________ 227 Geologic Division________________________________ 228 Topographic Division_____________________________ 229 Water Resources Division______________________( 229 Offices in other countries___________________________ 231 Geologic Division________________________________ 231 Water Resources Division_________________________ 232 Investigations in progress in the Geologic, Water Resources, and Conservation Divisions.. 233 How to order U.S. Geological Survey publications_______ 269 Contents of Geological Survey Research 1964, Chapters B, C, and D__________________________ 271 Publications in fiscal year 1964__________________________ 277 List of publications________________________________ 277 Index to list of publications________________________ 331 Index_____________________________________________________ 357 ILLUSTRATIONS Figure 1. Sketch of the exhibit on mineral resources and the Nation’s growth being shown in the Federal Pavilion at the New Page York World’s Fair________________________________________________________________________________________________________ A2 2. Geologic map showing location of beryllium deposits mapped at Spor Mountain, Utah_________________________ 9 3. Index map of the United States, showing areal subdivisions used in discussion of water resources_________________ 20 4. Percentage of total United States mineral production that comes from Federal land________________________________ 49 5. Index map of the conterminous United States, showing boundaries of regions referred to in discussion of regional geology-------•------------------------------------------------------------................................ 71 6. Index map of Alaska, showing boundaries of regions referred to in discussion of Alaskan geology_________________ 115 7. Index map of Antarctica_________________________________________________________________________________________ 121 8. Progress of 7K- and 15-minute quadrangle mapping._______________________________________________________________ 208 9. Status of 7%- and 15-minute quadrangle mapping______________________________________________________________ 210 10. Status of revision of large-scale mapping___________________________________________________________________ 211 11. Status of 1:250,000-scale mapping_____________________________________________________________________________ 212 12. Status of State maps____________________________________________________________________________________________ 213 13. Status of 1:1,000,000-scale topographic mapping------------------------------------------------------------- 214 14. Index map of Antarctica, showing status of topographic mapping by the U.S. Geological Survey, as of June 30, 1964........................................................................................................ 216GEOLOGICAL SURVEY RESEARCH 1964 INVESTIGATIONS OF NATURAL RESOURCES The Act of Congress that created the U.S. Geological Survey in 1879 charged its Director with the “classification of the public lands,” and with the “examination of the geological structure, mineral resources and products of the national domain.” Over the years the Survey’s program has evolved to meet the Nation’s changing needs, but the objectives spelled out in the organic act remain its cardinal guidelines. This volume, the fifth in the series of annual summaries, presents the more significant results of the many separate investigations underway in 1964. A broad outline of the Survey’s future plans, entitled “Long Range Plan For Resource Surveys, Investigations, and Research Programs of the United States Geological Survey,” was published during the present calendar year and is available without charge from the Geological Survey, Washington, D.C. 20242. MINERAL RESOURCES Growth in population and rise in level of living are steadily accelerating our consumption of minerals, fuels, and water, and are creating enormous future demands for these key resources. This problem is highlighted as a part of the “Challenge to Greatness” theme carried by the Federal Pavilion at the New York World’s Fair in an exhibit, reproduced in figure 1. The exhibit makes the points that minerals, fuels, and water are the essence of our industrial society; that increased per capita consumption of them is the physical basis for rise in level of living; that the needs of the present population are far larger than known supplies; and, most important, that future needs can be met provided we undertake the driving and imaginative research necessary to find and develop new supplies. This means acquiring better prospecting tools and methods, better knowledge of the origin, habits, and distribution of mineral deposits, better understanding of the three-dimensional geology of our real estate, and better knowledge of the extent and distribution of minerals that, are presently too costly to use but that may come within economic reach as technology advances. Results of Survey investigations that bear directly on mineral-resource studies are summarized in the following pages. Nearly all the Survey’s investigations help advance knowledge in these areas, but only those results that are directly concerned with mineral resources are described in this section. RESOURCE COMPILATION Resources of Utah, Alaska, and South Dakota Current knowledge of the economic mineral and water resources of Utah, Alaska, and South Dakota has been summarized in three reports prepared jointly by the Geological Survey and State agencies. In addition to describing known mineral deposits, the reports synthesize much recent work bearing on areas favorable for further prospecting. For example, in Utah (U.S. Geological Survey, 9-64),* 1 three beltlike areas contain most of the known hydrothermal deposits in the State from which all of the molybdenum, mercury, and hal-loysite, and 95 percent of the copper, lead, silver, gold, and zinc have been produced, as well as most of the manganese, tungsten, barite, fluorite, native sulfur, minor metals, and significant amounts of uranium, alunite, and gem materials. In addition, major potential resources of beryllium have been identified. (See also “Water Resources, . . . Utah.”) In Alaska (U.S. Geological Survey, 8-64), geologic structures are compared with the Cascade-Sierra cordillera, the Columbia and Colorado Plateaus, and the Rocky Mountains of the western conterminous States to point out the similarities in mineral resources and to suggest favorable areas for exploration. (See also “Water Resources, . . . Alaska”.) In South Dakota2 the distribution of pegmatites in the Black Hills is spatially related to the Harney Peak Granite, but of approximately 20,000 pegmatites only 200 are of the zoned type that have been mined for different minerals. Of these minable pegmatites, those worked for sheet mica tend to be near the granite, while those worked for scrap mica, beryl, and lithium '•See “List of Publications” (p. A277). This report Is the 9th citation for 1964 under entries for the U.S. Geological Survey and is listed on p. A324. 1 U.S. Geological Survey, 1964, Mineral and water resources of South Dakota : U.S. Cong., 8S,th, 2d sess., U.S. Senate Comm, on Interior and Insular Affairs Kept. [ In press] A1A2 INVESTIGATIONS OF NATURAL RESOURCES minerals tend to be farther from the granite, toward the margin of the pegmatite area. Favorable environments for metallic mineral deposits occur in the vicinity of Tertiary intrusive masses elsewhere in the Black Hills. (See also “Water Resources, . . . South Dakota.”) Mineral potential of the northern Cascade Mountains, Wash. Deposits of gold and copper, and of lead, zinc, and silver in the nothern Cascade Mountains of Washington are much more closely related spatially to granitic rocks of late Tertiary age than to older granites, according to a study by A. E. Weissenborn and F. W. Cater for the North Cascades Study Team, representing the U.S. De- partments of Agriculture and Interior and the State of Washington. Ultramafic rocks in and near the Twin Sisters Mountains are an important source of olivine and contain small deposits of chromite. Weathering of the ultramafic rocks before and during early Tertiary time formed residual deposits of nickeliferous iron ore containing a little cobalt. The area is favorable for both copper and gold deposits, although the chances of finding a large mining district seem poor. The likelihood of discovery of new gold deposits would be good under more favorable economic conditions, and the byproduct output of gold should be expected from any new copper mines. Figure 1.—Sketch of the exhibit on mineral resources and the Nation’s growth being shown in the Federal Pavilion at the New York World’s Fair as a part of its “Challenge to Greatness” theme. The exhibit provides a continuous tally of the Nation’s population and its consumption of key commodities, and shows on the one hand how growth in population and per capita consumption increase the demand for minerals, and on the other, how mineral consumption supports economic growth.MINERAL RESOURCES A3 HEAVY METALS IRON Marquette district, Michigan Working from geologic maps prepared by the Cleveland Cliffs Iron Co., J. E. Gair has studied the hard iron ores in the Cliffs Shaft mine at Ishpeming. He finds that concentrations of magnetite commonly occur adjacent to mafic intrusive rock, now altered to greenstone, in nominally hematitic ores, and in both hematitic and sideritic iron-formation. Minor veinlets of sulfides in iron-formation and ore also occur most commonly near contacts of altered mafic intrusive bodies. Cuyuna North Range, Minnesota In a comprehensive report on the iron and manga-niferous iron ores of the Cuyuna North Range, R. G. Schmidt (1-63) attributes the enrichment of the original iron-formation to two ore-forming stages. During the first stage, ground water heated by the admixture of magmatic emanations produced red-brown largely hematitic ore bodies, enriched in boron, that are spatially related to fracture zones and intrusions. All the largest deposits in the district include or consist entirely of ore of this type. The second stage of enrichment occurred during a period of very deep weathering when brown, largely goethitic ores formed as irregular blankets over exposures of iron-formation and on almost all the residual masses of unoxidized iron-formation that remained within the hematitic deposits. Porous hematitic ores that extended downward for several hundred feet served as channelways for the weathering solutions, so that brown ore formed to considerable depths. Some of the large ore bodies originated in this two-stage manner. Magnetic anomaly in southeastern Minnesota Isidore Zietz (1-64) found by aeromagnetic methods a high-amplitude anomaly in southeastern Minnesota that from its shape and size suggested the presence of Precambrian iron-formation in the basement, here over-lain by flat-lying lower Paleozoic sedimentary rocks estimated to be 500 to 1,000 feet thick. Subsequently the New Jersey Zinc Co. revealed (written communication) that it had previously discovered this anomaly in 1961, and that a drill hole had entered diabasic-textured gabbroic rock containing concentrations of iron and titanium oxides at a depth of 724 feet. MOLYBDENUM White River Badlands, S. Dak. R. U. King has studied molybdenum deposits of a previously unknown type found recently in the White River Badlands of South Dakota. A yellow molybdenum oxide, probably ferrimolybdite, cements lenses of sandstone, conglomerate, and claystone in the basal unit of the Chadron Formation, of Oligocene age, just above its contact with the underlying Pierre Shale. Individual deposits are as much as 100 feet long and 8 feet thick in outcrop; insufficient exploration has been done to delimit the third dimension. A small part of the material contains several percent of molybdenum, but the average grade is probably only a few tenths of 1 percent. CHROMIUM Stratiform and podiform chromite deposits contrasted E. D. Jackson and T. P. Thayer conclude that (1) sedimentary principles govern occurrences of the stratiform chromite deposits such as those in the Stillwater complex, Montana, and (2) metamorphic principles apply to the podiform deposits associated with alpine-type peridotites as, for example, along the Pacific coast of the United States. Field examination by Jackson and Thayer of the Vourinos complex in Greece during the Seminar of Chromite Prospecting sponsored by the Organization for Economic Cooperation and Development and held in Athens in 1963 showed that this igneous body, considered to be a typical ophiolite flow, has many features of alpine complexes as described by Thayer (2-63) together with podiform chromite deposits. Similarly, examination of chromite deposits in the Hindubagh district of Pakistan by Roger van Vloten and T. W. Offield, in three important districts of Turkey by Thayer, and in the Philippines by D. L. Rossman shows that layering, foliation, and linea-tion have been generally neglected and misunderstood as possible guides in exploration and mining of podiform deposits. Relict structures, mostly in chromite, show that the peridotite and gabbro in alpine complexes formed by fractional crystallization as in the stratiform complexes, and that the flowage features were imposed during reemplacement as crystal mushes. COPPER Arizona Alteration associated with copper deposits in Arizona was investigated with a truck-mounted gamma-ray spectrometer by R. M. Moxham, C. A. Anderson, and C. M. Bunker, of the Geological Survey, in cooperation with R. S. Foote, of Texas Instruments, Inc. Earlier work by Anderson and coworkers showed that potassium was added to the host rocks by hydrothermal alteration at the porphyry copper deposit at Bagdad and the massive sulfides at the Jerome, Iron King, and Old Dick mines. The present studies show that the potassic alteration extends a substantial distance fromA4 INVESTIGATIONS OF NATURAL RESOURCES the locus of mineralization and can be detected by the spectrometric method. At the Bagdad deposit an abnormal amount of uranium (as much as 65 parts per million) is associated with the mineralized zone. As a check on the method, the field measurements were compared with results of chemical analyses for one or more of the radioactive elements, K, U, Th, obtained on over 50 samples collected at the outcrops. Chewelah No. 1 quadrangle, Stevens County, Wash. A moderately dipping thrust fault with several miles of displacement is an important structural feature in the Chewelah No. 1 quadrangle, Stevens County. Studies by L. D. Clark and F. K. Miller have indicated that the upper plate of the thrust, composed largely of Precambrian argillite and quartzite, possibly acted as a low-permeability cover or “lid” that aided in concentrating copper deposits in the rocks of the lower plate. If so, exploration of the lower plate rocks beneath weakly mineralized areas of the upper plate might be warranted. To date, copper has been produced only from an area where the upper plate rocks have been removed by erosion. Springfield mine, Yellow Pine quadrangle, Idaho A new interpretation of the structure of the bedrock ore body below minable colluvium at the Springfield mine in Valley County has economic implications. This scheelite-pyrrhotite deposit, originally described and mapped by H. B. Nickelson (unpublished data), is a high-temperature replacement of garnet-pyroxene skarn developed from carbonate rocks included within the alaskatic facies of the Idaho batholith near the Little Pestol dike swarm. Recent studies of B. F. Leonard suggest that the deposit may be a warped lathlike shoot on the crest of a small anticline trending about N. 5° E. and plunging 30°-35° NNE. In other terranes, some ore bodies on the noses of plunging folds extend to considerable depths. The metasedi-mentary rocks in the area are involved in three systems of folds; exposures are poor in the vicinity of the ore body. Previous drilling of the bedrock for tungsten had proved disappointing partly because its structure had been difficult to decipher. If the tungsten and copper content of this deposit should be of interest, the new hypothesis concerning the. shape and structural localization of the mineralized body might be tested by geophysical surveys. LEAD AND ZINC Thompson-Temperly mine, southwest Wisconsin Qualitative X-ray fluorescence analyses of selected samples of the basal shale of the Quimbys Mill Member of the Ordovician Platteville Formation show marked changes in the amounts of potassium, calcium, aluminum, silicon, magnesium, iron, manganese, and titanium outward from the ore body through the altered wall-rock halo into the unaltered shale. According to A. V. Heyl, all these elements except calcium are abundant in the ore body, and diminish to a minimum in the outer part of the alteration halo. Calcium, however, shows an inverse relationship. Mount Wilson quadrangle, San Miguel and Dolores Counties, Colo. C. S. Broomfield (1-63) has concluded that veins of base and precious metal ores are spatially, and probably genetically, related to the belt of intrusive rocks that extend westerly across the northern half of the quadrangle. The veins themselves seem in turn to be restricted within the intrustive belt to an east-west zone, no more than a mile or two in width, that crosses the quadrangle from the Ames-Matterhorn area on the east to the Silver Pick-Navajo Basin area on the west. The elongate vein zone closely approximates an imaginary axis that joins the centers of the major igneous masses. Most of the productive veins are along steep fissures that nearly parallel the postulated ore belt. A less prominent northeast, system of veins and fissures has been prospected, but only one such vein has yielded substantial production. Northwest-trending joints or fissures are prominent, but have not been found to contain commercial ore shoots. Santa Rita quadrangle, Grant County, N. Mex. Soil samples collected above epidotized mafic dikes of pre-ore age exposed along the crest of Hermosa Mountain in Grant County contain anomalous amounts of zinc. The zinc anomaly appears to be at or near the center of a conspicuous magnetic anomaly recently mapped by W. R. Jones, J. E. Case, and W. P. Pratt (1-64) and may be worthy of further study. TIN Lost River mine, Alaska Numerous data on the Lost River mine area collected by the Geological Survey, the Bureau of Mines, and the U.S. Tin Corp. with the financial assistance of the Defense Production Administration and Defense Minerals Exploration Administration have been assembled and evaluated by C. L. Sainsbury (1-64). Deposits of this area constitute the largest known IJ.S. tin resource and contain appreciable quantities of tungsten. Mineralization is associated with granite that intruded and marmarized limestone; the best ore is in a rhyolite porphyry dike that has been extensively greisenized and kaolinized. The surrounding area contains potentially valuable beryllium deposits.MINERAL RESOURCES A5 Black Mountain, Seward Peninsula, Alaska Reconnaissance of the biotite-granite pluton at Black Mountain, western Seward Peninsula, by C. L. Sains-bury has disclosed that the granite locally contains cas-siterite and wolframite in quartz-topaz veinleits similar to those in the other tin-bearing granites of the general area. Neither tin nor tungsten had been found previously at Black Mountain. Although the known vein-lets are small, cassiterite placers may exist in the streams flowing south from the granite pluton. Black Mountain apparently was not glaciated heavily during the Pleistocene, and placer deposits would not have been destroyed by glaciation as were those formed near the richer tin lodes of the Lost River area. MANGANESE Aguila mining district, Maricopa and Yuma Counties, Ariz. A brief reconnaissance of the Aguila mining district by F. S. Simons has shown that most of the manganese oxide deposits, the principal ore of the district, are in intermediate to silicic volcanic rocks of presumed Tertiary age, and none is very far from outcrops of such rocks. Deposits of copper and lead, all apparently small, are mainly in Precambrian metamorphic rocks; a few copper prospects are in granitoid rocks that may be younger than Precambrian, and one lead deposit is in volcanic rocks. Gold deposits appear to be confined to Precambrian terrane. These observations suggest that ore deposits of 2 and possibly 3 ages are present: Tertiary (Mn, some Pb), Precambrian (Au, Cu, some Pb?), and possibly an intermediate age (Laramide?) (some Cu?). Furthermore, the close spatial association of deposits of manganese oxides with volcanic rocks strongly suggests a genetic relation. Finally, such widely different ages of mineralization indicate that no simple zonal relations exist among deposits of the various metals. TUNGSTEN Hamme tungsten district, North Carolina and Virginia The geologic setting of the Hamme tungsten mine in Vance County, N.C., which is by far the largest deposit of this metal known in the Eastern United States, is described in a recent publication by J. M. Parker, 3d (1-63). Quartz-huebnerite veins containing minor quantities of fluorite and a few metallic sulfide minerals cut phyllite and albite granodiorite along a narrow belt 71/2 miles long near the western contact of the granodiorite mass. The metasedimentary rocks of the district, derived mainly from graywackes and volcanic flows and subordinately from pyroclastic materials, are part of the Carolina slate belt and lie along the east edge of the Virgilina synclinorium. They, together with the albite granodiorite, are considered as probably of Paleozoic age; the latter may have formed by metasomatic replacement rather than intrusion of magma. MERCURY Red Devil mine, central Kuskokwim region, Alaska E. M. MacKevett, Jr., and H. C. Berg (3-63) show by detailed maps and a block diagram the geologic setting and ore controls of the Red Devil quicksilver mine, in the central Kuskokwim region about 250 miles northwest of Anchorage. This mine was Alaska’s largest mercury producer until it shut down recently. Northeastward-trending altered basic dikes of Tertiary age in Cretaceous graywacke and argillite have been cut by numerous north westward-trending faults; the dike-fault intersections localized the deposition of cinnabar, stibnite, and other minerals from hydrothermal solutions in later Tertiary time. Although individual deposits are not large, numerous ore shoots, some of exceptionally high grade, have been found in an area at least 600 feet wide, 1,500 feet long, and 600 feet deep. LABORATORY STUDIES OF SULFIDE ORE MINERALS The sphalerite geothermometer Paul Barton and Priestly Toulmin (1-64) have investigated the system Fe-Zn-S above 580°C and found that the widely used sphalerite geothermometer requires modification. The iron content of sphalerite in the common assemblage, sphalerite-pyrite, depends on the fugacity of sulfur, and can only be used as a geothermometer when an independent measure of FS2 is available. Kullerud’s3 solvus curve for the binary system system FeS-ZnS is considerably in error. Effect of sulfur upon the inversion temperature of chalcocite In a continuing study of the system Cu-S, E. H. Rose-boom has demonstrated by means of X-ray diffraction studies at high temperature that the inversion temperature of 104±1° C of low-temperature orthorhombic chalcocite (Cu2S) to the high-temperature hexagonal polymorph is lowered to 93±2°C by the addition of 0.1 weight percent sulfur. The univariant reaction at 93°C with rising temperature is orthorhombic chalcocite + digenitefc?hexagonal chalcocite. The univariant reaction d j urleitefc?digenite + chalcocite was found to take place at approximately (±1°C) the same temperature, resulting in a minor ambiguity of the 8 G. Kullerud, 1953, The FeS-Zn-S system—a geologic thermometer: Norsk Geol. Tidsskr., v. 32, p. 61-147.A6 INVESTIGATIONS OF NATURAL RESOURCES phase relations which could not be resolved because of the hysteresis of the reactions. No sulfur-rich deviations from Cu2S could be detected at 180°C and 25°C, and, as hexagonal chalcocite is Cui.99S at 93°C, the sulfur content apparently changes rapidly and reversibly in the 90°-140°C region. Roseboom has also shown that synthetic djurleite and its metastable tetragonal polymorph both have compositions very near Cu!.96S with little or no variation. B. J. Skinner, in conjunction with F. R. Boyd and J. L. England of the Geophysical Laboratory, has demonstrated that Cu2S has a dense high-pressure polymorph which has an X-ray powder pattern identical to metastable tetragonal Cu^sS. This dense Cu2S may be quenched to 25 °C and 1 atm pressure where it slowly inverts to orthorhombic chalcocite. Stability relations in the system Cu-Ag-S B. J. Skinner has completed investigations of the ternary system Cu-Ag-S at 250°C and 500°C which supplement Djurle’s 4 data at 25°C. As all the ternary compounds lie along the join Ag2S-Cu2S, this binary was studied in detail, using conventional quenching techniques and high-temperature X-ray diffraction techniques. Stromeyerite (CuAgS) inverts at 92.3°C to a compound with the hexagonal high-chalcocite structure. The phase Cu0.8Ag1.2S inverts at 94.5°C to a mixture of hexagonal high chalcocite plus C1io.45Agi.55S (jalpaite) wThich inverts at 117°C to a body-centered cubic argentite-type structure. At higher temperatures extensive solid solutions of the hexagonal chalcocite type, body-centered cubic argentite type, and face-centered cubic digenite type all exist. Above 600°C complete solid solution of Cu2S-Ag2S exists with a face-centered cubic structure. None of the higher temperature phases can lie quenched. LIGHT METALS AND INDUSTRIAL MINERALS PHOSPHATE Northern Utah An examination of the lower half of Permian rocks at Dry Bread Hollow, Weber County, by E. M. Schell and W. C. Gere (1-64) has revealed phosphate deposits totaling at least 46 feet of medium-grade (24 percent or more P205) and 82 feet of low grade (18 percent or more P205) rocks. This is the thickest zone of phosphate uncovered in the State, and its discovery will add substantially to the known reserves of phosphate in Utah. Trenching and sampling showed about 28 million short tons of phosphate rock in a 1-square-mile area alone. The upper part of the Permian rocks in- 4 S. Djurle, 1958, An X-ray study on the system Ag-Cu-S : Acta Chem. Scand., v. 12, p. 1427-1436. eludes the Retort Phosphatic Shale Member of the Phosphoria Formation and the Ervay Carbonate Member of the Park City Formation, the first recognition of these units in this part of Utah. Southeastern Idaho Estimates of tonnage of phosphate rock in the Stewart Flat TV^-minute quadrangle in the Peale Mountains, Caribou County, indicate that reserves in this area are among the richest in the western phosphate field. Geologic investigations by T. M. Cheney and Iv. M. Montgomery show that stratigraphic zones of phosphate rock, which are in the Meade Peak Phosphatic Shale Member of the Phosphoria Formation (Permian), are here thicker and higher in grade than in nearby areas. In addition, structures favorable to strip mining are more extensive than previously mapped. A zone at the bottom of the phosphatic shale member in the SW1/^ sec. 33, T. 8 S., R. 45 E., is more than 14 feet thick and contains more than 31 percent P205. Estimates of reserves of phosphate rock in the Stewart Flat quadrangle are: Millions of short tons according to grade (percent'P2O5) >S1 >21 >18 Beneath less than 500 feet overburden_________________________________ 270 790 930 Above entry level, 6,800 feet elevation...________________________________ 320 930 1, 120 Total in ground______________________ 2,030 6,250 7,350 Phosphate, uranium, and fluorine in southwestern Montana Completion of stratigraphic studies of Permian rocks in southwestern and west-central Montana has included estimation by R. W. Swanson of phosphate, uranium, and fluorine resources in the Meade Peak and Retort Phosphatic Shale Members of the Phosphoria Formation. The 2 shale members are estimated to contain more than 11 billion tons of P205. Reserves of v arious categories, all of which occur in beds 3 feet or more thick are: Millions of short tons according to grade (percent P2O5) >S1 >24 >18 Above 100 feet below lowest entry level_______________________________ 130 560 1,450 Total in ground___________________ 1, 000 8, 000 25, 000 Uranium contained in phosphatic rock of the above categories is shown in the table below: Thousands oj short tons according to grade (percent P2O5) >81 >2k >18 Above 100 feet below lowest entry level________________________________ 13 41 93 Total in ground________________________ 100 500 1, 500MINERAL RESOURCES A7 Fluorine occurs in the phosphate mineral in the approximate ratio of 1:10 relative to P205; total fluorine resources in the 3 grades of phosphate rock estimated on the basis of this ratio are more than 35, 200, and 500 million tons, respectively. Phosphate and uranium in western Wyoming According to R. P. Sheldon (1-63) the Phosphoria Formation of western Wyoming contains large resources of phosphate rock and uranium, but these do not compare in quantity with those of some other areas of the western phosphate field, notably southeastern Idaho. Phosphate reserves in the Meade Peak and Retort Phos-phatic Shale Members of the Phosphoria Formation are shown in the following table (after Sheldon, 1-63, table 20) : Millions of short tons according to grade (percent P2O5) >S1 >ti >18 Above entry level . . . ... 300 1, 500 5, 500 Entry level to 1,000 feet below entry level. ..... 250 1, 000 3, 500 1,000-5,000 feet below entry level.. 850 3, 000 10, 000 Uranium contained in phosphatic rock of greater than 0.005 percent uranium content amounts to 400 thousand short tons above entry level, 200 thousand short tons from entry level to 1,000 feet below entry level, and 550 thousand short tons between 1,000-5,000 feet below entry level (Sheldon, 1-63, table 28). The Permian sedimentary rocks of western Wyoming were laid down in two cycles, each involving the deposition of clastic rocks first, followed by carbonate, chert, and finally phosphatic shale accompanying eastward transgression of marine waters across a shelf, and then deposition of these rocks in reverse sequence accompanying regression of the sea. The Meade Peak Phosphatic Shale Member represents the climax of the first transgression, and the Retort Phospatic Shale Member the climax of the second. Phosphate is believed to have been precipitated from deep marine waters that welled upward and across the shelf, were warmed, and lost C02. Miocene phosphorite, Beaufort County, N.C. An area at least 25 miles square straddling the Pamlico River in Beaufort County is underlain by phosphorite of probable early middle Miocene age, according to J. B. Cathcart (see also the section “Zeolites”). The phosphorite bed ranges in thickness between about 20 and 100 feet, but the amount of recoverable phosphate based on 10 widely spaced drill holes drilled under contract to the Geological Survey is nearly uniform throughout the area and is about 20,000 short tons per acre. Total tonnage of phosphorite is estimated to be of the order of magnitude of 9,000 million short tons. The average grade of the phosphate pellets concentrated from this rock will probably be 30 to 31 percent P205. The phosphate pellets range from 25 to 32 percent P205 and from 0.005 to 0.010 percent uranium. The uranium analyses are from 80 samples of phosphate concentrate. California Field reconnaissance studies and a search of the literature by H. D. Gower and B. M. Madsen (chapter D) 4a have revealed more than 60 separate occurrences of phosphate in California. Phosphate is distributed over a wide stratigraphic range but most commonly occurs in marine rocks of Miocene age. Most of the phosphate lies in the Coast Ranges. Localities that contain sufficient phosphate to warrant attention are the Monterey Formation in the Carmel Valley, Monterey Formation on the west side of the Salinas Valley, upper part of the Monterey Formation in the Indian Creek area on the north side of the La Panza Range, Santa Margarita Formation on the east side of the La Panza Range, lower Miocene rocks on the west side of the San Joaquin Valley, Santa Margarita Formation on the south side of the Cuyama Valley, upper Miocene rocks on the south side of Pine Mountain in northern Ventura County, lower part of the Monterey Formation in the Santa Barbara-Santa Maria area, and upper Miocene “nodular shale” of the western part of the Los Angeles Basin. The main phosphate zone at Indian Creek, about 35 feet thick, is composed of phosphate pellet beds in-terbedded with siliceous shale and bentonite. The pellet beds make up about 10 to 15 percent of the phosphatic zone. X-ray studies of marine phosphorites from 18 separate localities indicate that they all are composed of carbonate-fluorapatite. Central Appalachian region Preliminary studies by W. D. Carter of phosphate associated with the Oriskany Sandstone (Devonian) of the central Appalachian region show that phosphate occurs both as small, scattered concretionary masses at the top of the Oriskany and as nodular shales, cherts, and clays at the base of the overlying Marcellus, Need-more, and Romney Shales, and the Pottsville Formation. Generally, where one phosphate type occurs, the other is absent. In most places phosphate deposits are thin, discontinuous, and low grade, and not likely to be of economic interest, but four localities in Pennsylvania and West Virginia have phosphate which may be of sufficient grade to be economic in the future. Preliminary analyses indicate that some of these deposits contain more than 10 percent P205. In Fulton County, Pa., phosphatic shale 7 feet thick was found. See “Contents of Geological Survey Research 1964, Chapters B, C, and D” (p. A271). This report is listed in the contents for chapter D; however, the chapter is in press and no page numbers are available. 746-002 0-64-2A8 INVESTIGATIONS OF NATURAL RESOURCES Influence of latitude on phosphate deposition In an evaluation of the worldwide occurrence of phosphate deposits, R. P. Sheldon (p. C106-C113) 4b points out that Recent phosphorite occurs at warm latitudes, between the equator and the 40th parallels. Ancient phosphorites commonly lie at much higher latitudes. When the ancient phosphorites are located according to their virtual geomagnetic poles, their resulting paleo-latitudinal distribution closely matches the latitudinal distribution of young phosphorites. Also, the paleo-geographic settings of the ancient phosphorites match the geographic setting of the young phosphorites. Combined study of paleomagnetic and paleogeographic data thus will aid the search for ancient phosphorite. Geochemistry of the Phosphoria Formation R. A. Gulbrandson has calculated the average composition of the phosphorites in the Phosphoria Formation in the States of Idaho, Wyoming, Montana, and Utah with the following results: SiOa Weight percent 11.9 TiOa .1 A1202 1.7 F62O3 _ . 1.1 MgO - .3 CaO - 44.0 Na20 _ .6 Weight percent KjO_____________________ 0. 5 P205___________________ 30. 5 OO*_____________________ 2. 2 F_____________________ 3.1 SO,_____________________ 1. 8 HaO (total)___________ 2.2 Carbonaceous material- 2.1 The term “phosphorite” includes all rocks containing more than 50 percent apatite by weight. This average phosphorite composition is characteristic of marine phosphorites of the world, and as might be expected, the range of types of phosphorite in the Phosphoria includes most of those known in the world. The Phosphoria Formation is in effect a large composite phosphate deposit. The same study shows also that the composition of the apatite mineral in the phosphorites of the Phosphoria varies significantly, and that the approximate ranges of the major components in the mineral are as follows: Weight percent CaO____________________________________ 58. 4-55.3 NaaO___________________________________ .2- 1.2 P2Os___________________________________ 36. 5-40. 5 CO*______________________________________ . 8- 3. 5 SOa______________________________________ . 3- 3.1 F_______________________________________ 3. 8- 4. 2 These values are common ones for apatite and do not include the extremes known in the world. 4b See “Contents of Geological Survey Research 1964, Chapters B, C, and D” (p. A271). This report is listed in the contents for chapter C. BERYLLIUM Spor Mountain, Utah In writing of beryllium resources in Utah, W. R. Griffitts (in U.S. Geological Survey, 9-64) states that The discovery in 1960 of multi-million ton deposits at Spor Mountain, Juab County, and in 1962 near Gold Hill, Tooele County, has shown that Utah contains the world’s largest known beryllium deposits. As a result of the successful exploration of the Spor Mountain deposits, the beryllium industry is beginning a shift from the use of imported high-grade ore to the use of domestic low-grade ore. Such a shift will permit greatly expanded consumption of beryllium and will provide a stable domestic source of ore. Thus great changes in the structure of the industry and in the amount and diversity of use of the metal and its compounds can be expected soon, largely based upon Utah resources. Resources to support active mining are assured, as at least 15 million short tons of material averaging at least one-half percent BeO are available in the Spor Mountain and Gold Hill areas. The amount of beryllium in these deposits is about 75 times the present annual consumption of beryllium in the United States. Griffitts states also that the same districts probably contain a similar amount of material averaging 0.1 to 0.5 percent BeO. Enormous tonnages of rock averaging 0.01 to 0.1 percent BeO are present in the Sheeprock Mountains and Gold Hill area. A low-angle fault in western Juab County, Utah, described in the section “Eastern Nevada and Utah” under “Regional Geology, Basin and Range Region,” conceals tuff that probably is correlative with tuff that contains the large beryllium deposits at Spor Mountain, and may conceal additional deposits. The location of the Spct'r Mountain, Gold Hill, and Sheeprock areas is shown on figure 2, together with a geologic map of the beryllium deposits at Spor Mountain. Geology of the beryllium deposits at Spor Mountain has been described by Staatz and Griffitts5 and Staatz.6 Sheeprock Mountains and near Gold Hill, Utah Geology of the beryllium-bearing granite in the Sheeprock Mountains has been described by R. E. Cohenour.7 According to Griffitts (in U.S. Geological Survey, 9-64) a group of exceptionally large beryllium deposits was found by the Vanguard Research Co. in 5 M. H. Staatz and W. R. Griffitts, 1961, Beryllium-bearing tuff in the Thomas Range, Juab County, Utah : Econ. Geology, v. 56, p. 941-950. 6 M. H. Staatz, 1963, Geology of the beryllium deposits in the Thomas Range, Juab County, Utah ; U.S. Geol. Survey Bull. 1142-M, 36 p. 7 R. E. Cohenour, 1963, Beryllium and associated mineralization in the Sheeprock Mountains ; in Beryllium and uranium mineralization in western Juab County, Utah : Utah Geol. Soc. Guidebook to the geology of Utah, no. 17, p. 8-13.MINERAL RESOURCES A9 1962 in the Rodenliouse Wash area about 3 miles southeast of Gold Hill, Utah. In this area, near the center of a stock of quartz monzonite, beryllium-bearing veins are numerous in a belt about 2 miles long. Individual veins are tens of feet in thickness and hundreds of feet in length. The veins are a fine-grained mixture of quartz, calcite, adularia, and a beryllium mineral (apparently the silicate, bertrandite). The veins are in the northeast-trending fracture zone shown by Nolan.8 113° 15' 113“10' 0 1 2 MILES 1 i i i I_____________I EXPLANATION Volcanic rocks, largely covered with silt Limestone and dolomite r Gold Beryllium Hill Sheeprock deposit • Mountains O Spor Mountain Fluorspar UTAH deposit Fault Figure 2.—Geologic map showing location of beryllium deposits mapped by W. R. Griffitts at Spor Mountain, Utah. Index map shows location of Spor Mountain, Gold Hill, and Sheeprock Mountains. Lake George area, Colorado Beryllium-rich granites and associated pegmatites and greisens occur in scattered localities in central Colorado. Production from the Boomer mine in the 8 T. B. Nolan, 1935, The Gold Hill mining district, Utah: U.S. Geol. Survey Prof. Paper 177, 172 p. Lake George area is comparable with that of exceptionally large pegmatites in different parts of the world. New chemical data obtained by C. C. Hawley (1-64, 2-64) for the Lake George area, Front Range, show that, ideally, the beryllium-bearing greisens consist of inner berylliferous and aluminous zones encased in a nearly barren, relatively siliceous zone. The deposits contain ore bodies in the form of veins, pipes, and complex irregular masses, localized by fissures, rock contacts, and rock units of favorable composition or orientation. The main deposit, that at the Boomer mine, is a body of complex form localized by a combination of nearly vertical northeast-striking fissures, a low-angle north-striking set, and the southern contact of the so-called Boomer stock. Most of the other deposits are much simpler in form. -Mount Antero area, Colorado Continuing work in the Mount Antero area by W. N. Sharp seems to support the classical interpretation of geochemical concentration of beryllium in late-stage granitic residual liquids. Accumulations of beryllium in the Mount Antero leucogranite stock are virtually restricted to late derivatives of the magma, and these accumulations have collected mostly within a finegrained facies which forms a high lobe of the stock. Small aggregate clots of beryl in the fine-grained granite segregation contain practically all the concentrated beryllium. The aggregate clots have a texture like the surrounding granite, but the place of quartz is occupied instead by beryl. Throughout the Antero stock and its outliers, beryllium shows a general but limited dispersion in the rockforming minerals of the granite. The average beryllium content of the granite stock, exclusive of the aggregate clots of beryl, is somewhat higher (7-9 parts per million) than the average value commonly accepted for granite (5 ppm), but the actual range of values is wide, 4 to 20 ppm. The beryllium content of the stock as a whole clearly is higher than the consistent 2 to 3 ppm of the surrounding' quartz monzonite host rocks. Greisenized outliers to the main stock have sharp local variations in beryllium content. Generally, the beryllium content (3^ ppm) is below that of unaltered granita However, small topaz-greisen zones range from 20 ppm to about 2 percent beryllium. In addition, common small beryl-bearing veinlets pervade the greisenized granite. Sierra Cuchillo, N. Mex. The discovery in 1961 of beryllium in volcanic rocks in the Sierra Cuchillo, Socorro County, has recentlyA10 INVESTIGATIONS OF NATURAL RESOURCES been announced.9 The occurrence is about 5 miles north of the helvite deposits at Iron Mountain 10 in a north-striking fault zone in latite. From field and laboratory work by W. R. Griffith and D. R. Shawe, it has been ascertained that the grade of rock locally exceeds 1 percent BeO, and that the beryllium probably occurs as bertrandite in latite that has been brecciated, silicified, altered to clay minerals, and stained by iron and manganese oxides along the fault zone. The deposit lies about 10 miles northwest of a fluorspar-uranium deposit near Monticello, N. Mex., and is in an area of topaz-bearing rhyolite. The similarity to the geologic setting of the Spor Mountain deposits suggests the possibility that additional volcanic-associated deposits may be discovered in the region. Beryl in Swain County, N.C. R. A. Laurence, together with Tennessee Valley Authority geologists J. H. Davis, J. M. Fagan, and R. C. Hale, has examined a newly discovered pegmatite in Swain County. The pegmatite is too small to be of economic value, but it contains 2 or 3 percent beryl in large crystal aggregates, and its finding extends the Bryson City pegmatite district to the southwest by at least 2 miles. Previously, beryl has been reported only as a minor constituent in 4 of 36 pegmatite mines in the district. Beryllium associated with granite in Alaska According to C. L. Sainsbury (1-64), some of the beryllium deposits in the Lost River area of the western Seward Peninsula are localized by a combination of structural and petrologic elements of different ages. Areas especially favorable for ore occur where granite plutons of Late Cretaceous age pierce, or underlie at shallow depth, thrust faults of pre-Late Cretaceous age. Normal faults and dikes of acidic and mafic composition of postgranite age apparently have guided ore solutions into areas of fracturing created by thrust faults. Hence, intersections of thrust faults and granite are favorable places to seek undiscovered ore bodies. At the contact of the granite along Tin Creek, the beryllium mineral helvite [ (Mn, Fe, Zn)8(BeSi04)6S2] occurs in banded magnetite-fluorite “ribbon rock” similar to that at Iron Mountain, N. Mex. The beryllium-fluorite veins in which most of the beryllium is concentrated lie outside of the magnetite-fluorite rock, which suggests that similar relations may exist elsewhere. 9 M. H. Milligan, quoted in Engineering and Mining Journal, 1963, v. 164, no. 12, p. 154. 10 R. H. Jahns, 1944, Beryllium and tungsten deposits of the Iron Mountain district, Sierra and Socorro Counties, New Mexico : U.S. Geol. Survey Bull. 945-C, p. 45-79. Beryllium content of different volcanic rock types Spectrographic and chemical analyses of 1,172 saturated and over-saturated volcanic rocks compiled by Stanley Bemold and D. R. Shawe (1-64) indicate that beryllium content has a marked tendency to increase with silica content. The beryllium content of rocks containing more than about 76 percent silica, however, tends to decrease. Five hundred and eighty-one volcanic rocks that contain more than 70 percent silica comprise 3 different rock types—glasses, flow rocks, and tuffs—that show interesting variations from the average beryllium-silica relation. In volcanic glasses (198 rocks) and flow rocks (102 rocks), beryllium increases with silica to a maximum at about 75 percent silica, and drops noticeably in rocks with higher silica. On the other hand, in volcanic tuffs (281 rocks), beryllium increases with silica to the highest silica compositions. Moreover, the average beryllium content of the volcanic tuffs containing more than 70 percent silica (3.4 parts per million Be) is significantly lower than that of volcanic glasses (4.8 ppm) and flow rocks (4.4 ppm). These facts suggest fundamental differences in composition and genesis between tuffs and other volcanic rocks that may bear on the origin of beryllium deposits in volcanic and associated rocks, but have yet to be evaluated. FLUORSPAR Browns Canyon district, Colorado Fluorspar deposits of the Browns Canyon district, Chaffee County, have yielded about 130 thousand short tons of concentrates and contain large resources, according to R. E. Van Alstine. They occur chiefly as epithermal veins along steep northwest-trending normal faults in Tertiary volcanic rocks and Precambrian igneous and metamorphic rocks. One of the faults contains fluorspar almost continuously for about 2,600 feet. Maximum thickness of the fissure veins is about 40 feet, and the CaF2 content ranges from about 25 to 75 percent. The veins consist mainly of fine-grained fluorite and quartz. Measured and indicated fluorspar is estimated at 250 thousand short tons containing more than 35 percent CaF. and 150 thousand short tons containing 15 to 35 percent CaF2; an additional 650 thousand short tons of fluorspar in the above grade categories is inferred. More than 1 million short tons of fluorspar averaging about 20 percent CaF2 is estimated for the nearby Poncha district, Chaffee County. Fluorspar deposits in both districts are regarded as resources rather than reserves, as they are not currently being mined. L. C. Huff and Van Alstine collected soil samples (sieved to —80 mesh) at 50-foot intervals along 3MINERAL RESOURCES All traverses across a vein in the Browns Canyon district, and alluvium samples (sieved to —1 mm) upstream and downstream from the vein to test the use of fluorine as an indicator of fluorite. Forty-four analyses for fluorine were made by S. M. Berthold. Fluorine ranged from 1.5 to 5 percent in samples of soil over-lying and downslope from the vein. These values contrasted with as little as 0.06 percent in a sample 150 feet upslope from the vein and 0.08 percent in a sample 250 feet downslope from the vein. The average fluorine content of the earth’s crust has been estimated as 0.08 percent.11 The geochemical anomaly associated with the fluorspar vein represents a 6 to 14 fold increase over the average fluorine value for samples of residual soil overlying the wallrocks (Precambrian gneiss and quartzite and Tertiary rhyolitic welded tuff). A sample of alluvium 1,000 feet downstream from the vein has 3 times as much fluorine as one collected 300 feet upstream from the vein. Panning of 10-pound samples of this alluvium increases the fluorine concentration 6 to 8 times. Cave-in-Rock district, Illinois Work by D. M. Pinckney in the Cave-in-Rock fluorspar district, Hardin County, has shown that ore bodies occur in gently dipping favorable beds of limestone (Mississippian) beneath thin shaly layers. Joints in zones parallel or perpendicular to major faults permitted access of hydrothermal solutions to favorable beds at a few centers. Solutions spread from these centers, causing solution of the favorable and underlying beds, and in most places slumping or collapse of overlying beds, and deposition of ore in favorable beds. Many stages of deposition have been identified, both on the basis of successions of minerals and successions of zones within crystals. Minerals of the earlier stages are largely confined to the centers of mineralization or the channelways leading away from the centers. Minerals of the later stages either completely surround the zones of earlier minerals, or lie at new centers that became active during later stages of mineralization. BAUXITE AND CLAY Clay in eastern Washington and adjacent Idaho Clay studies in Spokane County, Wash., and in nearby Idaho by J. W. Hosterman show that five genetic types of clay are available locally for making clay products. They are (1) brown silty clay of the Palouse Formation, (2) varicolored clay of the Latah 11 V. M. Goldschmidt, 1958, Geochemistry : London, Oxford University Press, p. 74. Formation, (3) white residual clay derived from gran-odiorite and related rocks, (4) bluish-gray residual clay derived from Columbia River Basalt, and (5) gray clay from Pleistocene lake beds. The first three have been or are now used for making refractory products and structural bricks. Three areas containing white clay of the Latah Formation have been found that are not described in the literature. One of these is of potential economic importance, for it extends over at least 1 square mile and contains more than 35 percent A1203 over a 10-foot thickness in the discovery hole on the west border of sec. 17, T. 48 N., R. 5 W., Kootenai County, Idaho. Ilmenite is abundant in residual clays derived from basalt, and is a potential byproduct. Monazite is found in residual clay derived from granodiorite, but it has a low Th02 content. Clay in Maryland Information gathered recently in Maryland by M. M. Knechtel, in collaboration with the staff of the Norris (Tennessee) Research Laboratory of the U.S. Bureau of Mines, amplifies the results of reconnaissance studies which led to discovery of large deposits of bloatable clay and shale. Materials believed to be suitable for lightweight-aggregate production occur in sedimentary strata of two formations, the St. Mary’s Formation (Miocene) exposed in Calvert and St. Mary’s Counties, and the Martinsburg Shale (Ordovician) exposed in Washington County. The State’s first plant designed for manufacture of rotary kiln-fired lightweight aggregate will soon be in operation in Frederick County, at a site along State Route 550 approximately three-quarters of a mile southeast of Woodsboro. Tentative plans call for production to begin late in 1964 for shipment to Washington, D.C., Baltimore, Md., and other nearby localities. Ample supplies of bloatable shale, suitable for firing in rotary kilns, are available near the plant site in strata of the Frederick Limestone (Cambrian) which crop out along a northeasterly-trending synclinal trough. The only competitive lightweight product heretofore manufactured in Maryland has been expanded furnace slag, a byproduct of steel making at Sparrows Point, which has for many years been marketed for use as aggregate in the city of Baltimore and its immediate vicinity. Bauxite in Hawaii S. H. Patterson12 has found allophane and alumina-silica gel in weathered basalt associated with low-grade bauxite deposits on Maui, Hawaii. The chemical com- 12 S. H. Patterson, 1963, Halloysitic underclay deposits and occurrence of an alumina-silica gel and an allophane-like mineraloid in Hawaii [abs.] : 12th Natl. Clay Minerals Conf., Atlanta. Ga.A12 INVESTIGATIONS OF NATURAL RESOURCES position of the allophane is approximately 50 percent. A1203, 26 percent Si02, 1 percent Fe203, and 0.1 percent Ti02, and the loss on ignition is 25 percent. The alumina-silica gel is approximately 4.9 percent A1203, 2.2 percent Si02, and 0.3 percent Fe203, and the water loss with air drying is approximately 90 percent. After air drying, the composition of the gel is very similar to that of the allophane. The similar compositions of these two amorphous materials and their close relation in the field suggest the formation of allophane by dehydration of gel. The manner in which the allophane gel occurs is similar to that of mixtures of gibbsite and hollysite that are common in weathered rocks on Maui, and both types of amorphous materials are probably intermediate stages in the formation of these minerals. Attapulgite and fuller's earth in Georgia Mapping of the geologic structure of a limestone aquifer in the fuller’s earth clay-mining area in southwestern Georgia has shown that all existing mines in deposits of attapulgite and fuller’s earth are near the axis of a southwest-plunging structural trough (Sever, p. B116-B118). The clay was deposited in a basin localized either by continued downwarping or by compaction of the underlying unconsolidated deposits in the deeper part of the trough. Recognition of this relation and delineation of the structural trough should aid in prospecting for other economically valuable deposits of this clay. ZEOLITES Western Mojave Desert, Calif. In recent years there has been accelerated interest in natural zeolites for industrial use. Industry now uses synthetic zeolites almost exclusively, but as economic methods are developed to convert natural material into a commercial product, large natural deposits may become important. Study by R. A. Sheppard and A. J. Gude, 3d (p. C114—C116) of tuffaceous rocks of Tertiary age from the western Mojave Desert and vicinity, southern California, has shown widespread zeolitization there. Vit-ric material in the tuffaceous rocks generally altered partly or wholly to zeolites, clay minerals, silica minerals, and (or) potash feldspar. The most abundant zeolite is clinoptilolite, but some beds are rich in anal-cime, erionite, and phillipsite. Mordenite is a minor constituent of some beds. Potentially economic deposits of clinoptilolite, analcime, and erionite have been located. Atlantic Coastal Plain X-ray diffractometer studies of the slime fraction (— 200 mesh) of samples of the phosphorite unit (Mio- cene) in Beaufort County, N.C., by Theodore Botinelly showed a zeolite mineral (probably clinoptilolite), cris-tobalite, and an amorphous material (probably glass). The minerals indicate the presence of altered volcanic ash. The samples were collected and prepared by J. B. Cathcart from cores of 2 drill holes about 20 miles apart. The minerals were not present in samples of the underlying Castle Hayne Limestone (Eocene), nor in a sample of the overlying Yorktown Formation (Miocene) . This is the first known occurrence of zeolite in the Tertiary sediment of the Atlantic Coastal Plain. EVAPORITES AND BRINES Searles Lake, southern California Geologic and petrographic investigations of the Searles Lake evaporite deposit (Quaternary), San Bernardino County, by G. I. Smith and D. V. Haines has shown many systematic differences among the assemblages of evaporite minerals that are related to their stratigraphic distribution. Some of the 25 evaporite minerals at Searles Lake formed as primary deposits on the bottoms of lakes, but most formed after burial when the primary suite recrystallized into larger crystals of the same or different species. A systematic habit variation among some of the recrystallized species suggests that, although their postburial growth reflects the lower free energy of larger crystals, their differences in crystal form also reflect kinetic factors controlled by differences in the physical and chemical environment extent at the time they grew. In spite of extensive recrystallization, the present mineralogy of the deposit is close to that of the primary deposit, and this permits an approximation of the composition, salinity, and prevailing temperatures in the several lakes responsible for the deposits. A theoretical study by H. P. Eugster and Smith of the Searles Lake brines is summarized in the section “Experimental Geochemistry.” Geothermal brines near Niland, Calif. Near Niland, Imperial County, at the southeast end of the Salton Sea, geothermal brines pumped from deep drill holes13 are being investigated by private companies as possible sources of geothermal energy and chemicals. Subsurface temperatures are in the order of 300°C. Some brines contain nearly 30 percent of dissolved matter, of which about 7 percent is potassium. (See also sections “Isotopic Tracer Studies,” “Field Studies in Petrology and Geochemistry,” and “Saline Water Resources.”) 18 D. E. White, E. T. Anderson, and D. K. Grubbs, 1963, Geothermal brine well; mile-deep drill hole may tap ore-bearing magmatic water and rocks undergoing metamorphism : Science, v. 139, p. 919-922.MINERAL RESOURCES A13 Borate in Nevada In a review of data on borate deposits in Nevada, W. C. Smith points out that Nevada deposits were the chief source of borate in the United States during the period 1872-92. Some borate was produced in 1921-28 and in 1939, but in other years the Nevada producers were unable to compete with large producers in California. The largest reserves of borate known in Nevada are in deposits of colemanite at White Basin and at Calleville Wash, Clark County. Their reserves are estimated to be about 2 million short tons. The borate marshes that produced most of the early-day borax, including those of Mineral and Esmeralda Counties, contain only thin surficial deposits that seem unworkable in the foreseeable future. Bromine in evaporites of Utah and Colorado X-ray fluorescence analyses of the marine saline rocks of the Paradox Basin by O. B. Raup show that the bromine content ranges from 0.008 to 2.0 percent by weight. Salinity gradients contoured by bromine distribution make it possible to outline in detail the configuration of the evaporite basin during each evaporite cycle, thereby aiding in the location of potentially commercial potash deposits. OTHER LIGHT METALS AND INDUSTRIAL MATERIALS Lithium in Utah The lithium content of bedded rhyolitic tuff is unusually high at the Roadside beryllium deposit, Spor Mountain, Juab County, according to D. R. Shawe, Wayne Mountjoy, and Walter Duke (p. C86-C87). Li20 averages 0.22 percent in 18 representative samples. It is probably present chiefly in montmorillonite. Though perhaps not economic by itself, the lithium may well be a byproduct if the deposit is worked for beryllium. Barium in southwestern Arkansas D. A. Brobst has applied a relatively simple turbidi-1' metric field chemical test developed by Ward and others14 to geochemical prospecting for barite in the Caddo Gap and DeQueen quadrangles. Bedded barite deposits in the Stanley Shale (Mississippian) proved to have barium halos that display a gradual outward decrease in barium and generally extend less than 150 feet in stratigraphic thickness above and below the ore zone. The target areas of barite deposits in the generally steeply dipping Stanley Shale therefore are small. Samples at intervals of 300 feet across strike would 14 F. N. Ward, H. W. Lakin, F. C. Canney, and others, 1963, Analytical methods used in geochemical exploration by the U.S. Geological Survey: U.S. Geol. Survey Bull. 1152, p. 44-45. probably be required to thoroughly prospect this formation. Halos around deposits in the Trinity Group (Cretaceous) are much more irregular. Barite ore bodies in the Trinity Group that are covered by more than a few feet of overburden probably cannot be identified by field chemical analysis of samples from the surface. Glauconite in the central Appalachian region According to W. D. Carter, glauconite, mined as a soil conditioner and water softener in New Jersey, is also found in the central Appalachians. It occurs mainly as sandstone and shale in the Huntersville Chert of Price (1929) (Devonian) of eastern West Virginia and southwestern Virginia, where it is as much as 4 feet thick. Preliminary analyses indicate that glauconite containing 3 to 7 percent potassium is found in Pocahontas County, W. Va., and Montgomery County, Va. Silica in the Great Basin and Appalachian regions According to K. B. Ketner, several formations in the Great Basin contain thick quartzite units of remarkable purity. Among these are the Big Cottonwood Formation (Precambrian), Tintic Quartzite (Cambrian), Valmy Formation (Ordovician), and Eureka Quartzite (Ordovician). The high purity of quartzite in the Big Cottonwood and Valmy Formations was unexpected. Work by W. D. Carter shows that the Oriskany Sandstone (Devonian) and Tuscarora Quartzite (Silurian) contain most of the silica resources of the central Appalachian region. The Oriskany Sandstone ranges from 0 to 250 feet in thickness and is thickest along a narrow south-trending belt extending from south-central Pennsylvania into northeastern West Virginia and northwestern Virginia where it is mined for glass sand. The Tuscarora Quartzite has been mined for refractories, mainly in Pennsylvania, and constitutes an even larger resource of silica than the Oriskany, although in most places it is more difficult to mine. Pegmatites and related deposits As a result of geologic mapping in the southeast corner of the Franklin quadrangle, Macon County, N.C., F. G. Lesure has located numerous small mica prospects and three emery prospects, and extended knowledge of a previously known area of kyanite-bearing rocks. RADIOACTIVE MINERALS URANIUM IN SANDSTONE Many similarities and some differences in the geologic setting, form, habits, and mineralogy of uraniumA14 INVESTIGATIONS OF NATURAL RESOURCES deposits in sandstone, conglomerate, and mudstone of diverse ages are recorded for widely separated areas such as Monument Valley, Ariz. (Witkind and Thaden 15); Deer Flat, Utah (Finnell and others 16); Capitol Reef, Utah (Smith and others, 1-63); Lees Ferry, Ariz. (Phoenix, 1-63); Edgemont, S. Dak. (Gott and Schnabel17); and the Lehigh ton quadrangle, Pennsylvania (Klemic and others, 2-63). Although sandstone deposited as channel fills directly or indirectly controls the occurrence of uranium deposits in Triassic rocks in Monument Valley, at Deer Flat, and many of the deposits in Cretaceous rocks near Edgemont, the selectivity noted among channels is still incompletely understood. Also noteworthy is the resemblance between size and form of some features in a deposit in rocks of Devonian age near Penn Haven Junction, Pa., and those in deposits in the Morrison Formation in the West. Ambrosia Lake and Laguna districts, New Mexico The Ambrosia Lake and Laguna uranium districts were described in five papers, by L. S. Hilpert,18 R. E. Thaden and E. S. Santos,19 H. C. Granger,20 E. S. Santos,21 and R. H. Moench,22 of the Geological Survey, in the comprehensive memoir on the Grants uranium region, sponsored in part by the Society of Economic Geologists. Geologic evidence presented by R. H. Moench 22 tentatively dates uranium deposition in the Laguna district to the period between early, near-surface deformation of the Jurassic host rocks and probable early Tertiary tilting in the southeast part of the San Juan Basin. Moench suggests that the uranium deposits formed in Jurassic time before the host rocks were deeply buried and possibly when they were exposed at the surface. The uranium deposits may have formed 15 I. J. Witkind and R. E. Thaden, 1963, Geology and uranium-vana-dium deposits of the Monument Valley area, Apache and Navajo Counties, Arizona : U.S. Geol. Survey Bull. 1103, 171 p. 18 T. L. Finnell, P. C. Franks, and H. A. Hubbard, 1963, Geology, ore deposits, and exploratory drilling in the Deer Flat area, White Canyon district, San Juan County, Utah : U.S. Geol. Survey Bull. 1132, 114 p. 17 G. B. Gott and R. W. Schnabel, 1963, Geology of the Edgemont NE quadrangle, Fall River and Custer Counties, South Dakota : U.S. Geol. Survey Bull. 1063-E, 190 p. 18 L. S. Hilpert, 1963, Regional and local stratigraphy of uraniumbearing rocks, in Geology and technology of the Grants uranium region : New Mexico Bur. Mines and Mineral Resources Mem. 15, p. 6-18. 19 R. E. Thaden and E. S. Santos, 1963, Map showing the general structural features of the Grants district and the areal distribution of the known uranium ore bodies in the Morrison Formation ; in Geology and technology . . .: New Mexico Bur. Mines and Mineral Resources Mem. 15. map opposite p. 20. 20 H. C. Granger, 1963, Mineralogy, in Geology and technology . . .: New Mexico Bur. Mines and Mineral Resources Mem. 15, p. 21-37. 21 E. S. Santos, 1963, Relation of ore deposits to the stratigraphy of host rocks in the Ambrosia Lake area, in Geology and technology . . .: New Mexico Bur. Mines and Mineral Resources Mem. 15, p. 53-59. 22 R. H. Moench, 1963, Geologic limitations on the age of uranium deposits in the Laguna district, in Geology and technology . . .: New Mexico Bur. Mines and Mineral Resources Mem. 15, p. 157-166. where the flow of near-surface ground water was impeded by the stratigraphic and early postdeposi-tional tectonic structures that characterize the mineral belt. H. C. Granger has found that oxidation taking place several hundred feet below the ground-water table in the Ambrosia Lake uranium district releases some selenium from the pyrite which is normally present in the unoxidized rocks. The pyrite contains as much as 1.5 percent selenium. As the pyrite is oxidized, some selenium is redistributed to form ferroselite. Further oxidation of the ferroselite-rich zone destroys the ferroselite, and the selenium is carried ahead of the oxidation front where some of it is deposited as native selenium. As a result, oxidation fronts defined by the limits of destruction of pyrite are characterized by concentrations of selenium in different forms on opposite sides of the interface. Shirley Basin, Wyo. From the spatial relation of uranium deposits to large tongues of altered sand, and from laboratory studies of elements in those deposits, E. N. Harshman concludes that uranium was carried into the lower part of the basin by oxidizing slightly acid or slightly alkaline ground water, moving laterally through permeable sand in the Wind River Formation. Uranin-ite was apparently deposited at an interface between the uranium-bearing ground water and semistagnant ground water in the lower part of the basin. Earlier concepts that uranium was carried as a carbonate complex and was reduced by H2S of biogenic origin are compatible with data on the Shirley Basin deposits. Texas coastal plain D. H. Eargle reports the discovery by a mining company of a significantly large concealed deposit of uranium ore in Karnes County, Tex., in the vicinity of radioactivity anomalies previously known from drilling by the Geological Survey and by companies. This discovery suggests that other concealed deposits may be present in this part of the Gulf Coastal Plain. The deposit is also possible evidence that uranium migrated downdip in ground water and was precipitated in a reducing environment. Results of a study of uranium and helium in the Panhandle gas field, Texas, which originally contained the largest commercial helium reserve in the United States, have been presented by A. P. Pierce, G. B. Gott, and J. W. Mytton (1-64). The highest concentration of uranium is in the caprocks, which have been estimated to contain between 10 and 20 parts per million through a thickness of about 250 feet. The uranium in these rocks is concentrated inMINERAL RESOURCES A15 asphaltite which contains about 1 percent uranium. The uranium and associated metals are thought to have been derived from the rocks in which the asphaltite now occurs, and were concentrated in petroleum compounds. The distribution of uraniferous asphaltite indicates that it is the source of the abnormally high radon in the gases from a number of wells. URANIUM AND THORIUM IN CRYSTALLINE ROCKS Southeastern Piedmont A type of radioactive deposit not previously recognized in the southeastern Piedmont has been reported by H. W. Sundelius and Henry Bell. The radioactive deposit, at the Heglar prospect in Cabarrus County, N.C., contains disseminated pyrite, other sulfides, and rare-earth elements in an andradite-opal-chalcedony-quartz gangue. The deposit occurs within a regional radiometric anomaly near the boundary between green-schist facies rocks of the Carolina slate belt and albite-epidote amphibolite facies rocks of the Charlotte belt, It appears to be related to a cross-cutting, highly sheared quartz monzonitic body. Thorium in the Wet Mountains, Colo. In the Ttosita quadrangle, Custer County, Q. D. Singewald and R. B. Laughon have found that radioactive anomalies due to thorium are in Precambrian rocks mainly in the northwest quarter of the quadrangle and that all strong anomalies are northeast of a northwesterly trending line about through the center of sec. 35, T. 22 S., R. 71 W. This northeast comer represents part of a poorly defined belt about 5 miles wide that trends north-northwest and also contains most of the thorium-bearing veins in the Mount Tyndall quadrangle just to the north. MINOR ELEMENTS RARE EARTHS AND NIOBIUM The calcium yttrium silicate-carbonate mineral, cen-osite, was found in a thorite vein near Porthill, Idaho, by J. W. Adams and M. H. Staatz—the second known occurrence of the mineral in the United States. Niobium, rare earth, and thorium minerals discovered in the alkalic rocks of Gem Park near Hillside, Colo., by F. A. Hildebrand and R. L. Parker include, in addition to lueshite,23 pyrochlore, fersmite, fergusonite, columbite, thorianite, and monazite. Gem Park is the second known locality for the occurrence of fersmite in the United States and the first for thorianite in Colorado. 23 R. L. Parker, J. W. Adams, and F. A. Hildebrand, 1962, A rare sodium niobate mineral from Colorado, Art. 61, in U.S. Geol. Survey Prof. Paper 450-C, p. C4-C6. Geochemical exploration by R. L. Parker, F. A. Hildebrand, Uteana Oda, and A. P. Marranzino has shown that part of the Gem Park alkalic intrusive body contains anomalous niobium and thorium. The niobium content of samples within the anomaly ranges from 100 to greater than 2,000 parts per million, and highest radioactivity within the anomaly occurs where the content of niobium is greatest. SELENIUM AND TELLURIUM An extremely sensitive method for the quantitative determination of tellurium has been developed by H. W. Lakin and C. E. Thompson (2-63), permitting the investigation of tellurium in all geochemical environments. Tellurium in amounts ranging from 5 to 125 parts per million has been found in manganese nodules from the floor of the Pacific and Indian Oceans (Lakin, Thompson, and Davidson, 3-63). The nodules represent the first recognized high tellurium concentration in a sedimentary cycle. Lakin, D. F. Davidson, and Thompson have found also that the tellurium and selenium content of volcanic sulfur exceeds that of hot-springs sulfur, and that their content in hot-springs sulfur exceeds that in sulfur of sedimentary origin. Such distribution suggests that tellurium and selenium are much more mobile in the gaseous state than in solution in water. Investigation of the distribution of tellurium by G. B. Gott and J. H. McCarthy, Jr., around the Ruth porphyry copper deposit near Ely, Nev., shows that the tellurium is most concentrated in a halo surrounding the copper. ORGANIC FUELS The Geological Survey conducts a variety of investigations that may be of direct or indirect value to private organizations in their exploration for organic fuels. These investigations include regional geologic and geophysical mapping and stratigraphic, paleontologic, and sedimentation studies which are described under other headings. Only studies pertaining directly to fuels, geochemistry of fuels, and fuels resources are reported here. COAL Southwestern Pennsylvania The first two of a series of geologic-quadrangle maps of areas where the Pittsburgh coal bed is extensively mined southwest of Pittsburgh, Pa., were published in 1964 (Berryliill and Swanson, 2-64; Berryhill, 1-64). These maps show structure contours of the Pittsburgh coal, the general lithology of the Upper PennsylvanianA16 INVESTIGATIONS OF NATURAL RESOURCES and Lower Permian stratigraphic units, and also the distribution and outcrop pattern of several poorer grade or thinner coal beds currently uneconomic to mine, including the Waynesburg and Washington coal beds. The lower member of the Pittsburgh Formation is commonly a sandstone in the area of Washington, Pa., and in places occupies broad channels that cut into the Pittsburgh coal bed, constituting a significant economic and mining problem. B. H. Kent and S. P. Schwein-furth report that in the western part of the area this member is generally a sheetlike sandstone, but that the sandstone-filled channels become more numerous and complex toward the southeast. Western Pennsylvania A report by E. D. Patterson (1-63) on the geology and coal resources of Beaver County, which is northwest of Pittsburgh, Pa., gives estimates of original reserves of high-volatile bituminous coal as 2,517 million tons, and remaining reserves of 2,489 million tons. Most of these reserves are in the Lower and Middle Kittanning coal beds and the Lower and Upper Freeport coal beds, all in the Allegheny Formation of Pennsylvania age. Eastern Pennsylvania Recent studies by H. H. Arndt in the Western Middle Anthracite field and by G. H. Wood, Jr., in the Southern Anthracite field show that the fixed-carbon and volatile matter in the coal are related to geographic location and structural position. Regionally, the percentage of fixed carbon increases and volatile matter decreases eastward in the direction of regional plunge and greater original depth of burial of the coal beds. On a smaller scale, there is a marked parallelism of lines of equal fixed-carbon and volatile-matter content with fold axes, the fixed carbon being greater and volatile matter less along synclinal axes; the fixed carbon is less and volatile matter greater along anticlinal axes. Southeastern Kentucky and northern Tennessee K. J. Englund reports that an appraisal of coal resources in rocks in Pennsylvania age in a four-quadrangle area of parts of Scott and Campbell Counties, Tenn., and McCreary and Whitley Counties, Ky., indicates total reserves of about 1 billion tons in beds exceeding 14 inches in thickness. This estimate includes data on several beds with previously unreported reserves. Iowa A recent investigation by E. R. Landis shows that coal-bearing rocks of Pennsylvanian age underlie some 20,000 square miles of the State of Iowa. Estimated original reserves of bituminous coal total 7.2 billion short tons, remaining reserves 6.5 billion tons, and 1.8 billion tons can be categorized as measured and indicated reserves in beds more than 42 inches thick. Northern New Mexico The geology and coal resources of the southwestern part of the Raton coal field in Colfax County, N. Mex., are described in a report by A. A. Wanek (2-63). The map area covers about 750 square miles and contains raserves estimated at nearly 1.5 billion tons of high-volatile bituminous coal. The area also includes rocks of Cretaceous and Pennsylvanian age that are possible reservoirs for oil and gas. Detailed study of the coal deposits of the Upper Cretaceous Fruitland Formation in the San Juan basin, Colorado and New Mexico, by J. S. Hinds (chapter D) indicates that on an “as received” basis the Btu values are highest in the northwest part of the basin. On a “moisture and ash-free” basis, however, the highest Btu values are in the northeast part of the basin corresponding to the youngest coals. • Montana The geology and the distribution of Upper Cretaceous coal beds in the Livingston coal field in south-central Montana are shown on eight quadrangle maps by A. E. Roberts (1-64 to 8-64) published in 1964. More than 260 million tons of high-volatile bituminous coal, much of it of coking quality, remain unmined in this coal field. Alaska The coal-bearing Kenai Formation of Tertiary age underlies a lowland region of at least 5,000 square miles at the head of Cook Inlet, between the Susitna River and the Alaska Range in southern Alaska, according to F. F. Barnes. Potentially valuable lignite and sub-bituminous coal deposits lie mainly within a 400-square-mile area in the southern part of the region, and include at least 2 beds 30 to 50 feet thick that have been traced for several miles. Indicated reserves in beds more than 2% feet thick and within 1,000 feet of the surface total about 2.4 billion tons; about 2.2 billion tons of this is in beds more than 10 feet thick. PETROLEUM AND NATURAL GAS Most of the studies contributing to the fund of stratigraphic, geophysical, and paleontologic data upon which the petroleum industry relies are reported under appropriate regional and topical headings. Yellowstone National Park, Wyo. For more than a century oil seeps and deposits of bitumen have been known in and near Yellowstone Park. J. D. Love investigated three of these occur-MINERAL RESOURCES A17 rences with J. M. Good, of the National Park Service, and they interpret them to be surface expressions of “natural refineries.” Light aromatic oil is probably being distilled from underlying Cretaceous and perhaps older organic-rich sedimentary rocks by somewhat deeper igneous intrusives. Interestingly, the oil has a low sulfur content, but the seeps are associated with hot springs and sulfur deposits. North-central Wyoming The geology of the east Thermopolis area in Hot Springs and Washakie Counties is described in a report by G. H. Horn (1-63). The map area, with accompanying text, covers about 480 square miles in the southeastern part of the Bighorn Basin, and the 10 oil and gas fields in the area are described. Southeastern Wyoming A geologic map at a scale of 1:24,000 by H. J. Hyden 24 includes an area of active petroleum exploration along the Rock River-Dutton Creek anticline in Carbon County. This map shows a series of previously unmapped northwest-trending reverse faults on the west flank of the anticline; these or similar faults presumably trap oil in Cretaceous rocks at depth in this area. Northern Alaska A report by R. L. Detterman, R. S. Bickel, and George Gryc (1-63) describes the Chandler River region, which adjoins Naval Petroleum Reserve No. 4 in northern Alaska. Four of the main anticlines mapped show closure, and the 10 formations mapped, which have a total thickness of 16,300 feet, include many beds of subbituminous to bituminous coal. Application of gravity studies to fluid reservoirs A study by T. H. McCulloh indicates that it may be possible to use detailed gravity observations to estimate the oil and gas content of porous rocks under favorable circumstances. Porous rocks saturated with petroleum or natural gas differ in bulk density from identical rocks saturated with relatively denser interstitial water by amounts ranging from 0.03 g/cm3 or more in rocks of 10-percent porosity to 0.11 g/cm3 or more in rocks of 30-percent porosity. Organic geochemical investigations Preliminary analyses by V. E. Swanson and J. G. Palacas of recent sand cemented with organic material, which is present at many places at or near the shore- 24 H. J. Hyden, 1963, Geologic map of Cooper Cove and Dutton Creek oil fields and vicinity, Albany and Carbon Counties, Wyoming : U.S. Geol. Survey open-file rept. line of bays and sounds along the Gulf of Mexico coast of the Florida panhandle, indicate that the water-transported organic material consists of 3 major fractions: about 81 percent humate, 15 percent “fulvic acid,” and 4 percent hydrocarbons. The hydrocarbons, which have been further fractionated into paraffinic, aromatic, and possibly asphaltic groups, may have been transported with the humic acids that coagulated to form the humate, or they may have been derived from the humate through chemical or biochemical reactions. Similar organic geochemical studies are currently underway on a suite of bottom-sediment cores from lake, river, bayou, swamp, and bay environments in the Choc-tawhatchee Bay area of north Florida; and on segments of cores of deep-sea sediment from the north Pacific Ocean, which were provided by G. W. Moore from the U.S. Coast and Geodetic Survey’s 1961 Pioneer cruise. OIL SHALE With recent revived interest in exploitation of the oil shale in Colorado, Utah, and Wyoming, the need for more detailed resources estimates has increased. These estimates are based largely on precise mapping and determination of the extent and thickness of rich oil-shale units by Geologic Division personnel, who also integrate data on cores and cuttings obtained from petroleum companies and the oil-yield analytical data provided by the U.S. Bureau of Mines to obtain the new estimates. New revised estimates of oil-shale resources have been made by D. C. Duncan and J. R. Donnell for a 1,350-square-mile area in the Piceance Creek Basin, Rio Blanco and Garfield Counties, Colo. Oil shale in this area assaying 5 or more gallons of oil per ton of shale will yield about 1.4 trillion barrels of oil. About 420 billion barrels of oil can be produced from shale units 15 to 540 feet thick that assay 25 to 65 gallons per ton, and 800 billion barrels of oil can be produced from shale units 15 to 1,000 feet that, assay 10 to 25 gallons per ton and are interbedded with or lie marginal to the richer shale. Two additional estimates, which consider other factors of economic significance, are that about 100 billion barrels of oil could be produced from 25 to 65 gallon-per-ton shale lying less than 1,000 below the surface; and that about 680 billion barrels of oil could be produced from interbedded rich and lean oil-shale units that would have an average yield of 25 gallons of oil per ton. In his study in the Firehole Basin quadrangle, Sweetwater County, Wyo., W. C. Culbertson has found that the upper 800 feet of the fluviatile Wasatch Formation of Eocene age contains several lacustrine tonguesA18 INVESTIGATIONS OF NATURAL RESOURCES consisting of oil shale and an underlying thin limestone with a fresh-water fauna. These tongues thicken and become more numerous southward, indicating that in Wasatch time a lake or lakes existed near the Wyo-ming-Utah border that periodically increased in size. Some of the tongues overlie coal beds, suggesting that the lake transgressed northward across a swamp, first depositing calcareous muds on a peat deposit, then becoming deeper with a stagnant hypolimnion that allowed accumulation of oil shale. W. B. Cashion (chapter D) has computed the potential oil content of kerogene-rich strata in the Green River Formation of the Uinta basin, Utah-Colo-rado, from samples from 40 core holes, 110 exploratory wells, and 25 surface localities. He estimates that a sequence of rocks 15 feet or more thick that yields an average of 15 gallons per ton contains about 321 billion barrels of oil. This resource occurs in an area of about 3,000 square miles and is of prime importance as a potential source of synthetic liquid fuel.WATER RESOURCES The U.S. Geological Survey investigates the occurrence, availability, and quality of surface and underground waters and the sediment discharge of streams. An extensive hydrologic network of stream-gaging stations, observation wells, and water-quality sampling stations throughout the country provides continuing basic data. Compilations of these basic data are published in the following U.S. Geological Survey Water-Supply Paper series: “Surface Water Supply of the United States,” “Ground-Water Levels in the United States,” “Quality of Surface Water of the United States.” The surface-water records are published at 5-year intervals in 14 numbered parts determined by drainage basins, for the 48 conterminous States, plus 2 additional reports for Alaska and Hawaii. The groundwater records are published in 6 parts representing geographical sections of the country. One part is published each year; 2 parts being published every fifth year. The records of quality of surface water are published annually. In addition, nationwide reports which describe flood frequency at selected gaging stations and extend the data to ungaged sites on major and minor streams are being published in the Water-Supply Paper series in several parts that correspond to the drainage-basin subdivisions of “Surface Water Supply of the United States.” Areal investigations of water resources are made largely in cooperation with State, local, or Federal agencies listed on page A221. These studies include the various aspects of the gelogic and hydrologic environment that relate to the occurrence and movement of water on the surface and underground. Such studies of water resources stress the evaluation of * sources of supply, chemical and physical composition, computation of the quantity available for use, description of the direction and rate of movement, evaluation of fluctuations in flow, and determination of disposition of the supply as use, waste, or outflow. Diversified water-resources investigations are in progress in nearly every State. These fall into two general qategories, “area” and “systems” studies. Area studies cover investigations of specific hydrologic problems within an area, generally comprising a political subdivision-—the problems of a municipality, a county, or a State. Systems studies, on the other hand, are investigations of the hydrologic environment of natural units such as a river basin or isolated valley or a major aquifer, whose area may include a number of political subdivisions. The purpose of these investigations is to determine the effect on the hydrologic system of changes in any part of it; for example, to predict how use of ground water in one municipality may influence streamflow in another part of a river system. Investigations stressing the economic aspects of water as a resource are treated in the following section under four areas (fig. 3), which correspond to the administrative subdivisions of the Water Resources Division. WATER USE Development and use of water in the United States have rapidly increased with the Nation’s growing population and expanding economy. However, because water supplies are limited in some parts of the country a less rapid increase in average per capita water use is expected in future years. The per capita withdrawal use of water in 1960, 1,500 gallons per day (MacKichan and Kammerer25), is estimated to have increased to 1,675 gpd in 1964. Future increases are estimated at about 80 percent of the projection of withdrawals, made by the Senate Select Committee26 which was based on the assumption that optimum amounts of water for irrigation are made available. In 3 of the past 4 years, streamflow as reported monthly by the Geological Survey’s “Water Resources Review” was either in the deficient range or well below median in most of the West, excepting the extreme Northwest. The exception was 1962, when streamflow was generally near median and was excessive in limited areas. It is estimated that the average per capita withdrawal demand will increase at the rate of about 0.77 percent per year. To meet the increasing demand for information for water management, the U.S. Geological Survey investigates and prepares reports on water resources. Many 25 K. A. MacKichan and J. C. Kammerer, 1961, Estimated use of water in the United States, 1960 : U.S. Geol. Survey Circ. 456. 26 U.S. Congress, Senate Committee on National Water Kesources, 1961, National water resources : U.S. 87th Cong., 1st sess., Rept. 29. A19A20 INVESTIGATIONS OF NATURAL RESOURCES of the area studies include some incidental information on water use, particularly those that report on pump-age from wells, which is usually a measure of withdrawal use. Other studies are more specifically concerned with water use, such as studies of specific industries, metropolitan areas, and States. In those studies, water use is determined in relation to time, population, area, unit of product, or the supply of water. Water requirements of the iron and steel industry Twenty-five steel plants with a combined production of 37 million tons of steel ingots per year—about 30 percent of the total United States steel production for 1956—withdrew 4 billion gallons of water per day, according to L. E. Otts and F. B. Walling. About 93 percent of this intake was used for cooling. Reuse of water varied from 1 to 45 times in steel-processing plants (plants that begin with pig iron or scrap) and from 1 to 19 times in integrated steel plants (plants that begin with iron ore). About 97 percent of the water intake was from surface-water sources, 1 percent from ground water, and 2 percent from reclaimed sewage. The industry supplied about 93 percent of its own water needs. The amount of water withdrawn (intake) by integrated steel plants ranged from 1,530 to 70,300 gallons per ton of steel ingot, with an average intake of 29,800 gallons per ton. Water use (intake plus reused water) by these same plants ranged from 11,200 to 110,000 gallons per ton of steel ingot, with an average of 39,800 gallons per ton. Some of this variation is caused by the inclusion of water used for power production and coke production and by differences in products and operation of the plants. In the 25 plants surveyed, average water use for blast furnaces (20,100 gallons per ton for pig iron) was much greater than that of other processes. But, large quantities of water were also used for open-hearth furnaces (4,990 gallons per ton of steel ingot), electric furnaces (3,210 gallons per ton of steel ingot), and primary rolling mills (3,880 gallons per ton of semifinished steel— blooms, billets, and slabs). Byproduct coking plants used an average of 5,850 gallons per ton of coke. Chemical quality of public water supplies Eight maps showing Statewide average dissolved-solids, sodium, and fluoride content and hardness in raw and finished public water supplies of the 50 States, the AC,F>C coast ('^luo£s AND HAwiS; &TLANT1C ^ COAST AREA (INCLUDES PUERTO RICCD midcontinent area rocky mountain area 500 MILES Figure 3-—Index map of the United States, showing areal subdivisions used in discussion of water resources.WATER RESOURCES A21 District of Columbia, and Puerto Rico have been prepared by C. N. Durfor and Edith Becker.27 The data were derived from 1,596 water systems that serve a total of 103 million people, or 81 percent of the urban population and about 57 percent of the total population. This survey showed that in 1962, 29 million people used water containing 100 parts per million or less of dissolved solids, 72 million people used water containing 250 ppm or less of dissolved solids, and 89 million people used water containing less than 500 ppm of dissolved solids. Hardness of public water supplies ranges from less than 60 ppm along the East Coast and far Northwest to more than several hundred parts per million in the midwestem and western States. About 80 percent of the population surveyed used water having a hardness of 180 ppm or less. Most States east of the Mississippi and several States west, of the Mississippi have an average sodium content of less than 20 ppm in finished water supplies. This amount is low enough to be ignored in planning sodium-restricted diets; however, in some water supplies the sodium content is high enough so that it must be considered in planning such diets. Water containing between 0.6 and 1.7 ppm of fluoride is used by 43 million people. This figure does not include New York City (more than 8 million people), which decided to fluoride its water supplies after the data for this project were compiled. Nitrate content was calculated but not mapped because about 86 percent of the raw and finished water supplies surveyed contained less than 10 ppm of nitrate, well below the acceptable limit of 45 ppm in drinking water.28 ATLANTIC CO AST AREA With the exception of major floods, the waters of the Atlantic Coast States are no longer surplus to the needs of the Eastern States’ economy and social pattern. Waters not required for public supply, industry, and agriculture are now in good part utilized for recreation and for the dilution and transport of pollutants. In the populous East, man is having an increasing effect upon the utility of natural water sources. Even the precipitation that recharges streams and aquifers has been found to have significant quantities of dissolved minerals picked up in passing through the atmosphere of industrialized areas. This requires in- 27 C. N. Durfor and Edith Becker, 1964, Chemical quality of public water supplies of the United States and Puerto Rico, 1962 ; U.S. Geol. Survey Hydrol. Inv. Atlas HA 200. [In press] 28 U.S. Public Health Service, 1962, Drinking water standards : U.S. Public Health Service Pub. 1956. creasing attention by the hydrologist to the content as well as the amount of available rainfall. Man’s desire for optimum quality of water for each of its many uses has made him sensitive to water characteristics, such as sediment content, which his forebears once accepted without question. A standard feature of many water investigations is the study of the points of origin and patterns of deposition of fluvial sediments produced by natural erosion and carried by floodwaters. Land use is seen as a major factor in sediment production. The water resources of estuarine areas are moving into a position of greater importance. Water problems, particularly along heavily industrialized and populated estuaries, are critical in number and magnitude. Greater competence in determining the volume and nature of tidal flows has given a better base for the study of water quality and deposition of solid pollutants. New areas in which large ground-water supplies may be developed were discovered during the year. Additional knowledge of the manner and extent of recharge to ground-water reservoirs was reported upon and will provide a better base for conservation and utilization and perhaps eventual artificial recharge of the resource. The following project studies for which specific findings are reported indicate that more and more investigations are designed around specific local water problems. NEW ENGLAND Ground water in Massachusetts Studies in the Assabet River basin by S. J. Pollock indicate several areas that are potential sources of large supplies of ground water. The areas are underlain by Pleistocene glaciofluvial deposits and appear to cover about 5 percent of the 175-square-mile basin. Investigations in the Merrimack River basin in Essex County by J. E. Cotton show that the most favorable aquifers are glaciofluvial sands and gravels in areas where some recharge can be supplied by lakes, streams, or swamps. Ground-water supplies for most uses would require treatment because of pollution in the Merrimack River, which partly recharges the aquifer. As part of a study of the water resources of the Housatonic River basin by R. F. Norvitch, preliminary information obtained by test drilling suggests that the materials underlying the main valley below Pittsfield are mostly fine grained, indicating that large yields of ground water cannot be expected. Expected yields from bedrock also may be low as indicated by low-flow stream measurements, which suggest that the bedrock is poorly permeable. However, large volumes of water may be obtained locally from bedrock wells that penetrate fault zones.A22 INVESTIGATIONS OF NATURAL RESOURCES Greater Boston area, Massachusetts The water resources of the 551-square-mile greater Boston area, with about 2.3 million population, were appraised by H. N. Halberg, J. A. Shaughnessy, and G. K. Wood. Of 418 million gallons per day of fresh water used in 1958, 34 mgd was ground water, and 384 mgd was surface water of which 206 mgd was imported from central Massachusetts. Public-supply systems furnished 279 mgd of which about 150 mgd was for domestic use, and the remainder for industrial, commercial, and public supply. Industries and commercial establishments supplied 139 mgd for their own use from private systems. About 1,300 mgd of salt water is used for cooling purposes, mostly in the production of thermal-electric power. The quality of the water from most of the streams and the more than 100 lakes, ponds, and reservoirs in the area is good to excellent for most purposes. The waters are generally soft and their dis-solved-solids content is low. Water in streams has higher iron content and color than the ponded water. Yields from wells in sand and gravel range from a few gallons per minute to 1,700 gpm, the water being generally good to excellent. The yield of wells tapping sedimentary rocks averages about 40 gpm and the yield of those tapping crystalline rocks about 20 gpm, the water being generally satisfactory. Rhode Island W. B. Allen, G. W. Hahn, and C. R. Tuttle (1-63) found that large increases in the use of water are feasible in the upper Pawcatuck River basin in southern Rhode Island. In 1959, the average use of water was about 1.5 mgd, nearly all of which was ground water. They estimate that as much as 18 mgd of ground water is available in the basin. Generally, the chemical quality of ground water is good except for locally excessive manganese, iron, and nitrate content. The chief source of fresh ground water of Block Island is a perched aquifer in the southern part of the island, according to A. J. Hanson, Jr., and G. R. Schiner. The aquifer is composed chiefly of sorted glacial deposits of sand and gravel less than 200 feet thick. Generally the water is of good quality but locally may be corrosive or contain excessive iron. With proper development, the aquifer will yield more than 1 mgd. Quinebaug River basin, Connecticut M. P. Thomas and A. D. Randall report that quantitative studies in the Quinebaug River basin in eastern Connecticut have emphasized the importance of the stratified glacial drift as a ground-water reservoir. Preliminary estimates indicate that during the moderately dry 1963 water year, ground-water recharge was about 8 inches in areas of till-covered upland and about 20 to 24 inches in areas of stratified drift. Regional flow-duration curves for the period 1931-60 show that the discharge per square mile for a stream draining a basin underlain by till exceeds that for a stream draining a basin underlain by stratified drift only about 10 percent of the time; furthermore, the 95-percent-dura-tion discharge per square mile from a basin underlain by stratified drift is about 30 times more than that from a basin underlain by till. In this region, the 95-percent-duration flow is about the same as the median annual 7-day low flow. Chemical quality of water in the Quinebaug River basin is generally good, according to C. E. Thomas, Jr. Only 5 percent of the ground-water samples analyzed had a hardness greater than 120 parts per million. However, dissolved iron and manganese in concentrations as high as 3.7 ppm and 5.7 ppm, respectively, are a problem locally. Precipitation containing sulfate ions, presumably originating from smoke, is the major source of sulfate over nearly half the basin. In other areas the mineral content of water is increased by solution of sulfide minerals from the bedrock and by industrial wastes discharged into some streams. Calcium, bicarbonate, and sulfate are the principal ions in precipitation from storms approaching the basin from the west or north. Waterbury-Bristol area, Connecticut The water resources of the Waterbury-Bristol area have been appraised by R. V. Cushman, F. H. Pauszek, A. D. Randall, and M. P. Thomas. Nearly 170,000 people live in this highly industrialized area. The principal sources of water are the Naugatuck and Pequa-buck Rivers and their tributaries, and ground water. Municipal water supplies are obtained from tributary streams, and rural supplies from wells. The chemical quality of the water in the Naugatuck River during low flows fluctuates erratically; extremes in pH of 4.5 to 9.1 have been observed, sulfphate concentrations have ranged as high as 93 parts per million, and iron concentrations as high as 1.8 ppm. The variations in quality and the high concentrations of individual constituents are attributed to industrial wastes, especially from brass and copper mills. Additional large water supplies are available from streams, but at present, pollution limits their use. Moderate supplies are available from ground water contained in sand and gravel. NEW YORK Comparison of high and low flows of streams The ratio of very high discharge to very low discharge for most unregulated streams draining more than 100 square miles in New York State is betweenWATER RESOURCES A23 100-to-l and 300-to-l, based on a statewide appraisal study of existing records by J. C. Kammerer in 1963. A major exception is the upstream part of the Schoharie Creek basin for which the ratio is more than 2,500-to-l, based on measurements at Prattsville, where the creek drains an area of 236 square miles. The high ratio results from this Catskill Mountain area being subject to intense storms and its soil and rocks having very limited infiltration rates and storage. The high streamflow factor used in this comparative analysis was the discharge of the once-in-50-year flood, and the low-flow factor was the minimum 7-day discharge with a recurrence interval of once in 10 years. Many streams draining small areas probably have ratios greater than 300-to-l. On the other hand, small streams on Long Island have low ratios because most of the flow consists of ground-water discharge. Therefore, peak discharges are lower on Long Island than elsewhere in the State, and minimum discharges are higher than average. Sources of ground water in Jamestown area Studies by L. J. Crain (1-63) in the Jamestown area show that recharge to a sand and gravel aquifer confined by dense clays is by infiltration from tributary streams in a glaciated bedrock valley. The streams drain till-covered bedrock hills and cross alluvial deltas which have been deposited outward into the valley at many places. These deposits connect with the deeper aquifer and serve as storage reservoirs for the aquifer. The city of Jamestown pumps 6 mgd from the aquifer. Water levels in wells near the apex of the alluvial deltas fluctuate as much as 40 feet annually. Tributary streams flow only following periods of heavy precipitation because most of the runoff from the adjacent highlands infiltrates to the aquifer. Discharge measurements indicate that the main-stem stream in the valley does not lose an appreciable amount of water to ground-water recharge. Ground water in lower Oswego River basin An investigation by I. H. Kantrowitz and J. A. Tan-nenbaum in the area lying roughly between the eastern Finger Lakes and the Tug Hill plateau is focused on locating sources of large supplies of ground water and on studying the occurrence of salty water. Preliminary findings indicate that potential sources of large supplies may be restricted to sand and gravel deposits in the northern ends of glaciated valleys in the Appalachian Plateaus and in the adjacent parts of the Mohawk-Ontario lowland. Salty water occurs in bedrock underlying some of the glaciated valleys, and in parts of the Mohawk-Ontario lowland that are farther from the Appalachian Plateaus. In some of these areas, the salty water has migrated upward into the overlying glacial deposits. Water resources of Syracuse area The water resources of the Syracuse area have been appraised by H. N. Halberg, O. P. Hunt, and J. A. Shaughnessy. Water is plentiful from streams and lakes and aquifers but it is not in all ways of the quality desired. In 1956 about 29 percent of the 198 million gallons per day of water used for all purposes was drawn from public-supply systems, about 1 percent from private domestic systems, and the remainder from self-supplied industrial systems. Much ground water is available from the sand and gravel of the Onondaga Creek basin, from stratified glacial deposits along the present streams, and in buried valleys. But, by the year 2000, the demands on public supplies are expected to be double their present capacity, and nearby lakes and rivers will have to be used to supplement ground-water sources. Water-level decline in Nassau County Water levels in the principal aquifer in west-central Nassau County have declined as much as 11 feet since 1953 as a result of heavy pumping, according to John Isbister. NEW JERSEY Water-quality characteristics of streams J. R. George and P. W. Anderson (1-63) have studied the interrelation between water quality and several environmental causative factors as part of a reconnaissance study of the chemical, physical, and bacteriological water-quality characteristics of New Jersey streams. The relations between most water-quality parameters and streamflow normally were found to be inverse. However, direct relations were found between dissolved-solids content and streamflow for several streams in the outer Atlantic Coastal Plain. The prevalent chemical character of streams in relation to geologic terrane was studied. Streams draining glacial-drift deposits in the Valley and Ridge province were shown to have a low dissolved-solids content, ranging from 30 to 90 parts per million. Streams draining limestone and dolomite deposits were found to have high concentrations of calcium, magnesium, and bicarbonate and a correspondingly high dissolved-solids content, ranging from 90 to 250 ppm. The predominant anion found in streams draining Triassic sediments was sulfate. Streams draining the Coastal Plain were found to have an extremely low dissolved-solids content, ranging from 20 to 60 ppm. Streams draining the highly industrial and urban areas generally were found to reflect the influence of waste-water discharges. The highest values of dissolved solids, synthetic detergents, turbidity, and coliform 746-002 0-64-3A24 INVESTIGATIONS OF NATURAL RESOURCES bacteria were found in streams draining these areas. Streams draining farmlands also tended to have high values of turbidity and coliform bacteria. Ground water in Camden County Large amounts of ground water are available from various aquifers in Camden County, according to Ellis Donsky (1-63). Most domestic and other small supplies can be obtained from wells less than 250 feet deep. Most moderate to large yields for industrial and public supplies can be obtained from properly developed wells at depths of 1,000 feet or less. Yields of up to 1,500 gallons per minute are obtained from properly spaced wells in the Raritan and Magothy Formations within 2,000 feet of the Delaware River. Elsewhere, yields of up to 1,000 gpm generally can be obtained from the Raritan and Magothy Formations. Small to moderate supplies are obtained also from other formations in the county. Yields up to 600 gpm are obtained from the Wenonah Formation, Mount Laurel Sand, and Cohansey Sand. Smaller yields, up to 100 gpm, are obtained from the Englishtown, Vin-centown, and Kirkwood Formations. The chemical quality of the water from the various aquifers is suitable for most uses; however, some of the constituents may be objectionable for certain purposes. PENNSYLVANIA Low flows and annual yield of streams A new minimum-runoff map for Pennsylvania, prepared by W. F. Busch and L. C. Shaw and based on all gaging-station records in the State with 5 years or more of record, shows the average 7-day minimum flows having a 2-year recurrence interval. On this map the State was subdivided into three classifications on the basis of flow: less than 0.1 cubic feet per square mile, 0.1 to 0.2 cfs per sq mi, and more than 0.2 cfs per sq mi. Numerous minor changes distinguish this map from a previous map compiled from available data for a lesser number of long-term gaging stations. An annual stream-yield map for Pennsylvania was also prepared. Average discharges for all years of record available at each gaging station were used to subdivide the State into three classifications of runoff: less than 20 inches, 20 to 25 inches, and more than 25 inches. These maps show that there is no correlation between minimum runoff and annual yield. Streams with high average annual yields do not necessarily have well-sustained low flows and, conversely, some streams with low yields have well-sustained low flows. The average 7-day minimum varies from no flows at a few gaging stations to a maximum of 0.56 cfs per sq mi at Yellow Breeches Creek near Camp Hill. Sixty percent of the gaging stations have a sustained flow of more than 0.1 cfs per sq mi for the 7-day minimum. Sediment content of Schuylkill and Susquehanna Rivers Preliminary appraisal of the quality of surface and ground waters of the Schuylkill River basin by J. E. Biesecker, J. B. Lescinsky, and C. R. Wood indicates a significant decrease in suspended-sediment yields from the upper basin between 1948 and 1960. Observations of chemical quality for the same period show no substantial change in the water chemistry. A primary objective of the study is evaluation of the effects of the Schuylkill River Restoration Project, 1950. Initial trap efficiency of three headwater desilting basins constructed during the restoration project was about 90 percent. Preliminary findings by K. F. Williams as part of a comprehensive interagency water-resources study of the Susquehanna River basin indicate that average annual sediment yields from selected subbasins range from 50 to 500 tons per square mile. Quality of water in Lehigh River The water of tributaries in the Lehigh River basin has been mapped into three general types on the basis of prevalent dissolved-solids content and predominant ions in solution, according to P. W. Anderson and L. T. McCarthy, Jr. (2-63) and W. B. Keighton. Most of the streams in the basin have a very low dissolved-solids content, 20 to 40 parts per million; are slightly acidic, pH 4.5 to 7.0; and contain calcium, bicarbonate, and sulfate as the predominant ions. However, several tributary streams draining the Middle Anthracite coal fields in the western portion of the basin contain much greater concentrations of dissolved solids, 100 to 500 ppm; are more acidic, pH 2.0 to 4.0; and contain calcium and sulfate as the predominant ions. Other tributary streams, draining extensive Cambrian and Ordovician limestone and dolomite beds in the southern portion of the basin, also have a high dissolved-solids content, 100 to 250 ppm, but contain calcium and bicarbonate as the predominant ions and are usually basic, pH 6.5 to 8.0. The studies show that each of these three water types influences the water chemistry of the main stem. The upper reaches of the Lehigh River have a low dissolved-solids content, are slightly acidic, and contain calcium, bicarbonate, and sulfate as the predominant ions. Below the confluence with streams draining the coal fields, the dissolved-solids content increases two to three fold; the calcium and sulfate content also increases, with a corresponding decrease in bicarbonate content; and the pH decreases slightly. Streams draining the southernWATER RESOURCES A25 part of the basin tend to neutralize the effects of these acidic tributaries, thereby increasing the bicarbonate-ion content and the pH value of the main stem. Monongahela River basin According to G. W. Whetstone, the overall water assets of the Monongahela River basin are good and in large measure untapped. Outflow from the basin averages about 12,500 cubic feet per second, or about 8,100 million gallons per day, at Braddock, Pa. For perspective, this is about three times the amount of water presently utilized by the municipal and industrial supply of the Pittsburgh area. Supplies of ground water for commercial, agricultural, and industrial use are available in parts of the basin, and with some local exceptions, adequate domestic well supplies are generally available. The major problem in relation to optimum water-resource-development is acid mine drainage. The Monongahela River receives more acid than it is capable of neutralizing. Long-term water quality and stream-flow measurements show that the Monongahela River carries 200,000 tons of sulfuric acid per year into the Ohio River at Pittsburgh. The larger tributary streams to the Monongahela River contribute only 30 percent of the mineral acidity to the main stem. The principal sources of the mineral acid reaching the Monongahela River are the numerous small tributary streams in the reach between Clarksburg, W. Va., and Pittsburgh, Pa. Ground-water supplies in Lancaster, Chester, and Delaware Counties Short-term pumping tests in 250 wells in the Cambrian and Ordovician carbonate rocks of Lancaster County indicate that these rocks are poorer aquifers than rocks of the same age in the Lebanon Valley, 5 miles farther north. Harold Meisler (1-63) and A. E. Becher report that 42 percent of the wells in the Lebanon Valley yielded as much as 10 gallons per minute per foot of drawdown, but in Lancaster County only 16 percent of the wells yielded that much. The tests showed that 25 percent of the wells in the Lebanon Valley and 52 percent of the wells in Lancaster County yielded less than 1 gpm per foot of drawdown. The two areas are similar in lithology and structure even though they are separated by a narrow ridge of Triassic sedimentary rocks. Preliminary findings in a ground-water investigation in Chester and Delaware Counties by C.W. Poth indicate that most wells yield 25 gpm or less, but much larger yields have been obtained. Maximum yields found were 204 gpm in the Baltimore Gneiss, 350 gpm in the Wissahickon Formation, and 100 gpm from a well in gabbro. The highest yield was 650 gpm from the Cambrian Vintage Dolomite. MARYLAND Quality of water in Lower Potomac-Chesapeake Bay area Because of an extended dry period, monthly sediment loads measured in the Potomac River basin during the summer of 1963 are believed to be the lowest in many years, according to F. J. Keller. Although the annual sediment load of the Potomac River at Point of Rocks was about normal (1.1 million tons), the average monthly load for July, August, and September was only 1,060 tons. Total load for the 3-month period amounted to less than 1 percent of annual load, whereas during March 89 percent was transported. A reconnaissance study by J. D. Thomas of the chemical quality of water in the Monocacy River basin in Maryland indicates water of the calcium bicarbonate type. The hardness ranged from 4 to 142 parts per million and the dissolved-solids content ranged from 19 to 187' ppm. Several towns and communities use the streams for the disposal of sewage, which is the main source of pollution in the basin. Concentration of several minor elements in the Patuxent River in Maryland is approximately the same as the median values for these elements in the largest rivers of North America. S. G. Heidel reports the following average results, in milligrams per liter, for the Patuxent River at Hardesty, Md. (median values for the largest North American rivers are given in parentheses for purposes of comparison) : strontium 0.034 (0.060), 'boron 0.044 (0.010), rubidium 0.0075 (0.0015), lithium 0.0008 (0.001), copper 0.0055 (0.0053), lead 0.004 (0.004), and nickel 0.0105 (0.0100). Measurable quantities of more than 17 minor elements were determined spectrographically, but only the concentrations of rubidium were consistently higher at several stations in the Patuxent River basin than those determined in the principal rivers of the United States and Canada. Water resources of Gunpowder Falls basin The total water resource of the Gunpowder Falls basin was studied by Deric O’Bryan and R. L. McAvoy with regard to its past, present, and probable future uses. Quantitative estimates indicate that about 80 percent of the runoff could be retained in the existing reservoirs, if needed, and diverted to the water-supply system of metropolitan Baltimore. The safe yield of 148 million gallons per day, computed by the City of Baltimore Bureau of Water Supply, is very conservative; queuing-theory application shows that a higherA26 INVESTIGATIONS OF NATURAL RESOURCES draft rate of 175 mgd would result in a deficiency only once in 100 years; 220 mgd, once in 10 years. Water supply is the first and established major use of the resource. Rapidly increasing pressures, which often are incompatible with water-supply management and with each other, are (1) expanding suburbanization of sections of the basin, and (2) development of the basin’s potential for recreational needs. Use of ground water in Salisbury area E. G. Otton reports that a nearly completed inventory of all large-capacity wells in the Salisbury area indicates increasing use of ground water for supplemental irrigation of crops. Most of the irrigation wells have been installed within the past 10 years. Recent well data indicate a major gravel-filled post-Miocene valley between Salisbury and the Delaware State line. This buried valley, nearly 200 feet deep in places, contains large untapped reserves of potable ground water. WEST VIRGINIA Ground water in Monongahela River basin Ground-water investigations by Gerald Meyer and B. M. Wilmoth in the Monongahela River basin suggest that pressure gradients probably extend downward through the knobby hills, which characterize the topography of the basin, to nearby streams and to the main body of ground water in rocks beneath the hills. Wells drilled successively deeper in the hills commonly have successively lower water levels. However, owing to horizontal stratification and alternation of beds of low transmissibility with beds of higher transmissibility, large amounts of water are shunted laterally to nearby hillside outcrops. Coal-mine drifts through the hills, acting as collectors, intercept part of the ground water and accelerate its discharge. Low flows in West Virginia streams1 Low-flow investigations in West Virginia indicate that the median annual 7-day minimum flows range from 0.1 to 0.2 cubic feet per second in parts of the Potomac and Monongahela River basins, and below 0.1 cfs elsewhere, according to E. A. Friel. The subbasins having the higher runoff are the South Branch Potomac River, Opequon Creek, and upper Cheat River basins. NORTH CAROLINA Quality of ground water in western North Carolina Findings by R. L. Laney in a geochemical investigation of western North Carolina show that ground water in this area is of good quality and generally contains less than 70 parts per million dissolved solids. Seventy percent of the water sampled from springs contained less than 30 ppm dissolved solids. In some localized areas, water contains more than 0.3 ppm iron. Relatively high concentrations of fluoride (0.2 to 1.3 ppm) were found in ground water in the northeastern half of the area. Ground water was classified into five general types on the basis of chemical analyses. The types are related to the rocks in the area. Rainwater in western North Carolina has a calcium sulfate-bicarbonate composition and generally contains less than 0.2 ppm silica and 10 ppm dissolved solids. GEORGIA Water resources of Georgia The water resources of Georgia have been appraised by J. T. Callahan, L. E. Newcomb, and J. W. Geurin. The average runoff from the State is about 39,000 million gallons per day. The largest use of water is for hydroelectric power, and averages 41,000 mgd. This exceeds the average supply because water for power is used many times, 13 times on the Cattahoochee River and 10 times on the Savannah River. Industrial use averages 2,130 mgd, mostly for steam-electric power. Public water supplies use 370 mgd, mostly from streams in northern Georgia and from wells in the Coastal Plain of southern Georgia. Rural supplies use about 91 mgd, and irrigation only 37 mgd. Base flows of streams in the Coastal Plain Much of the low flow in parts of the Coastal Plain in Georgia makes its first appearance as surface flow directly in or very near the channels of the major streams, according to A. N. Cameron and R. F. Carter. The inflow per square mile of surface drainage area for segments of the Ocmulgee, Altamaha, Chattachoochee, and Flint Rivers is many times as large as that for the small tributary streams that enter the major streams in the same segments. During low-flow periods the increments in flow range up to 1,200 cubic feet per second from increments of drainage areas of only 1,000 to 2,000 square miles. Ground water in Glynn County The transmissibility of the principal artesian aquifer in Glynn County, as determined by D. O. Gregg from aquifer tests, ranges from about 480,000 to about 2,000,-000 gallons per day per foot. An average transmissibility of about 1,100,000 gpd per foot was computed by analysis of piezometric maps. Preliminary data indicate that the relatively low transmissibility of the aquifer that underlies the south-central part of Glynn County may be responsible for steep hydraulic gradients in the southern part of the Brunswick Peninsula and in the Jointer and Colonel Islands area.WATER RESOURCES A27 At Brunswick an increase in water use of BO million gallons per clay in late 1962 caused a marked decline of water levels. These ranged from about 20 feet near the center of pumpage, 3 to 4 feet 13 miles northwest and west, 6 to 7 feet 10 miles eastward, and 1 to 2 feet 10 miles southeastward, according to R. L. Wait. Ground water in southwestern Georgia The Dougherty Plain region in Seminole and Decatur Counties, southwestern Georgia, has been shown by C. W. Sever to be one of the most favorable ground-water regions in the United States. In this region, a shallow limestone aquifer is capable of yielding an estimated 20 to 40 million gallons per day to properly developed well fields and is capable of a sustained yield of several hundred million gallons per day within the two-country area. Water resources of Atlanta Metropolitan Area Power operations on the Chattahoochee River at Buford Dam and the reregulation of power waves at Morgan Falls Dam are the principal factors affecting the occurrence of the main water resource in the Atlanta metropolitan area, according to M. T. Thomson and R. F. Carter. During the 1963 water year, 100 percent of the water passing Buford Dam was used for power generation. Peak power on Mondays through Fridays used about 82 percent of the flow. The remaining 18 percent was used for offpeak power during nights and weekends. The five power waves per week would pass Atlanta at night and be wasted if they were not reregulated at Morgan Falls Dam. The reregulation is intended to provide 750 cubic feet per second at all times at Atlanta to satisfy minimum water-supply and industrial needs with peak flows for dilution of sewage during each afternoon to match the pattern of sewage discharge. The desired daily flows, in cubic feet per second, for Saturdays, Sundays, Mondays, and the Tuesday-to-Friday periods, and the duration-curve data for natural conditions before regulation began and for the 1963 water year after reregulation began are shown by the following table: Day Desired flow Percent of time the desired flow was equalled or exceeded Daily Peak Daily Peak Natural 1963 Natural 1963 Saturday .. .. 1, 150 2, 000 75 83 43 70 Sunday 1, 000 1, 500 80 65 60 40 Monday 1, 340 2, 000 66 68 43 55 Tuesday-Friday 1, 510 2, 500 59 76 31 70 The table shows a great increase in the flows available for sewage dilution Tuesdays to Saturdays, which would have been even more impressive if the releases from Buford Dam' had not been severely reduced for 3 months during the winter. The reregulation on Sundays has not been so effective because depletion of the channel storage between Morgan Falls Dam and Atlanta causes a surplus of water at night, when it is not needed, instead of during the Sunday peaks. Attenuation of the power waves complicates the analysis of tests by the city for water-quality control. The waves during the periods of low inflows travel at an average rate of 2.7 miles per hour, but the water itself travels at rates of 0.7 to 1.4 miles per hour. Water samples taken where the dissolved-oxygen concentration is believed to be lowest, 37 miles downstream, represent municipal sewage discharged as much as 2 days earlier. FLORIDA Solution cavities in Tertiary limestone The distribution of cavities in the Tertiary limestone and the general decrease in size and numbers with depth and with distance from recharge and discharge areas suggest to Y. T. Stringfield that the present pattern of circulation developed chiefly during Pleistocene time when sea level stood both higher and lower than at present. During the lowest level of the sea, the water table in the limestone in north-central Florida may have been as much as several hundred feet below the present level, with deep underground drainage to the sea similar to that at the present time in the limestone in northwestern Jamaica. The solution cavities and caverns were formed chiefly in the upper part of the zone of saturation, which rose and declined with changes in Pleistocene sea level. Vertical shafts or natural wells, some of which are several hundred feet deep, were formed by solution of water moving down along vertical joints in the zone of aeration. Water atlas of Florida Maps of Florida that show the distribution of average annual runoff and contain information concerning the most commonly used aquifers have been prepared by W. E. Kenner, W. J. Shampine, and L. W. Hyde as part of a water atlas of Florida. Runoff throughout most of Florida averages between 10 and 20 inches per year. Southern Florida, however, with large expanses of low wet lands averages less than 10 inches per year. Northwestern Florida, with relatively few lakes and swampy areas and relatively steep valleys has a considerably higher runoff, averaging between 30 and 40 inches.A28 INVESTIGATIONS OF NATURAL RESOURCES The Floridan aquifer is the aquifer most commonly tapped for ground-water supplies in Florida. However, in the southern part of the State and along most of the east coast, it contains water with high chloride content, and ground-water supplies are taken from the shallow sand aquifer or, in the Miami area, from the Biscayne aquifer. In extreme northwestern Florida, although water in the Floridan aquifer has a low chloride content, the Floridan is little used as a source of ground water. In this area most ground-water supplies come from a prolific, more easily accessible, sand and gravel aquifer. Water budget of Green Swamp area Hydrologic studies by R. W. Pride, F. W. Meyer, and R. N. Cherry of the Green Swamp area in central Florida during the period 1959-61 show that although surface runoff varied through a wide range from wet to dry years, ground-water outflow and evapotranspira-tion varied little. Water-budget factors for the Green Swamp area show that average rainfall on the area ranged from 70.9 to 34.7 inches, surface runoff ranged from 31.1 to 2.3 inches, ground-water outflow ranged from 1.8 to 2.2 inches, water derived from storage ranged from insignificant amounts to about 4.3 inches, and evapotranspiration losses ranged from 34.5 to 39.1 inches. Quantitative and qualitative data indicate that recharge to the Floridan aquifer in the Green Swamp area is probably no greater than that in other parts of central Florida, although the highest piezometric levels on the Florida peninsula underlie the southeastern part of the area. Geohydrologic data indicate that the high piezometric levels are caused partly by hydrologic barriers formed by faulting and by solution collapse. Recharge of principal aquifer in Orange County The principal recharge area of the Floridan aquifer in Orange County is in the western part of the county and adjoining parts of Lake and Polk Counties. W. F. Lichtler, Warren Anderson, and B. F. Joyner (1-64) delineated the general recharge area by using the shape and slope of the piezometric surface, the relative streamflow from various basins in the county, and a knowledge of the geology of the region. Water resources of Myakka River basin The quantity and quality of surface and ground water are highly variable in the Myakka River basin and the adjacent coastal area. Preliminary data collected by B. F. Joyner, Horace Sutcliffe, and J. D. Warren have revealed that potable ground water is available in limited amounts from the Tampa and Hawthorn Formations in the northwestern part of the basin. Large quantities of ground water from the Suwannee and Avon Park Limestones are suitable for irrigation but not for public supplies because the dissolved solids exceed 1,000 parts per million, the sulfate content exceeds 500 ppm, and the hardness exceeds 500 ppm. All the streams in the basin go dry or recede to very low flows. During low-flow periods, discharge from heavily pumped irrigation wells and some wild flowing wells deteriorates the quality of the surface water. During periods of high runoff, the dissolved-solids content of the water generally is less than 100 ppm. At the beginning of each high-water period, the color index is high, generally greater than 100 color units. Eocene aquifer system of northeastern Florida Mapping of water-bearing Eocene limestones in northeastern Florida by G. W. Leve indicated that the Floridan aquifer there is an aquifer system rather than a single hydraulic unit. The system contains at least three permeable zones separated by relatively impermeable dolomite and limestone beds. The most prolific water-bearing zone is in the Lake City Limestone. Deeper zones contain water under higher artesian pressure than the shallower zones; however, tapping these deep zones may result in a more rapid upward intrusion of deep-seated saline water. Present contamination of the shallower artesian zones occurs in a limited area and is from a combination of vertical and lateral intrusion of saline water. Water supplies of Econfina Creek basin area A study of the Econfina Creek basin in northwestern Florida by R. H. Musgrove, L. G. Toler, and J. B. Foster indicates that ground-water levels along the Gulf coast have been drawn down as much as 60 feet. This drawdown is caused by heavy pumping by industry, municipalities, and military bases. Econfina Creek and small streams bring a supply of over 700 million gallons per day of good water to this area. This supply is being developed to relieve the excessive draft of ground water. PUERTO RICO Chemical character of Rio Espiritu Santo Preliminary studies by Raul Diaz and Rafael Dacosta of the chemical characteristics of Rio Espiritu Santo, which rises in the Luquillo Mountains in northeastern Puerto Rico, indicate that the principal chemical erosion products are silica and calcium carbonate. Somewhat more than 50 percent of the sodium chloride (salt) load transported by the river is a direct contribution from rainfall. Turbidity is extremely low at base andWATER RESOURCES A29 moderate streamflows. Despite the luxuriant, dense vegetative cover, color in the water does not exeed 5 units (Hellige colorimeter-Hazen scale) and is less than 3 units most of the time. In the upper basin, the total dissolved-solids concentrations are no greater than 40 parts per million, and where the stream enters the coastal plain the dissolved-solids content usually is less than 70 ppm, of which silica comprises almost 30 percent. Hardness does not exceed 50 ppm throughout the basin, and in the main stem of Rio Espiritu Santo it usually is less than 25 ppm. Utilization of Rio Loco In a study of the Rio Loco basin, southwestern Puerto Rico, to determine the potential of this predominantly agricultural area for industrial water-supply, N. E: McClymonds concludes that the Rio Loco and Loco Reservoir are the keys to obtaining additional water. On the average, about 8,000 acre-feet of water enters Loco Reservoir annually by natural drainage, and about 80,000 acre-feet enters by diversion from river basins adjoining on the east and north. Of the 88,000 acre-feet total, 18,000 acre-feet is diverted westward for irrigation of Lajas Valley. The remaining 70,000 acre-feet reaches the coastal plain of the Guanica area in irrigation canals (6,000 acre-feet) and in the Rio Loco. Wells pump 15,000 acre-feet annually for irrigation from alluvial deposits on the plain. When ground-water levels are low, up to 200 acre-feet of recharge per day can seep from Rio Loco into the ground-water system. Since much of the discharge of water from Loco Reservoir occurs in slugs at rates of 100 to 600 cubic feet per second related to hydroelectric operations, a large amount of water is lost to the sea. If this water were released with more uniform distribution during the year, it is estimated that another 15,000 acre-feet could be pumped annually from wells; and more could be obtained directly from Loco Reservoir. VIRGIN ISLANDS Test drilling under the supervision of D. G. Jordan and O. J. Cosner indicates that significant quantities of ground water are present on St. Thomas and St. John, U.S. Virgin Islands. Wells having highest yields are developed on the north side of the islands where rainfall is highest, and in guts (valleys) where runoff is concentrated. At present, potable water on these two islands comes from rain catchments, salt-water distillation, or barged supplies from Puerto Rico. The use of local ground water could result in large monetary savings and would give a more stable supply. During periods of heavy surf on St. John, salt water infiltrates beach sands to form a ground-water mound a few feet inland from the shore. The salt water pollutes fresh water moving seaward through the sand. The chemical quality of ground water in some wells on St. Croix deteriorates with depth. Water from shallower depths is potable, but from greater depths is brackish. MIDCONTINENT AREA The midcontinent area, a water-rich region by comparison with the western part of the United States, has its share of problems associated with increasing development and the maldistribution, in time and place, of the existing water resources. Work of the U.S. Geological Survey is directed toward the resolution of these problems, both present and future, by (1) appraising the available water resources in terms of quantity and quality and locating new and undeveloped water sources, (2) investigating specific problems to provide hydrologically sound guidelines for their solutions, and (3) improving hydrologic knowledge to facilitate water-management practices based on thorough understanding of the hydrologic environment. In response to an increasing demand for water and water information, the available supply has been appraised in many political and drainage units in the midcontinent States. These investigations indicate a generally abundant water supply and serve as a basis for orderly development of new facilities to meet accelerating public-supply, irrigation, and industrial water demands. In a few such studies, previously unknown ground-water sources have been discovered that add significantly to the available supply. For example, in Winston County, Ala., subsurface geologic studies revealed a previously untapped bedrock aquifer now being developed for municipal supplies. In Iowa, Minnesota, and other north-central States, studies continue to reveal buried bedrock valleys and aquifers of limited areal extent capable of yielding adequate supplies in some otherwise water-deficient areas. Specific problems of declining ground-water levels, deficient streamflow, and local overdevelopment of water sources have required increasing attention. The need for an alternate and supplemental supply for the city of New Orleans has led to exploration and confirmation of large reserves of ground water in deep aquifers underlying Lake Pontchartrain. In Missouri, expanding industrial activity in the Joplin area aroused increased interest in developing ground-water supplies from abandoned mines. Declining water levels in aquifers in Baton Rouge, La., will present future salt-water encroachment problems than can be resolved by planned development based on recently completedA30 INVESTIGATIONS OF NATURAL RESOURCES studies in the area. Deficient streamflow recorded in southern Michigan, as elsewhere in the midcontinent States, provides emphasis to the need for water-storage facilities and coordinated use of ground- and surface-water resources. Knowledge of the hydrologic environment has been furthered by increased emphasis on interrelations of ground and surface waters and the physical factors controlling their movement. Streams and aquifers that are hydraulically connected offer favorable conditions for coordinated use of the total water resource of an area, plus opportunity for artificial or induced ground-water recharge and storage of excess stream runoff. Studies in the glaciated northern part of the midcontinent area show numerous possibilities for improved water development and management practices utilizing these concepts. MINNESOTA Aquifers in glacial Lake Agassiz Prior to pumping tests by R. W. Maclay, T. C. Winter, and G. M. Pike, it was not certain whether adequate ground water for municipal supply could be developed in the water-poor area in the lake plain of glacial Lake Agassiz. Tests near Stephen, Marshall County, show that wells in a shallow aquifer of very fine sand and silt about 50 feet thick can furnish enough water for a town supply. Wells capable of yielding 50 gallons per minute can be constructed by proper screening and sand packing. Beneath the lake plain of glacial Lake Agassiz are many similar aquifers that are potential sources of moderate quantities of ground water. WISCONSIN Ground water in central Sand Plains region Glacial deposits in the Wisconsin River basin are sources of abundant ground water, and development can be increased significantly without seriously affecting water levels or depleting streamflow. Studies by C. L. R. Holt (1-63) in Portage County indicate that wells yielding 1,000 to 2,000 gallons per minute can be developed and ground-water pumpage increased substantially. Declines of water level and lake stages during 1955-60 were caused by deficiency in precipitation rather than irrigation pumpage. In the lower and central valley of the Wisconsin River, large-capacity wells can be developed in the highly permeable glacial deposits, and the annual rate of ground-water withdrawal is far less than the available supply. An abundant ground-water supply is available from the principal aquifer, which is estimated to be as much as 165 feet thick, according to R. W. Devaul and L. J. Hamilton. Ground-water potential of bedrock aquifers R. D. Hutchinson found that ground water of good chemical quality is available in moderate to large quantities from bedrock aquifers in Kenosha and Racine Counties. An important sandstone aquifer yields 1,000 gallons per minute or more to wells, and the Niagara Dolomite locally can yield as much as 500 gpm. In 1963 the total ground-water withdrawal in the 2 counties was about 2 million gallons per day, an amount that can be exceeded greatly without adverse effects. P. G. Olcott reported that sandstone aquifers of Cambrian and Ordovician age in Winnebago County can be developed much more extensively than at present. In the eastern part of the county, however, a zone containing water with more than 1,700 parts per million dissolved solids and more than 900 ppm sulfate limits ground-water development. In this area, where population and industry are concentrated, surface water is generally a more satisfactory source of supply. In the Milwaukee-Waukesha area J. H. Green and R. D. Hutchinson (2-64) found that ground-water pumpage from the sandstone aquifer has shifted to the northwest from near downtown Milwaukee. The water level declined about 98 feet in the northwestern part of the area during 1950-61 as a result of this shift. MICHIGAN Ground-water basins in Marquette iron range A study by T. G. Newport in the Marquette iron range area indicates substantial disparities between effective sizes of ground-water drainage basins and surface drainage basins. Water-level observations show that the ground-water divide is about 3 miles west of the topographic divide between the Chocolay and East Branch Escanaba River basins, and that ground water moves eastward from the Chocolay basin into the Escanaba basin. Where large differences in elevations between adjacent topographic basins exist, such disparities in effective size of ground-water basins can generally be expected. DroughI conditions in southern Michigan Computation of 1963 streamflow records is reported by L. E. Stoimenoff to show that runoff for the 1963 water year in the southern half of the Lower Peninsula was generally the lowest since 1931. New minimum daily mean discharges were reported for many gaging stations, and levels in 5 of 23 lakes that have been gaged for 15 years or more declined to new lows. Lakes Michigan and Huron fell to new lows in January 1964. In December 1963, ground-water levels were at new lows (based on records since the mid-1940’s) for the 17th consecutive month in the south-central part of theWATER RESOURCES A31 Lower Peninsula. Cumulative precipitation deficiency of as much as 19 inches for the past 2 yeaTS in southern Michigan is the principal cause of the drought condition. At Lansing the precipitation for 1962 and 1963 was in the lowest decile for the 100-year period beginning in 1864. OHIO Sandstone aquifers in northeastern Ohio A regional study by J. L. Rau of the most important of the bedrock aquifers in northeastern Ohio indicates that small to moderate supplies of ground waiter may be obtained from the Cussewago Sandstone of Mississip-pian age and Berea Sandstone of Devonian or Mississip-pian age. The Cussewago Sandstone yields potable water in parts of Ashtabula, Trumbull, Portage, and Mahoning Counties. The average thickness of the aquifer is about 50 feet, but it exceeds 80 feet in about 30 percent of the area. The Berea Sandstone yields potable water in a 3,500-square-mile area, where its thickness averages about 40 feet. The most promising areas for development of moderate supplies of ground water from one or both of these aquifers are in southern Cuyahoga, Geauga, northern Portage, southeastern Ashtabula, and Trumbull Counties. Adequate ground water at Lancaster An investigation by G. D. Dove shows ample ground water to be available from glacial sand and gravel deposits in the Hocking River valley near Lancaster, Fair-field County. This source can be contaminated, however, by substantial increase of ground-water withdrawal and consequent induced recharge, through the highly permeable glacial deposits, of wastes discharged into the Hocking River. Ground water in Miami River valley Electric-analog model studies by A. M. Spieker in the Miami River valley indicate that the glacial-out-wash aquifer in the Fairfield-New Baltimore area should be able to sustain pumping of at least 80 million gallons per day, or 3 times the present rate of withdrawal. The valley-train aquifer, which is about 2 miles wide and 150 to 200 feet thick, can be recharged by induced infiltration from the Great Miami River along the 15-mile length of the modeled area. INDIANA Surface-water supplies in Delaware County More than 50 base-flow measurements by R. E. Hog-gatt in the Mississinewa River basin above Marion and the White River basin above Noblesville show a general downstream increase in streamflow per square mile of drainage area for both streams. Stream discharges were greater than 0.01 cubic feet per second per square mile for approximately 80 percent of the area and 0-0.009 cfs per sq mi for about 20 percent of the area. C. R. Collier and J. H. Klingler found that the dis-solved-solids content of water in the Mississinewa and White Rivers and their main tributaries ranged from 240 to 1,900 parts per million during the base-flow period. Walter from the Mississinewa River and its tributaries contained from 337 to 1,900 ppm dissolved solids, and its hardness ranged from 300 to 700 ppm. Dis-solved-solids content of water in the White River system ranged from 240 to 732 ppm, and hardness from 200 to 438 ppm. In both stream systems dissolved-oxygen and detergent parameters used to measure stream pollution were generally within permissible limits set by health authorities. Aquifers in glacial outwash deposits J. S. Rosenshein and J. D. Hunn (2-64) differentiated four lithologic units of glacial deposits in Porter, La Porte, and St. Louis Counties, one unit of which is the principal source of ground water in northwestern Indiana. Regional transmissibility of this aquifer ranges from about 45,000 gallons per day per foot in Porter County to about 65,000 gpd per foot in La Porte County. The potential supply available from this source is much greater than the quantity now being withdrawn. In Yigo and Clay Counties, west-central Indiana, L. W. Cable and F. S. Watkins found the most important source of potential ground-water supply to be the glacial sand and gravel deposits in the Wabash and Eel River valleys. IOWA Ground water in Linn and Cerro Gordo Counties Limestone of Silurian age is one of the most important sources of ground water in Linn County. It supplies large quantities in Cedar Rapids, one of the industrial centers of eastern Iowa. R. E. Hansen reported that extensive pumpage from this aquifer has lowered the piezometric surface more than 50 feet since the 1920’s; however, the aquifer can continue to supply increasing quantities of water. Alluvial deposits filling buried bedrock valleys are also important but little-developed sources of large quantities of ground water. More than 10 million gallons per day is pumped from alluvial deposits in the city of Cedar Rapids. The Jordan Sandstone, the principal bedrock aquifer in Iowa, is extensively developed in the Mason City area, Cerro Gordo County. Large municipal and industrial withdrawals from the aquifer have caused aA32 INVESTIGATIONS OF NATURAL RESOURCES water-level decline of 140 feet in the Mason City area in the last 50 years. Ground water in Mississippian limestone Studies by P. J. Horick and W. L. Steinhilber show that rural domestic and small municipal ground-water supplies can be obtained from limestone of Mississippian age in most of Iowa. The quality of water from this source is suitable for most purposes in much of the State; however, in south-central Iowa the quality deteriorates because of gypsum and anhydrite deposits in the source rock. Sodium and fluoride contents of the water are high in a few localities. Drift-filled bedrock valleys as ground-water sources Test drilling and associated studies by J. W. Cagle indicate that buried bedrock valleys filled with glacial drift are favorable areas for moderate ground-water development in south-central Iowa. Test drilling in Decatur, Clarke, Wayne, and Lucas Counties indicates as much as 425 feet of drift overlying these bedrock valleys. In much of the area the underlying bedrock yields moderate quantities of ground water, but locally the water is highly mineralized and generally inadequate to meet present-day needs. Water resources of central Iowa Water is available in sufficient quantity to supply the needs of a 10-county area in central Iowa and, according to F. R. Twenter and R. W. Coble, will be adequate also for most future industrial requirements. The principal sources of water are streams, shallow alluvial aquifers, and deeper bedrock aquifers. The average flow in the major streams is more than 2.8 billion gallons per day. Shallow alluvial aquifers contain a minimum of 500 billion gallons of water in storage. Because these deposits are readily recharged they yield large quantities of water and are the principal source of ground water in central Iowa. Bedrock aquifers also contain large quantities of water, probably more than 35,000 billion gallons, and are important sources for many community supplies. The quality of water in streams and alluvial aquifers is generally good, and the water can be used for most purposes. Water in the bedrock aquifers, however, varies in composition according to aquifer and depth. In the south and southeastern parts of the area where the ground water deteriorates in quality with depth, alternate supplies are available from shallow aquifers along streams or from the streams themselves. MISSOURI Mine water used by industries in southwestern Missouri A large volume of water is in storage in abandoned zinc-lead mines in the Joplin area, according to E. J. Harvey. Early in 1964 about 3 million gallons per day was pumped from 7 mines in the area. Since these mines represent only a small part of the total mined area, a much larger quantity of water is available for future development. Pumping for industrial use, exclusive of mining and milling operations, began in the early 1940’s but increased considerably in 1958. The chemical quality of the mine water varies areally and with time. Iron content of water from one mine ranged from 0.21 to 12 parts per million over a period of 5 years, and the pH ranged from 7.3 to 5.9. Low-flow characteristics of Missouri streams According to studies by John Skelton of low-flow characteristics of Missouri streams, poorly sustained base flows are prevalent in the Till Plains (north of the Missouri River) and the Cherokee Plains (extreme west-central part of the State). Well-sustained base flows were noted in the spring-fed streams of the Ozark Plateau section. Preliminary analysis of data indicates that streams have been observed dry at least once at 40 percent of the continuous-record stations, 90 percent of which are located in the Till Plains and Cherokee Plains regions. The records also show that 12 percent of all continuous-record stations have a median annual minimum 7-day flow of zero, and 87 percent of these are in the plains regions. KENTUCKY Water supply at Mammoth Cave National Park Studies of additional water supply for Mammoth Cave National Park by R. V. Cushman, R. A. Krieger, and J. A. McCabe indicate that ample supplies of water of suitable quality can be obtained from streams in the area to meet any anticipated requirement. TENNESSEE Ground water in Highland Rim area Field investigations by R. H. Bingham and*G. K. Moore (2-63) in Montgomery County show that many wells in the northeastern part of the county yield water containing as much as 1,000 parts per million of sulfate. The source of this constituent is believed to be gypsum along partings and bedding planes in the St. Louis and Warsaw Limestones. Preliminary study by J. H. Criner in the valley of Trace Creek near Waverly indicates a large amount of ground-water underflow through alluvial deposits filling the bedrock valley. Moderate supplies of ground water are believed to be available in this area, one of the most promising in middle Tennessee for industrial development.WATER RESOURCES A33 New well field in “500-foot" sand in Memphis D. J. Nyman, in a study of the new Lichterman well-field site, found evidence that clays capping the “500-foot” sand aquifer have been breached by Nonconnah Creek 1 mile north of the well field. When the well field begins operation early in 1965, pumping an anticipated 8 million gallons per day, recharge to the aquifer will be induced from Nonconnah Creek and the chemical quality of the water being pumped may undergo gradual change. ALABAMA New source of ground water in Winston County A study of the subsurface geology of Winston County by W. J. Powell revealed extensive solution development near the contact of the Bangor Limestone and the Hartselle Sandstone at a depth of about 1,100 feet. Water in this solution system, based on interpretation of electrical logs and drilling reports, is of more satisfactory quality and quantity for municipal and industrial use than water in the overlying Potts-ville Formation. This interpretation has been verified at Lynn, where water from the solution system was tapped for the first time as a source of municipal supply for the town. Decline of artesian head in Pickens County K. D. Wahl has observed that numerous wells in Pickens County that previously flowed have ceased flowing or decreased in rate of flow owing to a decline of artesian head. This decline has been caused by the discharge of about 2 million gallons per day, of which 1.8 mgd is not for beneficial use. The total municipal and industrial use of ground water in Pickens County is about 1.4 mgd, or less than the amount currently flowing to waste. MISSISSIPPI Quality of water related to aquifer permeability In northeastern Mississippi, B. E. Wasson has found that the normal increase, with depth, of mineral constituents in ground water is reversed locally in aquifers of Cretaceous age. Mineral content usually increases downdip in aquifers in Mississippi; however, Cretaceous aquifers in northeastern Mississippi are more permeable with depth, and the deeper water in them sometimes contains less dissolved mineral salts. Tertiary aquifers have a more patternless range of permeability and contain water that generally is more mineralized in each successively deeper aquifer. The occurrence of very permeable aquifers containing good quality water at great depth is a large factor in the potential water-supply development in northern Mississippi. Ground-water supply in Alcorn County Pumping tests by Roy Newcome and J. A. Callahan (1-64) show wide variations in transmissibility of an aquifer in fractured chert of Paleozoic age at Corinth. In the northern part of the city, values of transmissibility are double those in the southern part, and four times those in the industrial park less than a mile south of the city. Test drilling to locate additional supply wells in the chert aquifer for municipal and industrial needs therefore is likely to be more successful in the northern area. Potentially the Paleozoic chert offers possibilities for additional withdrawal of moderately large water supplies of excellent quality. The water is superior in quality to that from the shallower Coffee Sand, which contains excessive iron but which is an important reserve supply. Aquifers overlying Tatum salt dome, Lamar County Studies by J. W. Lang, E. J. Harvey, R. V. Chafin, and R. E. Taylor have revealed 3 significant aquifers in the 900-foot section of Miocene clay and sand overlying the oaprock of the Tatum salt dome and 1 aquifer in the limestone part of the caprock. Exploratory drilling and testing have shown that the mile-wide flat-topped rock-salt stock, which has penetrated Tertiary and older formations, is covered by a caprock 500 to 600 feet thick. In descending order the caprock consists of limestone, thin beds of gypsum, and anhydrite. The limestone is Very cavernous and fractured and contains comparatively fresh water. Studies of water quality and water-level data indicate that ground water moves from an artesian aquifer in the Vicksburg Group on the flank of the dome into the limestone aquifer in the caprock and slowly percolates upward into the overlying Miocene strata. (See also “Investigations Related to Nuclear Energy, vela uniform Program.”) LOUISIANA Potential salt-water encroachment in Geismar-Gonzales area R. A. Long reported that large quantities of fresh water are available in most of the Geismar-Gonzales area of Ascension Parish from depths as great as 600 feet. The area is the approximate southern boundary of flushing of connate water from most of the aquifers that lie below a depth of about 300 feet. Structural and lithologic features of the aquifers complicate the fresh-water-salt-water relations. Pumping can induce encroachment of brackish or salty water from the lower parts of some of the fresh-water aquifers, laterally within aquifers, and from underlying salt-water aqui-A34 INVESTIGATIONS OF NATURAL RESOURCES fers having a higher artesian head. No significant water-level decline has been caused by pumping, and water levels remain from a few feet above to about 20 feet below the land surface. The most significant changes of ground-water levels are caused by changes in stage of the Mississippi River. Ground water pumpage in Greater New Orleans area Ground-water withdrawal from the “700-foot” sand in the New Orleans area has increased from about 5 million gallons per day in 1890 to about 51 mgd in 1962. J. R. Rollo reported that although the transition zone between fresh and salty water in the aquifer passes through this area, increased pumping does not appear to have caused significant advance of the salt-water-fresh-water interface. Most of the pumping is from wells located along the interface, and the pumping is believed to have formed a protective barrier that prevents the northward migration of the salt-water front. Water pumped from many of these wells is slightly to moderately saline; however, its salinity does not greatly restrict its use for air conditioning and cooling in industrial processes. Fresh ground water under Lake Pontchartrain G. T. Cardwell, M. J. Forbes, and M. W. Gaydos report that preliminary analysis of electrical logs of oil and gas wells and test holes in and around brackish Lake Pontchartrain indicates that fresh ground water underlies the entire lake. Depths to the base of fresh water range from 600 to 700 feet below sea level at the south Shore to 3,000 feet below sea level at the north shore. Water wells about the lake margins suggest that the water is soft and is confined under artesian heads as much as 120 feet above sea level. INTERSTATE INVESTIGATIONS Sparta Sand environmental studies Sand-percentage maps of the Sparta Sand, prepared by J. N. Payne (1-64), indicate a change in environment from predominantly deltaic in Arkansas, Louisiana, and Mississippi to predominantly nearshore in Texas. A comparison of sand percentage, maximum sand-unit thickness, and total thickness of fresh-waterbearing sand with available pumping-test data shows good correlation between sedimentation, lithology, and transmissibility. Initial studies of water quality in the Sparta Sand suggest a relation between maximum sand-unit thickness and water quality. Water resources of the Mississippi embayment region M. S. Hines, A. J. Calandro, and P. R. Speer found that streams in the embayment section of southern Arkansas that receive their base flow from sands of the Claiborne Group have better sustained low flows than those that receive their base flow from other geologic units. Streams that lie in the Quaternary alluvium and terrace deposits west of Crowley Ridge near lat 35° N. have relatively low base flows, but farther south at about lat 32°30' N. in Louisiana where larger streams such as Bocuf River, Tensas River, and Bayou Macon are incised into aquifers in the basal part of the alluvium, the base-flow yields are higher. In the embayment as a whole, the low-flow indices for streams east of the Mississippi River in Alabama, Mississippi, and Tennessee are much higher than those for streams west of the Mississippi River and north of Tennessee. E. H. Boswell (2-63), G. K. Moore, and L. M. Mac-Cary found that aquifers of Cretaceous age are used as sources of water supply in an area of about 30,000 square miles and are potential sources in an additional 15,000 square miles. The more extensive aquifers of Cretaceous age, the Ripley, Eutaw, and Gordo Formations, are in the eastern and northern parts of the embankment. Generally these aquifers are not extensively developed, the total withdrawal being about 90 million gallons per day. R. L. Hosman reported that data from a deep test hole drilled near Pine Bluff, Ark., indicate a new potential ground-water supply for a large area in the south-central part of the State (chapter D). The Carrizo Sand, virtually an undeveloped aquifer in Arkansas, was found to contain fresh water at a depth of more than 2,000 feet. The Carrizo Sand had not been tested previously, primarily because it is overlain by shallower highly productive aquifers. It represents an important ground-water reserve in the event that existing supplies are depleted and become inadequate to meet increased water demands. Ground water in Wabash River basin A reconnaissance investigation by F. A. Watkins (3-64) and P. R. Jordan indicates that large supplies of ground water are available for development in the Wabash River basin. The magnitude of the supply is indicated by the overflow of ground water into the rivers, which exceeds 3,400 cubic feet per second during base-flow periods. Nearly all this overflow is from the shallowest of the 3 principal aquifers, the glacial outwash, which yields more than 500 gallons per minute to wells less than 200 feet deep near the major streams. Limestone formations in the northeastern part of the basin yield 200 to 500 gpm to wells that penetrate about 300 feet of the aquifer, but deeper wells in the limestone produce salty water. A buried river valley extending west from Tippecanoe County, Ind., is filled with glacial outwashWATER RESOURCES A35 deposits that yield 100 to 500 gpm to wells 100 to 400 feet deep. Hardness of nearly all the water from these 3 sources is greater than 250 parts per million, but the water is suitable for many uses after little or no treatment. ROCKY MOUNTAIN AREA The wide diversity of hydrologic, climatic, and physiographic conditions, as well as expanding cultural developments, gives rise to varied and complex water problems in the Rocky Mountain area. Included in this discussion are 12 of the 17 Western States; the States of California, Oregon, Washington, Idaho, and Nevada are excluded. Most critical are supply problems in the arid regions of the Southwest, where “population explosions” in urban centers are resulting in rapidly increasing demands on available supplies. There is an expanding interest in the development of ground water and the possibilities for the management of underground reservoirs to supplement surface-water supplies. Overdevelopment resulting in the lowering of water tables is cause for concern in many areas and has increased the demand for quantitative evaluation of ground-water resources. Several years of deficient precipitation have also accelerated interest in the evaluation of total water supplies and in the need for conservation. Problems of quality of both surface and ground waters are of considerable concern in many areas. The use and reuse of available supplies, whether for irrigation, domestic, or industrial uses, inevitably cause some deterioration in quality. Moreover, many prospective supplies may be unsuitable for some uses, because of natural pollutants. Investigations of the U.S. Geological Survey are directed toward the collection of water facts and the conduct of studies that will aid in the resolution of these water problems. Some of the significant results of these investigations in the Rocky Mountain area are reported in the following section. MONTANA Thick valley fill in Missoula structural valley As part of a ground-water investigation of the Missoula structural valley by R. G. McMurtrey, R. L. Konizeski, and Alex Brietkrietz, a gravity survey aided in determining configuration of the bedrock floor of the valley and indicated a maximum thickness of fill of about 2,750 feet. Large development of artesian water in eastern Montana An investigation by O. J. Taylor of the Fox Hills-Basal Hell Creek artesian aquifer on the western flank of the Cedar Creek anticline in eastern Montana indicates that very little recharge occurs in the narrow outcrop, because of low precipitation, low aquifer trans-missibility, and small outcrop areas. About 4 billion gallons of ground water will be withdrawn from industrial wells in the artesian aquifer in the next 21 years, which can be expected to affect artesian head in wells west of the anticline and the water table in the outcrop area. Ground water in Missouri River valley An investigation of the Missouri River valley of northeastern Montana by W. B. Hopkins indicates that a considerable amount of water is available for irrigation, municipal, and industrial use but that water quality is a problem locally. Six lines of test holes were drilled across the bottom land to determine the thickness and extent of permeable gravel in the valley fill. Permeable gravel averages about 30 feet in thickness at the base of the valley fill, and is widespread but not uniformly distributed. Pumping tests indicate well yields as great as 1,500 gallons per minute where the gravel is more than-20 feet thick. Water from wells near enough to the Missouri River to induce infiltration of water from the river generally is of better quality. High artesian head in part of Judith Basin Studies of the western part of the Judith Basin, Mont., by E. A. Zimmerman reveal that the artesian head in some wells is more than 160 feet above land surface. These high artesian heads were measured in wells that penetrate sandstone beds in the Kootenai Formation of Early Cretaceous age—one of the most used aquifers in the western part of the Judith Basin. The water from this aquifer generally is of good quality, although dissolved gases in water from wells of high head make it corrosive to casing and plumbing. NORTH DAKOTA Drainage reversal in Burleigh County According to P. G. Randich (1-64), the preglacial eastward drainage channels in Burleigh County also were ice-front valleys of southwestward-moving glaciers. The largest concentrations of buried and surficial gravel, which yield water freely to wells, are along the northern edges of these channels. Tributaries generally contain only fine-grained sediments, are narrow, and have steeper gradients than the main channels. The present drainage is westward. Extensive sand aquifer in Richland County Q. F. Paulson and C. H. Baker, Jr., report that test drilling in Richland County indicates an extensive and productive aquifer in the sand deposits of the SheyenneA36 INVESTIGATIONS OF NATURAL RESOURCES delta (chapter D). More than 100 feet of medium-to coarse-grained sand was penetrated in some places. The ground water generally has a low dis-solved-solids content but is hard, and locally it contains considerable iron. Recharge potential is good, as the sand is exposed over a wide area. The water table generally is less than 10 feet below the land surface. The Sheyenne River picks up a considerable amount of ground water along its course through the delta. Buried-valley aquifer in Barnes and Stutsman Counties According to T. E. Kelly, the Spiritwood buried-valley deposits underlie approximately 350 square miles of western Barnes and eastern Stutsman Counties. Also, logs of test holes drilled north of Sutton, in Griggs County, 13 miles north of the Barnes County line, suggest a northward extension of the buried-valley deposits. Two aquifer tests in November 1963 on wells 12 miles apart in the buried-valley deposits indicate a coefficient of transmissibility of approximately 30,000 gallons per day per foot and a coefficient of storage of 0.008. This extensive aquifer, which contains water of fair to good quality, is virtually undeveloped at present. Buried outwash aquifer in Foster County Henry Trapp, Jr., reported that test drilling in northwestern Foster County indicates that the Carrington aquifer, a buried outwash sheet, adjoins other outwash bodies at different levels. Wells in the aquifer supply the town of Carrington and the Carrington irrigation branch station. Properly constructed wells yield as much as 1,700 gallons per minute. Outwash in the area is found from the surface to depths of about 100 feet, but the principal aquifer, the Carrington, is about 50 feet below the surface. Buried valley of Yellowstone River in Divide County Studies in Divide County by C. A. Armstrong indicate that wells in the larger outwash deposits yield as much as a few hundred gallons per minute, but that wells in small stringers of sand near prairie potholes generally yield only enough water for domestic use. Test drilling indicates that the buried preglacial valley of the ancestral Yellowstone River is considerably lower than that of the ancestral Missouri River. WYOMING Ground water in Powder River Basin Completion of hydrologic studies of the western part of the Powder River Basin by M. E. Lowry, H. A. Whitcomb, T. R. Cummings, and R. A. McCullough reveals that supplies of ground water adequate for stock and domestic use generally can be developed from relatively shallow wells in the Wasatch and Fort Union Formations. Flowing wells are common because of artesian head and, in some places, because of gas pressure in the aquifers. The chemical quality of the water differs greatly throughout the area, ranging from good to poor. Supplies adequate for moderate-to large-scale irrigation development probably can be obtained from the Tensleep Sandstone and from cavernous zones in the Madison Limestone in a narrow band along the western margin of the basin in central Johnson and northern Sheridan Counties. However, the strata dip steeply basinward, and drilling to them would not be feasible beyond a short distance from the outcrop. The chemical quality of the water near the outcrop is good enough that the water should be suitable for irrigation. At present, irrigation water is obtained largely from streams. Productive aquifer in Grand Teton National Park A previously untapped alluvial aquifer was found east of Jackson Lake in Grand Teton National Park by J. McGreevy and E. D. Gordon (1-64). More than 100 feet of saturated sand and gravel was located in the Pilgrim Creek valley north of Jackson Lake Lodge. Yields of several hundred gallons per minute are available, and the water is of good quality for drinking and most other uses (100 parts per million of dissolved solids). A public-supply well drilled in 1964 to provide additional water for developments at Colter Bay and at Jackson Lake Lodge yields 270 gpm. Much larger yields are available from this aquifer to meet increased future requirements. SOUTH DAKOTA Summary of water resources In a description of the water resources of South Dakota, J. E. Powell, J. E. Wagar, and L. R. Petri29 report that municipal water systems delivered 54.5 million gallons per day in 1960, an average of 132 gallons per capita per day. About 96 percent of the supply came from ground water. Ground-water supplies for irrigation in 1960 totaled 77,000 acre-feet, 45 percent of all water used for irrigation. Deep ground water in western South Dakota According to C. F. Dyer and M. J. Ellis, several oil-test holes drilled recently at widely separated localities have supplied valuable information on the artesian-water resources in western South Dakota. At least two of the holes have been completed as water wells. One oil-test hole in northeastern Stanley County was drilled to a total depth of 3,992 feet, plugged back to 2,538 feet, 28 J. E. Powell, J. E. Wagar, and L. R. Petri, 1964, Water resources, in Mineral and water resources of South Dakota : U.S. 88th Cong., 2d aess., Senate Comm, on Interior and Insular Affairs Kept. [In press]WATER RESOURCES A37 and gun-perforated from 2,412 to 2,430 feet. The well flows about 50 gallons per minute of warm highly mineralized water. Shut-in pressure at the land surface is 151 pounds per square inch. The water-bearing unit is a bed of gray sandstone 18 feet thick that is probably a basal Cretaceous sandstone deposited on an erosion surface of Jurassic age. No other wells are known to obtain water from this unit. Estimate of withdrawal of water from Dakota Sandstone C. F. Dyer and A. J. Goehring report that an estimated 62 million gallons per day of water is withdrawn from the Dakota Sandstone in 21 counties of southeastern South Dakota. This estimate is much higher than earlier ones. Rural users withdraw nearly 61 mgd; about 24 mgd by wells flowing more than 20 gallons per minute, about 33 mgd by wells flowing less than 20 gpm, and about 3.6 mgd by pumped wells. Municipalities withdraw 1.6 mgd by pumped or flowing wells. At least two-th.irds of the 24 mgd withdrawn by wells flowing more than 20 gpm is unused. (See also “Ground Water.”) Ground water in glacial drift in Sanborn County Studies by L. W. Howells indicate that more than 2.2 million acre-feet of water is in transient storage in glacial-drift aquifers that underlie more than 400 square miles of Sanborn County. Although the water is somewhat saline, it can be used for irrigation if salt-tolerant crops are grown and salinity-control practices are followed. Although relatively undeveloped, the Greenhorn Limestone is an aquifer throughout much of the county. Water from the Greenhorn normally is soft, saline, of sodium sulfate type, and contains as much as 4.5 parts per million of boron. Geochemical and drilling data indicate that the Greenhorn receives recharge of very hard calcium sulfate water from the Dakota Sandstone near highs in the Precambrian surface in southeastern Sanborn County. Ground water in Skunk Creek-Lake Madison area According to M. J. Ellis and D. G. Adolphson, the glacial outwash in the Skunk Creek-Lake Madison drainage basin is not fully developed as a source of ground water, and can yield large additional supplies for irrigation and industrial use. In 1962, the outwash held an estimated 167,000 acre-feet of ground water in transient storage. Water from the outwash is very hard, but otherwise is of good quality; most of it is suitable for irrigation and industrial use. Of the estimated 768,000 acre-feet of water that enters the drainage basin each year as precipitation, 44,500 acre-feet leaves by surface runoff, about 700 acre-feet leaves by ground-water outflow, and the rest, 722,800 acre-feet, is lost by evapotranspiration. Large outwash aquifer in Big Sioux River basin M. J. Ellis and D. G. Adolphson report that glacial-outwash deposits occupy an estimated 55,700 acres in the Big Sioux River drainage basin in South Dakota, between Brookings and Sioux Falls, and have great potential for future ground-water development. Test drilling indicates that the outwash sand and gravel deposits are as much as 50 feet thick and average about 25 feet in thickness. Springs on Pine Ridge Indian Reservation M. J. Ellis reports that springs at contacts along the northern and southern boundaries of the Pine Ridge Indian Reservation are an important source of good quality water, particularly along the northern edge of the reservation, where the aquifers used elsewhere are thin or absent. The springs along the northern boundary are at contacts between (1) terrace deposits and the Pierre Shale or White River Group, (2) Arikaree Formation and White River Group, and (3) eolian sand deposits and the White River Group. Along the southern boundary of the reservation, the springs occur at the contact between eolian sand deposits and the Ogallala Formation or the Arikaree Formation. NEBRASKA Saline water migrates from underlying Dakota Sandstone Philip A. Emery reports localized bodies of saline water in some Pleistocene aquifers in the southeastern comer of Saline County, apparently owing to movement of water with high chloride content from the Dakota Sandstone into the overlying Pleistocene deposits. , Huge ground-water reservoir beneath Adams County Although more than 650 irrigation wells each yield an average of about 1,000 gallons per minute to irrigate more than 60,000 acres in Adams County, C. F. Keech reports that the ground-water supply will be adequate for many years to come. During the last 10 years, water levels in wells in the vicinity of Hastings have declined an average of more than half a foot per year, but in the later years, water levels generally have declined at a smaller rate, and some have risen. Thick deposits of saturated sand and gravel of Pleistocene age underlie all of Adams County and contain an estimated 11.5 million acre-feet of water. Precipitation is the principal source of recharge to the reservoir, but some seepage from the tri-county irrigation district, which is irrigated with water diverted from the Platte River, enters by underflow from the west.A38 INVESTIGATIONS OF NATURAL RESOURCES UTAH Summary of water resources In a report on statewide mineral and water resources, M. T. Wilson, R. H. Langford, and Ted Amow (U.S. Geological Survey, 9-64) show that Utah’s water supply is substantial, but is small in relation to the large area and potential water demand of the State. Annual runoff averages 7,600 million gallons per day. Fresh-water use in 1960 was about 3,900 mgd, mostly for irrigation, which accounted for 3,350 mgd. Hydroelectric power, a nonconsumptive use, required about 1,800 mgd. Saline water from faults contaminates shallow aquifers in Tooele Valley J. S. Gates reports that wells and springs near three inferred faults in Tooele Valley yield thermal water of high chloride content which apparently rises along the faults and contaminates shallow ground water. Four springs and 31 of 34 wells near the inferred faults yield water that contains more than 300 parts per million chloride and is from 2° to 32° F above normal ground-water temperature. Water from 2 of the springs and 5 of the wells contains more than 1,000 ppm chloride and averages 17° F above normal. Little change in quality of wells and springs Utah now has a network of 295 wells and springs in areas of considerable population and water development, from which analyses of water are collected periodically to determine changes in quality of water. C. A. Horr reports that analyses of water samples collected during 1957-62 have shown very little change in chemical character, except for ground water in southern Pavant Valley (reported in 1963 by R. W. Mower in U.S. Geological Survey, 18-63, p. 439) and from a few wells in other areas. Seasonal changes in content of dissolved solids are less than 10 percent from most wells. Total content of dissolved solids in most wells is less than 1,000 parts per million, but ranges from about 100 to 3,000 ppm. Additional ground-water development possible in upper Sevier River basin According to C. H. Carpenter, G. B. Robinson, Jr., and L. J. Bjorklund, large quantities of ground water are stored in valley fill of the upper Sevier River drainage basin above Kingston. Sand and gravel beds in the upper 200 feet alone (more than 800 feet thick in some places) contain about 1 million acre-feet of water. The annual discharge of ground water from the alluvium includes about 27,000 acre-feet from springs, 43,-000 acre-feet by evapotranspiration, 3,000 acre-feet from wells, and 3,000 acre-feet from drains. This repre- sents about 8 percent of the water in storage in the upper 200 feet of alluvium. It is estimated that about 15,000 acre-feet of additional ground water might be developed from the alluvium in the various valleys by lowering water levels and thus salvaging part of the water discharged by evapotranspiration. Sinkholes in alluvium give clue to hidden solution openings in limestone According to L. J. Bjorklund and G. B. Robinson, Jr., sinkholes in the north half of Scipio Valley, a closed basin, and in the hills to the north have developed along fault lines in limestone beds of the North Horn and (or) Flagstaff Formations of Late Cretaceous and Tertiary age. Solution channels drain Scipio Valley and control ground-water levels in the northern half of the valley; water from the valley moves through the channels and discharges from Moulten and Blue Springs. An apparent lack of large fluctuation in spring discharge indicates that a large amount of water is in storage. Great Salt Lake approaching stabilized low level Great Salt Lake reached its lowest level in recorded history on November 1,1963, when its elevation receded to 4,191.3 feet above mean sea level. This is a decline of 20.3 feet from the all-time high recorded in 1873. The decline in lake level has also reduced the water area from 1,500,000 acres to about 600,000 acres, with a proportionate reduction in evaporation losses. It is believed that at present levels, inflow and evaporation are about equal and that the lake level will not recede materially in the near future. Reduced water supply in northern Utah Valley, R. M. Cordova reports that the amount of surface inflow to northern Utah Valley generally has declined since 1946, even though the amount of imported water has increased. It is assumed also that the amount of recharge to ground water also has declined. However, the decreased recharge and increased pumping have not caused water-development problems in the area. COLORADO Summary of water resources In a statewide summary on water resources, John W. Odell, Donald L. Coffin, and Russell H. Langford find that a substantial supply of water is available in most of Colorado, particularly in the mountain areas adjacent to the major streams, and in areas underlain by extensive aquifers. Supplies generally are of good quality in the mountain areas but deteriorate progressively downstream owing to increased mineralization caused by return flow from irrigation and to contami-WATER RESOURCES A39 nation from industrial and municipal wastes. An average of about 16 million acre-feet runs off in the major streams. In 1960 about 10.8 million acre-feet was used, mostly for irrigation. Interstate compacts and Supreme Court decrees limit consumptive use to somewhat less than half the average yield of water. Future development of water resources will depend increasingly on additional storage, reuse of available supplies, and management practices that reduce consumptive use by nonbeneficial plants and increase efficient use of surface- and ground-water supplies. Ground water in Pueblo and Fremont Counties A study by H. E. McGovern, E. D. Jenkins, and Robert Brennan describes the quantity and quality of ground water from the Pleistocene and Recent deposits in parts of Pueblo and Fremont Counties. During the study, average pumpage in the area was 37,O0O acre-feet per year, and average annual diversion from the Arkansas River and Fountain Creek was 412,000 acre-feet. About 75,000 acre-feet, or 26 percent, of the water diverted for irrigation below Pueblo was available for reuse through return flow and ground-water recharge. Recharge from floods along Middle Big Sandy Creek Flow measurements by D. L. Coffin in the Big Sandy Creek valley of east-central Colorado indicate that percolation of flood flows is a major source of recharge. This is indicated by rising water levels in wells during floods and by the downstream exponential decrease in channel width. Measurements indicate that about 3 feet of water is recharged during a bankfull flood. The data also indicate that the vertical permeability of the valley fill is less than 1/10 of the horizontal permeability. Irrigation wells increasing in Colorado high plains The number of irrigation wells tapping the Ogallala Formation of the Colorado high plains is increasing at a rate of about 100 per year. In 1963, at least 525 irrigation wells were being used, each of which pumped more than 300 gallons per minute, according to A. J. Boettcher. Comparison of the water requirements of the crops and the average per acre use indicates that the amount of water pumped in 1962 (72,500 acre-feet) was about the same as the potential consumptive use computed by the Blaney-Criddle method. Water management in Arkansas River valley A pilot study by E. A. Moulder and others (2-63) of a 25-milefreach of the Arkansas Valley has shown that the ground-water reservoir can provide additional supplemental water for irrigation and that substantial amounts of water now consumed wastefully by phreato-phytes can be salvaged. Analysis of ground-water and surface-water records for 1940-60 indicated that the consumptive use of water in the study reach increased by about 20,000 acre-feet, although the irrigated acreage remained practically the same. The major factor causing increased consumptive use is the increased use of ground water to supplement the surface-water supply. KANSAS Ground-water levels in Grant and Stanton Counties J. D. Winslow, C. E. Nuzman, and S. W. Fader (1-64) report that ground-water levels in Grant and Stanton Counties continued to decline at an alarming rate during 1963. Water-level-change maps show the decline in water levels from the 1940 base to be more than 90 feet in the area of greatest decline, approximately 8 miles southeast of Ulysses. The decline has been more than 20 feet over an area of approximately 570 square miles. Increased dissolved solids and chloride in South Fork Ninnescah River A quality-of-water survey in April 1963 and monthly data from four chemical-quality stations in the South Fork Ninnescah River basin indicated to A. M. Diaz the location of an increase in total dissolved-solids and chloride content. The major increase in chloride concentration occurs between Cairo and Cunningham and is caused principally by inflow of natural brines from underlying formations of Permian age and from localized pollution of shallow ground water in or near oil fields. Total dissolved-solids and chloride concentrations ranged from 217 to 1,150 parts per million and from 12 to 534 ppm, respectively, in the main stem. The water in most of the tributary streams is of good quality and has a relatively low dissolved-solids contents. ARIZONA Ground water in Big Sandy Valley, Mohave County An investigation of the Big Sandy Valley, Mohave County, by William Kam, indicated that Recent stream deposits are capable of yielding large quantities of water to wells. In the 21-year period 1940-60, water levels in observations wells showed little net change, indicating that draft has not exceeded the perennial recharge to the aquifer. Surface and subsurface outflow, excluding floodflow, is about 2,000 to 3,000 acre-feet per year. Water shortage at Williams due to leaky reservoirs The city of Williams has a serious water-supply shortage despite average annual precipitation exceeding 20 inches. Studies by B. W. Thomsen indicate that the 7 public-supply reservoirs impound sufficient surface runoff in 1 year to meet 'the demand for several years, but 746-002 0 - 64 -4A40 INVESTIGATIONS OF NATURAL RESOURCES that seepage from the reservoirs results in rapid escape of the stored water. The rocks underlying the reservoirs are highly permeable, and the seepage probably drains to the regional water table, which is more than 2,300 feet below land surface at Williams. Aquifer serves as regulating reservoir for Verde River An annual water yield of about 5,000 acre-feet is obtained from 165 square miles of a dominantly granitic mountainous area in Maricopa County that receives an average annual precipitation of 18 inches, according to B. W. Thomsen and H. H. Schumann. Only 5 percent of this water reaches the Verde River as surface flow over a 9-mile reach of alluvial channel below the mountain front. Only when flow from the hard-rock area exceeds 200 cubic feet per second does any surface flow reach the Verde River. The 95-percent “loss” is temporarily stored in the ground-water reservoir formed by permeable materials in the lower 9-mile reach of the stream. Some of this water is lost by evapotranspira-tion and some is slowly released to the Verde River as underflow out of Sycamore Canyon. Ground-water movement in Mogollon Rim area One of the controls of water movement in the Mogollon Rim area of northern Arizona is the relation of topography to structure. Compilation of structural data by T. L. Finnell indicates that a 5-mile-wide belt of northwestward-trending en echelon high-angle faults and small domes extends along the steep south-facing Mogollon Rim for about 20 miles west of Show Low, in Navaj o County. This belt forms a structural barrier to the migration of ground water which normally would move northward down the regional dip to the Little Colorado River basin. Instead, water percolating along permeable beds is probably deflected southward to issue as springs that feed the Salt River. Ground-water flow net aid* hydrologic studies in central Arizona According to W. F. Hardt, a ground-water flow net including the central part of Arizona from Red Rock to Phoenix shows that (1) regional groimd-water movement corresponds to major drainages and is locally deflected by the mountains, (2) the ancestral Gila River probably was formerly north of its present course in the reach from Florence to the Salt River, and (3) the average coefficient of transmissibility of the alluvial aquifer is about 100,000 gallons per day. Streams could supply one-third of water needed by Fort Huachuca S. G. Brown, L. R. Kister, and B. W. Thomsen report that about one-third of the average water demand of Fort Huachuca, Cochise County, can be met from the flows of creeks and springs in the Huachuca Mountains. Use of this water would relieve some of the demand on the present well field. The water from the creeks and springs has a very low sediment and total dissolved-solids content, and would be suitable for use in the present water system with minimum treatment. In places the water from creeks and springs is supersaturated with calcium carbonate, which must be removed before recharge through wells or infiltration pits could be practiced with any water in excess of the demands of the fort. NEW MEXICO New well for Carlsbad Caverns supply According to W. A. Mourant and J. S. Havens (1-64), one of several test holes drilled in the Rattlesnake Springs area, Eddy County, could be developed as a well that will readily yield the 225 gallons per minute required for the Carlsbad Caverns water supply, and probably would yield more than 1,000 gpm. The quality of the water in Rattlesnake Springs improves when the pool is lowered by pumping of irrigation wells to the southwest. The better quality water entering the pool probably moves from the west or northwest through solution channels in conglomerate. Deep test well yields rare gases A test well 1,675 feet deep drilled at Mesita pueblo, Valencia County, in search of a water supply yielded appreciable amounts of carbon dioxide, nitrogen, helium, and argon. According to G. A. Dinwiddie, the well penetrated 1,620 feet of the Triassic Chinle Formation and 55 feet of the Permian San Andres Limestone. Water from a zone in the San Andres between 1,649 and 1,650 feet flowed 4 gallons per minute at the surface, had a temperature of 60°F, and a specific conductance of 23,000 micromhos at 25°C. Analysis of gas from the well indicated mainly carbon dioxide and nitrogen and some helium and argon. Water from another zone in the San Andres from 1,663 to 1,665 feet increased the flow to 15 gpm, had a temperature of 83° F, and a specific conductance of 25,000 micromhos. Another analysis of the gas yielded similar results. Although the water was unsuited for domestic use, the test is of interest because of the rare gases that issued with the water. In .adjoining Bernalillo County, H. E. Koester reports significant differences in the composition of gases yielded with ground water. Carbon dioxide is the principal gas present, composing as much as 98.4 percent of some samples from along the eastern flank of the Acoma sag. Nitrogen and helium exceed 2 percent only in deeper parts of the Acoma sag. Helium appears to be restricted to the San Andres Limestone and theWATER RESOURCES A41 Glorieta Sandstone (both of Permian age); only trace amounts were yielded from rocks of Pennsylvanian age. Ground-water supplies in southern San Juan Basin A recent well-drilling program on public domain lands in the southern San Juan Basin in northwestern New Mexico indicates that small to moderate amounts of water, suitable for livestock and construction use, can be obtained from sedimentary rocks of Late Cretaceous and Tertiary age underlying the area, according to M. C. Van Lewon. Of 39 wells, 13 yielded in excess of 20 gallons per minute, 24 yielded from 4 to 20 gpm, and 2 yielded less than 3 gpm and were abandoned. Depths of the wells ranged from 125 to 960 feet, and water levels stood as much as 486 feet below the land surface. Total concentrations of dissolved solids in the water ranged from approximately 500 to 8,000 parts per million. Yields of more than 100 gpm of moderately mineralized water were obtained from sandstones in the Nacimiento Formation. All formations in the Mesa Verde Group yielded from 5 to 50 gpm of water more highly mineralized than that obtained from the Nacimiento. Yields from the Ojo Alamo Sandstone generally were small, probably because of the high degree of cementing. Small yields of water containing hydrogen sulfide were obtained from coal beds in the Fruit-land Formation. A few wells tapped standstone beds in the upper part of the Kirtland Shale. Very small yields of highly mineralized water were obtained from the Pictured Cliffs Sandstone, and no water of usable quality was found in the Lewis Shale. OKLAHOMA Summary of water resources In study of statewide water resources, T. B. Dover, A. R. Leonard, and L. L. Laine estimate that the annual water supply averages roughly 17 billion gallons a day, not all of which can be captured, as for example, excessive flood waters. About 1 billion gallons a day is withdrawn for use, two-thirds of it surface water, mostly in the east, and one-third ground water, mostly in the west. Future growth of water use is indicated by recent growth in a 20-year period: irrigation, from 3 to 240 million gallons per day; municipal, from 90 to 200 mgd; and industrial, from 30 to 520 mgd. Undeveloped ground-water reserves in Woodward County P. R. Wood and B. L. Stacy (1-63) report that the ground-water resources of Woodward County are largely undeveloped. They estimate that approximately 1.3 million acre-feet of ground water is stored in the unconsolidated alluvial deposits of the North Canadian River valley and about 3 million acre-feet in the Ogallala Formation, which covers the southwestern part of the county. Present use of water from wells for all purposes in the county is less than 10,000 acre-feet per year. Alluvium of Arkansas River valley is a reservoir Recent studies by Harry H. Tanaka indicate that a ground-water reservoir of considerable magnitude underlies the 100-mile segment of the Arkansas River valley between Muskogee, Okla., and Fort Smith, Ark. The total area of the alluvium is about 90,000 acres, its thickness averages 42 feet, and the thickness of saturated material averages about 27 feet. Assuming an average specific yield of 20 percent, the available water stored in these deposits totals almost half a million acre-feet. Annual recharge to the alluvium is computed to be 9 inches, or approximately 60,000 acre-feet. Total annual pumpage from the alluvium (in 1963) was estimated to be 1,700 acre-feet, or less than 3 percent of annual recharge. The water table in the alluvium declined an average of about 7 feet during 1962 and 1963, because of deficient rainfall. At Webbers Falls, near the middle of the segment, precipitation was about 27 inches less than the normal 86 inches for the 2-year period. Because they respond rapidly to recharge from precipitation, water levels are expected to recover promptly when precipitation returns to normal. Surface-water resources of Kiamichi River basin L. L. Laine (1-63) finds that base flow in the Kiamichi River basin is small in the Ouachita Mountain province, which comprises the larger part of the basin, but that there is considerable pickup of ground water in the Coastal Plain province, in the lower part of the basin. From samples collected during • base-flow periods, T. L. Cummings concluded that the surface water of the basin is of excellent quality for most domestic, industrial, and agricultural uses. The water is soft, and the specific conductance generally is less than 100 micromhos at 25°C. Streams draining rocks of Mississippian and Pennsylvanian age in the Ouachita Mountains generally contain less chloride than those draining Cretaceous rocks of the Coastal Plain province. Surface water in Little River basin A study by A. O. Westfall (1-63) of streamflow records in the Little River basin in southeastern Oklahoma shows that during the period 1930-61 the surface-water yield averaged 2.4 million acre-feet per year and ranged from 1 million acre-feet in the worst drought year to almost 5 million acre-feet in wet years.A42 INVESTIGATIONS OF NATURAL RESOURCES TEXAS Electric analog duplicates operation of Houston aquifer An electrical analog model of the aquifer underlying the Houston district was constructed under the direction of E. P. Patten, Jr., from data compiled and analyzed by L. A. Wood and R. K. Gabrysch (1-64). The model was tested and modified until it would duplicate historical water-level-decline maps for different periods of pumping. After it was verified that the model was an analog of the aquifer, water-level decline through 1970 was predicted from the amount and distribution of future pumping as estimated by city of Houston officials. Base flow of Sabine River, Texas-Louisiana S. P. Sauer and Jack Rawson found that in 268 miles, the base flow of the Sabine River increased from 43.4 to 470 cubic feet per second. The largest gains were in the southern half of the study area. Much of the gain was attributed to direct ground-water accretions to the main stem; measured tributary inflow was 218 cfs, only about 51 percent of the total gain. The dis-solved-solids concentrations in the main-stem water ranged from 118 to 505 parts per million. In some reaches the amount of dissolved solids, particularly sodium chloride, increased significantly; but in other reaches the dissolved solids decreased much more than could be ascribed to the volume and quality of measured inflow. The wide variation of sodium chloride indicated intermittent pollution of the river by slugs of brine. Base flow of Blanco River H. D. Buckner and G. L. Thompson (1-64) found that the 15-mile reach of the Blanco River upstream from Wimberley, Tex., had an increase in base flow of 28.4 cubic feet per second exclusive of 14.2 cfs tributary inflow. The study was made of the 27-mile reach upstream from Wimberley and included the site proposed for the Cloptin Crossing Reservoir. The upper 12 miles of the reach lost all surface flow (1.5 cfs measured) to the exposed Hensell Sand and Cow Creek Limestone Members of the Travis Peak Formation. In the reach crossed by the Spring Branch fault (about 12 miles upstream from Wimberley), springs discharge about 14 cfs into the Blanco River. In this reach, water under hydrostatic head in the lower member of tlie Glen Rose Limestone or in the Cow Creek Limestone Member, or in both, evidently moves upward along the fault zone and discharges through the gravels of tlie streambed. The Tom ('reek fault (alx>ut 7 miles upstream from Wimberley) was found to be taking 1.6 cfs streamflow, while the Wimberley fault sys- tem was discharging about 12 cfs in the 6-mile reach immediately upstream from Wimberley. Base flow of Lampasas River W. B. Mills and Jack Rawson (1-64) found that during periods of base flow, the lower 80 miles of the Lampasas River in the Brazos River basin is a gaining stream. In the reach studied, the flow increased from 2.27 to 16.0 cubic feet per second, a gain of 13.7 cfs. Tributary inflow was 19.2 cfs. Dissolved solids ranged from 887 parts per million near the head of the reach to 247 ppm near the mouth. The water with the higher dissolved-solids content at the head of the reach was contributed by Sulphur Creek, a spring-fed stream. Below the confluence of Sulphur Creek with the Lampasas River, ground-water accretions and tributary inflow generally diluted the river water. Base flow of Cibolo Creek P. H. Holland and C. T. Wellborn (4-64) found that the base flow increased from no flow to 18.6 cubic feet per second in the lower 80-mile reach of Cibolo Creek. Base flow in the upper 23 miles of the reach was sustained solely by sewage effluent (1.77 cfs, including flow from storm sewers) from the Randolph Air Force Base complex near San Antonio. About 95 percent of the base-flow gain found in the 80-mile reach originated in a 27-mile reach beginning about 23 miles downstream from Randolph Air Force Base. The inflow in this reach came from rocks of the Wilcox and Claiborne Groups; about 70 percent from the Carrizo Sand of the Claiborne Group. In the lower 30 miles of the reach, although a gain of only 0.4 cfs was found, considerable interchange of ground and surface water is indicated. COLORADO RIVER BASIN Effects of water use on Upper Colorado River basin A study of the effects of natural factors and water-use developments on stream regimen in the Upper Colorado River basin recently completed by W. Y. Iorns, C. H. Hembree, and G. L. Oakland indicated that with the facilities existing in 1957 for storage, withdrawal, and use of water, the average annual yield of water from the upper basin as measured at Lees Ferry, Ariz., was 12.733 million acre-feet. Average annual dissolved-solids discharge was 8.676 million tons, and the weighted-average concentration was 501 parts per million. Had the developments not been in existence the hypothetical average annual water yield at Lees Ferry would have been about 15.2 million acre-feet, the hypothetical dissolved-solids annual discharge would have been about 5.2 million tons, and the hypothetical average concentration would have been about 253 ppm. Substantially all the increase in dissolved-solids dischargeWATER RESOURCES A43 is construed as an effect of irrigation on 1.4 million acres of land, which contributed an average of 2.4 tons of dissolved solids per irrigated acre per year. From one part of the area to another, this contribution ranges from 0.1 ton to 5.6 tons. Most of the water originates from the melting of snow in the mountains and high plateaus, but most of the dissolved solids comes from the lower parts of the basin where little water is contributed to the streams. The rocks exposed in the mountains generally are more resistant to the solvent action of water than the rocks which underlie the lowlands. Man’s activities are mostly confined to the lowlands where rocks of Tertiary and Cretaceous age are at the surface. PACIFIC COAST AREA The Pacific coast area comprises the States of Alaska, Washington, Idaho, Oregon, Nevada, California, and Hawaii. Collectively, the area is characterized by a widely diversified spectrum of water-resources problems. The difficulties in overcoming these problems are compounded by the extreme contrasts in geologic and hydrologic environment, and by the ever-increasing demands of industry, public supply, and crop production. The problems are rendered more complex by the effects, sometimes deleterious, of multipurpose water demands on existing surface-water and ground-water reservoirs. One of the most spectacular hydrologic features of the several States that constitute the Pacific coast area is the extreme range in precipitation. Places occur in each of the States where the average annual precipitation is 8 inches or less. Places also occur in each, except Idaho and Nevada, where the average rainfall exceeds 100 inches—in Washington and Alaska, over 200, and in Hawaii, over 400 inches. Unfortunately, the areal distribution of rainfall does not correspond with the regional water demands. As a result, much of the runoff in some areas is not used and probably never will be consumed within the watershed. Elsewhere, irrigation or public-supply and industrial demand so greatly exceeds the local available runoff that importation of water is necessary. Examples of such areas are southern California and central Washington. Locally, such as in much of the Puget Sound lowland in Washington, application of prudent water-management policies can insure an equitable balance between available water and multipurpose demand for many years in the future. The IT.S. Geological Survey currently is making water-resources studies in all States in the Pacific coast area. The studies are designed to solve urgent problems when the need is greatest and to provide hydro-logic data for areas where problems are incipient or inevitable. In the first category are studies, largely quantitative, of artificial recharge, sustained yield, surface- and ground-water relations, chemical and physical quality, well-field development, and flow forecasting. Included in the second category are areal ground-water appraisal studies, observation-well and gaging-station networks, reconnaissance sediment and chemical-quality determinations, estimated sustained-yield studies, and peak-discharge observations. ALASKA An important aspect of the water-resource program in Alaska concerns the development of water supplies for communities and military installations. Although surface water is available at many places and in abundant quantity, winter freezeup of streams renders its year-round use impracticable in many parts of the State. Although ground water can satisfy much of the domestic and municipal demand, even this source of supply has limitations. Where the ground is perennially frozen, in many places to great depths, obtaining any firm water supply may be difficult or impossible. The program of the U.S. Geological Survey encompasses a hydrologic data-collection network, including sampling for sediment load, on many of the streams as a basis for flood-frequency studies, and for the evaluation of streams for waterpower potential. The Geological Survey also makes investigations of the chemical character of ground and surface waters. Some effects of the Alaskan earthquake of March 27,1964, involving water facilities are described in the section on “Alaskan Earthquake.” Summary of water resources In a report on the statewide water resources, A. O. Waananen and G. C. Giles (U.S. Geological Survey, 8-64) show that Alaska has enormous resources of water and power that are still at a very early stage of development. Alaska, with an estimated 17 million kilowatts of waterpower at potential and developed sites, ranks second only to Washington, among the States, in this resource. Installed waterpower facilities in Alaska produced 76 megawatts of power in 1960 and used about 410,000 acre-feet of water—about half of 1 percent of the resource estimated to be available. Public water supply sought at Angoon W. N. Lockwood (1-64) finds that not enough ground water could be developed from steeply dipping marble and schist at Angoon to meet the demands of the village. Of 3 wells drilled, 1 was dry and the other 2 yielded 1 gallon per minute or less. Possible alternate sources of supply include (1) ground water in buried beach gravels under muskeg swamps, (2) ground water inA44 INVESTIGATIONS OF NATURAL RESOURCES deposits of Eocene age on Favorite Bay, and (3) impoundment of surface water in a tidal flat near Killisnoo. Ground-water supply at King Salmon found adequate A. J. Feulner (1-63) reports that an adequate supply of ground water is available at the village of King Salmon and the U.S. Air Force station there. Supplies of water in excess of 100 gallons per minute can be developed from wells that tap aquifers in the outwash-plain deposits that underlie the village to a depth of 300 feet or more. Existing wells that range in depth from 97 to 228 feet below land surface yield as much as 100 gpm. PACIFIC NORTHWEST The Pacific Northwest comprises the States of Idaho, Oregon, and Washington. Within this area is included most of the drainage basin of the Columbia River, and the Puget Sound lowland, which is an area of potentially great industrial development. Although the Pacific Northwest, as a whole, has enough water to support the area’s anticipated development, numerous water-resource problems are evident. These include unbalanced areal development of surface-water and ground-water potential, water logging, conflicts in water use, and pollution of streams and shallow ground-water bodies. The Geological Survey program in the region includes studies of chemical and physical properties of water, (see also “Distribution of Minor Elements as Related to Public Health”) occurrence and distribution of ground water, low flow of streams, the effect of de-nudiation on streamflow and sediment content, and probable future base flow. The location of water supplies in national parks, Indian reservations, and at military installations is a significant part of the program. Springs common in Columbia River Basalt The layered arrangement of the permeable interflow zones in the Columbia River Basalt and the relatively low permeability of the rock elsewhere result in many permanent springs, even where the annual precipitation is only 10 inches. According to R. C. Newcomb those springs give much of the region a fairly good and widespread supply of water for stock and wildlife, in contrast to the inhospitable deserts where similar amounts of rain falls on the highly permeable and sievelike lavas of some of the Pleistocene volcanic rocks elsewhere in the Pacific Northwest. Ground-water supplies adequate in Thurston County, Wash. On the basis of an appraisal of ground-water resources in Thurston County, Wash., J. B. Noble and E. F. Wallace report that throughout much of the popu- lated parts of the county, enough water can be supplied from wells to satisfy most or all the municipal and rural domestic and irrigation demand. Virtually all the ground water now developed or capable of development occurs in glacial or interglacial permeable deposits of Pleistocene age. Locally along the shore of Puget Sound, salt-water intrusion has occurred and water from a few wells is affected. In the upland part of the county, where rocks of Tertiary age are exposed or are near the land surface, attempts to develop water have met with little success; these rocks are of low permeability almost everywhere and the ground water is, in general, of poor quality. Ground-water yield of Spokane River basin In a study of the usable-water yield of various components of the Spokane River basin, R. L. Nace shows that the ground-water yield of this basin east of Spokane is equivalent to a continuous flow of 1,00 cubic feet per second. Exceptional spring discharge to Green River, Wash. In a study of water resources in King County, Wash., J. E. Luzier and Donald Richardson measured an exceptionally large amount of discharge from springs into the bedrock gorge of the Green River near Black Diamond, Wash. Springflow along an 11-mile section of the gorge is as much as 175,000 gallons per minute during the winter, decreasing to about 2,000 gpm during the summer. About half the discharge is from four springs; many small springs and seepage zones account for the remainder. A thick and areally extensive deposit of glacial outwash through which the Green River has carved its course is the principal ground-water reservoir. Conserving stock water in Oregon In a reconnaissance of stock-water resources in the Lakeview Grazing District in southern Oregon, F. F. Zdenek found that long narrow pits dug in small ephemeral lakes provide an effective means of storing small amounts of runoff. These pits hold water during most of the summer, much longer than most shallow basins, and permit the use of grazing land and forage that otherwise would be wasted. Construction of these pits are suggested for remote areas where development of ground water through wells is not feasible. Summary of water resources in Idaho In a summary on statewide water resources, W. I. Travis, H. A. Waite, and J. F. Santos report that although Idaho is generously supplied with water, there is considerable maladjustment of supply and demand, both areally and in time. Average annual inflow is 32.4 million acre-feet and outflow is 66.5 million acre-feet—WATER RESOURCES A45 a contribution to downstream areas of 34 million acre-feet. About 2.6 million acre-feet of ground water was withdrawn in 1960 as the sole or principal supply for irrigation of more than 800,000 acres of land. Nearly 3 million acres are irrigated in the Snake River basin of Idaho and Oregon. Most of the water resources are suitable for irrigation, and for most other uses only a minimum of treatment is needed. Spring contribution to Snake River declining C. A. Thomas reports that the Snake River between the gaging stations at Milner, Idaho, and King Hill, Idaho, has gained more than 7,500 cubic feet per second on the average during the period 1910-62. The gain is largely from scores of springs within a 46.5-mile reach along the north bank, which discharge water from an aquifer beneath the Snake River Plain. The aggregate flow of the 21 springs was 3,380 cfs in 1902, 5,380 cfs in 1956, and 4,300 cfs in 1962. Based on correlation with total inflow between the Milner and King Hill gaging stations, the discharge of the springs increased markedly from 1902 to 1917, probably as a result of irrigation on the Snake River Plain. The discharge increased at a lesser rate from 1917 to 1946, remained relatively steady from 1946 to 1959, and then declined in the period 1959 to 1962. The decline since 1959 indicates that increased pumpage from the aquifer has more than offset the effect of factors that tend to increase discharge. Precipitation and evapotranspiration in Malad River basin Studies by R. L. Nace and E. J. Pluhowski in the Malad River basin, Idaho, indicate that the annual precipitation ranges from about 15 inches in the lowlands to 30 inches or more in the highest areas and that potential evapotranspiration ranges from about 24 inches on the floor of the basin to 16 inches in the highlands. The average lapse rate was computed to be 2.7°F per 1,000 feet. NEVADA The principal water-resource problems in Nevada are attributable to the relatively small natural supply available to the State. For the State as a whole, the average annual precipitation is less than 9 inches; of this amount, probably less than 8 percent becomes available either as surface-water runoff or as recharge to the valleys. Among the problems are maldistribution of supply, flood damage, low yield of aquifers in some places, water use by phreatophytes, and loss from surface-water bodies by evaporation. According to Nevada ground-water law, if depletion of a ground-water basin is imminent, the State Engineer is empowered to estab- lish necessary regulatory measures for control of the ground-water basin for sound conservation and the best interests of the public welfare. The U.S. Geological Survey is attempting to supply hydrologic information at a rate that will permit effective management of the State’s water resources. An important part of the program is the continuing basic-records inventory for both surface and ground water. Basin or valley studies are categorized as reconnaissance, areal, comprehensive, and specific-problem studies. In sequence, they represent successive stages of work intensity for a given area. Summary of water resources In a statewide report on water resources of Nevada, H. E. Thomas points out that 93 percent of the State’s population live in the 20 percent of the State having the largest perennial sources of water. The rest of the State has a population density considerably less than one person per square mile. Conservation of water in surface reservoirs in the more arid parts of Nevada involves great evaporation losses. Evaporation from Lake Mead, for example, is 3 times as great as the quantity of Colorado River water allocated to Nevada. The preponderant proportion of all the water stored in Nevada is ground water—a volume many times as great as the gross supply received annually by precipitation. Estimates of ground-water yield in desert basins Statewide ground-water reconnaissance studies in Nevada by T. E. Eakin, W. C. Sinclair, Philip Cohen, F. E. Rush, D. E. Everett, and E. G. Crosthwaite provided preliminary estimates of recharge, discharge, and (or) perennial yield for 15 ground-water basins, The preliminary estimates of perennial yield, which provide a management guide, are evaluated from estimates of natural recharge to and discharge from particular ground-water basins. Preliminary estimates of perennial yield for 10 of the ground-water basins studies are: 14,000 acre-feet in Middle Reese River valley, and 9,000 acre-feet in Antelope Valley, Lander County; 40,000 to 50,000 acre-feet for nine basins tributary to the Black Rock Desert, Pershing and Humboldt Counties; 6,000 acre-feet in Virgin Valley, 3,000 acre-feet in Gridley Lake valley, 11,000 acre-feet in Continental Lake valley, and 2,000 acre-feet in Pueblo Valley, Humboldt County; 18,000 acre-feet in the Dixie-Fairview Valley area, Churchill and Pershing Counties; 12,000 acre-feet in Lake Valley, Lincoln and White Pine Counties; and 27,000 acre-feet in the Meadow Valley area, Lincoln and Clark Counties. Interbasin movement of ground water Reconnaissance investigations in several topographically closed valleys in the southeastern part of NevadaA46 INVESTIGATIONS OF NATURAL RESOURCES indicate that estimated replenishment and discharge are not in balance. (See also “Nevada Test Site Studies.”) T. E. Eakin (1, 2, 3-63) finds that most of the discharge occurs by underflow from one valley to another through Paleozoic carbonate rocks. Estimates of annual recharge to valleys having interbasin movement of ground water are: 6,000 acre-feet to Dry Lake and Delamar Valleys, Lincoln County, and 12,000 acre-feet to Garden and Coal Valleys, Lincoln and Nye Counties. Eakin estimates that the recharge from precipitation within Pahranagat Valley is only about 1,800 acre-feet per year, although natural discharge is at least 25,000 acre-feet per year. The excess discharge is supplied by underflow from the surrounding valleys to the north, northeast, and possibly northwest. Ground-water barrier prevents interbasin movement Field determinations of specific conductance, hardness, pH, and iron show a marked difference in chemical character between water in the playa deposits in Rhodes Valley, Mineral County, and that in the alluvial deposits of Soda Spring valley to the north, according to C. T. Snyder. This evidence, coupled with that provided by trends in chemical character of the ground water, suggests strongly that there is a barrier between the two valleys that effectively prevents ground-water movement between them. CALIFORNIA One of the most troublesome water problems in California is the inequitable distribution of supply. In the southern part of the State, where the demand is greatest, the supply is deficient, while the supply is abundant in the northern part of the State, where demand is light. Other outstanding problems are land subsidence, changes in runoff resulting from urbanization, uncontrolled transpiration by phreatophytes, and sea-water intrusion in coastal water supplies. A significant part of the water-resources program in California is the collection and publication of basic hydrologic data. Included is a continuing series of measurements of stream-flow, water levels in wells, chemical quality of water, and sediment in streams and reservoirs. Areal interpretive studies are being made in many parts of the State. Examples of these are the comprehensive appraisal studies in Santa Barbara County, in Antelope Valley, and in the San Joaquin Valley. Urban growth increases volume of storm runoff at Mountain View Urban development has greatly increased the volume of storm runoff produced by rainfall in the city of Mountain View, Santa Clara County, according to E. E. Harris and S. E. Rantz (1-63). The hydro-logic effect of urban growth was studied in a 5-square-mile area that is drained by Permanente Creek and its tributary, Magdalena Creek. Both creeks have permeable streambeds through which water seeps to recharge the underlying ground-water body. In 1945, when the greater part of the study area was orchard, and only 4 percent of the area was covered by impervious surfaces such as roofs and pavements, the volume of local storm runoff was consistently less than the seepage capacity of the channel. The ratio of the total outflow from the area to the streamflow entering was 1.18. By 1958, urban development had reached the stage where 19 percent of the study area had been made impervious. As a result of this increase in impervious surface, the ratio of total flow to inflow rose to 1.70, indicating about a fourfold increase in local storm runoff since 1945. Interbasin movement of ground water in northeastern California Drainage basins between the Warner Range to the east and the Cascade Range to the west are underlain by vesicular, blocky lava flows of Pleistocene and Recent age. These flows are, in turn, underlain by relatively impermeable lava flows of Miocene and Pliocene age. According to R. H. Dale, the flows of Miocene age, exposed in both the Warner and Cascade Ranges, form effective barriers that prevent the eastward or westward migration of ground water. Water levels in wells tapping the permeable lava flows of Quaternary age that underlie the intermontane basins show that ground-water movement is generally southward, from basin to basin. For this reason, ground-water divides, if they exist, do not necessarily coincide with the low topographic divides that separate individual basins. Artificial-recharge study in San Joaquin Valley Preliminary results of detailed studies by R. W. Page indicate that parts of the east slope of the San Joaquin Valley between the San Joaquin and Kings Rivers would be insuited for artificial recharge by water spreading where the slope is underlain by poorly sorted, poorly permeable material, or by extensive clay beds. Except in the area of the Kings River, poorly permeable material extends valleyward about 6 miles from the crystalline bedrock foothills of the Sierra Nevada, and extensive clay beds underlie a belt about 4 miles wide, east of the trough of the San Joaquin Valley.WATER RESOURCES A47 Ground-water supply for Mission Creek Indian Reservation A reconnaissance investigation of ground-water conditions on the Mission Creek Indian Reservation by J. W. Giessner (1-64) shows that a small supply probably could be developed from shallow wells. Mission Creek, the principal stream of this part of the south slope of the San Bernardino Mountains, crosses the reservation, and ground-water storage in the permeable gravel beneath the intermittent stream probably is sufficient to sustain a modest amount of pumping each season. Quality of ground water in Santa Ynez River basin Analyses of water from irrigation wells in the Lompoc subarea of the Santa Ynez River valley, sampled periodically since 1934, suggest deterioration in chemical character of ground water. R. E. Evenson reports that the deterioration in some places is caused by an increase in chloride content and in others by an increase in both chloride and sulfate content. In general, the deterioration attributable to increase in chloride is believed to result from mixing of ground water with connate water from marine sediments. Deterioration characterized by increases in both chloride and sulfate may be due to recycling of irrigation water. Salt-water intrusion in Santa Maria coastal basin Overdraft of the Santa Maria coastal ground-water basin since about 1940 has resulted in a significant decline in water levels throughout the basin as ground water has been removed from storage. Estimates by G. A. Miller and R. E. Evenson of storage depletions are not consistent with estimates of ground-water recharge and discharge. The discrepancy can be accounted for largely by movement of the fresh water-sea water interface at the offshore end of the aquifer system in response to the continued inland decline of head. Natural barrier protects ground-water supplies at Santa Barbara Studies of ground-water supplies in the Santa Barbara city area by K. S. Muir indicate that ground water in storage is protected from sea-water intrusion by an offshore barrier, probably a fault of considerable lateral extent and considerable vertical displacement. This barrier extends at least as far as Carpinteria, 10 miles easterly, and there, too, is an effective natural barrier marking the offshore submarine truncation of the freshwater aquifers. HAWAII Among the vexing water-resource problems in Hawaii are sea-water intrusion, the effect of recurring volcanic activity on the ground-water body, and local overpumping. Water-resource studies include investigations of the base-flow characteristics of streams and their relation to ground water, the amount of precipitation that can be collected from artificial catchments, and drainage-basin yield. Basic data of many different types are being collected. Probably the most unusual are the records of precipitation at the site of the highest known mean annual rainfall in the world, and records of wave action in Hilo harbor. Water supply for Kau area is adequate The water supply of the Kau area of the island of Hawaii appears to be sufficient for normal needs, according to D. A. Davis and G. Yamanaga. Although the average annual rainfall is 125 inches or more in an area of 6 to 10 miles inshore, there is no perennial surface flow to the ocean. There are, however, large springs along the coast that discharge fresh and brackish water. Of those that discharge fresh water, the largest is between Punaluu and Honuapo; its visible discharge ranges from 30 to 50 million gallons per day. Pumpage from the aquifer that yields water to this spring is less than 3 million gallons per day. Perched water is developed through numerous tunnels. The aggregate yield ranges from 1 to 8 mgd. Ptigh-level water is impounded at a height of 230 feet above sea level and is drawn on at a rate of about 1.5 mgd. Tunnel discharge related to precipitation on Oahu C. P. Zones finds a near-linear relation between rainfall and discharge from ground-water tunnels in the Waianae district of Oahu. A plot of cumulative tunnel discharge against cumulative precipitation is a straight line whose slope is a measure of the tunnel discharge per unit amount of rainfall. A long-term change in tunnel discharge relative to rainfall is indicated by a change in slope. This type of plot, or doublemass curve, is being used to evaluate the effects of new ground-water development on the quantities of water discharged from existing tunnels. Several tunnels were constructed near the head of Waianae Valley in about 1900, and two others were built several years later. Graphical analysis of tunnel discharge shows that each time a new tunnel was built, a new equilibrium between tunnel discharge and rainfall was established in less than 5 years. Although discharge of the combined tunnels increased after each new tunnel was built, the yield of preexisting tunnels declined. Ground-water draft in Kahuku area, Oahu The Kahuku area, Oahu, includes 61 square miles of the northern end of the Koolau range and of its bordering coastal plain, which consists of extensive marshes and large irrigated areas. The average annual rainfallA48 INVESTIGATIONS OP NATURAL RESOURCES over the 61-square-mile area is 84 inches or about 273,200 acre-feet per year. K. J. Takasaki finds that the average annual ground-water draft is about 33,000 acre-feet (30 million gallons per day) or roughly 12 percent of the rainfall. Perennial surface-water flow is small and is not utilized. Between 20 and 25 percent of the rainfall flows into the sea as runoff during and after heavy rains. On the basis of preliminary data the average evapotranspiration is estimated at 50 to 60 percent of the rainfall. It is less than 5 percent in the high-rainfall areas and is more than 250 percent in the windy, low-rainfall coastal plain. SALINE WATER RESOURCES Mapping saline ground-water resources of the United States Saline ground water is considered as a natural resource, not a problem, in a map of the 48 conterminous United States prepared by J. H. Feth and others.30 The map illustrates the shallowest known occurrences of saline and slightly saline ground water. Concentration ranges of dissolved solids illustrated are 1,000- 3,000 parts per million, 3,000-10,000 ppm, 10,000-35,000 ppm, and more than 35,000 ppm. Areas inferred to have saline ground water, though no wells have been drilled that encounter it, are also shown. Depth from land surface to the shallowest saline-water occurrence is illustrated in the ranges of less than 500 feet, 500-1,000 feet, and more than 1,000 feet. Investigations of saline waters that pose a threat to fresh-water supplies are reported under the section “Water Contamination Studies.” Saline ground water of Michigan A study of the saline ground-water resources of Michigan by J. R. Rapp and K. E. Vanlier indicates relatively large supplies of saline ground water in the State. This saline water occurs in Paleozoic bedrock underlying glacial drift, which nearly everywhere contains fresh ground water. In the central upland areas the high head of fresh water depresses the fresh-water-saline-water interface considerably below the level of Lakes Michigan and Huron. In the lowland areas ad-jacent to the Great Lakes and along some inland streams, there is little fresh-water head and the interface is shallow. Saline water is discharged into lakes and streams in a few places where the interface is above the level of the stream or lake. The discharge of saline water is facilitated by the basin structure of the bedrock formations which allows the water to move updip from the center of the basin to the lowland areas. The salinity 30 J. H. Feth, compiler, 1964, Resources of mineralized ground water in the conterminous United States : U.S. Geol. Survey open-file rept. of well water increases in areas of large-scale ground-water development where the fresh-water head has been lowered by pumping. Brine is produced for industrial use in many places in the Lower Peninsula. Saline ground water of Utah Ground water ranging from slightly saline (1,000- 3.000 parts per million of dissolved solids) to brine (greater than 35,000 ppm of dissolved solids) occurs in many parts of the Basin and Range, Colorado Plateaus, and Middle Rocky Mountains physiographic provinces in Utah, according to C. A. Horr and others. In the Uinta Basin, lake deposits of Paleocene or Eocene age, and parts of the Mesa Yerde, Uinta, Green River, and Duchesne River Formations and the Mancos Shale contain saline water with a dissolved-solids content of from 1.000 to 10,000 ppm. In southeastern Utah the Mancos Shale and the Mesa Yerde and Morrison Formations produce small amounts of water containing from 1,000 to 10,000 ppm of dissolved solids. Locally, the San Rafael Group and Glen Canyon Group produce similar water. The underlying Paradox Formation contains water with dissolved solids exceeding 35,000 ppm. Scattered occurrences of slightly saline water are found in rocks of Jurassic, Cretaceous, and Tertiary age along the northern flank of the Uinta Mountains. Most of the saline ground-water resources within the State occur in the alluvial valleys in the Great Basin. The saline water in these areas is derived from Lake Bonneville beds and older deposits of Tertiary and Quaternary age and ranges in salinity from 1,000 to over 200,000 ppm of dissolved solids. In general the freshest water is found near the flanks of these valleys and grades into water containing 3,000 to 10,000 ppm of dissolved solids in the lower parts of the valleys. The Great Salt Lake Desert would probably yield ground water having more than 3,000 ppm of dissolved solids. In the Bonneville Salt Flats area there are known occurrences of ground water containing over 200.000 ppm of dissolved solids. Saline ground water of California Studies by J. S. Bader (1-64) indicate large supplies of saline ground water throughout much of California. Ground water containing more than 1,000 parts per million of dissolved solids occurs in about 30 alluvium-filled valleys in the desert area of southern California. Other bodies of saline ground water occur in the San Joaquin Valley and in several other smaller basins as far north as the Oregon border. Wells in these areas are seldom completed and developed when they tap bodies of saline water. Even when completed, the wells are frequently short-lived because of the corrosive action of the water on well casings,MANAGEMENT OF NATURAL RESOURCES ON THE PUBLIC LAND A49 screens, and pumping equipment. However, as the need for water increases and as techniques for desalination are perfected, the large supplies of saline water will become available as a water resource in areas previously considered uninhabitable because of the lack of fresh water. MANAGEMENT OF NATURAL RESOURCES ON THE PUBLIC LAND An expanding economy for the future is dependent upon wise management of the resources of the Nation. The public lands contain a significant portion of these resources, and responsibility for management of the land and use of the resources is exercised by several agencies of the U.S. Government. The U.S. Geological Survey, through its Conservation Division, classifies these lands for such resources as leasable minerals and sites for waterpower projects, and supervises the prospecting, development, and recovery of certain minerals from wells and mines under lease, permit, or license on Federal and Indian lands. Contribution from the Federal lands to total mineral production of the United States is shown on figure 4. The classification functions of the Conservation Division are performed by the Branch of Mineral Classification and the Branch of Waterpower Classification. The supervisory functions are performed by the Branch of Mining Operations and the Branch of Oil and Gas Operations. The Conservation Division also supervises the administration of the Connally Act of February 22,1935. Field offices of the Division are listed on page A227. Geologic and hydrologic work in progress by geologists and engineers of the Conservation Division is given in the list of investigations starting on page A233, under the categories of geologic mapping, glaciology, water- Figure 4. Percentage of total United States mineral production that comes from Federal land. power classification, and various commodities such as coal and petroleum and natural gas. Scientific and economic results of these investigations are published as books and maps in the regular series of Geological Survey publications. CLASSIFICATION OF MINERAL LANDS The principal leasable minerals are oil, gas, oil shale, coal, phosphate, sodium, and potash. Since 1906, public lands believed to contain leasable minerals have been withdrawn from entry by the Secretary of the Interior, on the advice of the Geological Survey, pending their classification as mineral or nonmineral lands. At present about 41 million acres of land is so withdrawn. In order to classify land for its mineral value, the geology must be mapped in detail, usually at a scale of 1:24,000. Existing geologic maps are used where of suitable quality and scale. Mapping for mineral-land classification differs in some details from general geologic mapping in that more measurements of stratigraphic sections per quadrangle are required to show thicknesses of coal or other leasable minerals, and more frequent sampling is necessary to determine mineral quality. Drill-hole cuttings or cores and electric or radioactivity logs provide subsurface data for classification. Samples obtained from surface and subsurface operations are analyzed in the laboratory. When the areal extent, thickness, and grade of mineral deposits are established, the land containing them is classified as to its value for mineral resources. The geologic maps produced for classification purposes are published in the standard map series of the Geological Survey. WATERPOWER CLASSIFICATION Classification of public lands to conserve and utilize water resources was begun in 1888, to preserve reservoir sites for irrigation. It has been continued chiefly for hydroelectric development. Present activity includes stream-basin investigations, a review of land classifications and reserves, and the measurement of selected glaciers. The program of stream-basin investigations is a systematic search for basins and subbasins where water projects can be developed in the future to serve the needs of a growing population. Sites that meet the criteria for classification are set aside by the Secretary of the Interior on the recommendation of the Geological Survey, through procedures established by Congress and the Department of the Interior. Land set aside by these procedures may be disposed of onlyA50 INVESTIGATIONS OF NATURAL RESOURCES according to procedures which provide that it may be reacquired by the Government for purposes of waterpower development without cost. A program to reassess all land classifications and reserves was begun in 1956. Many classifications and reserves had been made before 1920 under Congressional and departmental urging for immediate protection of sites for waterpower development. Because of this urgency many of the classifications were based on inadequate map and hydrologic data. Under the present program all reserves are being reevaluated and classified by rigorous standards. Lands that do not qualify as waterpower sites are removed from the reserves and are opened to disposition under the public-land laws. Progress through fiscal 1964 on this program indicates that as much as 50 percent of lands now reserved for waterpower may eventually be eliminated from the reserves. River and lake basins are mapped mostly at a scale of 1:24,000. Contours of lake bottoms are compiled by precise sounding surveys. The results of investigations are published as special maps and sheets. A special project to gather information on the rates of ablation and the recession or advance of selected glaciers was started in 1941 on Nisqually Glacier in Mount Rainier National Park, Wash., and in 1944 on Grinnell and Sperry Glaciers in Glacier National Park, Mont. Annual measurements are made at monumented cross sections, and the glaciers are mapped fcompletely at 5-year intervals. In 1961, at the request of and in cooperation with the Bureau of Reclamation, measurements were begun on Barrier Glacier, Mount Spurr, Alaska, to determine what effect the growth or shrinkage of the glacier has on fluctuations in the level of Lake Chakachamna. SUPERVISION OF PROSPECTING, DEVELOPMENT, AND RECOVERY OF MINERALS Supervision of operations under mineral leases entails the investigation of lands and deposits under application for mineral leases, oil and gas leases, and prospecting permits; recommendation of lease terms and unit areas; enforcement of operating regulations and measures to assure the safety and welfare of workmen; maintenance of production records; and determination and collection of royalties and rentals. The mineral supervisory branches of the Conservation Division also act as advisors to the Secretary of the Interior, to other bureaus of the Department, and to other Government agencies concerned with the administration of the Mineral Leasing Laws. Royalties from public lands are distributed 52% percent to the Reclamation fund, 37% percent to the States in which the minerals or fuels are produced (except for Alaska, which receives 90 percent), and 10 percent to the Federal Treasury. Royalties from other land categories are distributed in many different ways as provided by law, but the largest share of these royalties is returned directly to the Federal Treasury. Mining operations The Branch of Mining Operations supervises operations concerned with discovery, development, and production of coal, oil shale, phosphate, potassium, solid and semisolid bitumin, and sodium from public land; and of sulfur from public land in Louisiana and New Mexico. The branch also supervises the production of silica sand on certain lands in Nevada; mercury on certain Spanish land grants; all minerals except oil and gas on restricted, allotted, and tribal Indian lands; and all minerals recoverable in commercial quantities, except oil and gas, on acquired lands. The following table shows production of minerals and royalties received from leased Federal lands under supervision of the Branch of Mining Operations for the fiscal year ending June 30,1964. Land category Production (tons) Value (dollars) Royalty (dollars) Public. . 22, 693, 000 159, 809, 000 6, 677, 000 Acquired . . ... 164, 000 2, 309, 000 92, 000 Indian 7, 713, 000 22, 964, 000 2, 234, 000 Total 30, 570, 000 185, 082, 000 9, 003, 000 Oil and gas operations The Branch of Oil and Gas Operations supervises the discovery, development, and production of crude oil and natural gas and associated products from leased public, acquired, Indian, Outer Continental Shelf, and Naval Petroleum Reserve lands. About 12 percent of United States oil production in 1962 came from leases on Federal lands. The following table shows the production of crude oil, the value of petroleum products, and the royalties received from supervised leases on the various categories of Federal and Indian lands during fiscal 1964. Land category Oil production (barrels) Qas production (million cu ft) Liquid petroleum gas (gallons) Value (dollars) Royalty (dollars) 177,800, 000 573, 700,000 433,600,000 567,700,000 72,180,000 Outer Conti- nental Shelf... 114, 200, 000 566,800,000 456,100,000 81,260,000 Acquired lands.. 5, 510,000 77, 240, 000 1,360,000 20, 550,000 2, 585, 000 Military and miscellaneous 2, 510,000 74, 410, 000 80, 600, 000 21,860, 000 4, 506,000 Naval Petro- leum reserves. 4,180, 000 6, 200, 000 13. 500, 000 15,190, 000 1,938, 000 Indian 42,100,000 106,400, 000 158,300,000 133,310,000 17, 510,000 Total 346,300,000 1,404, 750,000 687,360, 000 1,214, 710,000 179,979,000GEOLOGY AND HYDROLOGY APPLIED TO ENGINEERING AND PUBLIC HEALTH A substantial part of the effort of the U.S. Geological Survey is directed toward specific application of geology and hydrology to engineering and public health. Major activities include (1) investigations on behalf of the U.S. Atomic Energy Commission of the geology and hydrology of underground nuclear explosions and disposal of radioactive waste; (2) studies of contamination of water supplies and of the distribution of mineral matter as related to public health; and (3) investigations of geology and hydrology related to engineering problems in construction (including those activities related to nuclear-power reactor sites), mining, water management, and flood control. A timely special activity this year was a study of the geologic aspects of the Good Friday earthquake in Alaska on March 27,1964. INVESTIGATIONS RELATED TO NUCLEAR ENERGY Underground nuclear explosions and the generation of power by nuclear reactors release radioactive products to the geologic and hydrologic environments. In brder to safeguard the public, the distribution, movement, and concentration of these products must be determined and the potential public hazard evaluated. In addition, the engineering and construction of facilities for underground nuclear explosions and nuclear reactors pose unique and difficult problems requiring a thorough knowledge of geologic and hydrologic conditions in a variety of natural environments. Since 1956 the U.S. Geological Survey has provided geologic and hydrologic data on the environment of reactor and underground test sites at the Nevada Test Site, and at sites for the plowshare (peaceful uses of nuclear explosions) and vela uniform (detection of underground nuclear explosions) Programs, and has evaluated these data for the Atomic Energy Commission. During 1963, intensive geologic and hydrologic studies were carried on because of continued underground testing of nuclear devices, increased interest in the peaceful application of nuclear explosions, continued experimentation in the detection of underground explosions, and experimentation leading to the development of nuclear energy for space engines. Hydrologic studies of disposal of radioactive wastes focused chiefly on transport of radioactive materials in streams, particularly in the Columbia and Tennessee River basins; development of acceptable methods of disposing of wastes to the ground; and evaluation of hazards to water supplies from proposed nuclear reactor plants. NEVADA TEST SITE STUDIES Investigations during 1963 at the Nevada Test Site were concentrated on (1) the geologic history and structure of the Timber Mountain and Black Mountain calderas; (2) a geologic-hydrologic appraisal of the Pahute Mesa underground test area; (3) geologic reconnaissance of the region north of the Nevada Test Site; (4) definition of test media and evaluation of the effects of underground nuclear tests in Yucca Flat; (5) interpretation of the subsurface geologic structure of the Nevada Test Site, using gravity and aeromagnetic data; (6) hydrologic studies of the regional ground-water regimen and the effects of a nuclear explosion below the water table; and (7) investigation of the ion-adsorption properties of various rock types used as testing media. During the year, the first 3 geologic quadrangle maps (Tippipah Spring, Oak Spring, and Rainier Mesa), of a projected total of 33 maps for the Nevada Test Site, were published (Orkild (1-63); Barnes, Houser, and Poole (1-63); Gibbons, Hinrichs, Hansen, and Lemke (1-63)). Also published was a report describing the geologic setting of the first underground nuclear explosion—the rainier explosion (Hansen and others, 1-63). Timber Mountain and Black Mountain calderas Geologic mapping has made possible reconstruction of the detailed history of the Timber Mountain caldera and a tentative history of the Black Mountain volcanic center. The wall of the Timber Mountain caldera can be defined reasonably well: it consists of highly fractured pre-caldera tuffs overlain unconformably at many places by tuff probably ejected from beneath the caldera area. Within the caldera, potassium-argon age determinations indicate that the tuffs of Cat Canyon, which form a dome structure, are only slightly older than the tuffs of Ammonia Tanks, which are distributed circum- A51A52 GEOLOGY AND HYDROLOGY APPLIED TO ENGINEERING AND PUBLIC HEALTH ferentially around the caldera on radii as great as 25 miles. Petrographic and chemical analyses indicate that the tuffs are genetically related. The geographic limits of some of the tuffs related to the caldera are incompletely known, but some have been traced south-westward to the California-Nevada boundary, south into the Amargosa Desert, north and northwest to Gold Flat, and east to Paiute Ridge. Dikes of intrusive tuff occur in the inner ring-fracture zone of the caldera and range from a few inches to several tens of feet in width. The dikes are believed to be correlative with one of the uppermost cooling units of the tuffs of Timber Mountain. The Black Mountain area, on Pahute Mesa, 25 miles northeast of Beatty, Nev., was a Pliocene volcanic center which erupted a suite of chemically and petro-graphically distinctive rocks with alkalic affinities. The volcanism is characterized by the successive formation of central volcanoes of intermediate to rhyolitic lavas followed by periods of voluminous rhyolitic ash-flow eruptions. The extent and thickness of rocks produced in each of these eruptive cycles indicate that the volcanism commenced abruptly and continued in episodes of progressively decreasing intensity. Following each major period of ash-flow eruption, the summit area of the preceding volcano collapsed to form a caldera with a major diameter of about 9 miles. Each succeeding group of lavas filled or partly filled the earlier caldera, but the ash flows spread widely to form the welded to nonwelded Thirsty Canyon Tuff (Noble and others, 4-64). The last ash flows were of small volume and were not followed by caldera collapse. Pahute Mesa The complex geology of Pahute Mesa has required the fullest use of many geologic techiques in the evaluation of the mesa as a test area. Drill-hole information indicates that the mesa is made up of more than 13,000 feet of volcanic rocks that were derived from at least four different source areas. Geologic maps by E. B. Ekren and others, and gravity maps by D. L. Healey and C. H. Miller (1-63) have provided the data for the selection and exploration of test sites. In addition, remanant magnetism studies by G. D. Bath, in conjunction with aeromagnetic maps, have delimited the distribution of buried rhyolite lava flows of high water yield. From surface data, K. A. Sargent has identified more than 12 separate rhyolite flows on the basis of their heavy-mineral content. Reconnaissance north of the Nevada Test Site A reconnaissance of the area north of the Nevada Test Site was made to obtain regional geologic information for use in evaluating possible test areas. The Pahute Mesa test area was selected on the basis of infor-mati'on obtained from this reconnaissance. A byproduct of geologic mapping of 2,000 square miles north of the Nevada Test Site by E. B. Ekren, R. E. Anderson, C. L. Rogers, D. C. Noble, and Theodore Botinelly was the recognition of the possibility of buried mineralized areas. Hydrothermal alteration and weak precious-metal mineralization are widespread in the older volcanic rocks, which include lavas and intrusive masses of intermediate composition and which appear to be of the same type as host rocks of ore deposits at Goldfield, Nev. An ash-flow sheet of Pliocene age, the Thirsty Canyon Tuff, which throughout most of its areal extent averages less than 100 feet in thickness, was extruded on an erosional surface of considerable topographic relief and thus partly blanketed the older strata. Areas that were topographically high during Thirsty Canyon time and were not covered by the tuff are topographically high today. The high areas include the hills around Goldfield, the only area that to date has been extensively prospected. There is a good possibility that some ore deposits are concealed by the Thirsty Canyon Tuff. Another byproduct of the reconnaissance was the discovery of an ash-flow tuff unit with a higher than average beryllium content, the Gold Flat Member of the Thirsty Canyon Tuff, which contains as much as 60 parts per million of beryllium. Yucca Flat Study of surface and subsurface geologic information from continued drilling in Yucca Flat is resulting in a detailed three-dimensional analysis unique in the Basin and Range province. Significant changes in thickness and extent of some rock units have been delineated, and this knowledge, together with structural information, has been used to relocate and (or) redesign certain experiments. The detailed information is also providing a basis for a more efficient use of Yucca Flat as a test area. Nuclear explosions in Yucca Flat have caused renewed movement along Yucca fault, a regional structure, and have developed fractures parallel to local structural features.INVESTIGATIONS RELATED TO NUCLEAR ENERGY A53 Structural and stratigraphic control of interbasin movement of ground water A recently completed map of the potentiometric surface of Confined water in Paleozoic aquifers at the Nevada Test Site indicates a remarkable correspondence with certain elements of the regional structure and stratigraphy of the Paleozoic rocks. The map lends support to an early hypothesis that the Paleozoic clastic rocks act as “ground-water dams” and are also, in effect, the “hydraulic basement,” with respect to interbasin movement of water. The map suggests that the outcrop pattern of the clastic rocks may be utilized in some basins to determine the dominant direction of interbasin ground-water movement in the principal aquifer—the Paleozoic carbonate rocks. Geophysical studies Geophysical techniques, particularly gravity and magnetic surveys, are useful in delineating subsurface distribution of igneous bodies and in the correlation of lava flows. An example of the application of the gravity method to determine the shape of an igneous body is reported by D. L. Healey and C. H. Miller (1-63) for the Gold Meadows stock. Field and laboratory measurements of remanent magnetism by G. D. Bath are proving to be a valuable aid for correlation of volcanic rocks as well as for the interpretation of aeromagnetic maps. No lateral variations in the polarity of remanent magnetism have been found in the welded-tuff cooling units tested, some of which have an areal extent of more than 1,000 square miles. Nine of a total of 14 cooling units tested in the Timber Mountain caldera area have reversed polarity. As some of these units appear nearly identical and have discontinuous outcrops, their polarity, which is easily and quickly measured in the field, is commonly a unique identifying criterion. This criterion is also useful for identifying rhyolitic lava flows. One sequence of flows in particular produced intense negative aeromagnetic anomalies which appear to be useful for locating the flows in the subsurface of Pahute Mesa. Such data are extremely important for selecting sites for exploratory drill holes. Studies of aquifer response to underground nuclear explosions W. E. Hale, I. J. Winograd, and M. S. Garber have analyzed the changes in water levels in wells in the vicinity of underground nuclear explosions. Rises in water level of 10 to more than 400 feet have been observed in wells 8,000 and 2,000 feet, respectively, from an underground explosion of intermediate yield deto- nated within the zone of saturation. Rises as great as 1 foot have been detected at distances of 3 miles from another explosion of smaller yield detonated within the zone of aeration. The observed rises in water level began within a few seconds to a few minutes following the detonation and reached a peak within several hours to several days. The water level then declined over a period of months before approaching the preshot water level. The tentative conclusion as to the principal cause for the rise in water levels is a slight net compaction of the aquifer skeleton in the vicinity of the shot, with attendant increase in water pressure. This response results in a water-pressure mound or ringlike water-table mound, surrounding the shot, that decays slowly to the original piezometric surface. Within the rubble chimney or collapse cylinder over the shot in the zone of saturation, the wTater level dropped markedly, and the depression may persist as a hydrologic sink for a number of years. The alteration of the flow system in the vicinity of shots made in the zone of saturation will have some effect on the distribution and transport of radionuclides in the vicinity of the shot. PLOWSHARE PROGRAM The aim of the plowshare Program of the Atomic Energy Commission is to develop peaceful uses of nuclear explosions. The Geological Survey participates in and contributes to this effort in various ways, including selection of sites potentially useful for experiments, making detailed studies of the geology and hydrology of explosion sites, and making feasibility studies of methods of beneficial water-resources development by use of nuclear explosions. Site selection The Geological Survey contributed to an investigation of possible sites for Project schooner, a proposed nuclear cratering experiment in igneous rock. The purpose of the future experiment is to determine the cratering effects of nuclear explosions in a hard competent igneous rock and to compare the effects with those of the sedan nuclear cratering explosion in alluvium at the Nevada Test Site. Geologic mapping, seismic exploration, and drilling were done at several sites; final selection of a site for Project schooner has not been made. The Geological Survey also contributed to an investigation of possible sites for Project dogsled, a proposedA54 GEOLOGY AND HYDROLOGY APPLIED TO ENGINEERING AND PUBLIC HEALTH nuclear cratering experiment in sandstone. This experiment is comparable to the proposed schooner experiment and the accomplished sedan explosion. Project GNOME Project gnome involved the detonation of a 3-kiloton nuclear device on December 10, 1961, in a salt bed near Carlsbad, N. Mex. D. D. Dickey (1-64) has shown by preshot and postshot in-place acoustical measurements in the salt surrounding the point of explosion that the acoustic velocity of the salt decreased, owing to fracturing of the rock, for a radial distance of about 200 feet from the shot point. Breakthrough curves were measured for tritiated water, iodine-131, strontium-90, cesium-137 and fluorescein during tracer studies in the Culebra dolomite aquifer at the gnome site. Preliminary data analysis has shown promise in the use of field tracer experiments in predicting movement of certain ions in relation to water movement. In connection with determination of tracer concentrations of tritiated water in saline waters, R. W. Vernon and W. A. Beetem have shown that low concentrations of surface-active agents prevent coprecipitation interference in the liquid scintillation-counting procedure without the necessity of sample distillation. Transport of radionuclides in ground water F. W. Stead (1-63) has evaluated the available data on the distribution and transport in ground water of radionuclides from large underground nuclear explosions. The initial explosion-produced distribution of the biologically significant radionuclides around an underground nuclear explosion will be at, or a few orders of magnitude greater than, the maximum permissible concentration for these nuclides in drinking water, after the nuclides reach equilibrium between the rock matrix and the associated ground water. After restoration of the ground-water flow pattern to preexplosion conditions, the radionuclides will be transported by ground water down the regional hydraulic gradient and away from their initial explosion-produced area of occurrence. With a reasonable amount of data on the geologic and hydrologic setting of the area within which a nuclear explosion is to be detonated, the average rates and concentrations of radionuclide transport by ground water can be calculated, with validity within one or two orders of magnitude. Strontium-90, a radionuclide characterizing the long-lived fission products, is significantly retarded in ground-water transport in virtually all geologic environments; its rate of movement will rarely be more than a few percent of the average velocity of ground-water flow, and in many environments will be a small fraction of a percent. Cobalt-60, a nuclide characterizing long-lived induced activities, also is significantly retarded in ground-water transport, more so than strontium-90. Tritium, a residual nuclide from fusion reactions, is not significantly retarded in ground-water transport; tritium may well prove the most important of all the long-lived nuclides in evaluating possibly hazardous radionuclide concentrations in ground water. Project CHARIOT Project chariot is a proposed nuclear cratering experiment in northwestern Alaska to create an artificial harbor; the project has been deferred pending other cratering experiments being undertaken at other sites. Results of laboratory studies made in 1961 on adsorption equilibria between samples from the chariot site and biologically significant radionuclides were reported by J. H. Baker, W. A. Beetem, and J. S. Wahl-berg (1-64). Strontium-90 adsorption from solution was found to be independent of sodium-ion concentration but decreased with increasing concentrations of the calcium and magnesium in the solutions. Strontium-90 adsorption from the solution by the solids tested was found to be relatively complete after only 1 day. Cesium-137 adsorption was also found to decrease with increasing total calcium-magnesium concentrations in the solutions. Distribution coefficients increased markedly with time in the case of cesium. This may be due in part to “fixation” reactions. Adsorption of iodine-131 was shown to increase with corresponding increases in the organic content of the adsorbing solids. In all cases, the dissolved radionuclides tested showed rapid uptake by the contacting earth materials. Field studies were made by W. A. Beetem, V. J. Jan-zer, and Reuben Kachadoorian at the chariot site in 1962 to obtain information regarding the removal and transport by water of the radionuclides iodine-131, cesium-137, and strontium-90. Test plots were chosen to represent a variety of micro-drainage patterns, vegetative cover, and soil types. Tracer isotopes were mixed with dry sifted soil of the same type as found in the vicinity of the test plot and then were applied uniformly to the plot. Water then was applied as a spray to simulate rain. Analysis of runoff water and soil samples indicate that very little radioactivity was transported in dissolved form from any of the test plots, regardless of the type of cover on the plots chosen. TheINVESTIGATIONS RELATED TO NUCLEAR ENERGY A55 character of the potential fallout evidently governs the movement of the radioactivity; with no movement of particulate material, there should be no transport of radioactivity. VELA UNIFORM PROGRAM The vela uniform Program of the Advanced Research Projects Agency of the U.S. Department of Defense is concerned with research on methods of detecting underground nuclear explosions. The Geological Survey, through the Atomic Energy Commission, provides information on the geologic and hydrologic environment of sites for nuclear explosions in this program. Project DRIBBLE Project dribble is a proposed series of nuclear explosions in salt at Tatum dome, Lamar County, Miss., to test the effect of decoupling on the detectability of underground nuclear explosions. Basic hydrologic studies, completed during the current year, relating to the ground-water-contamination potential at the site involved primarily the hydrologic relation of the limestone caprock of the dome to the overlying and surrounding sand and limestone aquifers. Measurements of water level in the various aquifers indicate that the head in the limestone caprock is higher than in the overlying sand aquifers and lower than the head in the sand and limestone aquifers at depth along the flank of the salt dome. Pumping tests in a limestone caprock indicated a hydraulic connection with the overlying sand aquifers but no evidence of connection with the deeper aquifer. Nevertheless, the higher head of water in the limestone caprock suggests the possibility of some movement of water from the deeper aquifers through conduits along the flank of the dome and thence into the overlying and adjacent sand aquifers. To aid in the interpretation of the seismic energy that will be propagated from explosions in Tatum dome, D. H. Eargle (1-64) has completed a study of the stratigraphic section of southeastern Mississippi. DISPOSAL OF RADIOACTIVE WASTES MOVEMENT OF RADIOACTIVITY IN STREAMS Two major stream systems into which large quantities of radioactive waste are discharged have been intensively investigated by the Geological Survey in studies of radioactive-waste disposal. Columbia River The movement and deposition of radioactivity in the Columbia River below the Hanford, Wash., facility of the Atomic Energy Commission have been studied by W. L. Haushild, H. H. Stevens, Jr., and G. R. Dempster, Jr., in close cooperation with scientific personnel of the General Electric Co. They have found that the low-level radioactivity is mostly in solute form or is sorbed on suspended sediments of the river. Smaller amounts of radioactivity become associated with the biota. Significant quantities of scandium-46, chromi-um-51, zinc-65, zirconium-95—niobium-95, ruthenium-103—rhenium-103, and cerium-141, have been found. Ratios between the radioactivity in solution and that sorbed by the sediments vary considerably with time and place; they are not linearly related to the total amount of radioactivity, nor are the concentrations constant along a river cross section. All bed sediments sorb some radioactivity, but relatively larger amounts are sorbed by sediments that contain larger amounts of silt- and clay-sized particles. However, large amounts of radionuclides are sorbed by bed sediments that contain less than 1 percent by weight of silt and clay. Chromium-51 and zinc-65 are most commonly sorbed by the bed sediments, but scandium-46, magnesium-54, and cobalt-60 are also found in close association with the bed sediments. Tennessee River system In a comprehensive study of the Clinch-Tennessee River system below Oak Ridge National Laboratory (ORNL), Geological Survey scientists in cooperation with those of the Health Physics Division, ORNL, and other federal and State agencies have studied the distribution of radioactive materials carried in solution and deposited in stream sediments over a distance of nearly 600 river miles. The work has included an investigation of the hydraulic effects of the new Melton Hill Dam upstream from Oak Ridge. B. J. Frederick and P. H. Carrigan, Jr., of the Geological Survey and F. L. Parker of ORNL have found that hydroelectric peaking operations at Melton Hill Dam will lead.to pulsed releases of waters from White Oak Creek, which drains the laboratory area, into the Clinch River. The largest pulse is released during the weekend shutdown of a typical sequence of summertime operations at the dam. Labeling the pulses with fluorescein dye has enabled the investigators to trace the water masses through a 16-mile reach. Maximum concentrations of the dye are reduced by a factor of 50 in the first 6.4 miles of the reach; a 746-002 0 - 64 -5A56 GEOLOGY AND HYDROLOGY APPLIED TO ENGINEERING AND PUBLIC HEALTH further twofold reduction occurs in the next 9 miles of the reach. In predicting diffusion in this unsteady flow system, the problem has been approached as an analog to flow in a tidal estuary. The distribution of bottom sediments and the radioactivity associated with them have been studied by USGS-ORNL teams. P. H. Carrigan, Jr., and R. J. Pickering have found that in the first 8 miles downstream from the mouth of White Oak Creek, the lower water level of Watts Bar Reservoir and high discharges in the winter season lead to scour of sediments deposited in the summer. The beginning of thermal stratification from late spring to early fall centers about a section between 8 and 11 miles downstream. Stratified conditions do not seem to lead to any significant seasonal change in the longitudinal distribution of radioactivity in the bottom sediments in the vicinity of this section or farther downstream. Variations in gross gamma radioactivity with depth in undisturbed cores of bottom sediment from the Clinch River have been measured in a “core scanner.” Several of the longer cores show a repetitive general pattern of radioactivity which is very similar to the pattern of annual releases of cesium-137 from Oak Ridge National Laboratory since 1943. Most of the cesium-137 was associated with suspended sediment when it entered the river, and the observed repetitive pattern of radioactivity is considered by R. J. Pickering to be evidence that there has been continuous sedimentation at the locations from which the cores were taken. The persistence of the pattern in some cores whose length indicates an average yearly accumulation of only a fraction of an inch, in spite of known rather wide weekly variations in amounts of cesium-137 released to the river, testifies to the stability of the sorption reaction by which the radionuclide became fixed on the sediment particles. The longitudinal distribution of cesium-137, cobalt-60, and trivalent rare-earth elements in the bottom sediments appears to be controlled by the same mechanism in the reach from Melton Hill Dam on the Clinch River to Kentucky Dam on the Tennessee River. The observed downstream decreases in concentrations are much greater than would be predicted on the basis of flow dilution alone. This suggests to P. H. Carrigan, Jr., that the mechanism is a sedimentation process. Somewhat different mechanisms may control the distribution of zirconium-95, niobium-95, and strontium-90. In studies of the transport of radionuclides by White Oak Creek, W. M. McMaster has shown that the radioactivity load is more variable during base flow than at high discharges. Dye tracer tests in a 6,000-foot reach of White Oak Creek have shown that for flows ranging from 4.5 cubic feet per second to 200 cfs, peak concentration of the dye slug was nearly three times greater for flood flow than that during base flow, even though the quantity of dye and other conditions of the experiment were the same. Studies of radioactive transport Laboratory flume and theoretical analyses of the hydraulic problems of sediment dispersion and transport, fundamental to a knowledge of the processes controlling the movement of low-level radioactive wastes in streams, have been made by W. W. Sayre, D. W. Hubbell, and F. M. Chang. The transport and dispersion of bed-material particles in alluvial streams have been described by Sayre and Hubbell in terms of a mathematical model in which the transport of a particle is represented as an alternating sequence of steps and rest periods of variable length and duration. In the language of stochastic processes, the model would be called a compound Poisson process with exponentially distributed increments. Using the initial condition of an instantaneous plane source of contaminated particles, uniformly distributed in the bed at a cross section, they arrived at a concentration-distribution function which agrees with observed distributions of radioactive-tracer particle concentrations along the North Loup River, Nebr., and in a laboratory flume, obtained at various dispersion times. A method was also devised for determining the probability density function for the duration of rest periods of bed-material particles in an alluvial channel with bed forms. The only data required are continuous records of bed elevation obtained at a point. Investigations of the dispersion of fluorescent dyes and suspended silt-size particles in a wide laboratory flume with a rough bottom using fluorometric and nephelometric tracing techniques have been initiated by Sayre, Hubbell, and Chang. Results to date indicate that the longitudinal dispersion of the dye from an instantaneous plane source follows closely the prediction of the Taylor-Elder theory of dispersion in a turbulent shear flow. In the theory a virtual coefficient of longitudinal dispersion is calculated from the velocity distribution and the Reynolds analogy for the equivalence of mass and momentum transfer. The suspended silt particles behave in a similar manner except that the tendency of the particles to settle is superimposed on the dispersion process. The rates of lateral dispersion of dye from a continuous pointWATER CONTAMINATION STUDIES A57 source within the flow and of floating polyethylene particles from an intermittent point source at the water surface were found to be virtually the same. The magnitude of the longitudinal diffusion coefficient was observed to be approximately 30 times that of the lateral diffusion coefficient. Measurements of the vertical distribution of dye from a continuous point source at mid-depth indicate that complete vertical mixing is obtained at a distance of about 15 times the depth downstream from the source. The results of both the longitudinal and the lateral dispersion experiments fit within the framework of the Fickian diffusion analogy. DISPOSAL OF WASTES TO THE GROUND At the Atomic Energy Commission’s Savannah River Plant in South Carolina, I. W. Marine has used hydraulic data from pumping tests to estimate the degree of continuity of fracture systems between wells in crystalline bedrock, and has classified fractures in the bedrock according to their effect on gross rock permeability. Because of minute, very slightly permeable, interconnected fractures the rock mass can be considered as a single hydrologic system, but another system of fractures that are far more permeable transmit most of the water yielded by the test wells. Values for the coefficient of permeability derived from pumping tests range from less than 0.002 gallon per day per square foot for sound rock to about 1 gpd per sq ft for fracture zones. The common practice in disposal of low-level wastes to the ground is to discharge them near the land surface into pits or cribs. Under these circumstances, a detailed knowledge of the occurrence of ground water and the geologic framework through which it flows and of the geochemical relations between waste, ground water, and the associated rock and soil materials are essential to an accurate prediction of the movement of wastes and the changes in concentration during transport. R. M. Richardson (1-63) emphasized that sites for the disposal of release of radioactive wastes in arid regions are in general greatly superior to those in humid regions. In an arid climate, the great depth to ground water provides an unsaturated porous reservoir in which wastes are he*ld temporarily while they decay; stream spacing is greater, thus requiring long travel times to points of discharge into streams; soils are more saline favoring ion-exchange reactions; and roots of vegetation do not commonly extend to the water table, thus eliminating a mechanism for recyling radionuclides that operates in humid regions. A film illustrating the dispersion of aqueous radioactive waste in a heterogeneous aquifer, prepared from time-lapse photographs of dye in a series of hydraulic models, was presented by P. H. Jones and H. E. Ski-bitzke. This study showed that flow path, dispersion, and attenuation of radionuclide concentration were prominently influenced by aquifer geometry and permeability distribution. In a general study of the hydrologic problems of injecting liquid wastes into deeply buried sedimentary rocks, W. J. Drescher (2-63) points out that precise definition of the flow, or even the forces affecting flow, cannot be quantitatively calculated for any one location on the basis of data available. SITES FOR NUCLEAR POWERPLANTS Julius Schlocker and others, in a detailed study of the site of a proposed nuclear steam powerplant at Bodega Bay, Sonoma County, Calif., made on behalf of the Atomic Energy Commission, found faults cutting Pleistocene sediments which rest on intensely faulted and fractured granitic bedrock at the site. The site is about 1,000 feet west of the edge of the San Andreas fault zone. Sites at San Onofre, Calif., Haddam Neck, Conn., Malibu Beach, Calif., and Oyster Creek, N.J., have also been evaluated as to geologic and hydrologic suitability. WATER CONTAMINATION STUDIES The continued growth of population and industry is resulting in an increase in waste products in the geologic and hydrologic environments. A great variety of waste products tends to spread into ground-water and surface-water supplies in many instances restricting the use of an accessible supply, and in general complicating the development of water resources. In addition to pollution or contamination by waste products, some of our usable water resources are shrinking or are endangered at places where the pumping of wells (or some other action by man) alters a fresh-water—saltwater contact and causes salt-water movement. Investigations concerned mainly with contamination are mentioned in this section; investigations in which the described contamination is incidental to other matters are reported in the section “Water Resources,” under Louisiana, South Dakota, Nebraska, Utah, Pacific Northwest, and California.A58 GEOLOGY AND HYDROLOGY APPLIED TO ENGINEERING AND PUBLIC HEALTH Environmental classification for disposal of wastes Aspects of the hydrogeologic environment pertinent to ground-water contamination are being synthesized by H. E. LeGrand. He has developed a system for evaluating the contamination potential of sites where wastes are disposed of near the ground surface. His system uses the following interrelated factors: permeability, sorption, hydraulic gradient, depth to the water table, and distance from sources of contamination to a well supply. DETERGENTS AND PESTICIDES IN WATER SUPPLIES Laboratory studies C. H. Wayman and colleagues have been studying the influence of physicochemical and biochemical properties on the movement of detergent solutions through both saturated and unsaturated ground-water zones. Their biodegradation studies show that under aerobic conditions, the newer type of “soft” ABS (alkylbenzenesul-fonate) cannot be degraded in less than 1 week; under anaerobic conditions, satisfactory breakdown is not achieved even after 2 weeks. One of the nonionic surfactants, sucrose ester (a combination of sugar and natural oil), achieves nearly complete breakdown in about 1 day under both aerobic and anaerobic conditions. This is a significant finding that deserves careful consideration in the development of legislation regarding the production, use, and disposal of detergents in waste water. Laboratory studies have disclosed also that two organisms, closely resembling Flavobacteriwm peregrimum and Achromobacter, could grow successfully on the fungicide DODINE (n-dodecylguanidine acetate), utilizing it as a sole source of carbon. This suggestion, that certain soil organisms can utilize specific fungicides as a carbon source, may further suggest that some soil sprays may become biodegraded before entering water supplies. Detergents in Long Island ground water N. M. Perlmutter, Maxim Lieber, and H. L. Frauen-thal (p. C170-C175) report that water in the upper 20 feet of the water-table aquifer in the South Farming-dale area of Nassau County, N.Y., is contaminated by ABS (alkylbenzenesulfonate) in concentrations generally between 1 and 5 parts per million, but locally as high as 32 ppm. Most of the water in the remainder of the aquifer contains less than 1 ppm and does not foam. The source of contamination is effluent from hundreds of randomly distributed cesspools. Detergent in the Martinsburg Shale in Pennsylvania A ground-water investigation by L. D. Carswell and J. R. Hollowell in Dauphin County, Pa., indicates that water in the Martinsburg Shale is locally contaminated in the upper few feet of the saturated zone. Analyses of water samples from 44 wells showed low concentrations of ABS (alkylbenzenesulfonate) in most samples; only a few had concentrations exceeding 0.4 parts per million. The ABS in well waters is due to leakage around old, defective, and shallow well casings; leakage around uncemented casings and well seals; and widespread contamination of the limestone aquifers of the Martinsburg Shale. Pesticides in Michigan water A study of pesticide contamination in ground and surface waters of Van Buren County, Mich., by G. E. Hendrickson showed small but detectable contamination of some water sources by chlorinated hydrocarbons and organophosphates. Estimated concentrations of chlorinated hydrocarbons ranged from a few tenths to 5 parts per billion. Concentrations of organophosphates were estimated at 0.1 part per billion or less. Seven out of nine samples were lacking in one or both types of pesticides. ACID MINE WATERS Acid waters and sediment of the West Pork River basin, West Virginia A reconnaissance of the water quality of streams tributary to the West Fork River between Weston and Clarksburg, W. Va., by G. W. Whetstone and C. R. Collier, showed that most of the tributaries are affected by acid mine-water inflow. However, only Lost Creek and Browns Creek are sufficiently contaminated to be classed as acid waters. Drainage from active and abandoned coal mines in the Browns Creek basin contains as much as 1,100 parts per million of H2SO„. Throughout most of its length, except in its extreme upper reaches, Browns Creek is acid (pH less than 4.5) and contributes about 6 tons of acid per day to the West Fork River. Approximately 1 ton of acid per day is from active mines; the rest is contributed by drainage from abandoned drift and strip mines. Sediment concentrations as high as 13,&00 ppm during runoff from the thunderstorm were measured in one tributary draining a strip mine. The sediment concentration of Browns Creek is expected to range from 1,000 to 5,000 ppm during most storm-runoff periods.WATER CONTAMINATION STUDIES A59 High weathering rates in parts of the Monongahela River basin, Pennsylvania-West Virginia Chemical weathering rates vary widely in the Monongahela River basin, Pennsylvania-West Virginia, because of lithologic and cultural influences. Measurements made during base flow in September 1963 by J. W. Wark showed natural removal of mineral matter in solution ranging from 0.003 to 0.07 tons per day per square mile, whereas calculated rates for streams receiving acid mine drainage were in excess of 1.0 ton per day per square mile. Dissolved load in the Cane Branch basin, Kentucky According to J. J. Musser, chemical weathering and erosion reached peak levels in 1959 in the Cane Branch basin, McCreary County, Ky. Acid drainage resulted from the weathering of pyrite exposed by coal strip mining in 1956 and 1959; since 1959, however, the concentration of dissolved solids in Cane Branch has slowly declined. The average dissolved-solids content for the low-flow months of 1959, 1960, and 1961 was 449, 367, and 336 parts per million, respectively, and for the high-flow months of 1959-60 and 1960-61, it was 213 and 148 ppm. Even though declining, these concentrations greatly exceeded those of nearby streams not affecting by mining. Excessive manganese in the Muskingum River, Ohio An increase in the manganese content of the Muskingum River between Zanesville and Beverly, Ohio, was observed by P. G. Drake during the low flow in the summer and fall of 1963. Surveys of the Muskingum River and selected tributaries made in July and October 1963 indicated that the manganese content of the river water averaged about 2 parts per million during the summer, approximately 3 times the normal concentrations observed in previous years. Moxahela Creek and Brush Creek, two tributaries which drain coal-mining areas, contained 4.8 and 13 ppm of manganese, respectively, in July and 18 ppm and 29 ppm in October. INDUSTRIAL WASTES Gasoline in ground water at Savannah, Ga. A subsurface accumulation of refined gasoline described by M. J. McCollum (1-63) in downtown Savannah, Ga., floats on the water table adjacent to a building which houses stream-turbine generators of the Savannah Electric and Power Co. Fumes from the gasoline entered the sub-basement of the power-company building, creating a serious hazard. Auger holes were drilled to outline the gasoline body and to find the source of the gasoline. Apparently about 50,000 gallons of gasoline is present, lying from about 8 to 15 feet below land surface, depending on the local topography. To prevent fumes from entering the power-company basement, well points were installed to lower the water table and “gasoline table” and, at the same time, to concentrate the gasoline in the resulting cone of depression. A pumping system was installed and is presently removing the gasoline. Waste load of the Passaic River, N.J. Measurements of streamflow and dissolved-solids content at about 60 sites at low flow during September 1963, were used by P. W. Anderson and E. G. Miller to determine relative densities of dissolved solids on all significant tributaries and at several points on the main stem of the Passaic River, N.J. Preliminary information at Little Falls, N. J., indicates that the average dissolved-solids load per unit volume of water has increased consistently, while the average dissolved-oxygen content has decreased by about 20 percent during the past 20 years. OIL-FIELD BRINES Brine in water supplies near Alabama oil fields Study by W. J. Powell, L. E. Carroon, and J. R. Avrett (1-63) of the Pollard, Gilbertown, Citronelle, and South Carlton oil fields in Alabama has revealed two major sources of contamination of fresh-water supplies: (1) brine-disposal pits underlain by permeable sands, and (2) leaking pipelines and wellheads that allow brines to percolate downward to the ground-water reservoir. Source of saline water at Brunswick, Ga. In a small area of salt-water-contamination in the city of Brunswick, Ga., the chloride content of water has remained at about 800 parts per million according to R. L. Wait. Increases in the chloride content of water from wells near the north (downgradient) side of the contaminated area indicate northward movement of water of high chloride content. Test drilling in the contaminated area showed that a dolomitic bed found above the salty water zone is very porous and is not an effective confining bed near the focus of chloride contamination. Brine contamination of the Green River, Ky. Continued study by R. A. Krieger of the oil-field brine discharge into the upper Green River in Kentucky shows that during the extremely low streamflowsA60 GEOLOGY AND HYDROLOGY APPLIED TO ENGINEERING AND PUBLIC HEALTH of 1963 about one-third of the brine was derived from the Metcalf County oil field and about two-thirds from the Greensburg field. However, total brine discharge to the Green River continues to decline. During the 1963 water year, the Green River at Munfordville was always well below the acceptable maximum of 250 parts per million chloride of the U.S. Public Health Service drinking-water standards. SALT-WATER CONTAMINATION Controls on brine discharge in Permian basin Preliminary results of an investigation obtained under the direction of P. R. Stevens on the occurrence and movement of brine at many places in the Permian basin of Texas and adjacent States suggest that controls on brine discharge are regional, not local, and hence that efforts at control based on the assumption that the brines are generated by local circulation of infiltrated rain water are likely to fail. Salt inflow to the Pecos River cut by pumping About 420 tons of dissolved minerals, of which about 370 tons is sodium chloride, is added daily to the Pecos River through seeps and springs along a 3-mile reach of the river at Malaga Bend in southern Eddy County, N. Mex. The discharge of about 0.4 cubic foot per second (200 gallons per minute) of concentrated brine is from an artesian aquifer, at a depth of about 200 feet, near the base of the Rustler Formation. Studies by E. R. Cox indicated that the discharge of the brine to the river could be reduced substantially by pumping a well that taps the brine aquifer and by discharging the brine into a natural depression nearby. Pumping of about 550 gallons per minute of brine from July 22, 1963, to November 22 resulted in a reduction in head of about 8 feet in the brine aquifer. The head in the brine aquifer had been about 10 feet above river level before pumping began. Spot discharge measurements and chemical analyses indicate that the amount of salt entering the river at Malaga Bend had decreased about 50 percent by September 6, and about 60 percent by November 22. By December 27, about 328 acre-feet of brine containing more than 120,000 tons of salt had been pumped into the nearby depression. Leakage of brine from the depression has been less than 10 percent and may possibly be as low as 1 percent. Saline ground' water of the Outer Banks, N.C. The movement of the salty ground water introduced into the sandy aquifers of the Outer Banks of North Carolina by the Ash Wednesday storm of March 7,1962, was studied by H. B. Wilder. The initial slug of ocean water, which covered most areas less than 10 feet above mean sea level, moved rapidly down to the water table (2 to 10 feet) and by March 12 had contaminated wells less than about 15 feet deep. Along the beach, water having unusually high concentrations of chloride continued to move downward through the zone of saturation at rates usually ranging from 0.8 to 1.4 feet per day. Downward movement was slower farther inland. Once the salty water reached the water table, the most significant movement appears to have been lateral. Maximum chloride concentrations did not exceed 5,000 parts per million in most wells, indicating that most of the recharging sea water did not permeate the zone of saturation. The pattern of chloride variation in individual wells was more erratic than would have resulted from a primarily downward mode of movement. Some shallow wells (less than 15 feet deep) did not show any effects of the salty water for more than 30 days after the storm, by which time the maximum contamination had already occurred in comparable wells known to have been inundated. Once the hydraulic energy of the storm-introduced water had dissipated, additional movement was very slow. One inland well, 60 feet deep, which was covered by sea water for several hours, did not show salt contamination for about 18 months. Other shallower wells which had yielded fresh water a few weeks after the storm, following an initial contamination, became salty again when subjected to heavy pumping during the summers of 1962 and 1963. Saline ground water moving toward Baton Rouge, La. Salt-water movement has been detected in the major aquifers of the Baton Rouge area, and appears to be moving northward toward centers of public-supply and industrial ground-water pumping according to C. O. Morgan and M. D. Winner (1-64). The decline of water levels aroimd these centers has caused a reversal of natural hydraulic gradients, inducing movement of salt water toward areas of lower head. Preliminary estimates based on meager data indicate that salt water may be detectible at the nearest pumping center in 5 years at the present rate of pumping. Salt water flow up Pascagoula River, Miss. The severe drought of 1963 in southeastern Mississippi resulted in the lowest flow recorded in the Pascagoula River since 1936. Salt water from Mississippi Sound penetrated up the tidal reach of the river a record disance of 20 miles, 2 miles above any previously recorded penetration, according to H. G. Golden andENGINEERING GEOLOGY A61 S. F. Ivapustka. During a period of high tides and extremely low flows in October, salty water, for the first time known, reached above the division point of the main stem of the Pascagoula River. Programmed disposal of salt from Project DRIBBLE R. G. Lipscomb identified streambank vegetation along Half Moon and Lower Little Creeks, Lamar County, Miss., and established limits of chloride concentration that can be tolerated for specific periods of time. The studies were made in connection with proposed disposal of brine associated with mining of 40,-000 tons of salt from Tatum dome in conjunction with Project dribble. See “vela uniform Program.” It was concluded that the bank vegetation can tolerate water having a concentration of more than 1,000 parts per million, and possibly as much as 3,000 parts per million, of chloride if controlled release of brine is made into the streams. Using the estimated steamflow, which exceeds 17 cubic feet per second about 95 percent of the time and 30 cfs about 50 percent of the time, it was found that 75 tons per day of salt can be disposed of as brine into Half Moon Creek without exceeding a concentration of 1,000 parts per million of chloride. When the flow exceeds 30 cfs, 135 tons per day can be disolved in the stream without exceeding 1,000 parts per million of chloride. Disposal of 40,000 tons of salt could be effected from Tatum dome within 17 months without exceeding the limit of 1,000 parts per million of chloride in the Lower Little Creek system. DISTRIBUTION OF MINOR ELEMENTS AS RELATED TO PUBLIC HEALTH Environmental studies are receiving increasing attention in the field of public health. The rocks on which we live, the soils in which our foods grow, and the water that we drink are highly significant factors in the human environment, and the U.S. Geological Survey is participating in investigations of how these factors affect health. The natural distribution of elements in this context is treated in the following section; artificial distribution of mineral matter as related to health is treated under sections “Water Contamination Studies” and “Disposal of Radioactive Wastes.” Fluoride in ground water in Pacific Northwest In an appraisal of fluoride content of ground water in the Pacific Northwest, A. S. Van Denburgh reported on water from 152 sources containing more than 1.0 part per million of flouride. Of these sources, 89 are in Idaho, 40 in Oregon, and 23 in Washington. The largest amount of fluoride recorded for each State is 24, 12, and 2.8 ppm, respectively. Thirty-two spring and well waters in Idaho contained more than 10 ppm. The high-flouride ground water is chemically distinctive in that it is soft, has a high pH, and contains large amounts of silica. Most of the high-fluoride water is obtained from deep wells that commonly tap aquifers in volcanic rock. Arsenic in ground water in Lane County, Oreg. E. L. Goldblatt, A. S. Van Denburgh, and R. A. Marsland report above-average arsenic content of ground water in Lane County, Oreg. Water containing the greatest amount of arsenic is confined to the Fisher Formation. Arsenic in amounts exceeding the 0.05 parts per million (the limit according to U.S. Public Health Service drinking-water standards) is found largely in the ground water within a 100-square-mile area west and south of Eugene. Most of the ground water in Lane County contains little arsenic and does not constitute a health hazard, but water from wells in that part of the county in the Willamette Valley south of Eugene should be tested for arsenic content prior to intended domestic use. (See also “Geochemistry of Water”.) ENGINEERING GEOLOGY Clay a hazard in part of the Washington, D.C., area Clay of the Patapsco Formation of Late Cretaceous age presents a geologic hazard to construction in the eastern and southern parts of the Washington, D.C., metropolitan area, where it has been used extensively for making brick. Exposures of the clay on steep slopes are generally stable only so long as they are undisturbed. Moreover, the clays are subject to expansion and rebound when they are unloaded by removal of overburden, as was recognized by C. F. Wellington (1-64) during a study of a slope failure in an excavation at Greenbelt, Md. Although the rebound is not great, it is enough to open incipient joints in the clay, and where they are parallel to the wall of a vertical cut, the cut stability is impaired. Swelling days discovered in Seattle freeway Excavation for a freeway on Capitol Hill in Seattle, Wash., revealed previously unrecognized greenish weathered montmorillonitic clay. Studies by D. R. Mullineaux, T. C. Nichols, and R. A. Speirer (chapter D) indicate that the weathering occurred prior to the Vashon glaciation, before 15,000 years B.P. The distribution of the weathered clays is important in planningA62 GEOLOGY AND HYDROLOGY APPLIED TO ENGINEERING AND PUBLIC HEALTH for heavy construction because they are characterized by higher swell pressures and lower shear strength than comparable unweathered clays in the Seattle area. Swelling clays in Palo Alto, Calif. Mapping by E. H. Pampeyan in the Palo Alto quadrangle has led to recognition of a zone of Eocene mont-morillonite-rich clayey siltstone that passes through two residential developments. Homes and roads along the zone had been damaged by the swelling and contracting movements that accompany seasonal climatic changes. Free-swell tests for unconfined volume change on wetting show as much as 80 percent swell for some of the clayey beds as compared with 10 percent for adjacent sandstones. Plans for using as yet undeveloped land underlain by the swelling clays need to be carefully reevaluated. Distribution of coal-mine bumps at Sunnyside, Utah Continuous seismic recording of bumps in coal mines near Sunnyside, Utah, during the fall of 1963 revealed a cyclic occurrence of these events. According to F. W. Osterwald, the maxima occur at intervals of 5 to 9 days. The number of bumps recorded per day increased steadily during November but decreased during the first part of December, whereas the intensity of individual bumps increased. During December, several bumps occurred along a fault system that extends through the Sunnyside No. 2 and the Columbia mines. These bumps seemed to increase progressively in number and in intensity. An extremely violent bump occurred on December 24 in which two men were injured and much damage was done to the Sunnyside No. 2 mine. Preceding the violent bump, two moderately violent bumps associated with the fault system were recorded in the same area. Tire “epicenter” of this bump was only about 300 feet from a major fault intersection, whereas the center of physical damage was in a large coal pillar surrounded by small ones. The faults apparently provided convenient places for stress accumulation that was released violently by mining activity in the large pillar. As a result of this sequence of documented events, it may be possible in the future to predict areas in which stress is accumulating. Hence it might be possible to increase the safety of mining operations by avoiding certain dangerous areas during periods of intense bumping activity as recorded by seismographs on the surface and underground. Recent surface movements in the Baldwin Hills, Los Angeles, Calif. Surface movements in the north-central part of the Baldwin Hills have been observed and measured in recent years by several city and county organizations. Data available to the middle of 1962 were obtained as supplemental information during the U.S. Geological Survey investigation of the surface geology of the Baldwin Hills area by R. O. Castle31 and have been correlated with the local geology and summarized (U.S. Geological Survey, 10-64). These data indicate that the movements consist predominantly of subsidence and cracking of the ground. Contours of equal rate of subsidence form a pattern that is elongated somewhat along a northwest-southeast line roughly paralleling the axis of the Inglewood oil field structural dome. Cracking that developed in the period 1957-62 is along five north-northeast-trending ruptures in the vicinity of the intersection of La-Brea Avenue, Stocker Street, and Overhill Drive. Offsets on the cracks ranged from less than an inch to about 5 inches and defined a trough several hundred feet wide and about 2,500 feet long. The surface cracks conform in direction to northeast-trending bedrock faults that offset the major north-northwest-trending Inglewood fault. Possible causes of ground movements are (1) changes in reservoir pressure due to oil-field operations, (2) changes in ground-water conditions, (3) compaction of sedimentary materials, and (4) tectonic movements. Similar factors are being evaluated by several State and municipal boards of inquiry that are considering the failure of the Baldwin Hills Reservoir on December 14,1963. Landslide at portal of highway tunnel, Colorado The use of an approach road under construction and the start of the estimated $50 million Straight Creek tunnel were threatened by development of a landslide in the cut at the east portal of the tunnel. C. S. Robinson, R. A. Carroll, and F. T. Lee (1-64), in cooperation with the U.S. Bureau of Public Roads and the Colorado Department of Highways, used geological and geophysical methods to define the extent of the landslide in fractured bedrock and surficial material and to predict its possible behavior. Resistivity surveys 81 R. O. Castle, 1960, Geologic map of the Baldwin Hills area, California : U.S. Geol. Survey open-file report.ENGINEERING HYDROLOGY A63 made by the Bureau of Public Roads and geologic and shallow seismic surveys made by the U.S. Geological Survey yielded complementary and generally concordant data that allowed a definition of the volume and mass of the landslide. These data were used by the Bureau of Public Roads to design methods of stabilizing the landslide so that construction of the tunnel could proceed. Gravity surveys can detect caverns under reservoir A precision gravity survey of areas of known leakage on the floor of Anchor Reservoir in Wyoming, made by G. P. Eaton at the request of the U.S. Bureau of Reclamation, indicated that areas of potential leakage associated with cavernous openings in bedrock beneath shallow alluvium can be detected readily by the gravity method. Negative anomalies ranging from —0.1 milli-gal to —1.0 mgal were found to be associated with areas of actual leakage and to show up clearly on a gravity map prepared from observations made on a station grid with spacing of 50 by 100 feet. Uncertainties in the seismic determination of “top of rock" In Southborough, Mass., a quartzite of normal lithology and structure, but with compressional-wave speed of 3,100 to 4,300 feet per second, led to misidentification of actual bedrock as till composing the second seismic layer. Geologic mapping by N. P. Cuppels, and additional field seismic measurements by C. R. Tuttle and R. N. Oldale show that the speed is unrelated to frequency and to instrument malfunction. The “seismic top of rock” boundary is commonly unrelated to the base of primary weathering, to the “shattered rock” boundary, to shear zones, or to the original ground surface. Two 180° fan arrays of geophones show that surface vector speeds measured directly on the quartzite are fastest normal to the strike of points; a third fan discloses fastest compressional speed both parallel and also at 60° to the strike of major joints and lithic contacts; these measurements contradict ray-path theory. Ray paths are evidently not guided by dip because the critical angle is an average of 20.7° normal to the strike, and 17.2° parallel to strike, whereas dip of geologic structure averages 50° in the vertical plane of seismic-transverse azimuth and ranges from 38° to 63°. Relation of elasticity to strike of bedding Elastic-parameter measurements were made at two seismic field model sites in Massachusetts by C. R. Tuttle, using nonexplosive energy sources and a cathode ray tube-type interval timer. At North Attleboro, measurements were made through 11.5 feet of till in underlying fine-grained arkosic conglomerate. Modulus of elasticity (E) normal to strike of the bedding, compared with E at about 45° to the strike, was in the ratio of 2.3 to 1.0. On the theoretical curve of Poissons ratio versus the ratio of compressional to shear speeds, the data normal to the strike lie on the curve, whereas a measurement at 45° to the strike of bedding lies far outside this curve. When supported by additional field measurements, this relation might be diagnostic of the direction of concealed geologic structure. Shear measurements at a site where bedrock was covered by about 12 feet of sand were unsuccessful, probably because of attenuation through a nonrigid material. ENGINEERING HYDROLOGY Hydrologic science is widely applied in engineering practice, but for the most part such applied work is done by private firms or public agencies involved directly in construction or management of projects. The work of the U.S. Geological Survey in this field is directed toward broad fundamental studies that are common to many areas and projects. LAND SUBSIDENCE Draft on confined ground-water reservoirs throughout the country is increasing, causing increased decline in artesian head and consequent increased effective stress on the confined aquifer systems. For this reason, subsidence of the land surface resulting from aquifer compaction can be expected to become more widespread and intense. Subsidence causes serious problems in the construction and maintenance of engineering structures, especially overland water-conveyance systems. In addition, the compaction of aquifer systems in subsiding areas has caused the destruction of hundreds of wells owing to compressive failure of the casings. In contrast to its destructive aspects, aquifer compaction supplies large quantities of water from storage in the finegrained semipervious compressible interbeds or confining beds. Such water is, however, a nonrenewable resource, and the process of mining it changes the hydrologic properties of the system, especially the coefficient of storage. Studies of land subsidence caused by decline in artesian head are continuing in California, Nevada, Arizona, and Texas. These studies are contributing to knowledge of the mechanical and hydraulic properties of leaky aquifer systems, the storage characteristics ofA64 GEOLOGY AND HYDROLOGY APPLIED TO ENGINEERING AND PUBLIC HEALTH semipervious interbeds and confining beds, the change in the coefficient of storage with time and change in effective stress, and the inability of most well casings to resist the compacting forces. A special case of land subsidence occurred during the earthquake in Alaska in March 1964, described under “Alaskan Earthquake.” A special case of compaction due to nuclear explosion is described in the section “Investigations Related to Nuclear Energy.” Reduced land subsidence and compaction in California B. E. Lofgren finds that a marked change in the rate and areal extent of subsidence occurred in the Tulare-Wasco area in the southeastern San Joaquin Valley during the years of 1962 and 1963 when surface-water supply was ample. Partial releveling of the bench-mark net by the U.S. Coast and Geodetic Survey in Febraury 1964 indicated that the rate of subsidence in much of the area was greatly reduced compared to the average rate from 1959 to 1962, a period of deficient surface-water supply. A direct relation exists in each part of the area between the rate of subsidence and the ground-water pumpage, which in turn is inversely related to the surface-water supply. Only in the vicinity of Pixley, where surface-water deliveries have been limited, did subsidence rates exceed 0.2 foot per year from 1962 to 1964. Total subsidence in the cone of subsidence near Pixley from 1930 to 1964 has been 11.5 feet. Compaction recorders installed in central California Highly senstitive compaction recorders have been installed at several sites in central California to measure the compaction of the aquifer system due to artesian-presure decline. Using a gear mechanism to expand the compaction record as much as 48 times, the sensitive response of the unconsolidated deposits to slight increases in effective overburden stress has been recorded. Within minutes of the time that water levels are drawn down by nearby pumping at a compaction recorder near Pixley in Tulare County, compaction of the producing aquifer system is recorded. Declines in artesian head of as little as 5 feet are sufficient to cause noticeable compaction of fine-grained deposits 500 to 700 feet below the land surface. The change in effective stress represented by the 5-foot decline is less than 1 percent. Well casing shortened by compaction in California In the southern part of the Los Banos-Kettleman City subsidence area, on the west side of the San Joaquin Valley, measurements have been made on the compression and shortening of a heavy oil-well casing encased in cement. J. F. Poland and R. L. Ireland have found that in the 20 months from August 1962 to April 1964, total measured compaction of sediments from land surface to a depth of 1,930 feet was 1.08 feet and concurrent shortening of the 11%-inch 54-lb (per foot) oil-well casing was 1.03 feet. In this period the top of the casing moved up 0.05 foot with reference to the land surface. These measurements indicate that the skin friction between the casing system (casing and cement) and the sediments is sufficient to overcome the compressive strength of the heavy casing and cement envelope when compaction of the sediments occurs. Therefore, in sediments undergoing compaction due to fluid withdrawal and increase in effective stress, such structures obviously cannot be utilized as reference bench marks for leveling control, even if they pass completely through the compacting sediments. Furthermore, the increase in protrusion of the casing top above land surface may represent only a negligible part of the land subsidence. Rate of subsidence increasing in Las Vegas Valley, Nev. According to G. T. Malmberg (1-64), analysis of a releveling of part of the Hoover Dam level network by the U.S. Coast and Geodetic Survey during May and July 1963 indicates that land subsidence since 1935, resulting principally from ground-water withdrawals in Las Vegas Valley, has affected an area of about 200 square miles and that maximum subsidence exceeds 2 feet. Subsidence has been most pronounced in Las Vegas and North Las Vegas, and since 1951 the rate of subsidence has been about 0.1 foot per year, or more than double the rate during 1935-51. The accelerated rate of subsidence since 1951 is the result of the increased overdraft on the ground-water reservoir and the consequent reduction in artesian head. Precise leveling by the Coast and Geodetic Survey in 1935, 1941, 1950, and 1963 indicates that the volume of subsidence resulting largely from the compaction of saturated valley-fill deposits during successive intervening periods was about 2,000, 12,000, and 28,000 acre-feet, respectively, or about 3 to 4 percent of the pumpage during those intervals. Subsidence and earth cracks in southern Arizona In southern Arizona, land-surface subsidence has been recognized in several valleys where water levels have been lowered substantially by pumping. Collapse of well casings below the water table is indicative of compaction of sediments and reservoir volume change due to vertical shortening. Increased protrusion of the top of a well casing above the land surface indicatesENGINEERING HYDROLOGY A65 subsidence but supplies only a minimum clue to the magnitude, because most of the compaction of sediments may be represented by casing shortening or failure at depth (as shown by the measurements reported near Westhaven in the San Joaquin Valley, Calif.). William Kam has measured the increased protrusion of well casings above the land surface at Luke Air Force Base, Maricopa County, Ariz. The rate of protrusion at two wells, 501 and 1,200 feet deep, is about 0.02 foot per month. At some places, well-casing collapse below the water table and the development of nearby earth fissures at land surface appear to be related to land subsidence as indicated by casing protrusion. There also seems to be a correlation at some places between the occurrence of earth fissures and facies boundaries in the subsurface deposits. Compaction of aquifer measured at Houston, Tex. Two compaction recorders are being operated in the Houston area. At a well 1,650 feet deep in a city of Houston well field, R. K. Gabrysch reports measured compaction from September 1959 to March 1964 was 0.15 foot. At a well 770 feet deep at the NASA Manned Spacecraft Center, Clear Lake, Harris County, measured compaction from October 1962 to March 1964 was 0.12 foot. The U.S. Coast and Geodetic Survey is now releveling the Houston area as part of a 5-year releveling program. However, results of this releveling are not yet available for comparison with measured compaction. EVAPORATION SUPPRESSION Efficiency of films proportional to length of carbon chain Laboratory experiments to suppress evaporation by monomolecular films lead G. E. Koberg to conclude that the longer the carbon chain is in the film molecule, the more effective the film is in reducing evaporation. Mixtures of compounds of different chain lengths will not be as effective as a film composed only of the compound having the longest chain. The laboratory experiments also revealed that the films are more effective under an unstable atmospheric condition (when the temperature of the water surface is higher than that of the ambient air) than under a stable condition. Bubbler method successful in field test An investigation in collaboration with the Escondido Mutual Water Co. of a method of reducing evaporation by mixing the cold and warm water of Lake Wohlford, in southern California, indicated a saving of water through below-average evaporation of 14 percent for the period May through July 1962. For the period Sep- tember through November 1962 a comparable loss-through increased evaporation of 8 percent was noted by G. E. Koberg (chapter D). The increase in evaporation was attributed to the additional energy stored in Lake Wohlford during the May through July period because of the reduction in evaporation. During the 1963 year, similar evaporation results were obtained. Mixing of the water was accomplished by forcing 210 cubic feet per minute of free air into the water at a point 40 feet below the surface of the lake. The bubbling of air in Lake-Wohlford is now considered a routine operation by the water company because of the improvement of water quality and the net reduction in evaporation. One significant change was made in the operation schedule of the system during 1963 from that of 1962. The 1962 schedule required the system to operate 9 hours each day. However, circulation studies during the 1962 year indicated that for optimum operation, the system should be operated over an interval of at least 24 hours or longer to obtain complete circulation in the lake. The schedule for 1963 was changed to two operations a week of 30 hours duration each. Further studies are planned in southern California to determine if such systems are economically feasible on larger reservoirs. FLOODS Three major categories in the study of floods by the U.S. Geological Survey are (1) measurement of stage and discharge, (2) definition of the relation between the magnitude of floods and their frequency of occurrence, and (3) delineation of the extent of inundation of flood plains by specific floods or by floods having specific recurrence intervals. The following section, accordingly, is subdivided into outstanding floods of 1963-64, studies of flood frequency, and flood mapping. OUTSTANDING FLOODS OF 1963-64 Flood of August 7, 1963, at Buffalo, N.Y. More than 3 inches of rain in the metropolitan Buffalo area on July 29,1963, was followed by 3.88 inches on August 7. The 24-hour rainfall on August 7 was the greatest since 1893 at Buffalo, and the resulting flood was the most damaging in the history of the city. Damage was estimated at $7 million to public property and $28 million to private property. Flood of August 20, 1963, in Alexandria-Arlington, Va. Severe flooding in the Alexandria-Arlington metropolitan area occurred on August 20, 1963, as a resultA66 GEOLOGY AND HYDROLOGY APPLIED TO ENGINEERING AND PUBLIC HEALTH "Of cloudburst rainfall of 3.4 to 3.9 inches in 1 y2 hours over most of the Fourmile Run drainage basin. The peak flow of 11,400 cubic feet per second at the gaging station on Fourmile Run at Alexandria was the greatest known and was estimated to have a recurrence interval of 100 years. One life was lost in the floodwaters of Long Branch along Army-Navy Drive in Arlington. Damage was estimated to be in excess of 1 million. Floods of early August 1963 in Puerto Rico M. A. Lopez reports damaging floods in southwestern Puerto Eico during the period July 30-August 3, 1963. On July 30, the highest flood since 1933 on the Rio Yagiiez inundated homes, schools, stores, and industries close to the center of Mayagiiez, Puerto Rico’s third largest city. Flooding of 4,000 acres of reclaimed land in the Lajas valley project resulted from 9 inches of rain on August 2-3. Inundation lasted as long as 5 days, and damage to young sugarcane was considerable. The flood was the most sever since drainage works were started in 1955. On August 3, the highest flood since 1954 occurred on the Rio Guayanilla. Moderate damage occurred to sugarcane lands and low-lying homes and business establishments in the small city of Guayanilla, and the main Highway 2 was inundated. Floods of March 1963, Alabama to Ohio H. H. Barnes, Jr. (1-63) reports that widespread disastrous floods struck the western slopes of the Appalachian Mountains from Alabama to Ohio as a result of three storms moving over the area during the period March 4-19,1963. The initial storm, March 4-6, established conditions favorable for maximum runoff from subsequent storms. Heavy rainfall during March 11-13 produced record-breaking floods on many streams. The third storm, March 16-19, prolonged flooding and produced high-volume runoff in some areas. Alabama.—Three people died as a result of the storms, and flood damage was estimated in excess of $1 million. The peak discharge at three gaging stations exceeded the maximum previously known, and had recurrence intervals ranging from 80 to more than 100 years. Tennessee.—Records from 18 stream-gaging stations in the eastern part of the State reflect the maximum peak discharge since systematic data collection began. The March 13 peak discharge of 56,700 cubic feet per second on the Clinch River at Tazewell is second only to the flood of 1862. The March 12 peak discharge of 25,800 cfs on the Sequatchie River near Whitewell is the maxi- mum known since at least 1867. The March 12 peak discharge of 35,000 cfs on the Elk River above Fayette-ville equaled the flood of 1949, and the stage reached within half a foot of the record 1842 crest. During the predawn hours of March 12, an unprecedented flood crest of 32,700 cfs from a drainage area of 97.5 square miles swept through the Little Sequatchie River valley above Alum Cove, claiming four lives and causing much destruction. Statistics compiled by the Tennessee Division of Water Resources reveal: more than 3,000 homes damaged or destroyed, about 1,500 head of livestock lost, more than 100,000 acres of winter crops damaged, almost half a million acres of cropland damaged, and 1,000 bridges damaged or destroyed in 50 counties, with the total damage appraised in excess of $10 million. Kentucky.—Flood peaks at many gaging stations in southeastern Kentucky approached the maximum for the period of record, and new maximums were established at five gaging stations. Extreme flooding occurred in the upper basins of the Big Sandy, the Cumberland, and the Kentucky Rivers. The range of peak discharge was between 60 and 200 cubic feet per second per square mile, and the recurrence interval was between 15 years and 1.9 times the 50-year flood. The Army Corps of Engineers and the U.S. Weather Bureau estimated the total damages in Kentucky to be about $50 million. West Virginia.—The floods of March 12 in the Guyan-dotte and the Big Sandy River basins were the highest of record and the highest since at least 1915. As a result of more than 2 weeks of flooding in the western sector of the State, 5 lives were lost, about 5,000 persons were forced from their homes, and estimates of property damage amounted to more than $10 million. Virginia.-—In general, the floods of March 12 on streams in the Tennessee River basin in southwest Virginia were the second highest in 100 years, being exceeded only by the 1957 floods. The flood of March 13 on the Clinch River at Speers Ferry was the greatest since 1862. Floods at two gaging stations in the Big Sandy River ranged from 2 to 2y2 times the 50-year discharge. Ohio.—In the flood of March 1963 in central Ohio, peaks on some streams in the Hocking River and the Scioto River basins exceeded those for the disastrous flood of March 1913. Profiles of the Hocking River flood stages and an inundation map of Athens, Ohio, provide useful information for the design of highway bridges and culverts and other structures in the Hocking River valley.ENGINEERING HYDROLOGY A67 Floods of March 1964 in the Ohio River valley Two intense storms within a week during the first half of March 1964 caused outstanding floods on the Ohio River and many of its tributaries. The storms covered a wide band that generally parallels the Ohio River. Floods along the Ohio River were the highest since 1945 at some gaging stations, and flood records were broken at many points in Indiana, Ohio, and Kentucky. The peak discharge for many streams tributary to the Ohio River exceeded the discharge for the 50-year flood. Preliminary estimates of flood damages exceed $20 million. According to estimates by the Army Corps of Engineers, flood crests were reduced 2 to 10 feet and many millions of dollars were saved by the Engineers’ flood-control works in the Ohio River basin. Flood of July 16, 1963, at Hot Springs, Ark. A thunderstorm on July 16, 1963, at Hot Springs, Ark., and vicinity produced floods on Gulpha Creek and tributaries, Hot Springs Creek, Glazypeau. Creek, and many smaller streams. The peak discharge at some points was more than twice the magnitude of the 50-year flood discharge. In Hot Springs, the downtown was flooded in the worst flood since May 1923. Estimate of property damage in the city of Hot Springs was $1 million to private property and $150 thousand to streets, bridges, and sewerlines, and in the remainder of Garland County damage was estimated as $1 million to private property and $200 thousand to public property. Floods of June 24—25, 1963, in Nebraska Studies by E. W. Beckman indicate that peak runoff rates at least as high as 2,900 cubic feet per second per square mile from a 0.3 square-mile area and 1,800 cubic feet per second per square mile from a 40 square-mile area occurred June 24,1963, around a storm center in east-central Nebraska. The recurrence interval for the peak discharge at many points exceeded 100 years. Data collected by the U.S. Weather Bureau, the Army Corps of Engineers, and others show a principal storm center in eastern Butler and western Saunders Counties. The highest storm-total rainfall measurement was 16.5 inches, of which a maximum of 3.8 inches fell in 1 hour. Four inches or more of rain fell over an area of 4,300 square miles. Flood of September 17, 1963, in southeast Texas Hurricane Cindy caused torrential rains approaching 24 inches in the Beaumont-Port Arthur area of the southeast corner of Texas on September 17, 1963. This is apparently the highest 24-hour rainfall in Texas since the storm of May-June 1935. Although flood damage was extensive, no lives were lost. Several streams in the area had peak discharges in excess of 50-year frequency, and one recorded peak was H/& times the discharge for the 50-year flood. Floods of August 1963 in Prescott, Ariz. Several rainstorms during the early part of August set the stage for high runoff from an intense rain on August 19, 1963 (Aldridge, 1-63). At about 8 p.m. on Monday, August 19, 1963, four small tributaries of Granite Greek poured water into Prescott at a combined rate of over 7,000 cubic feet per scond, causing $400 thousand damage to real estate, streets, sewers, waterlines, and personal property. Houses were washed off their foundations; cars, trucks, and trailers were washed away; but miraculously no one was killed or injured. Higher floods may have occurred in the last 50 years, but none of them caused nearly as much damage. Floods in southern Idaho during February 1963 C. A. Thomas reports that extreme flooding occurred in rather widely scattered tributaries of the Snake River in southern Idaho during the first 4 days of February 1963. Conditions that caused the flood were very similar to those that caused the extreme floods of February 1962; however, the area affected was smaller. Peaks on several streams exceeded those for the February 1962 flood. The recurrence intervals for some peaks ranged from 50 to more than 100 years. Severe flood in Nevada, early February 1963 Widespread flooding occurred in northwestern Nevada during January 31-February 1, 1963, as a result of intense precipitation of about 72-hours duration, according to S. E. Rantz and E. E. Harris (4—63). The flood-producing storm was of the warm type; precipitation fell as rain at altitudes as high as 8,000 feet. The heavy precipitation, totaling as much as 20 inches or more in the Sierra Nevada, fell on frozen ground or on a sparse snowpack at higher altitudes. The response of runoff to rainfall was dramatic; streams throughout northwestern Nevada rose rapidly. Major flooding ocurred throughout the Walker, Carson, and particularly the Truckee, River basins, where flood peaks either reached record-breaking heights or rivalled the discharges attained in the memorable floods of November 1950 and December 1955. Because of the relatively short duration of the storm, the volume of flood flow in 1963 was not outstanding. The flood peak for the gaging station on the Truckee River at Reno, Nev., was only slightly less than the devastating flood of Decern-A68 GEOLOGY AND HYDROLOGY APPLIED TO ENGINEERING AND PUBLIC HEALTH ber 23, 1955; this was due in part to the newly constructed Prosser Creek Reservoir in the upper watershed. Ice-jam flooding in Alaska R. E. Marsh reports that Lake George, near Palmer, which usually forms behind Knik Glacier, did not break out in 1963. This is the first time that there was no breakout since at least 1948, when the U.S. Geological Survey began studies of the high-flow period, and probably since 1918, according to personnel of the Alaska Railroad. The maximum stage of the Yukon River at Rampart (58.69 ft, from floodmarks) was much higher than any other stage for the period of record, and according to local residents, it was the highest stage ever reached from an ice jam. Floods of March-May 1963 in Hawaii Intense localized rains during March through May 1963 caused damaging floods in several areas of the Islands as reported by W. C. Vaudrey (1-63). Excessive rains occurred in the Koloa district, Kauai, on March 5-6; near Waimanalo, Oahu, on March 6; and near Hana, Maui, on March 13. In the latter area, rainfall intensity was 4 inches in 45 minutes. Heavy rains fell on all islands on April 14—15, the resulting flood damage being greatest on Kauai and windward Oahu. A driving storm hit suddenly May 14 and dropped nearly 6 inches of rain in 3 hours on leeward Oahu. One child was drowned in the flood from this storm. At 22 gaging stations, peak discharges resulting from the series of March-May storms exceeded previous maxi-mums. On April 15, the previous 45-year maximum discharge at Hanapepe River near Eleele, Kauai, was exceeded by 11,800 million gallons per day, and at South Fork Wailau River near Lihue, Kauai, the previous 48-year maximum discharge was exceeded by 18,400 mgd. The March-May floods caused 4 deaths and property damage in excess of $2 million. The Army Corps of Engineers estimates that its flood-control works on the Hanapepe River prevented an additional $292 thousand damage. FLOOD FREQUENCY Effect of urbanization on floods at Jackson, Miss. Preliminary analysis of 10 years of record on streams draining the city of Jackson reveals that some flood crests are increased appreciably by urbanization. K. V. Wilson and others have found that the increase ranges from 200 to 300 percent, depending upon the degree of development and the relative magnitude of the flood. The study reveals that the degree of effect decreases with increasing flood magnitude. Discharge-frequency relations in Mississippi Preliminary analysis of peak discharges from drainage areas of less than 2 square miles reveals that runoff rates increase as drainage areas decrease. According to recent studies by K. V. Wilson and colleagues, the discharge-frequency relations for small drainage areas do not conform to the relations previously established32 for larger streams in Mississippi. Eight years of annual peaks at 25 gaging stations and outstanding floods at many miscellaneous sites were used in the analysis. Rainfall-runoff relations in Mississippi and Louisiana More than 900 floods above an arbitrarily chosen base have been analyzed to determine the rainfall-runoff relation for streams that drain southwestern Mississippi and southeastern (Florida parishes) Louisiana. A. J. Calandro and colleagues have determined that a family of curves will relate total rainfall to total runoff. Different curves are applicable for the several seasons of the year. Magnitude and frequency of storm runoff in Mississippi and Louisiana V. B. Sauer (chapter D), used records from 17 gaging stations ranging in drainage area from 0.73 to 1,330 square miles to define the relation between magnitude and frequency of storm runoff for individual storms within a 7,500-square-mile area in southwestern Mississippi and southeastern Louisiana. It was demonstrated that the recurrence interval for a given storm runoff is not necessarily the same as the recurrence interval for the peak discharge resulting from that same storm. Flood-frequency relations of Alaska streams According to V. K. Berwick, the magnitude-frequency relations of floods in Alaska south of the Yukon River can be determined with a reasonable degree of accuracy for most sites, gaged or ungaged, on streams that are unaffected by the works of man. Drainage area alone is used as the independent variable for correlation with the mean annual flood. Results are limited to sites above which the drainage area is within the range of that covered by the base data. 32 k. V. Wilson, and I. L. Trotter, Jr., 1961, Floods in Mississippi, magnitude and frequency : Mississippi State Highway Dept.ALASKAN EARTHQUAKE A69 Flood-frequency relations of Texas streams The magnitude of a flood of any selected frequency between 1.2 and 50 years can be estimated for most natural-flow streams in Texas that drain areas of 40 square miles or more, according to a report by.J. L. Patterson (1-63). The report contains tables of maximum floods at gaging stations and miscellaneous sites, and tabulations of floods above a selected base discharge for gaging stations having 5 years or more of record as of September 30, 1961. Flood-frequency relations of Wyoming streams A report by J. R. Carter and A. R. Green (1-63) describes methods for estimating the magnitude of a flood of any frequency between 1.1 and 50 years for any site, gaged or ungaged, on most unregulated streams in Wyoming, within the limits of basin size for which records have been collected. Flood-frequency relations are not defined for a large part of the headwaters of the North Platte River in south-central Wyoming because of the scarcity of streamflow data. Nationwide flood-frequency reports Nine reports have been completed in the nationwide series of 19 reports on the magnitude and frequency of floods, and 6 will soon be submitted by authors for approval. Each report is for a part corresponding to a drainage-basin subdivision used by the Geological Survey. The following reports have been published: Part 3-B, Water Supply Paper 1676 (Speer and Gamble; 2-64); Part 7, WSP 1681 (Patterson, 1-64); Part 13, WSP 1688 (C.A. Thomas, Broom, and Cum-mans, 1-63); Part 14, WSP 1689 (Hulsing and Kallio, 1-64), WSP 1673 (Speer and Gamble, 1-64); and Part 12, WSP 1687 (Bodhaine and Thomas, 2-64). FLOOD MAPPING Flood maps of urban areas Flood-inundation maps showing the limits of inundation by major floods, flood profiles, Stage-frequency relations, and descriptive text have been published as Hydrologic Investigations Atlases for the following areas during the current year: Highland Park, 111. (HA-69); Aurora North, 111. (HA-70); Wheeling, 111. (HA-71); Fortuna, Calif. (HA-78); Park Ridge, 111. (HA-85); Palatine quadrangle, Illinois (HA-87); and Raritan and Millstone Rivers in Somerset County, N.J. (HA-104). ALASKAN EARTHQUAKE Arthur Grantz, George Plafker, and Reuben Kacha-doorian, have completed preliminary geologic evaluation of the March 27,1964, earthquake in Alaska, based upon a reconnaissance study (2-64). The earthquake, which had a Richter magnitude variously estimated as between 8.4 and 8.75, was one of the largest in the history of the United States and probably released at least twice the energy of the 1906 San Francisco earthquake. The epicenter of the main shock, which lasted between iy2 and 4 minutes, was in the northern part of Prince William Sound, on the east side of Unakwik Inlet at lat 61.05° N., long 147.50° W. The aftershock zone extended from northern Prince William Sound southwestward as far as southern Kodiak Island. The earthquake and its aftershocks, as suggested by their location and nature, occurred along a fault or broad zone of faulting possibly several hundred miles long and associated with the Aleutian Islands arc and the Aleutian Trench. Preliminary aerial reconnaissance in the area of the epicenter, within the area where the Aleutian fault zone intersects the continent, failed to reveal signs of surface breakage. Tectonic changes in land level of regional extent occurred on both sides of the fault zone. To the west of the zone an area of at least 22,000 square miles, which includes the Kenai Peninsula and at least the northern part of Kodiak Island, subsided as much as 5.4 feet relative to sea level. To the east of the fault zone there has been tectonic uplift of as much as 7.5 feet over an area of at least 12,000 square miles that includes eastern Prince William Sound, the adjacent mainland, and the continental shelf. Major losses of life and property were from several types of earthquake-generated waves in coastal areas, and earthquake-triggered submarine and subaerial landslides. Seismic shock, compaction and lurching due to shaking of unconsolidated materials, and rock-slides and avalanches also caused significant damage and changes in landscape over more than 50,000 square miles of land area. A train of seismic sea waves that originated in the Gulf of Alaska was particularly destructive along the tectonically subsided coast of Kodiak Island and at Seward on the Kenai Peninsula. They also resulted in losses of life and property along the coasts of British Columbia, Oregon, and California.A70 GEOLOGY AND HYDROLOGY APPLIED TO ENGINEERING AND PUBLIC HEALTH Local waves of unknown origin within Prince Wil-lian Sound struck within minutes of the earthquake, took a total of 31 lives, and virtually wiped out the native village of Chenega. Submarine landslides, particularly at the waterfronts of Valdez and Seward, destroyed most of the harbor facilities at these two port cities. Waves that immediately accompanied the landslides, and a train of seismic sea waves that followed later, resulted in virtual destruction of the waterfront areas. Submarine landslides also destroyed the small boat harbor at Homer and were reported along the coast as far away as southeastern Alaska, where the Skagway-Haines telephone cable was broken by a slide. Three large landslides and at least 8 smaller ones located in weak glaciolacustrine clay deposits33 along the bluffs facing Knik Arm and Ship Creek caused most of the 9 casualties and the extensive property damage in the Anchorage area. The L Street slide, which was 4,000 feet long and 1,150 feet wide at the widest point, and the 4th Avenue slide, which was 2,500 feet long and 1,150 feet wide, moved laterally as relatively coherent masses. A large landslide at Turnagain Heights, 8,000 feet long and 1,200 feet wide, and several smaller slides, broke into narrow slices which rotated as they moved, thereby destroying most structures within the slide areas. Substantial damage due to seismic shock was sustained by structures in the Anchorage area and to a lesser extent in Seward, Valdez, and Whittier. High- 33 R. D. Miller and Ernest Dobrovolny, 1959, Surficial geology of Anchorage and vicinity, Alaska : U.S. Geol. Survey Bull. 1093, 128 p. way and railroad bridges from the Copper River to the Kenai Peninsula were also extensively damaged by earth tremors. Damage was most severe to those structures on thick saturated alluvial deposits and markedly less to structures founded on bedrock. Fissuring and compaction of unconsolidated deposits were widespread, and many of the cracks formed were destructive to structures and earth fills founded on such deposits. The lowered land-surface levels, particularly in coastal areas such as Turnagain Arm and Homer Spit which had also been affected by tectonic subsidence, resulted in subsequent property losses by inundation during high tides. Lowered water levels in artesian wells were recorded and some surface streams were temporarily reduced in flow following the earthquake, presumably due to local slight increases in porosity caused by shaking. R. M. Waller reports that considerable subsidence of the land surface occurred by compaction of unconsolidated deposits in south-central Alaska during the earthquake. At Homer, for example, the total lowering of land surface with respect to sea level was 4.5 feet. Of this, at least 2.5 feet was due to compaction of unconsolidated sediments, as demonstrated by protrusion of that amount of a well casing that penetrated 468 feet of alluvium and is anchored in the underlying bedrock. The remaining 2 feet of subsidence is ascribed to tectonic causes. Detailed followup studies on the geologic aspects of the earthquake are now underway by the U.S. Geological Survey, and additional more detailed reports on the geologic implications of the March 27 earthquake will be prepared as these studies are completed.REGIONAL GEOLOGY Much of the geologic and geophysical work of the U.S. Geological Survey consists of the mapping of specific areas, mostly for publication in quadrangle maps at scales of 1: 62,500 and 1:24,000. Some of these studies are for the purpose of extending the detailed geologic knowledge in areas of known economic interest; some are to gain detailed knowledge at localities or areas for engineering planning or construction. Still other mapping studies are carried on with paleontology, sedimentary petrology, or some other specialized topic as the primary objective. The systematic description and mapping of rock units to show local and regional relations likewise constitute a major scientific objective. Mapping the geology of the United States is a mandate of the Organic Act establishing the Geological Survey, and the completion of geologic maps for the country at scales that will fulfill foreseeable needs and uses is a long-range goal. A summary of recent results of this mapping, especially in the fields of stratigraphy, structural geology, and regional geophysics, is discussed here according to subdivisions of the conterminous United States shown on figure 5. Figure 5. Index map of the conter showing boundaries of regions referred to in discussion of regional A71 746-002 0 - 64 -6A72 REGIONAL GEOLOGY MAPS OF LARGE REGIONS The preparation of geological and geophysical maps of national or continental scope is an established part of the work of the U.S. Geological Survey. Such maps synthesize data from other maps and topical studies by Geological Survey personnel, data from published sources, and unpublished data supplied by State geological surveys, private companies, and universities. Some of the maps are prepared and published by the Geological Survey in collaboration with national and international scientific organizations. Maps of large regions currently being prepared in collaboration with other organizations include: 1. Geological map of North America, scale 1: 5,000,000. Compilation of this map, which is now completed, was done by a committee of the Geological Society of America, E. N. Goddard, University of Michigan, chairman. A new base map of North America has been prepared by the U.S. Geological Survey, and the geologic map will be published on the new base. 2. Tectonic map of North America, scale 1:5,000,000. This is being compiled for the Subcommission for the Tectonic Map of the World, International Geological Congress, by P. B. King, of the Geological Survey. Preliminary drafts of the map were corrected during 1964. It is planned to show the distribution of tectonic (rather than stratigraphic) map units over all of the continent. A nearly completed version of the map will be on exhibit at the International Geologic Congress in New Delhi, India, at the end of 1964. 3. Basement map of North America from latitude 20° N. to 60° N., scale 1: 5,000,000. This map has been compiled by the Basement Hock Committee of the American Association of Petroleum Geologists, P. T. Flawn, University of Texas, chairman. It is to be published by the Geological Survey on the new base map of North America. The basement map will show the altitude of the upper surface of basement rocks as determined from wells, geophysical measurements, and geological inference. 4. Basement rock map of the United States, scale 1: 2,- 500,000. As an outgrowth of the basement map of North America, the Advanced Research Project Agency, Department of Defense, is sponsoring the compilation of a basement rock map of the United States under the direction of W. R. Muehl- berger, University of Texas. The map will show subdivisions on the basis of age and lithologic type of the buried basement as well as the altitude of the basement surface by contours. As a companion project, R. W. Bayley, U.S. Geological Survey, is directing compilation of a map of exposed basement rocks showing subdivisions on the basis of age and lithologic type. Trend lines on this map will show some internal structures of the rocks. The two compilations will be combined and published by the Geological Survey. 5. Bouger gravity anomaly map of the United States (exclusive of Alaska and Hawaii) and part of Canada, scale 1:2,500,000. This map has been compiled by the Committee for Geophysical and Geological Study of the Continents, American Geophysical Union, G. P. Wollard, University of Hawaii, chairman, and is being prepared for publication by the Geological Survey. Paleotectonic maps A program to compile and publish paleotectonic maps of the conterminous United States for each of the geologic systems is continuing. The maps record geologic events on a nationwide scale and are accompanied by a text that provides documentation and assists interpretation. Interpretive maps reconstruct the former extent of the sediments of the geologic system, the position and relative heights of former land areas, changes in the patterns of sedimentation, environments of deposition, and other features of regional geologic importance. Folios for the Jurassic and Triassic Systems have been published to date. Maps for the Permian, Pennsylvanian, and Mississippian Systems are in various stages of preparation. The Permian maps have been compiled and are being readied for publication. The maps for the Pennsylvanian and Mississippian Systems are being assembled concurrently, and are in preliminary stages of preparation. For purposes of representation on lithofacies and isopach maps, rocks of the Pennsylvanian System are being divided into five map units or intervals corresponding in age in a general way with the Virgil, Missouri, Des Moines, Atoka, and Morrow Series of the midcontinent region. Rocks of the Mississippian System are being divided into four maps units corresponding roughly in age to the Chester, Meramec, Osage, and Kinderhook Series of the central United States.COASTAL PLAINS A73 COASTAL PLAINS ATLANTIC COASTAL PLAIN Paleontology of Tertiary deposits A recent study of the macrofauna and microfauna of the Miocene and Pliocene deposits of the Atlantic Coastal Plain, by T. G. Gibson, has shown the area to be more structurally and stratigraphically complex than formerly thought. Positive features which subdivided the large embayment into smaller elements arose at different times during the Miocene, causing marked differences in environments. Correlation across the positive areas and into the different basins has been accomplished by the use of the more mobile mollusks, such as the Pectinidae, and the planktonic Foraminifera. Subsurface material has yielded the downdip equivalents of many of the surface units, but much of the middle Tertiary, thought to be absent because of lack of surface exposures, is represented in the subsurface. T. C. Gibson also reports that study of the Mollusca, particularly the Pectinidae, of the Miocene and Pliocene of the Atlantic Coastal Plain has led to the vertical zonation of the deposits. The presence of mobile groups like the Pectinidae in various environments has made possible the correlation of many small outcrops over a large geographic area. Other molluscan groups have also been used to substantiate the zoning. Cyclic deposition in Cretaceous and Tertiary time The cyclical nature of the coastal-plain deposits, which range from Turonian through Pliocene(?) in age, in New Jersey and Delaware provides an important clue to the mechanism of deposition for these units. J. P. Owens and J. P. Minard report that this cyclical deposition taken in association with the relatively immature composition of the sediments (primarily feld-spathic sands) suggests deposition on a relatively unstable platform. They believe that this interpretation is compatible with the geophysical investigations off the coast of New Jersey by Drake,34 in which he depicted large downwarps in the mantle relatively close inshore. Petrography of basement gneiss beneath coastal-plain sequence in New Jersey D. L. South wick (p. C55-C60) described the petrography of an 8-foot core taken 3,873 to 3,881 feet below 84 C. L. Drake, W. M. Ewing, and G. H. Sutton, 1959, Continental margins and geosynclines—the east coast of North America north of Cape Hatteras, in L. H. Ahrens and others, eds., Physics and chemistry of the earth, v. 3 : London, Pergamon Press. the land surface and about 75 feet below the base of the sedimentary rocks of the coastal plain at Island Beach State Park, N.J. The core consists of strongly foliated garnet - microcline - biotite - quartz - plagioclase veined gneiss close to migmatite in structure. A K-Ar age of 235 million years suggests recrystallization during the late Paleozoic metamorphic event that affected parts of southeastern New England. Subsurface stratigraphy at Cape May, N.J. Significant zones and horizons were recognized in a cursory examination of samples from Dickinson test well 1, Cape May, N.J., by H. R. Berquist and J. E. Johnston. Samples in the top 920 feet were largely barren of micro, fossils and consisted mainly of conglomeratic sands, suggestive of channel or estuary fill. Tertiary rocks are represented by Paleocene, lower to upper Eocene, and Miocene beds. The top of Upper Cretaceous was tentatively identified at 1,980 feet. H. R. Bergquist recognized a thin but significant zone of charophytes. From a comparison with published material by Peck,35 the utricles and gyroganites were tentatively identified as Atofochara trivolvis Peck and were judged to be of very early Cretaceous (Aptian) age. Subsequently, the find was verified through Esther Applin, who had submitted specimens from this well to Raymond E. Peck and was informed that so far as is known this fossil is confined to the Aptian, though it has worldwide distribution. More significantly this may indicate down warping, and (or) eustatic change of sea level, of nearly 4,500 feet since Early Cretaceous, as the charophytes are nonmarine aquatic plants. Their occurrence in the subsurface could be explained by post-depositional slumping into a nearshore deep, or less likely, by fresh-water upwelling on the shelf during the Cretaceous. The top of the “granite wash” was identified at approximately — 6,130 feet, the top of the saprolite zone at —6,370 feet, and the top of the basement complex at — 6,400 feet, sea level datum. High gravels of Maryland yield Cretaceous spores Identification of fossil spores by Jack Wolfe in peat interbedded with high-level gravels (Bryn Mawr and Brandywine Gravels) of Cecil and Harford Counties, Md., indicates an Early Cretaceous age for these gravel beds now considered Pliocene (?) in age. » R. E. Peck, 1957, North American Mesozoic Charophyta: U.S. Geol. Survey Prof. Paper 294-A.A74 REGIONAL GEOLOGY Age of basement schist in south-central New Jersey Recent K-Ar age determination of mica schist recovered at 2,078 feet below land surface from a Geological Survey core hole at New Brooklyn Park, Camden County, N.J., gave an age of 301 million years according to analysts H. H. Thomas, R. F. Marvin, Paul Elmore, and Hezekiah Smith. More age determinations are needed in the vicinity before meaningful interpretation can be made. Cretaceous fossils from Chesapeake and Delaware Canal N. F. Sohl’s analysis of Upper Cretaceous fossils from the Chesapeake and Delaware Canal documents the presence of Merchantville, Marshalltown, and Mount Laurel faunas. Contrary to published record, no Red Bank or Navesink faunas are present along the canal. The Merchantville Formation can be correlated with the lower part of the Blufftown Formation of Georgia and the lower part of the Coffee Sand of Mississippi. The Mount Laurel Sand is equivalent to the upper part of the Cussetta Sand of Georgia, the upper part of the Bluffport Marl Member of the De-mopolis Chalk of Mississippi, and the lowermost part of the Ripley Formation of Tennessee. Foraminifera date zone of Marshalltown Formation The Upper Cretaceous Marshalltown Formation near the top of the Matawan Group, is exposed at Auburn, Del., where it contains abundant specimens of Exogyra ponderosa (Roemer) and Ostrea species. This locality yielded an abundant foraminiferal fauna consisting of 30 identified species, 8 of which are planktonic. Comparison of these Foraminifera, by J. F. Mello, J. P. Minard, and J. P. Owens with the age ranges of the same species on the Gulf Coast suggests that the sample is of late Taylor age (p. B61-B63). Eocene to Recent offshore stratigraphy of Georgia Working with rock cores and cuttings from two test holes about 10 miles offshore from Savannah Beach, Ga., M. J. McCollum and S. M. Herrick (chapter D) found that upper Eocene to Recent stratigraphic sequence is similar to that onshore, but that the post-Miocene section is thinner. GULF COASTAL PLAIN AND MISSISSIPPI EMBAYMENT Geologic mapping and stratigraphic studies in the Jack-son Purchase area, Kentucky Geologic mapping and stratigraphic studies in the Jackson Purchase area (the part of Kentucky west of the Tennessee River) have added substantially to the knowledge of the stratigraphy and areal distribution of Mesozoic and Cenozoic rocks in the northern Mississippi Embayment, and of the structural framework of the area. Stratigraphic investigations have been greatly enhanced by palynological studies by R. H. Tschudy, Estella B. Leopold, and Helen Pakiser. Mapping by T. W. Lambert (1-63), W. W. Olive (1-63), H. G. Wilshire (1-63, 2-63), and E. W. Wolfe (1-63) has shown that the Tuscaloosa and McNairy Formations (Upper Cretaceous), the basal units of the embayment sequence, rest on an intricately eroded surface of considerable relief developed on Mississippian rocks composed for the most part of residual chert and clay derived from leaching of limestone. The Tuscaloosa Formation, composed dominantly of chert gravel and tripolitic silt, occurs as scattered lenses, as much as 150 feet thick, that fill the deepest pre-Tuscaloosa channels. The McNairy Formation comprises about 200 feet of sand that contains widely spaced clay lenses. It un-conformably overlies the Tuscaloosa Formation and overlaps the Mississippian rocks. The Clayton Formation (Paleocene) is Composed of clay and sand deposits that closely resemble those of the upper part of the McNairy Formation. For this reason, and because the Clayton is poorly exposed, the two units have been combined for purposes of mapping in the Jackson Purchase area. Evidence from field observations, palynological studies by Tschudy of samples collected by W. W. Olive from the western part of the Hico quadrangle, and subsequent unpublished palynological studies indicates that deposition in Kentucky was continuous from the Cretaceous into the Tertiary and was not interrupted by an hiatus as L. W. Stephenson36 contended. The Porters Creek Clay, 150 to 250 feet thick, is composed dominantly of montmorillonitic clay but commonly is sandy in the upper and lower parts. This unit, which with the Clayton Formation makes up the Midway Group (Paleocene), conformably overlies the Clayton Formation throughout most of the area, as studies by L. V. Blade (1-63), W. W. Olive, and E. W. Wolfe (1-63) suggest; however, W. I. Finch reports an unconformity between the two units in the Symsonia quadrangle in the northern part of the area. A sequence consisting of as much as 165 feet of inter-bedded argillaceous sand, sandy clay, and lignite above 36 L. W. Stephenson, 1915. The Cretaceous-Eocene contact In the Atlantic and Gulf Coastal Plain : U.S. Geol. Surrey Prof. Paper 90-J, p. 155-183.NEW ENGLAND AND EASTERN NEW YORK A75 the Porters Creek Clay lithologically resembles sediments of the Wilcox Group in Mississippi. On the basis of lithologic similarity and of palynological evidence provided by E. B. Leopold, Helen Pakiser, and R. H. Tschudy the sequence is tentatively designated as the Wilcox Formation (lower Eocene). The unit is discontinuous at the outcrop, because of overlap by younger Eocene sediments. In the Kirksey (Wilshire, 2-63), Dexter (Wolfe, 1-63), Hazel (Blade, 1-63), and Symsonia quadrangles the areal distribution of the Wilcox (?) suggests that it was deposited in shallow depressions eroded into the underlying Porters Creek Clay. * A unit dominantly composed of sand and scattered clay lenses tentatively designated as the Claiborne Group (middle Eocene) by W. W. Olive overlies with marked unconformity the Wilcox (?) Formation and Porters Creek Clay. In the Lynn Grove quadrangle the unit is as much as 200 feet thick (Olive, 1-63). Westward, the Claiborne (?) is overlain by lithologically similar but younger deposits that on the basis of palynological evidence provided by Tschudy (Blade, 1-63) may be as young as Oligocene or Pliocene in age. Owing to lithologic similarity, scarcity of palentologic information, and very poor exposure, the younger deposits cannot be differentiated from the Claiborne (?); therefore, these sediments have been grouped by Blade (1-63), Finch (1-63), and Wilshire (2-63) into one unit that is designated “coastal plains deposits.” Surficial deposits ranging from Pliocene (?) through Recent, in age, blanket older rocks, concealing them over extensive areas. The oldest unit of these surficial deposits consists of gravel, sand, and clay as much as 100 feet thick, and is designated “continental deposits.” Leopold and Pakiser conclude that pollen from a clay sample collected by T. W. Lambert from such deposits in the Lynnville quadrangle is Pliocene or younger in age. Loess of Pleistocene age, which ranges in thickness from 1 or 2 feet in the easternmost of the mapped quadrangles to 26 feet in the westernmost, generally overlies the continental deposits; and alluvium of Recent and Pleistocene age and as much as 142 feet thick (L. N. Baker, 1-63) fills the stream valleys. Studies of valley deposits along the Ohio and Tennessee Rivers by W. I. Finch, W. W. Olive, and E. W. Wolfe (p. C130-C133) indicate the existence of an ancient lake of probable late Pleistocene age. A study of the thickness and size distribution of gravel deposits and of the configuration of the surface de- veloped on rocks beneath the surficial deposits suggests that the continental deopsits entered the Jackson Purchase from the southeast and poured onto a gently northward and westward sloping surface of low relief that rose to an altitude slightly above 500 feet in the southeastern part of the area. In some areas the surface is traversed by narrow deeply incised channels, filled with continental deposits. These channels reflect increased precipitation and rapid lowering of base level that accompanied the deposition of the continental deposits. Subsequent to deposition, probably during glacial epochs, the continental deposits in some areas were worked and redeposited at lower elevations. Northeasterly and northwesterly trending faults with displacements of as much as 150 feet displace rocks as young as Pliocene (?) and Pleistocene in age in parts of the Jackson Purchase area. Relation of clay mineralogy to depositional environment in Upper Jurassic shale, northeastern Texas K. A. Dickson has recognized a relation of clay mineralogy to depositional environment in shale of Late Jurassic age in Bowie and Cass Counties, northeastern Texas. The nonmarine “pastel” shale which contains illite and kaolinite grades into dark-gray or black offshore marine shale containing illite and iron-rich chlorite. Intermediate nearshore shale contains a mixture of illite, kaolinite, and chlorite. Caloosahatchee beds of Florida believed to be Tertiary A newly discovered outcrop of the Pliocene Caloosahatchee Formation on Shell Creek, in Florida, west of the late Miocene “Buckingham arch,” is reported by Druid Wilson. A previously known outcrop in North Ft. Myers no longer exists. Both localities produced specimens of a new species of the extinct pelecypod genus Agnocardia, previously known from beds no younger than the middle Miocene of Jamaica. The presence of Agnocardia in the Caloosahatchee supports a Tertiary rather than Pleistocene age for these beds. NEW ENGLAND AND EASTERN NEW YORK Geologic map of New England compiled A preliminary geologic map of New England has been compiled by Richard Goldsmith (1-64), based on much recent detailed mapping and unpublished information. The geologic map is supplemented by maps that show metamorphic zones and radiometric ages.A76 REGIONAL GEOLOGY MAINE Eastern border of “ribbon rock” facies located Continuing work by R. B. Neuman (1-64) on collections of Ordovician brachiopods from Maine and adjacent provinces of Canada has revealed additional European genera. However, a collection from Blue Bell, New Brunswick, yielded none of these, but does contain Zygospira, a genus common in North America but rare in Europe. The rocks from which this collection came are of the same age as at least part of the “ribbon rock” of Aroostock County and bordering New Brunswick, and thus the eastern boundary of that facies lies not far east of the international boundary. Structural history of Katahdin pluton A breccia zone as much as a mile wide has been found by R. B. Neuman in the Stacyville quadrangle in north-central Miane, along a 20-mile segment of the eastern and southeastern margin of the Katahdin pluton. The breccia consists of fragments, as much as tens of feet across, of metamorphosed and partially assimilated fine-grained sedimentary rocks in a matrix of granite or quartz monzonite. The Katahdin magma is believed to have stoped its way upward along a moderately inclined eastward-dipping surface across the steep structures of the sedimentary and volcanic units of the area. Apparently pure, fossiliferous Upper Silurian reef limestone was found through an area of about half a square mile, a mile east of the Katahdin pluton near the middle of the quadrangle. This limestone is interpreted to lie in a fault wedge that is part of the fault system followed by the East Branch of the Penobscott River in this area. Anticlinorium recognized in Maine and New Brunswick An extensive belt of limy rocks, thought to be Silurian by earlier workers, is of Middle to Upper (?) Ordovician age, according to Louis Pavlides and others (p. C28-C38), and extends from the Smyrna Mills quadrangle eastward and thence north and northeastward across northeast Maine. On the basis of reconnaissance and on mapping in Canada by a Canadian geologist, it appears that this Ordovician belt extends more or less continuously from Maine across northern New Brunswick and the southern part of the Gaspe Peninsula to Gaspe. Thus, it appears to form the core of a heretofore unrecognized anticlinorium, in the northern Appalachians, which is to be named the Aroostock-Matapedia anticlinorium. Tectonic activity in Aroostook County The northeast nose of a large anticline that lies to the northwest of the Aroostook-Matapedia anticlinorium has been mapped by Louis Pavlides in the Howe Brook and Smyrna Mills quadrangles, Aroostook County. On the northwest flank of this anticline is a discontinuous Silurian unit about 1,000 feet thick that contains brachiopods and corals. On the southeast side of the anticline a thick (probably exceeding 5,000 feet) sequence of quartzite, siltstone, and slate contains at least 18 graptolite localities that range from early Llandovery to early Ludlow in age. The contrast between the shelly fauna on the northwest flank of the anticline and the graptolitic fauna on the southeast flank suggests that this anticline acted as a positive landmass during most of Silurian time and strongly influenced the sedimentary and biologic regimen of the region. Local uplift along its northwest flank in Silurian or Early Devonian time has been recognized from reworked Silurian shelly faunas and clasts of Ordovician rocks that were apparently shed from this anticline and incorporated in the basal beds of the Seboomook Formation (Early Devonian age). Plant fossils were found by Louis Pavlides in the Howe Brook quadrangle at two localities. At one locality they have been recognized as of the psilophyton type and of Devonian age. Mapping indicates they are in rocks equivalent to the Chapman Sandstone of Early Devonian (New Scotland) age that occurs to the north in the Presque Isle quadrangle: Plant fossils date Acadian orogeny in northern Maine Identification of psilophytic plant fossils from the Mapleton Sandstone of northern Maine by J. M. Schopf (chapter D) indicates that the Mapleton, which was not deformed during the Acadian orogeny, is of early Givetian (Middle Devonian) age. The collections included new species described as Barrandeina{?) aroostookenis and Calamophyton forbesii; Calamophy-ton has not been previously reported in North America. This new work appears to bracket the beginning of the Acadian orogeny between the deposition of the Champman Sandstone (Early Devonia) and the Mapleton. Ostracodes date “nubbly beds” of Aroostook Limestone The “nubbly beds” of the Aroostook Limestone of Maine have been dated as Silurian (Clinton) by Jean Berdan’s discovery in them of ostracodes belonging to the genera Zygobolba, Apatobolbina, and Bolbineossin.NEW ENGLAND AND EASTERN NEW YORK A77 Formerly these beds were considered to be possibly of Late Ordovician age. Two types of schistosity found in western Maine Schistosity in the Rangeley quadrangle, Franklin County, is the end product of two contrasting processes, according to R. H. Moench. Pervasive earlier schistosity developed with advancing metamorphism from slaty cleavage, which originated at shallow depths when deformation of newly deposited sediments began. The slaty cleavage formed by flattening and dewatering of sediments at high pore pressures, and was accompanied at places by the formation of sedimentary dikes, where pore pressures were momentarily equal to lithologic pressures. Later, schistosity developed locally at the expense of a widespread slip cleavage and is a product of shearing and recrystallization at a relatively late stage in the tectonic history of the area. Structure of the Moxie mafic pluton Continuation of study of the Moxie mafic pluton by G. H. Espenshade shows that it is at least 50 miles long. It is 1 to 2 miles wide over much of this distance, but is 6 to 9 miles wide on the east side of Moosehead Lake, in Piscataquis County, where a gravity high suggests the site of a major feeder. The pluton is possibly an enormous irregular dikelike mass; it is not a simple layered body, but may be a complex of several intrusions. It must have been emplaced in a fluid state because cataclastic structure is rare, occurring only locally with faults. Mineral composition ranges from troctolite, to olivine-rich norite and gabbro, to olivine-free norite and gabbro. No regular pattern of compositional variation is evident. Probable flow structure is common; compositional layering is very rare. Pyrrho-tite with a little nickel and cobalt occurs at several places; exploration has failed to find deposits of min-able size. Age determination (K-Ar) of biotite by Henry Faul indicates an Early Devonian age for the pluton. Exploration target in west-central Maine Stream-sediment sampling on a tributary of Bean Brook in Somerset County, Maine, by F. C. Canney and E. V. Post (chapter D) indicates a metallic anomaly well above average for the region. Analysis of samples of active stream sediment showed lead and zinc contents as high as 2,500 and 7,000 parts per million, respectively. Known exposures of galena- and pyrite-bearing vein quartz are inadequate to account for the intense anomalies. Heavy-metal anomalies in southeastern Maine A geochemical map (VanSickle, Dennen, and Post, 1-64), based on colorimetric analyses of 1,100 samples of stream sediment from southeastern Maine, outlines an area of numerous copper and heavy metal (copper, lead, zinc) anomalies in a belt 18 miles wide east of the Penobscot River and extending northward from Blue Hill. These anomalies appear to be related to large masses of porphyritic granite of Devonian age, as well as to smaller bodies of pink biotite granite. The discovery of this belt of anomalies opens up an extensive area for mineral exploration, which heretofore has been directed principally toward coastal Maine. Heavy-metal anomalies related to Katahdin batholith Rechecking by E. V. Post and W. H. Dennen of some geochemical anomalies shown on a recent map (Post and Hite, 1-63) confirms the existence of several significant heavy-metal (copper, lead, zinc) anomalies in the Rainbow Lake-Nahmakanta Lake region, in the Harrington Lake quadrangle, eastern Piscataquis County, Maine. This region is part of a larger province in the southwestern part of the Katahdin granite batholith which has a relatively high metal content as compared to the rest of the batholith. Extensive topographic trenches suggestive of large faults in the geochemically anamalous area make it of greater than average interest for mineral exploration. Three Wisconsin glaciations recognized Maine may have been glaciated at least three times during Wisconsin time, according to G. C. Prescott, Jr. The principal evidences for multiple glaciation are till of two different ages and differences in directions of glacially produced lineations. The last glaciation probably occurred less than 12,000 years ago. MASSACHUSETTS Units correlated in Green Mountain anticlinorium The Cambrian (?), Ordovician, Silurian and Devonian metamorphic rocks of the east flank of the Green Mountain anticlinorium are being mapped in the Heath quadrangle, northwestern Franklin County, by N. L. Hatch, Jr. Efforts to trace the Vermont section south into Massachusetts indicate that the Pinney Hollow, Stowe, and possibly Ottauquechee Formations are not continuous across the State line, although similar rocks at the same stratigraphic positions are present to the south. Many excellent exposures of the Taconic unconformity are present in the area.A78 REGIONAL GEOLOGY The Cambrian and Ordovician stratigraphy east of the southern extension of the Green Mountain anti-clinorium has also been delineated in the Windsor quadrangle, Berkshire County, by S. A. Norton. There is evidence that the Ottauquechee Formation lenses out toward the south, and there is no distinct boundary between the Pinney Hollow and Stowe Formations, two units whose distinction from each other was based on the intermediate position of the graphitic schists and black quartzites of the Ottauquechee Formation. Deformation dated in southwestern Massachusetts A major unconformity separating Wilderness and Trenton rocks from older rocks has been established by E-an Zen in southwestern Massachusetts. In the Bash-bish Falls quadrangle, rocks as old as unit 2 of the Stockbridge Limestone (Zen, 1-64) are adjacent to the post-unconformity rocks. This observation is consistent with findings in Vermont where the same unconformity cuts down locally to the Precambrian basement. An episode of early, major deformation of the Stockbridge Limestone involves large-scale isoclinal recumbent folding. Several large-scale, apparently geometrically independent, structural elements, perhaps separated by thrust faults, exist in the Stockbridge, and may be related to the early deformation, which in turn may well prove to be preunconformity. An isotopic age of 360-890 million years was obtained from porphyro-blastic biotite and muscovite from a Berkshire Schist outcrop in the Bashbish Falls quadrangle. This age corresponds to the growth of the mica crystals, and also to the last known episode of major deformation. Therefore, the age determination casts doubt on the importance or even existence of an episode of regional retrograde metamorphism, postulated for these parts by numerous past workers. Ayer Granite dated near Worcester coal mine It. E. Zartman and R. F. Marvin have reported radio-active ages for samples collected by G. L. Snyder in east-central Massachusetts. The Millstone Hill body of Ayer Granite has a whole-rock age of 355 ± 10 million years. The Upper Devonian (?) age of emplacement of this body of Ayer Granite is of interest in that the granite crops out a quarter of a mile from a reported Pennsylvanian fossil locality at the Worcester coal mine. A new collection of fossil plant remains from this area tends to confirm the Pennsylvanian age, according to J. M. Schopf. Possibly the fossiliferous rocks are restricted to the area of the coal mine and are unconformable on the Ayer Granite. A muscovite K-Ar age of 242 m.y. on this granite suggests that some late Paleozoic thermal activity also affected this area. Three flows recognized in Deerfield Diabase The Deerfield Diabase in the Triassic rocks at Greenfield, hitherto considered to be 1 flow, has been shown by Andrew Griscom to consist of at least 3 flows with rather different magnetic properties and directions of remanent magnetization. Shelburne Falls dome found to be funnel shaped Preliminary analysis by R. W. Bromery of aeromag-netic and gravity data in the area of the Shelburne Falls dome of Franklin County indicates that the low-density magnetic rock mass of the dome is funnel shaped with thickest section at its southeastern end. The northeast lobe of the mass is probably a spoon-shaped body whose central part is approximately 4,000 feet thick. Basement surface mapped on Cape Cod Interpretation of seismic measurements in the Harwich and Dennis quadrangles on Cape Cod by R. N. Oldale discloses an eastward-trending basement ridge composed of crystalline rocks of Paleozoic age or older, with compressional speeds of 14,100 to 22,000 feet per second. The altitude of the basement surface ranges from about 180 to 560 feet below sea level, and the maximum depths occur in four south-sloping valleys. Three seismic layers distinguished above the basement are believed to consist of an upper layer of unsaturated stratified drift, a middle layer of saturated stratified drift and minor amounts of till, and a lower layer of compact till and possibly minor amounts of coastal plain deposits of Tertiary or Mesozoic age. Seismic studies elsewhere on Cape Cod by R. N. Oldale and C. R. Tuttle (1-64) show that crystalline basement rocks are overlain by Pleistocene, Tertiary, and possibly Mesozoic deposits that range from 250 to possibly more than 960 feet in thickness. A trough in the basement surface extending to about 900 feet below sea level was found on outer Cape Cod near Truro. Other seismic studies in Massachusetts are described in the section “Engineering Geology.” Glacial units delineated in southeastern Massachusetts Six drifts and the deposits of one interglaciation have been recognized on Martha’s Vineyard by C. A. Kaye (p. C134—C139). It is thought that they represent Nebraskan Glaciation, Aftonian Interglaciation, and Kansan, early and late Illinoian, and early and late Wisconsin Glaciations. Periglacial effects of the middle Wisconsin Glaciation, whose terminal moraine isNEW ENGLAND AND EASTEEN NEW YOEK A79 nearby at the Elizabeth Islands, are also evident. The stratigraphy, which is very much complicated by severe ice thrusting, is remarkably similar to that worked out by Fuller and Woodworth half a century earlier. Three of these drifts of Martha’s Vineyard are in part terminal moraines, according to Kaye (p. C140-C143). The oldest is a fragmentary early lllinoian moraine. The hills and valleys of the western part of the island are the eroded remains of a very large moraine pushed up by late lllinoian ice. Early Wisconsin ice generally stopped against the high late lllinoian moraine, but built an extensive moraine in the eastern part of the island. Studies of till in the Taunton quadrangle of southeastern Massachusetts by J. H. Hartshorn show that it is possible to distinguish between flowtill (a superglacial till) and subglacial till by stone counts, in addition to the usual criterion of position in or on ice-contact stratified drift. The proportion of rock types from the Narragansett basin, within which the quadrangle lies, relative to that of rock types from north of the basin, increases southward within the quadrangle in subglacial till, but decreases southward in flowtill. Three readvances of last glaciation in Boston area According to C. A. Kaye, the retreat of the last ice sheet across the Lynn quadrangle, just north of Boston, was characterized by at least three readvances, each falling short of the maximum extent of the previous one. The direction of ice flow was different for each readvance and it is this fact that made possible the recognition of this retreatal pattern. Glacial striations of each of three main azimuths are grouped into oblate belts, which also correlate with the distribution of out-wash deposits. The readvances probably mark climatic fluctuations of periods of less than a century. Pleistocene beaches recognized Pleistocene marine beaches ranging in altitude from present-day sea level to 70 feet above sea level have been recognized in the Newbury port East quadrangle in northeastern Massachusetts by J. E. Cotton. Drilling evidence indicates that these beaches are underlain by 30 to more than 50 feet of marine clayey silts. Glacial lake deposits The Boylston, Clinton, and Ayer stages of glacial Lake Nashua have been outlined by Carl Koteff in the Clinton quadrangle, Worcester County, virtually as by previous workers. However, the Leominster stage is recognized as a separate glacial lake about 80 feet higher than the Clinton stage. Lake Leominster came into existence after the Clinton stage, and was completely drained before the lowering of Lake Nashua from the Clinton stage to the Ayer stage. Deposits of glacial Lake Bascom in the Williamstown area of northwestern Massachusetts include silt, clay, and delta gravel. The laminated silt and delta gravel occur mostly at the level suggested by F. B. Taylor to be the highest and most prominent shoreline, about 1,125 feet above sea level. Blue and yellow clays occur mostly below about 950 feet above sea level, and as deep as 116 feet below the flood plain of the Hoosic River at Williamstown (or about 485 feet above sea level). The clays are interbedded with and overlain by coarse gravel, probably glaciofluvial in origin; this suggests several generations of lake deposition, alternating and concluding with stream deposition. RHODE ISLAND Geologic map of Rhode Island completed A preliminary geologic map of Rhode Island has been compiled by A. W. Quinn (1-64). The major groups of rocks include metasedimentary rocks of the Black-stone Series of Precambrian (?) age, metasedimentary rocks of middle Paleozoic age or older, very widespread plutonic rocks of Mississippian (?) age or older, granites and volcanic rocks of the East Greenwich Group of Mississippian (?) age, sedimentary rocks of Pennsylvanian age in the Narragansett basin, and granites of Pennsylvania age or younger. Feldspathization widespread in metamorphic rocks According to Tomas Feininger, extensive feldspathization of schists derived from politic rocks has been an important process in southwestern Rhode Island. Feldspathization was the result of alkali metasomatism from granitic magmas during and immediately following intrusion. The effects of this process are visible in the gneissic granitic rocks which ultimately crystallized from the magmas as well as in the metasomatites. Absalona Formation believed igneous Abundant inclusions of different lithologic character in the Absalona Formation in the Clayville quadrangle, west of Providence, mapped by G. E. Moore, Jr., indicate that this formation is possibly igneous in origin. The lithology of the formation is similar to that of the probably magmatic quartz diorite gneiss of the quadrangle.A80 REGIONAL GEOLOGY Late Paleozoic igneous relations clarified Reports on two adjacent areas, the Coventry Center quadrangle, by G. E. Moore, Jr. (1-63), and the Crompton quadrangle, by A. W. Quinn (1-63), cover an area southwest of Providence that is almost entirely underlain by the Scituate Granite Gneiss and related rocks. These plutonic rocks show evidence of magmatic origin, and are of Mississippian( ?) age or older. Still older are small bodies of metasedimentary rocks. Mississip-pian (?) granite and volcanic rocks of the East Greenwich Group underlie much of the eastern part of the Crompton quadrangle, which also contains a very small area of the Pennsylvanian sedimentary rocks of the Narragansett basin. The rocks of these quadrangles were affected by at least two and perhaps three periods of metamorphism, the last of which followed the deposition of the Pennsylvanian rocks. The gabbro of the northwestern part of the Coventry Center quadrangle is unmetamorphosed, and possibly is younger than the time of metamorphism of the Pennsylvanian rocks. Extensive moraine mapped across Rhode Island A discontinuous morainic line in southwestern Rhode Island and southeastern Connecticut extends almost 50 miles north-northeastward, according to recent mapping and reconnaissance by J. P. Schafer. The line includes to the east the short moraine segments mapped by earlier workers near Kingston, R.I., and to the west the two closely parallel moraines recently mapped by Goldsmith near Niantic, Conn. This morainic line lies about 4 miles south of the similar Ledyard moraine37 and 5 to 9 miles north of the much larger Harbor Hill-Charles-town moraine. CONNECTICUT Tunnel mapping provides new information on Triassic rocks near Hartford The geology of the mile-long Talcott Mountain Tunnel in the Avon quadrangle, west of Hardfort, was mapped by R. W. Schnabel. The tunnel exposed a complete section through the upper part of the New Haven Arkose (siltstone and sandstone), the Talcott Basalt, the Shuttle Meadow Formation (77 feet thick, nearly all siltsone), and the lower part of the Holyoke Basalt. The Talcott Basalt, 180 feet thick, is a heterogeneous mixture of basalt and basalt-sandstone breccia, and may be composed of several flows. The Holyoke Basalt, 330 feet of which is exposed in the tunnel, is massive to pris- *> Richard Goldsmith, I960, A post-Harbor Hill-Charlestown moraine in southeastern Connecticut: Am. Jour. Sci., v. 258, p. 740-743. matically jointed, and contains in the upper part of the exposure a red vesicular and amygdaloidal zone that indicates that here the Holyoke Basalt consists of at le'ast two flows. Gabbro body near Lebanon outlined Geologic and gravity studies by M. F. Kane and G. L. Snyder (p. C22-C27) have shown that the discordant gabbroic instrusive body near Lebanon, Conn., is a northeast-trending boat-shaped mass 10 miles long, 2 miles wide, and 3,000 feet deep attached by its stem to a dominantly northwest-trending curved sheet 15 miles long and as much as % a mile wide. Gneissic granitic rocks recognized as magmatic Evidence from the Ashaway and Voluntown quadrangles, along the Connecticut-Rhode Island border, mapped by Tomas Feininger, strongly suggests that the gneissic granitic rocks of the area were intruded as magma. Some of the more silicic granites contain layers of nodules, from 1 to 15 cm in diameter, of quartz-sillimanite, or quartz-muscovite-sillimanite. The layers of nodules are believed to reflect highly per-aluminous domains within a magma which had an overall peraluminous composition. Igneous events dated in eastern Connecticut R. E. Zartman and R. F. Marvin have reported several useful radioactive ages for rock and mineral samples collected by G. L. Snyder and H. R. Dixon in eastern Connecticut. The premetamorphic Canterbury Gneiss and related rocks and a postmetamorphic pegmatite have been dated directly, and a minimum age has been obtained for the gabbro of Lebanon. The Canterbury Gneiss gives a Rb-Sr whole-rock age of 405 ± 20 million years as its time of emplacement, and a related granite dike has a Rb-Sr whole-rock age of 390±20 m.y. This granite dike transects, and contains, schlieren of the gabbro of Lebanon, indicating that the gabbro was emplaced before 390 m.y. ago. The strontium in the granite underwent isotopic homogenization during a metamorphism 285 m.y. ago, and its muscovite gives a 237 m.y. K-Ar age. In the area of the Willim-antic dome, muscovite in an unmetamorphosed pegmatite has a Rb-Sr age of 245 m.y. Periglacial features in northeastern Connecticut An exposure of a polygonal network of late-glacial ice-wedge structures in glacial outwash at Thompson, in northeastern Connecticut, was studied by J. P. Schafer. Individual structures have been seen at other localities, but this is the first known network in NewAPPALACHIAN REGION A81 England, and it confirms the existence of permafrost conditions as the last ice sheet retreated. ADIRONDACK MOUNTAINS Phacoliths ascribed to metasomatism Work by A. E. J. and Celeste G. Engel38 indicates that the 14 phacoliths in the northwest Adirondack Mountains are products of large-scale granitic and mafic metasomatism. The parent rock was a thick calcareous quartzite at the base of the exposed Grenville sequence. Both granitization and amphibolitization of beds in this quartzite accompanied its deformation into complex and refolded folds. The flanks of the phacoliths are commonly a plagioclase-rich granitic rock with numerous amphibolite interlayers; both of these rocks grade laterally into quartzite and calcareous quartzite. The end product of metasomatism is alaskitic granite with scattered interlayers of amphibolite; these rocks form the cores of the phacoliths and appear in the crests of the folds and diapiric domes. At least 120 cubic miles of the phacoliths is demonstrably of meta-somatic origin. The proof lies in the complicated patterns of relict bedding in granite and amphibolite. This bedding forms a distinctive stratigraphic sequence that may be traced from phacolith to phacolith throughout an area of 1,200 square miles. Analagous “phacoliths” appear in the southwest and southern Adiron-dacks. Very probably, more than three-fourths of the granitic rock in the northwestern and southern Adiron-dacks, outside the central massif, is of metasomatic origin; an equivalent percentage of the layered amphibolites in the same regions is formed by mafic metasomatism and metamorphic differentiation along beds of initially quite different sedimentary composition. Gravity anomaly mapped near Lake Champlain Local gravity highs near Chateaugay and Ellenburg, N.Y., Jericho, Vt., and Plattsburgh, N.Y., are roughly alined along a regional gravity arch which strikes approximately west-northwest and intersects the Appalachian structural trends at a high angle, according to W. H. Diment (1-64). The centers of the largest gravity (25 milligals) and magnetic (2500 gammas) anomalies nearly coincide, about 4 miles north of the center of Plattsburgh, N.Y. The area is covered by Cambrian and Ordovician sedimentary rocks, and the rocks causing the anomalies are not exposed. The tops 38 A. E. J. Engel, and C. G. Engel, 1963, Metasomatic origin of large parts of the Adirondack phacoliths : Geol. Soc. America Bull., v. 74, p. 349-354. of the shallowest anomalous rocks are no more than several thousand feet below the surface, but because the thickness of the Paleozoic rocks is of the same order, it cannot be determined from the available data whether the anomalous rocks intrude the Paleozoic sedimentary rocks or whether they are wholly contained in the Precambrian basement rocks. The trend of the anomalies parallels that of the Monteregian Hills 50 miles to the north, and the local anomaly at Plattsburgh resembles the anomalies caused by the more mafic intrusions of alkalic rocks that form the Monteregian Hills. Therefore, the anomalies may be the expression of subsurface intrusives of the Monteregian type. Glacial lake deposits in Lake Champlain area In the region near Plattsburgh, N.Y., a moraine built on west side of an ice lobe in the Champlain Valley during later Wisconsin time dammed large valleys, such as the Saranac River valley, that drain northeastward from the mountains, according to C. S. Denny. Nonglacial waters from these valleys flowed along the edge of the ice and swept away large masses of moraine, leaving broad expanses of bare rock, locally cut by small canyons. The withdrawal of the edge of the Champlain Valley ice lobe from the moraine initiated small marginal lakes. The deposits formed in these lakes were formerly believed to have been deposited in a proglacial lake that filled the Champlain Valley, named the Coveville stage of Lake Vermont. Further withdrawal of the Champlain Valley ice lobe led to formation of one large lake, the Fort Ann stage of Lake Vermont of Chapman. APPALACHIAN REGION STRATIGRAPHIC STUDIES Most current stratigraphic studies in the Appalachian region are being done in the Valley and Ridge province, but progress is being made also in the stratigraphy of parts of the Blue Ridge and Piedmont provinces. Revision of Helderberg Group in New York and Virginia Continued work by J. M. Berdan (1-64) on the Helderberg Group of east-central New York supports previous work by L. V. Rickard, of the New York State Geological Survey, showing that the type Manlius Limestone is of Devonian rather than Silurian age and belongs in the Helderberg Group. The previously accepted Silurian age for at least part of the formation was based on miscorrelation with beds in other areasA82 REGIONAL GEOLOGY actually equivalent to the underlying Cobleskill Limestone. In the Valley and Ridge province, work on a similar problem by R. L. Miller, L. D. Harrris, and J. B. Roen (p. B49-B52) in Scott, Wise, and Lee Counties, southwestern Virginia, has shown that a unit of abundantly fossilferous calcareous sandstone 40 to 45 feet thick lies disconformably on the Hancock Limestone (or Dolomite) of Silurian age and disconformably beneath the Chattanooga Shale of Late Devonian and Early Missis-sippian age. At its type locality in the Big Stone Gap area the sandstone seems to be entirely of Helderberg age, but its upper part in several other places contains beds that are of Oriskany and Schoharie ages. These post-Helderberg rocks are probably remnants of a more extensive but thin layer of late Middle Devonian sediments only locally preserved from pre-Chattanooga erosion. Conodonts suggest correlatives of Big Stone Gap Shale Member of Chattanooga Shale, Virginia J. W. Huddle’s discovery of the conodont, Spathog-nathodus anteposioomis in the lower part of the Big Stone Gap Shale Member of the Chattanooga Shale of southwest Virginia (Roen and others, p. B43-B48) suggests a correlation with the Bedford Shale of Ohio, Knapp and Riceville Formations of northwest Pennsylvania, and the Louisiana Limestone of the Mississippi Valley. This conodont species is characteristic of the Gnathodus n. sp. A zone of Charles Collinson and others.39 Age of Rome Formation in central Kentucky L. D. Harris has compared detailed surface mapping of the Rome Formation and Conasauga Group in northeastern Tennessee with deep well records from adjacent parts of Virginia and Kentucky. From this comparison he concludes that the Rome Formation, which is of Early Cambrian age in its outcrop areas, is probably of Middle Cambrian age in the subsurface of central Kentucky (Harris, p. B25-B29). Paleokarst features on Knox Group surface Continuing studies of the upper part of the Knox Group in the Sequatchie Valley of southeastern Tennessee have provided additional information on paleokarst features developed on the surface of the Knox Group before renewed deposition in Middle Ordovician 39 Charles Collinson, A. J. Scott, and C. B. Rexroad, 1962, Six charts showing biostratigraphic zones, and correlation based on conodonts from the Devonian and Mississippian rocks of the Upper Mississippi Valley : Illinois Geol. Survey Circ. 328, p. 870. time. Collapse breccias found by R. C. Milici, of the Tennessee Division of Geology, and Helmuth Wedow, of the U.S. Geological Survey, occur along the interface between the uppermost thick limestone of the Knox Group and overlying fine-grained dolomite about 400 feet below the post-Knox unconformity. Ancient channels or sinkholes on the unconformity, filled with basal Middle Ordovician sediments, exhibit a stratigraphic relief of more than 100 feet. Mount Rogers Volcanic Group subdivided in Virginia In the Blue Ridge province of southwestern Virginia, a stratigraphic sequence in the Mount Rogers Volcanic Group has been worked out by D. W. Rankin. Three principal units are recognized: a lower heterogeneous unit consisting of conglomerate, graywacke, mafic silt-stone, and basalt; a middle unit consisting of rhyolite and latite flows; and an upper unit of maroon mudflow conglomerate, arkose, rhythmite, shale, and minor basaltic pillow lava. The upper unit with mudflow conglomerate at the top underlies the Chilhowee Group or Early Cambrian and Early Cambrian (?) age with apparent conformity. Because several of these units from the oldest to the youngest lie on older Precam-brian granitic rocks, the Mount Rogers Group must have been deposited in an area of basement rocks with considerable topographic relief. Subdivision of the Glenarm Series in Maryland Recent work by D. L. Southwick in the difficult and complex metamorphic rocks of the Piedmont in Maryland has provided better information than previously available on the stratigraphy of the Glenarm Series. So far recognized are a provisional lower sequence containing schistose quartzite (Setters Formation), marble (Cockeysville Marble), a thick unit of pelitic schist (eastern facies of the Wissahickon Formation), and a unit of metamorphosed slump breccia and related pre-tectonically disrupted metasedimentary rocks, probably part of the Sykesville Formation of Hopson.40 A supposedly upper sequence containing conglomerate, quartzite, and interbedded phyllite and micaceous quartzite (Peters Creek(?) Quartzite) and a thick section of garnet-muscovite schist (compare western facies of the Wissahickon Formation) appears to be separated from the lower sequence by a discontinuity that is probably an unconformity or a major fault. 40 C. A. Hopson, 1963, Large-scale submarine landslip deposits in the Glenarm Series, Maryland Piedmont: Geol. Soc. America Spec. Paper 73, p. 10-11.APPALACHIAN REGION A83 Corals in the Marcellus Shale in Virginia Corals from a limestone nodule in the Marcellus Shale near Christiansburg, Va., collected by J. T. Dutro, Jr., and R. B. Neuman, were identified as Nalivkinella sp. by W. A. Oliver, Jr. The Virginia species is closely related to, or identical with, a species from the Stony Hollow Member (Cooper, 1941) of the Marcellus in eastern Pennsylvania, and suggests a correlation of the Virginian unit with the Cherry Valley Limestone Member of the Marcellus in New York. Graptolites in Martinsburg Shale in New Jersey Graptolites from two outcrops of the Martinsburg Shale near Clinton, N.J., discovered by Harry Dodge during graduate work at Princeton, were re-collected by Dodge and R. B. Neuman and have been identified by W. B. N. Berry (University of California, Berkeley) as of Early and Middle Ordovician age. The shale appears to overlie the Middle Ordovician Jacksonburg Limestone which, in turn, lies above a Cambrian and Ordovician carbonate sequence. One explanation is that the Martinsburg in this area may contain exotic slump blocks comparable to those bordering the Taconic Mountains in the Hudson River Valley. Structural history of Ordovician rocks in Pennsylvania and New Jersey A statistical study of minor structures in the Jacksonburg Limestone, Martinsburg Shale, and related rocks, recorded during mapping in easternmost Pennsylvania and western New Jersey by A. A. Drake, Jr., provides good evidence that these rocks have been deformed at least twice. Plots of slaty cleave age show regional rotation around well-defined tectonic axes, and later-developed slip cleavage is conspicuous locally. The Paleozoic rocks in this area can best be interpreted as the normal limb of a large recumbent fold that has been refolded and faulted. Gaps in eastern Pennsylvania not due to superposition Geologic mapping of a classic area of wind and water gaps in the vicinity of Delaware Water Gap, eastern Pennsylvania, recently completed by J. B. Epstein, shows that most of the gaps are located where erosion-ally resistant rocks are cut by faults or are otherwise thinned. This evidence is opposed to interpretations that the major drainage lines were superposed from a former peneplain or coastal-plain cover. Two ages of diabase dikes in South Carolina Recent mapping by N. C. Koch has shown that the granites and gneisses of Greenville County, S. C., are cut by many northwest-trending diabase dikes probably of Triassic age. Another set of diabase dikes trends about N. 25° E. These dikes are clearly older and somewhat metamorphosed; they are probably of Paleozoic age. GEOPHYSICAL STUDIES Airborne magnetic and radiometric surveys in support of geologic mapping and structural investigations in the Blue Ridge and Piedmont provinces were carried out (1) in western New Jersey, (2) in an area of large gabbro bodies in the vicinity of Baltimore, Md., and (3) in areas of crystalline rocks in northeastern and southwestern Virginia. This work almost completes aero-magnetic coverage of a belt of varying width in the crystalline Appalachians extending from central Virginia to the Maine-New Brunswick border. Crystalline rocks at two levels in Reading prong Analyses of aeromagnetic and gravity data by R. W. Bromery indicate that the crystalline rocks at the west end of the Reading prong in southeastern Pennsylvania occur at two levels, one exposed at the ground surface and one at a deeper level approximately a mile below the surface. Rocks of contrasting physical properties are interpreted as separating these levels of crystalline rocks. Structural trends in basement rocks mapped by aero-magnetometer Depths recently calculated from contoured aeromagnetic maps have provided new information needed in preparing a contour map of the top of the Pre-cambrian surface in the Appalachian region and in defining structural trends in the basement rocks. The results (Griscom and Zietz, 1-64) indicate that magnetic basement rocks lie at much shallower depths than predicted from stratigraphic and structural evidence in the Taconic region of southwestern Vermont, in Clearfield County, Pa., in southwestern Virginia, and in northwestern Georgia. Northeast trends of elongate magnetic anomalies in west-central Pennsylvania interpreted by M. E. Beck, Jr., and R. E. Mattrick indicate a small but consistent divergence of Precambrian and Paleozoic structural trends, the Precambrian axes having a more northerly orientation. A markedly linear magnetic gradient, traceable from near Wheeling, W. Va., to Venango County, Pa., coincides with a slight break in basement slope and may record the presence of a major basement fault.A84 REGIONAL GEOLOGY Radiometric highs in North Carolina Analysis of aeromagnetic and radiometric data previously obtained in the Concord area, North Carolina, reveals two radiometric highs within an aeromagnetic low. One of the radiometric highs is over an exposed granite pluton, but the other is over an area of me-tagabbro and metadiorite injected by abundant granitic material and cut by granite dikes. This granitic material is probably the cause of the high radioactivity level but is not sufficient to cause the negative aeromagnetic anomaly if the mafic rocks extend to any depth. GEOCHEMICAL EXPLORATION High Rock quadrangle, North Carolina Results of analyses of samples of stream alluvium from the High Rock quadrangle, North Carolina, reported by A. A. Stromquist, A. M. White, and J. B. McHugh (p. C88-C91) indicated slight but significant enrichment of base metals in the western half of the quadrangle compatible with the pattern of mineralization as indicated by prospects and mines northwest, west, and southwest of the area. GEOCHRONOLOGICAL STUDIES Data on age of the slate belt, North Carolina Two lead-alpha age determinations by T. W. Stem on zircon from felsic crystal-lithic tuff from the Carolina slate belt suggest an Ordovician age for these rocks studied by A. M. White and others (1-63). The two samples are from the southeastern part of the Albemarle quadrangle, North Carolina. The new data add further support to the concept that much of the southeastern Piedmont province is of Paleozoic rather than Pre-cambrian age. QUATERNARY GEOLOGY Studies of surficial deposits in the Appalachian region during the year were done mainly in conjunction with geologic mapping in several widely separated areas. J. B. Epstein found that ice of the Wisconsin Glaciation crossed Kittatinny Mountain in the Stroudsburg area, Pennsylvania, and that a hitherto unreported proglacial lake, called Lake Sciota, formed between the Wisconsin terminal moraine and the mountain. An exposure of peat and associated clay and sand, first described by Kerr in 1875, was restudied during geologic mapping of a part of the Piedmont near Mor- ganton, N.C., by J. C. Reed, Jr. (4-64). Pollen assemblages studied by E. B. Leopold and Louise Weiler showed that this deposit, located in a former valley 100 feet below the Piedmont upland surface, is not glacial but probably represents an interglacial episode in Pleistocene time. The Piedmont surface is significantly older and therefore is probably older than Pleistocene. Unconsolidated clay, sand, gravel, and boulders in the buried valley of the Susquehanna River in Luzerne and Lackawanna Counties, Pa., were studied by M. J. Bergin, J. F. Robertson, and L. M. McNey in connection with the problem of mine drainage in the northern anthracite field. Preliminary results show that these deposits lie on an irregular surface with as much as 100 feet of topographic relief. A main channel and several tributary channels of the ancient glaciated valley system can be identified. EASTERN PLATEAUS PENNSYLVANIA Revision of Devonian-Mississippian boundary The need for revision of the Devonian-Mississippian boundary in north-central Pennsylvania is suggested by continuing geologic investigations in Tioga County. Strata previously believed to be of Mississippian age are reported by G. W. Colton to be of Late Devonian age on the basis of a preliminary field examination of fossil plant material by J. M. Schopf. If this conclusion is substantiated by laboratory examination, the boundary between the two systems will be raised, thus increasing the thickness of rocks assigned to the Upper Devonian Series and sharply decreasing the thickness of the Mississippian System. The fossil plants and a closely related regionally extensive and distinctive thin conglomerate bed together may furnish the most easily recognized boundary between the two systems yet reported in the State. KENTUCKY Geologic mapping of State A major undertaking to provide complete detailed geologic map coverage for the State of Kentucky was begun in the fall of 1960, in cooperation with the Kentucky Geological Survey. The maps are being published as 7y2 minute quadrangles (scale 1: 24,000 in the Geologic Quadrangle Map series). As of June 30, 1964, 91EASTERN PLATEAUS A85 quadrangles have been published, 29 are in press, 106 are completed and in review, and 92 are currently being mapped. Quadrangles published during fiscal year 1964 are given in the “List of Publications” (see Kentucky, geologic maps, in the “Index to Publications”). Upper Mississippian revised in Cumberland Mountains The stratigraphy of the Lee Formation has been revised by K. G. Englund on the basis of studies in the Cumberland Mountains of southeastern Kentucky (p. B30-B38). The Lee, which grades into and laterally intertongues with the Pennington Formation of Mississippian age, is redefined to include seven mappable members, in ascending order: the Pinnacle Overlook, Chad well, White Rocks Sandstone, Dark Ridge, Mid-dlesboro, Hensley, and Bee Rock Sandstone Members. Subdivisions of the Lee are based on lithologic changes in a repetitious sequence of massive conglomeratic sandstone and nonresistant units of thin-bedded sandstone, siltstone, shale, coal, and underclay. Predominance of massive quartzose conglomeratic sandstone with intervening coal beds distinguishes the Lee from the shale and limestone sequence of the Pennington. Devonian sequence revised Biostratigraphic study of the pre-New Albany Devonian succession in Kentucky by W. A. Oliver, Jr., and J. T. Dutro, Jr., has demonstrated the widespread nature of both new and previously recognized faunal zones. Rocks of Schoharie age include in the Louisville area the lower part of Jeffersonville Limestone; and at Kentucky Lane, the Camden Chert. Possibly some rocks of Schoharie age occur at Lake Cumberland. Rocks of Onondaga age include the remainder of the Jeffersonville and unnamed units at Kentucky Lake and Lake Cumberland. A coral fauna of Onondaga age is found in the Boyle Formation at one locality in the Broadhead quadrangle, southwest of Berea in eastern Kentucky, but other rocks; previously reported to be of Onondaga age, are of Hamilton age. The Boyle Formation is largely Hamilton in age; the Pegram Limestone may be entirely Hamilton in age. Rocks of Hamilton age, though widespread elsewhere, are not known in western Kentucky. Mississippian channel fill mapped Detailed mapping of an extensive channel-fill sandstone of Late Mississippian age along the eastern edge of the western Kentucky coal basin by W. C. Swadley, E. G. Sable, and W. L. Peterson has confirmed earlier work by L. L. Ray and others.41 The deposit was traced for about 18 miles across the Flaherty, Big Spring, and Constantine 7%-minute quadrangles, and eroded remnants were found to extend northeastward about 3 miles to the vicinity of Tip Top in the Fort Knox quadrangle. The recent mapping indicates that the sandstone forms part of the Morretown Formation of Late Mississippian age and fills a channel that was cut as much as 140 feet into the underlying Paoli and Ste. Genevieve Limestones. In the northernmost outcrops the channel deposit is medium-grained sandstone but grades southward to medium- to fine-grained sandstone and clay shale containing small amounts of sandy limestone. Extensive sandstone bar mapped in Mississippian A large body of sandstone of Mississippian age has been partly delineated in south-central Kentucky by C. H. Maxwell, R. O. Lewis, and R. E. Thaden, during geologic mapping in the Russell Springs, Montpelier, Dunnville, and Knifley (Maxwell, 1-64) quadrangles, Russell and Adair Counties. The sandstone body is elongate, having a length of about 18 miles, a maximum width of 6 miles, and a maximum thickness of at least 240 feet. Trend of the sandstone is northwestward parallel to limestone reefs in the Fort Payne Formation that lie southwest of the sandstone. Contemporaneous development of sandstone and reefs is suggested. The sandstone body possibly formed as a nearshore bar; the reefs grew farther offshore. The proximity of the sandstone and reef limestone may be of commercial importance. The reefs are oil reservoirs in Adair and Metcalf Counties, but little is known of the extent of the sandstone in the subsurface. Cryptoexplosion feature mapped in Bluegrass region A circular cryptoexplosion feature 3y2 miles northeast of Versailles, Woodford County, has been mapped by D. F. B. Black (p. B9-B12). The previously unreported structure has a diameter of about 5,000 feet and consists of (1) a brecciated central dome, (2) a marginal depression partly bounded by normal faults, and (3) an outer semicircular anticline of low amplitude on the east margin. Similarity of the Versailles structure to structures of known and supposed meteorite-impact origin and the high degree of breccia-tion, otherwise rare in the region, may indicate a similar origin for the Versailles structure. 41L. L. Ray, A. P. Butler, Jr., and C. S. Denny, 1947, Relation of sand deposits at Tip Top, Kentucky, to the Meramec-Chester boundary : Kentucky Dept. Mines and Minerals, Geologic Div. Bull., ser. 8, no. 9, 16 p.A86 REGIONAL GEOLOGY SHIELD AREA AND UPPER MISSISSIPPI VALLEY Rift-valley hypothesis for midcontinent gravity high Geologic features in the Lake Superior region provide a basis for interpretation of a prominent gravimetric anomaly that extends for 800 miles south westward from Lake Superior. According to W. S. White, the size and configuration of the midcontinent gravity high lead naturally to a hypothesis, among others, that it is a fossil rift valley filled with Keweenawan lavas and sediments. Geologic information from the Lake Superior region, where the rocks causing the gravity high emerge from beneath their Paleozoic cover, offers some support to the rift-valley hypothesis, and also presents some puzzles. Supporting facts and inferences are the following: (1) The Keweenawan rocks are depressed with respect to the older rocks on either side. (2) The lava-filled trough has faults at or close to its margins in many places. (3) In Michigan, the Keweenawan rocks thin away from Lake Superior at a rate that suggests no great difference between the ancient and present margins of the trough. (4) The Lake Superior basin is probably not a simple syncline, and may well have irregularities in the form of uplifted and depressed blocks such as typify the great rifts of the world. As an example, both geologic and geophysical evidence suggest that the large gravity low mapped by Thiel42 under the Bayfield Peninsula in Wisconsin is more readily explained as an ancient positive area (or horst) over which the lavas are thin or absent than as an area of extradordinarily thick sedimentary cover. The presence of a horst of this sort would mean that the Duluth Gabbro and Keweenawan lavas of Minnesota lie in one trough (or graben), and the Keweenawan rocks in the vicinity of the Michigan-Wisconsin State line lie in another. The following features complicate the rift interpretation. (1) Border faults that can be seen today are reverse faults rather than normal faults; they dip toward the axis of the trough opposite to the direction of dip for the reverse faults that some geologists have postulated as a cause of grabens. (2) Relatively uniform basinward thickening of stratigraphic units observed in Michigan suggests that the margin of the basin was a hinge zone rather than a fault zone. (3) Keweenawan sedimentary rocks only locally contain abundant pebbles of more ancient (pre-Keweenawan) rocks, such as would « Edward Thiel, 1956, Correlation of gravity anomalies with the Keweenawan geology of Wisconsin and Minnesota: Geol. Soc. America Bull., V. 67, p. 1079-1100. normally be eroded from the uplifted margins of a steep-walled rift valley. MICHIGAN Geophysical-geological studies of Marquette iron district Magnetometer surveying by K. L. Wier and geologic mapping by J. E. Gair (2-64) northeast of Palmer in the Marquette iron-bearing district have provided the following information: (1) A magnetite-bearing unit, 50 to 100 feet thick, is in the lower part of the Siamo Slate. The magnetic expression of this unit appears to be a dependable stratigraphic marker and has been used to determine structural details. The unit is strongly magnetic in several places where it is in contact with metadiabase, and although the magnetite content may be quite large, such occurrences are probably too small in volume to be of economic importance. (2) A previously unrecognized body of the Negaunee Iron-Formation extends east of a tabular body of metadiabase in secs. 17 and 20, T. 47 N., R. 26 W. (3) A “sill-like” intrusion of metadiabase cuts across sedimentary beds, indicating that such intrusive bodies may not be reliable stratigraphic markers, as previously supposed. (4) Faulting occurred both before and after intrusion of metadiabase masses. Angular unconformity at base of Ajibik Quartzite Mapping by C. E. Fritts along the north limb of the Marquette synclinorium near Negaunee, Mich., has shown that the much debated angular unconformity at the base of the Ajibik Quartzite is well displayed about a quarter mile to half a mile east of U.S. Highway 41, rather than adjacent to the highway. Typical Kona Dolomite exposed several miles east of Negaunee grades westward into a nearshore facies of at least three slate-quartzite units, the lowest of which formerly was mapped in part as Ajibik near U.S. Highway 41. Age of mafic intrusives in Gogebic district Restudy of the east end of the Gogebic iron-bearing district, Michigan, by W. C. Prinz has revealed that the mafic intrusives in the Ironwood Iron-Formation in the area east of Wakefield are metamorphosed and are thus not Keweenawan in age as most previous workers believed. This interpretation casts doubt on the generally accepted idea that the mafic dikes and sills that localize many of the ore deposits of the district are Keweenawan in age. This difference in geologic age of intrusion might have significant bearing on hypotheses of the origin of the ore deposits.SHIELD AREA AND UPPER MISSISSIPPI VALLEY A87 Aeromagnetic surveys in Gogebic district Aeromagnetic surveys have been made over about 800 square miles in Gogebic and Ontonagon Counties, Mich., covering the east end of the Gogebic iron range and the area immediately east of the range. Interpretation to date by J. E. Case (1-64), W. C. Prinz, and R. G. Reeves indicates that aeromagnetic anomalies are as much as 12,000 gammas over magnetic Ironwood Iron-Formation. Anomalies over a unit of magnetic clastic rocks reach 4,000 gammas in amplitude. Anomalies over the gneissic basement rocks are discontinuous, and the values are comparatively low. Diabase dikes that trend northeastward yield negative anomalies. Aeromagnetic survey of central Upper Peninsula An aeromagnetic survey has been made of approximately 2,000 square miles in parts of Baraga, Marquette, Dickinson, Alger, and Schoolcraft Counties in the Upper Peninsula of Michigan. Aeromagnetic maps by J. R. Balsley and F. A. Petrafeso (1-64) show four distinctive patterns in which anomalies are: (1) well defined, narrow, parrallel, and of east and west trend; or (2) poorly defined but of the same direction; or (3) well defined, wider, and passing from southerly to southeastemly courses; or (4) mainly broad, partly of easterly trend, partly without trend. Negaunee Moraine reinterpreted The Negaunee Moraine, although marked locally by kame-and-kettle topography, is characterized generally by its relatively low elevation and low relief as revealed from investigations by Kenneth Segerstrom (p. C126-C129). Thus, this feature is not a typical moraine, in that it is not ridgelike. The relief of the moraine and its resemblance to a kame terrace are characteristic of other features which have been mapped as late Wisconsin moraines in the Upper Peninsula. Reappraisal of the area between the Green Bay and Keweenaw sublobes may alter drastically the concept of well-ordered, convex-northward moraines in this interlobate zone, as depicted in glacial maps of the region. IOWA Aeromagnetic survey A preliminary geologic interpretation of the central and southwestern parts of a 15,000-square-mile aeromagnetic survey in Iowa was prepared by J. R. Henderson, Isidore Zietz, and W. S. White (1-63). A provisional geologic map shows the distribution of Pre-cambrian rocks beneath a Paleozoic and Mesozoic cover, and the principal conclusions are in general agreement with results from other geophysical studies to the northeast and southwest. The major feature is a section of lavas of Keweenawan age, several miles thick, in a downward folded or faulted structure. Flanking the lava are basins filled mostly with sandstones of late Keweenawan age. Shallow to moderately deep basins are believed also to occur on the upper surface of the lava trough. Magnetic evidence suggests a northeast extension of the Thurman-Redfield structural zone. New exploratory drilling for oil and gas may be justified along this zone and its possible equivalent on the western margin of the lava. WISCONSIN Structural control of zinc and lead ore Zinc and lead ore in the Dodgeville and Mineral Point areas has been mined from joint-controlled and pitch-and-flat deposits in flat-lying beds of limestone and dolomite of Ordovician age, according to J. W. Ailing-ham (1-63). Structure contours on the geologic maps delineate large asymmetric anticlines and intervening broad shallow basins that contain a rhombic pattern of small cross folds. ILLINOIS Major structural trends may have originated in Pre-cambrian Aeromagnetic, gravimetric, and well-log data were examined by M. E. Beck, Jr., for interpretation of structure, lithology, and topographic configuration of the concealed basement complex underlying much of northeastern Illinois. A number of prominent structures, particularly the La Salle anticline and the Ashton arch, seem to be underlain by analogous basement features, which themselves may correspond to major crystalline lithologic units. On the basis of this correlation, alternative genetic relations between Precam-brian and Paleozoic deformation are postulated. Sedimentary rocks may be draped over crystalline ridges and troughs, the trends of which reflect Precambrian tectonism. In view of the large scale of some of the features involved, however, Paleozoic renewal of deformation along Precambrian structural trends seems a more likely explanation. MINNESOTA Aeromagnetic survey in northern part of State An aeromagnetic survey of 47,000 square miles of northern Minnesota shows the magnetic effects of known iron-formations and igneous rocks in northeastern Min- 746-002 0-64-7A88 REGIONAL GEOLOGY nesota and provides a basis for identifying similar rocks to the west in areas of unknown geology and thick glacial drift. According to G. D. Bath, strongly magnetic values are caused by iron-formations with dominant remanent magnetization along the direction of the bedding and by Keweenawan mafic rocks with dominant remanent magnetization along a geomagnetic field. In striking contrast, the pre-Keweenawan igneous rocks give a dominant induced magnetization that reaches a maximum average of only 0.0020 gauss total magnetization. Interpretations for western areas indicate discontinuous belts of iron-formation of the Soudan type extending westward and southwestward completely across Minnesota. Anomalies adjacent to the iron-formation belts resemble those found over large batholiths in the eastern part of the State, and they are interpreted as the effects of large masses of igneous rock of silicic composition. The presence of these features suggests that the Keewatin basement province of Canada extends into Minnesota and across the area of the aeromagnetic survey. INTERIOR HIGHLANDS AND EASTERN PLAINS ARKANSAS Deformation in west-central Arkansas B. R. Haley reports that a well in the Greenwood quadrangle of west-central Arkansas cuts through a zone of normal faulting at a depth of about 10,580 feet. The displacement of beds in the subsurface is 1,100 feet, but no displacement is observed at the surface. He concludes that some of the faulting occurred during early and middle Atoka time and that southward thickening of the Atoka Formation toward the Ouachita geosyncline is due to both downwarping and normal faulting. MISSOURI Aeromagnetic interpretation of St. Francois Mountains lead district Aeromagnetic anomalies of less than 200 gammas are associated with topographic relief of exposed Pre-cambrian granitic and volcanic rocks of the St. Francois Mountains in Missouri, according to J. W. Allingham. Anomalies resulting from hills of coarsely crystalline granite range up to 100 gammas in amplitude, whereas anomalies over comparable hills of fine-grained rocks, such as granophyre or devitrified volcanic rock, range up to 200 gammas. Anomalies related to normal faults or shear zones in igneous rocks have amplitudes less than 100 gammas, and are observed best in profile. Analyses of compound anomalies yield the subsurface configuration of isolated roof pendants. Analytical methods used by Allingham in this study of total-intensity aeromagnetic data intensify the low-amplitude anomalies associated with buried hills and ridges of resistant Precambrian granitic and volcanic rocks. The hills and ridges, by controlling Cambrian sedimentary structures, localized lead deposits in over-lying carbonate strata. The observed total-intensity aeromagnetic field was continued downward toward its source, vertical derivatives were calculated, and residual anomalies were separated by use of an electronic digital computer. Of these methods, continuation of the total-intensity aeromagnetic field downward to the level of the Precambrian surface yielded the best correlation with extensive mine workings in the lead district. TEXAS Uplift of Edwards Plateau dated as Quaternary An incomplete analysis by V. L. Freeman, based on gravel deposits and geomorphic evidence, indicates that much of the uplift of the southwest flank of the Edwards Plateau of south Texas has occurred since deposition of the oldest gravel deposit. This gravel is believed to have been deposited at about the beginning of Pleistocene time. Since the early Pleistocene the Rio Grande has downcut through the Cretaceous limestones of the area, producing the presently entrenched meandering river. That the downcutting has been nearly continuous to the present day is shown by a scarcity of terraces and the narrowness of the canyon. Within the Rio Grande canyon more widening probably has been accomplished by rainwater solution of the limestone walls than by lateral erosion of the river. New Paleozoic plant-fossil collection A large suite of plant fossils collected by S. H. Mamay from upper Paleozoic sediments of North Texas includes the first plant fossils yet found in the Arroyo Formation of Leonard age, and several collections from new localities in the uppermost Pennsylvanian Harpers-ville Formation. The Arroyo collection contains elements characteristic of the Angara flora of Siberia, and other evidence in the new collections supports a close affinity between the Permian floras of Siberia and eastern Asia and those of the southwestern United States. The apparent abundance of well-preserved plants in the uppermost Pennsylvanian Harpersville Formation points up a strong possibility that the Pennsylvanian-NORTHERN ROCKY MOUNTAINS AND PLAINS A89 Permian boundary will eventually be pinpointed on paleobotonical evidence in an area where marine sediments are almost absent. NEW MEXICO Madera Limestone mapped Over most of the Tajique quadrangle of central New Mexico the upper part of the Madera Limestone is composed of a rhythmic sequence of limestone, shale, and channel-fill deposits of arkose and sandstone, according to D. A. Myers. The limestone beds, which are in units as much as 100 feet thick, are fairly persistent from south to north, but wedge out into shale to the west. Locally, in the southeastern part of the quadrangle, the limestone beds have merged to form bio-stromelike deposits 200 feet or more in thickness. One rhythmic sequence of rocks, mapped as unit B by D. A. Myers, has been traced from south to north across the quadrangle. Fusulinid evidence indicates that the top of this unit is at about the Missouri-Virgil time line. NORTHERN ROCKY MOUNTAINS AND PLAINS NORTHEASTERN WASHINGTON Deposits of breccia in the Klondike Mountain Formation (Oligocene) have been traced from the Bodie Mountain quadrangle, just south of the international boundary, into British Columbia by H. W. Little of the Geological Survey of Canada, and by R. C. Pearson. These are the first middle Tertiary rocks reported in this part of British Columbia. The locally derived breccias had previously been considered part of nearby Mesozoic and Paleozoic bedrock. To the southeast, limestone of late Middle or early Late Devonian age, found by A. B. Campbell in the Inchelium quadrangle, provides the first definite evidence of Devonian sedimentation in the area. The age of the limestone is based on the identification of conodonts by J. W. Huddle. These rocks may correlate with the probable Devonian limestone reported by Park and Cannon43 near the Washington-British Columbia boundary. The use of soil profiles in the correlation of glacial deposits has led to recognition by P. L. Weis and G. M. Richmond of five separate glacial advances in and near the Greenacres quadrangle close to Spokane. Only the ice of one advance, the next to the oldest, is known to 43 C. F. Park, Jr., and R. S. Cannon, Jr., 1943, Geology and ore deposits of the Metallne quadrangle, Washington: U.S. Geol. Survey Prof. Paper 202, p. 22. have entered the Greenacres quadrangle; this ice advance blocked the Spokane River in two places above its mouth, forming glacial lakes, but did not reach the main surface of the Columbia Plateau. The edges of the other advances lay well north of Spokane Valley. IDAHO Purcell trench may be major fault zone Rocks and structures on opposite sides of the northtrending Purcell trench differ markedly from each other, according to A. B. Griggs, suggesting that the trench is a major fault zone. This linear trench, 1 to 10 miles wide, is occupied by Coeur d’Alene Lake at the south and glacial outwash deposits to the north. The west wall of the trench is composed of high-grade metamorphic rocks, including sillimanite gneiss, of unknown age, cut by granitic intrusions. The east wall is made up of Precambrian Belt Series rocks that have been only slightly metamorphosed except where horn-felsed by granitic plutons. Opposite sides of the trench also are characterized by different structural trends, and the gross composition of the rocks before metamorphism differed, too. Zones of progressive metamorphism related to temperature Distinct episodes of synkinematic and postkinematic metamorphism are evident in textures and pseudo-morphs of minerals in schist southwest of the St. Joe River, Idaho. Metamorphism increases markedly from the St. Joe River southward toward the Idaho batholith, where the following metamorphic zones have been mapped by Anna Hietanen: biotite, garnet, staurolite, kyanite-staurolite, kyanite, kyanite-silli-manite, and sillimanite. Pseudomorphs after large staurolite crystals in the northeastern part of the kyanite-staurolite zone consist of kyanite, muscovite, garnet, and small staurolite crystals, indicating that the second episode of metamorphism was at higher temperature. Each isograd moved 2 to 3 miles outward during the second metamorphism, which also indicates higher temperatures. The first metamorphic episode was contemporaneous with deformation and likely accompanied formation of magma at depth; greater temperatures accompanying the second episode probably record postkinematic intrusions at higher levels in the crust. Dike swarm of possible middle Tertiary age reported A dike swarm at least 3 miles wide trends east-northeast across the southeast corner of the YellowA90 REGIONAL GEOLOGY Pine quadrangle in west-central Idaho, and may be part of the northeast-trending Lowman-Middle Fork zone. According to B. F. Leonard, the swarm contains more than 180 mappable dikes, mostly of monzonite, rhyolite, and granite porphyry. Some dikes cut roof pendants, granodiorite and alaskite of the Idaho batho-lith, and Challis Volcanics (Eocene( ?), Oligocene, and Miocene (?)). Granite porphyry dikes of this swarm resemble those in the adjacent Big Creek quadrangle, where one has a K-Ar age of 30 to 42 million years. Volcanic rocks in the Yellow Pine quadrangle Rocks in the eastern part of the Yellow Pine quadrangle previously identified as Casto Volcanics (Permian (?)) are assigned by B. F. Leonard to the Challis Volcanics (Eocene(?), Oligocene, and Miocene(?)). The tuffaceous lowest members of the volcanics contain sparse pebbles and cobbles of Idaho batholith (Cretaceous) rocks, confirming their postbatholithic age. The rocks are in part nonconformable on the batholith and in part faulted down against it. Porphyroblastic gneiss near Idaho batholith Porphyroblastic gneiss in the Blackbird Mountain quadrangle, west of Salmon, Idaho, has long been regarded as a border zone of the Idaho batholith. The gneiss, which is both underlain and overlain by quartzite of the Belt Series, is now thought by J. S. Vhay to be a product of dynamo-metamorphism. Elsewhere, intrusions of batholithic quartz monzonite into quartzite and argillite of the Belt Series have produced hom-fels rather than gneiss. Kinnikinic Quartzite near Clayton subdivided Kinnikinic Quartzite near Clayton, Idaho, has been separated by K. B. Ketner into two units on the basis of stratigraphic, lithic, and metamorphic features. Ketner believes that the upper unit resembles Middle Ordovician strata in Utah; the lower, Cambrian and Pre-cambrian quartzite in Utah. In the southern Lemhi Range, he believes that the Kinnikinic and part of the underlying Swauger Quartzite resemble Middle Ordovician strata of Utah. Milligen Formation found to be thick and variable The Milligen Formation of Early Mississippian age is thicker in the northern Lost River Range than previously estimated, and changes markedly in thickness within the Doublespring quadrangle, according to W. J. Mapel. The formation thins northeastward from 3,200 feet at McGowan Creek to 2,000 feet at Mill Creek, or 185 feet per mile in 6y2 miles; it also thins southeast- ward to between 2,000 and 2,400 feet near Sheep Creek, or 100 to 140 feet per mile in 7 miles. Pleistocene faulting in basin-ranges of east-central Idaho and adjacent Montana The Lost River Range, Lemhi Range, and Beaverhead Mountains, basin-ranges in east-central Idaho and adjacent Montana, were broken in Pleistocene time by north-trending, dominantly right-lateral strike-slip faults, reports E. T. Ruppel (p. C14-C18). The faults, which control the striking zigzag pattern of these ranges, are in a zone about 50 miles wide that extends northward about 150 miles from Arco, Idaho, into the Big Hole Basin, Mont. Occurrence of Olenellus in southeastern Idaho The first known specimens of the Lower Cambrian index fossil Olenellus from southeastern Idaho have been found 170 feet below the top of the thick Brigham Quartzite in the Portneuf Range near Bancroft, reports S. S. Oriel. Previous assignment of the bulk of the Brigham to the Middle Cambrian is therefore erroneous. High boulder gravel near Pocatello Boulder gravel that mantles several square miles south of the Portneuf River, near Pocatello, and is more than 1,000 feet above present stream level, is interpreted by D. E. Trimble as a combined alluvial fan of Mink and Gibson Jack Creeks, graded to a temporary base level that may have been controlled by extinct Raft Lake of probable late Pleistocene age. Snake River fault in southeastern Idaho The Snake River fault, between the Swan Valley-Grand Valley graben and the Caribou Range in southeastern Idaho, is not a simple fault but a fault zone, report D. A. Jobin and M. L. Schroeder. In the Irwin quadrangle it consists of three closely spaced step faults, all thrown down to the northeast. In the Caribou Range, two thrust faults of early Tertiary age have been discovered by H. F. Albee and H. L. Cullins. Thickening in Gallatin Limestone and Bighorn Dolomite inversely related In the north-central part of the Snake River Range the Cambrian Gallatin Limestone thickens and the over-lying Ordovician Bighorn Dolomite thins northwestward, according to D. A. Jobin, M. H. Staatz, and H. F. Albee. The Gallatin thickens from 150 feet to 435 feet within 8 miles; the Bighorn thins from 400 feet to 300 feet within the same distance, and to 80 feet at the northwestern end of the range.NORTHERN ROCKY MOUNTAINS AND PLAINS A91 WYOMING Very pure dolomite reported from Snake River Range In the Wells Formation (Pennsylvanian and Permian) of the Snake River Range in western Wyoming, H. L. Cullins and H. F. Albee have found a 10-foot-thick bed of pure dolomite of unknown but probable great extent. The dolomite is so pure that random samples may be used as dolomite standards in X-ray analysis. Gravity low on north side of Wind River Basin Bouguer anomalies range from a low of —230 milli-gals in the Wind River Basin to —190 milligals northward in the Owl Creek Range and to —160 milligals southward in parts of the Wind River Range and Granite Mountains. The major gravity low is asymmetrically located along the north side of the Wind River Basin, reflecting the position of the thickest sequence of sedimentary rocks just south of the Owl Creek Range, report J. E. Case and W. R. Keefer. Reverse faulting along the southern margin of the Granite Mountains, near Jeffrey City, is well expressed by a steepened gravity gradient of 6 milligals per mile above Precam-brian rocks thrust over Mesozoic sedimentary rocks, as indicated by deep drill holes. Silurian outlier found northwest of Sheridan An outlier or tongue of Silurian rocks about 30 feet thick has been recognized by C. A. Sandberg in the Ash Creek oil field, northwest of Sheridan in northern Wyoming, and 45 miles south of the previously determined southern erosional limit of Silurian rocks. These newly recognized Silurian rocks may extend west to include outcrops between Tongue and Little Bighorn Canyons in the Bighorn Mountains. Structure of Gros Ventre Mountains W. R. Keefer (chapter D) concludes from studies in the southwestern part of the range that the Gros Ventre Mountains are an asymmetric anticlinal uplift, steep and faulted along the southwest margin. The range lies between structures typical of Laramide deformation (Late Cretaceous and early Tertiary) in central Wyoming and those of late Tertiary deformation in northwestern Wyoming. Keefer suggests that the Gros Ventre Mountains and adjacent Hoback Basin were formed during the Laramide and were modified by later movements. Amsden Formation in Wyoming subdivided The Amsden Formation in Wyoming has been subdivided into three units in a regional study by W. W. Mallory. The basal unit, the Darwin Sandstone Member, is clean and well sorted, making it an ideal reservoir for oil and gas; the middle unit is red shale of uniform thickness and composition; the upper unit is widespread cherty limestone. Mallory believes that the sand in the Darwin Sandstone Member and in the Tensleep Sandstone that overlies the Amsden was derived from an older sandstone, possibly of Ordovician age, in southern Canada. Carbonate rocks in Park City Formation Carbonate rocks in the Park City Formation of central Wyoming are believed by E. K. Maughan to have accumulated as skeletal detritus in offshore bars along the continental shelf and as lime mud in shoreward lagoons, comparable to similar deposits of the Bahama Islands. Suitable environment and abundant organisms account for the accumulation of oil in these rocks. Lithologic study of Mowry Shale Ten bentonite beds within the Mowry Shale have been used for basin-wide correlations as a result of detailed study by G. P. Eaton of six trenched sections along the west side of the Wind River Basin. An oft-suggested volcanic source to the west is affirmed by systematic variations in thickness and grainsize of the nonclay fraction. The lithology of the Mowry Shale and current-direction measurements in the underlying Muddy Sandstone Member of the Thermapolis Shale and the overlying Frontier Sandstone indicate that the sea floor sloped eastward in Mowry time and that the shoreline lay between long 109° and 110° W. Continental Peak Formation dated The Continental Peak Formation has been dated by means of fossil vertebrates found by H. D. Zeller and E. V. Stephens in the Oregon Buttes area. Orohippus uintanus (Marsh), found 65 feet below the top of Continental Peak, has been identified by G. E. Lewis, indicating that these rocks are a local facies of the upper part of the middle Eocene Bridger Formation. Glacial chronology in Wind River Range revised New work in the Wind River Mountains by G. M. Richmond (chapter D) and J. F. Murphy indicates that the youngest of three tills previously described as pre-Bull Lake in age instead represents an early stage of Bull Lake Glaciation. Another, as yet unnamed, till lies beneath the oldest of the pre-Bull Lake tills previously described. Terrace gravels correlative with each of these tills have been recognized along the Wind River. Recognition of a fourth important glacial advance during Pinedale Glaciation in the Pinedale areaA92 REGIONAL GEOLOGY has resulted from G. M. Richmond’s discovery of very blocky moraine in canyons along the margin of the Wind River Range at about the lower limit of the Pine-dale ice cap. Pleistocene limits of Yellowstone Lake interpreted The Pleistocene extent of Yellowstone Lake is recorded in lacustrine sediments north of the lake recently examined by J. D. Love, in company with J. M. Good of the National Park Service. The sediments merge with similar strata in the now-abandoned Pelican Arm of Yellowstone Lake. Similar beds in Jackson Hole may represent a southern extension of the lake. MONTANA Major folded thrust northeast of Helena A major folded thrust, named the Moors Mountain thrust, has been traced for 25 miles in and east of the Holter Lake quadrangle, northeast of Helena, Montana. The fault, which was discovered by W. B. Myers, nearly parallels bedding of overlying rocks and forms a northwest-plunging fold pair that shifts the fault trace 7 miles across regional strike, explaining the reversed-S pattern of Paleozoic units on the State geologic map. Southwest dips of the fault range from 20°to 55°; northeast dips in the reversed limb, from 30° to 45°. Grey son Shale (upper Precambrian) overlies rocks as young as Kootenai (Lower Cretaceous). The fault rises stratigraphically to the northwest. At the south edge of the quadrangle it places the basal part of the Greyson on the upper part of the Greyson strata and becomes hard to trace. Overturned anticline north of Helena mapped A large, eastwardly overturned, imbricately faulted anticline with a structural relief of about 10,000 feet has been mapped by R. G. Schmidt in the Wolf Creek area north of Helena. This fold is the north end of the Big Belt anticlinorium, in which superficial crustal shortening has been at least 6 miles. Highland thrust south of Butte part of long zone A long-known east-trending north-dipping thrust fault, in the Highland Mountains south of Butte, has been mapped in detail by H. W. Smedes and M. R. Klepper and named the Highland thrust. The thrust has moved Precambrian Belt Series rocks eastward over pre-Belt metamorphic rocks and apparently over the older Melrose thrust zone. They regard the Highland thrust as part of a 60-mile-long zone of similar thrusts that extends from the Pioneer Mountains to the Tobacco Root Mountains. The faults all trend east, dip north, and have moved Belt rocks eastward over younger rocks that had been folded along north to northwest-trending axes. These thrusts are interpreted by Smedes and Klepper as segments of a once-continuous thrust zone along which relative eastward displacement was at least 60 miles. Magnetic anomalies found near Boulder batholith Aeromagnetic studies near the Boulder batholith, by W. E. Davis, show large positive magnetic anomalies in places along the margins of the batholith, over Bull Mountain and the foothills of the southern part of the Elkhorn Mountains, and over the northern part of the Elkhorn Mountains. Intensity of folding decreases eastward from Madison Range The Tepee Creek quadrangle lies between overthrust Precambrian crystalline rocks of the Madison Range on the west and gentle open folds in younger sedimentary rocks in the Upper Gallatin Valley on the east. Intensity of folding within the quadrangle has been found by I. J. Witkind (1-64) to decrease eastward and northeastward; overturned folds and thrust faults in the west give way to broad open flexures that may form suitable oil traps in the north and east. These flexures are concealed in the northeastern part of the area by volcanic rocks erupted from vents to the east. Folding thought to reflect laccoliths at depth The Hughesville quadrangle lies along the north flank of the Little Belt Mountains laccolithic complex, which I. J. Witkind believes is reflected in domes and elongate anticlines in the exposed sedimentary rocks. A parent stock centered beneath Hughesville seems to have been the source of satellitic radial laccoliths. Isotopic ages of glauconite beds in Belt Series R. A. Gulbrandsen has recognized two principal glauconite horizons in Belt Series rocks (Precambrian) that have been correlated for a distance of 100 miles from Glacier Park south to Sun River, Mont. Additional K-Ar age determinations on the glauconite have verified the original determination of about 1,100 million years.44 More than twenty glauconite-bearing beds have been found by M. R. Mudge in Belt Series rocks in the Sun River Canyon area. Two samples collected from the Hoadley Formation, about 3,100 feet below the Flat- “ R. A. Gulbrandsen, S. S. Goldich, and H. H. Thomas, 1963, Glauconite from the Precambrian Belt Series, Montana: Science, v. 140, no. 3565, 390-391.NORTHERN ROCKY MOUNTAINS AND PLAINS A93 head Sandstone (Middle Cambrian), and analyzed by S. G. Walthal and C. E. Hedge, yielded Sr-Rb ages of 1020±50 m.y. and 1070±55 m.y. The glauconitebearing beds have been traced for more than 25 miles and may prove useful in regional correlation. Volcanic rocks of Livingston Group subdivided and dated Deformed epiclastic volcanic rocks of the Livingston Group in the Maudlow quadrangle have been subdivided into eight map units by B. A. Skipp and interpreted as an allochthonous mass moved a few miles on low-angle faults. Textures and thicknesses suggest a nearby source for the volcanic rocks, though no contemporaneous intrusive masses are recognized in the map area. The volcanic rocks are assigned to the Upper Cretaceous on the basis of Lance pollen identified by R. H. Tschudv from 900 feet below the top of the 5,000-foot-thick sequence. Stratigraphy of Livingston Group in Madison Range The Livingston Group of the Madison Range has been divided into three members in the Cameron quadrangle by J. B. Hadley and E. J. Young. The lowest member, 300 to 500 feet thick, consists of interbedded chert-bearing and pyroxene-bearing sandstone, chert-pebble conglomerate, and plant-bearing volcanic silt-stone. The middle member, about 900 feet thick, consists of coarse volcanic flow breccia, mostly polymict but partly homogeneous. The top member, at least 1,200 feet thick, consists of massive to crudely stratified volcanic cobble and boulder conglomerate. Many blocks of red felsite, several hundred feet long, in the middle unit may be intrusive. The area clearly lay near an eruptive center in Late Cretaceous time, but the center has not been found. Significance of fossil fish in Maywood Formation C. A. Sandberg and W. J. McMannis (p. C50-C54) report that a channel-fill deposit of the generally marine Maywood Formation in the Gallatin Range contains fish remains identified by D. H. Dunkle as Bothriolepis sp., permitting positive assignment of an early Late Devonian age and suggesting deposition in brackish or fresh water. Valleys previously inundated by an Early Devonian sea may have controlled and localized transgressions of the Late Devonian sea. Volcanic vents discovered southeast of Bearpaw Mountains Twelve volcanic vents have been found by B. C. Hearn, Jr., and C. P. Sabine in a faulted area near the Missouri River, southeast of the Bearpaw Mountains. The vents are 500 to 1,300 feet across and contain bedded pyroclastic rocks, intrusive breccias, olivine-rich igneous rocks, and slices of Fox Hills Sandstone and Hell Creek Formation (Upper Cretaceous), Fort Union Formation (Paleocene), and Wasatch Formation (lower Eocene) that have been dropped 1,000 to 4,500 feet. Vent activity may have begun in middle Eocene time, accompanying igneous activity in the Bearpaw Mountains. At least one vent was active late enough to incorporate rounded pebbles derived from igneous rocks of the Highwood Mountains or from a young (early late Eocene) series in the Bearpaw Mountains. History of glacial Lake Missoula interpreted Near Polsen, Mont., G. M. Richmond has found that sediments of glacial Lake Missoula are interbedded with each of three Bull Lake tills and with the oldest till of Pinedale age. Disconformities intervene between tills and lake sediments, indicating at least four separate stages of development of Lake Missoula. During the early stage of Pinedale Glaciation, rapid erosion of the lake’s ice dam at Clark Fork produced the Spokane flood and the last major erosion of the channeled scablands. Widespread unconformity separates Mississippian and Pennsylvanian strata Preliminary interpretations of data gathered during work on the Mississippian and Pennsylvanian folios are providing a better understanding of ancient tectonic events in parts of the Rocky Mountain region. According to E. K. Maughan, an unconformity recognized in outcrops of the Heath Shale in central Montana can be traced widely in Montana and the Dakotas. In Maughan’s opinion, rocks below the unconformity are Mississippian in age; rocks above it in the Heath begin a new cycle of deposition and are mostly Pennsylvanian in age rather than Mississippian as believed heretofore. In addition, Maughan’s study suggests that Pennsylvanian rocks were widespread in Montana prior to northward beveling by pre-Permian erosion and subsequent complete removal in central to northern Montana prior to Jurassic deposition. NORTH DAKOTA AND SOUTH DAKOTA Synthesis of Quaternary geology of northern Great Plains Several hundred man years of work on the Quaternary geology of the northern Great Plains have been synthesized in a cooperative project with the North Dakota and South Dakota Geological Surveys. The eastern parts of North Dakota and South Dakota wereA94 REGIONAL GEOLOGY invaded by Nebraskan, Kansan, Illinoian and Wisconsin glaciers, report R. W. Lemke and R. M. Lindvall, of the U.S. Geological Survey, W. M. Laird, State Geologist of North Dakota, and M. J. Tipton, Assistant State Geologist of South Dakota. It now seems clear that the eastern parts of North and South Dakota were covered by ice during the Nebraskan, Kansan, Illinoian, and Wisconsin Glaciations. Western North Dakota and eastern Montana probably were glaciated by continental ice only during Wisconsin time. Six significant Wisconsin advances are recognized in the northern Great Plains; successive advances were, in general, more lobate in outline near their termini, their courses determined largely by high areas of bedrock. Pre-Fall River folding in southern Black Hills Surface and subsurface study of the Inyan Kara Group of Early Cretaceous age along the southern margin of the Black Hills by G. B. Gott (chapter D) indicates discordant relations between the Fall River Formation and the underlying Dakota Formation. This indicates that structural readjustments were in progress during the deposition of the Lakota. One domal structure, near Edgemont, S. Dak., showed 40 feet of closure on the top of the Morrison Formation, which underlies the Lakota, but no closure on the base of the overlying Fall River. SOUTHERN ROCKY MOUNTAINS AND PLAINS GEOLOGY OF PRECAMBRIAN ROCKS OF COLORADO Plastic folding and catadasis along Idaho Springs-Ralston shear zone Detailed work on Precambrian rocks in the Southern Rocky Mountains continued to be focused on the Front Range, Colo., which has been the target of intensive study for several years. Studies by R. B. Taylor in the Blackhawk quadrangle near Central City have further clarified details of the complex structural history of the Preecambrian rocks in this area. Cataclasis resulting from the last of the 3 main periods of deformation has long been recognized, but Taylor has found that the east-northeast-trending Idaho Springs-Ralston shear zone, the largest structure formed during this period, began as a plastic monoclinal fold and progressed into a clearly defined zone of cataclasis by shearing along the steep limb. The closely compressed and sheared synclinal bend on the northwest side of the monocline is preserved as the prominent Coal Creek syncline. Precambrian control of Laramide structures Recent work by C. T. Wrucke in the Boulder quadrangle near the northeast end of the Front Range mineral belt has demonstrated close parallelism between faults, dikes, and veins of early Tertiary (Laramide) age and shear zones and mafic and granitic dikes of Precambrian age. This parallelism of structures of different ages in the mineral belt has been noted many times in the past, but the coincidence is particularly pronounced in the Boulder quadrangle. Cordierite in Idaho Springs Formation D. J. Gable, D. M. Sheridan, and C. T. Wrucke have found cordierite-bearing rocks in several different lithologic assemblages in the Precambrian Idaho Springs Formation in the central Front Range of Colorado. The cordierite-bearing rocks occur in part as discrete layers in metasedimentary sequences that crystallized during progressive regional metamorphism to a facies characterized by sillimanite, almandine, and microcline. The various layers commonly retained their compositional identities through metamorphism, and probably reflect original stratigraphic units. Other cordierite-bearing rocks are associated with igneous bodies, and were formed by more local contact metamorphism. First occurrence of lepidolite in Front Range Nearby in the southwestern part of the Squaw Pass quadrangle, D. M. Sheridan has found lepidolite in a zoned Precambrian pegmatite in association with cleavelandite, quartz, tourmaline, and muscovite. Although the small amount of lepidolite exposed does not necessarily indicate an economic deposit, the find is interesting mineralogically as lepidolite is not known to have been recognized previously in the Front Range. Rocks of low metamorphic grade in Front Range Whereas most of the metasedimentary rocks in the central Front Range are of high metamorphic grades and commonly contain sillimanite, a suite of rocks in the Cache la Poudre River area of the northeastern Front Range is of lower metamorphic grade. W. A. Brad-dock has determined that these rocks range from mus-covite-chlorite-biotite phyllites through muscovite-chlorite-biotite-garnet-staurolite schists to muscovite-biotite-sillimanite schists and gneisses. These metasedimentary rocks have been intruded by plutons of Boulder Creek Granodiorite, of tonalite that resembles the Mount Olympus Granite, of Sherman Granite, and of biotite-muscovite granite.SOUTHERN ROCKY MOUNTAINS AND PLAINS A95 Boulder Creek zircon yields highest isotopic ages reported in Front Range T. W. Stem has completed isotopic lead-uranium measurements on zircon from 5 samples of rock collected by George Phair and David Gottfried from the Boulder Creek batholith area in the central Front Range; four of these samples are from typical Boulder Creek Granite, and one is from a younger granite dike that is regarded as a variant of the Silver Plume Granite. The measured Pb207/Pb206 ages from the Boulder Creek batholith are all close to 1,730 million years. The Pb208/U238, Pb207/U235, and Pb207/Pb206 ages are strongly discordant, as was anticipated from the range of Pb/ alpha ages previously obtained on 25 different zircon samples from the same batholith. The Pb/alpha ages parallel the Pb200/U238 ages, and both range down to a minimum of 1,050 million years. Zircon from the dike of probable Silver Plume Granite yielded Pb207/ Pb206 ages of 1,410 million years, roughly similar to the age of the Silver Plume Granite at its type locality, whereas Pb206/U238 and Pb/alpha ages of the same rock are close to 1,050 million years. The age of 1,730 million years obtained by Pb207/Pb206 ratio for Boulder Creek Granite is the highest so far reported for any rocks in the Front Range. Most other determinations have been made by isotopic methods on minerals more susceptible to modification by younger thermal episodes. The Pb207/Pb20G age obtained on the dike of probable Silver Plume Granite indicates that rock of this type is Silver Plume in age and not a younger rock as was suggested by earlier Pb/alpha determinations. Large folds noted in Black Canyon region In western Colorado, W. R. Hansen has found that the Precambrian metamorphic rocks exposed in the Black Canyon of the Gunnison River have been folded into a series of north- to northeast-trending anticlines and synclines. Individual folds are 2 to 8 miles across, and have a structural relief of many thousands of feet. During the folding, the original rocks were transformed to gneisses, many of which exhibit the high metamorphic grade characterized by sillimanite. STRATIGRAPHIC AND PALEONTOLOGIC STUDIES Thinning of Triassic red beds along Park Range Geologic mapping by W. J. Hail indicates that Triassic red beds along the east flank of the Park Range, Colo., thin southward from the Wyoming State line to the Lake Agnes quadrangle near Muddy Pass, and then gradually thicken farther southward toward Gore Pass. In the Barber Basin-Frantz Creek area in the Lake Agnes quadrangle, the red beds are only about 100 feet thick and are equivalent to only a part of Moenkopi Formation of Early and Middle (?) Triassic age. The thinning results both from (1) a wedging of the lower beds against the Precambrian rocks of an element of the ancestral Rockies positive area, and (2) erosion of strata equivalent to the Upper Triassic Chinle Formation prior to Jurassic sedimentation. In addition to the pattern of thinning in a north-south direction, thinning occurs eastward in the subsurface at an even higher rate. The Triassic rocks and also some of the overlying Jurassic rocks pinch out beneath the floor of North Park about 5 miles east of the foot of the Park Range. This overlap against Precambrian rocks of the old highland offers some potential for oil entrapment in sandstones of the Sundance or Entrada and Morrison Formations of Jurassic age. Environment of deposition of Entrada Sandstone After studying the stratigraphic relations of Jurassic and Upper Triassic sedimentary rocks in south-central Wyoming and northwest Colorado in detail, G. N. Pipi-ringos has interpreted a shallow-water marine environment of deposition for the Entrada Sandstone of Colorado and its counterpart, the Canyon Springs Sandstone Member of the Sundance Formation of Wyoming. At more than 100 localities, Pipiringos has found this sequence to consist dominantly of homogeneous, massive, crossbedded sandstone, but at 7 of the localities, the otherwise uniform lithology is interrupted by flat, thin beds of ripple-marked sandstone containing marine pelecypods, discrete lenses of gray oolite, and thin beds of red sandy siltstone. The fossils, oolites, and crossbedding suggest deposition in agitated shallow marine water. This interpretation is strengthened by lateral facies changes within the sequence. From the McCoy area on the west side of the Gore Range in Colorado, northeastward to near Kremmling, typical crossbedded Entrada Sandstone thins from 165 to 50 feet, and intertongues with and grades into gray-green shale and fine-grained sandstone containing marine pelecypods and microfossils. Northward from Kremmling, this Entrada equivalent grades into red sandy siltstone only 30 feet thick, then thickens and grades first into a sequence of marine shale, sandstone, and red siltstone beds, and then into the familiar massive crossbedded sandstone at Frantz Creek, 18 miles northwest of Kremmling, where it is again about 165 feet thick and comprises the Canyon Springs Member of the Sundance Formation.A96 REGIONAL GEOLOGY Unconformity may help to subdivide Tertiary rocks An angular unconformity has been mapped by D. M. Kinney within the sequence of lower Tertiary continental sedimentary rocks called Coalmont Formation in North Park and called Middle Park Formation in Middle Park, Colo. Porphyritic andesite pebbles in a greenish volcanic sandstone are characteristic of the unit below the unconformity. They are coarse and abundant in Middle Park, but decrease in size and abundance northward and are absent in northern North Park. In the unit above the unconformity, porphyry pebbles are rare in Middle Park and absent in North Park. In places, the two units are markedly discordant structurally, but in others they seem to be only subtly disconformable. If the unconformity can be traced over a sufficiently wide area, it will provide a convenient horizon for subdividing the stratigraphy of the lower Tertiary rocks, and should help greatly to clarify the geologic history of the North Park-Middle Park basin and adjacent areas. Goose Egg Formation traced eastward into Wyoming E. K. Maughan (p. B53-B60) has extended the Goose Egg Formation eastward into the Permian and Triassic red-bed sequence of southeastern Wyoming, and has restricted and redefined many of the names previously used in the area, giving them member status. The sediments that formed the Goose Egg Formation probably were deposited in a vast shallow lagoon or tidal flat that extended eastward from the deeper Phosphoria sea in central and western Wyoming. Sharon Springs Member of Pierre Shale becomes younger southward along Front Range Studies of the Pierre Shale along the east side of the Front Range, Colo., by W. A. Cobban and G. R. Scott have revealed that the Sharon Springs Member is a recognizable unit in the lower part of the Pierre near the Wyoming State line and near Pueblo, but not in the area between Loveland and Castle Rock, where shale in this part of the formation lacks the black, organic-rich aspect characteristic of the Sharon Springs. Bacidites asperijorrrds is found in a sequence of beds about 40 feet thick in the upper part of the Sharon Springs Member at Pueblo. Near the Wyoming State line, however, this fossil is found through about 800 feet of sandy shale that lies above the Sharon Springs and represents an unnamed sandy unit in the Pierre Shale of southeastern Wyoming. These relations indicate that, the Sharon Springs Member is not time equiva- lent in all occurrences, but is progressively younger southward. Stratigraphy of Raton Formation in New Mexico The Raton Formation of Cretaceous and Paleocene age is about 2,100 feet thick on the east flank of the Vermejo Park dome, Colfax County, N.M., as measured by C. L. Pillmore. The lower 1,000 feet of the formation is virtually barren of coal, and comprises 200 feet of coarse-grained to conglomeratic sandstone overlain by 800 feet of sandstone and minor ihterbedded clay-stone and siltstone. The upper 1,100 feet contains many layers of coal and consists mostly of claystone and silt-stone containing interbeds of sandstone as much as 50 feet thick. Most of the coal beds are less than 5 feet thick, but the York Canyon coal bed, about 1,400 feet above the base of the formation, is as much as 11 feet thick. It is currently being developed. Mapping of the coal beds will appreciably increase the known coal reserves of the Raton field. GEOLOGY OF VOLCANIC AND HYPABYSSAL INTRUSIVE ROCKS Volcanic rocks in San Juan Mountains Important stratigraphic and time correlations of volcanic rocks in the northern, western, and central San Juan Mountains, Colo., have resulted from work on five separate mapping projects there. Relations between cauldron complexes in the central and western San Juan Mountains have been established jointly by T. A. Steven and R. G. Luedke. The youngest rocks from the western source are ash-flow units in the Potosi Volcanic Group; these unconformably underlie the Mammoth Mountain Rhyolite from the central source. Dacitic lavas and breccias of the Huerto Formation, from another source area to the south, intertongue with both the western and central San Juan assemblages, and indicate that no significant break in volcanic activity intervened. Steven and Luedke traced two of the ash-flow units in the Potosi Volcanic Group 50 miles northward to the Gunnison River, where they are interbedded with other ash-flow formations. The Tertiary volcanic stratigraphy in the central San Juan Mountains, Colo., has been described by T. A. Steven and J. C. Ratte (2-64). Ash-flow deposits in San Juan Mountains J. C. Olson and D. C. Hedlund have mapped the ash-flow deposits on the north flank of the San Juan Mountains in an area of five 7y2 minute quadrangles sur-SOUTHERN ROCKY MOUNTAINS AND PLAINS A97 rounding the Powderhom district. These deposits are divisible into four formations, each of which may be divided into smaller units on the basis of degree of welding, devitrification, and other characteristics. The lowest ash-flow formation is found only in the vicinity of Lake Fork Canyon on the west side of the area and near the Gunnison River on the north, but remnants of the other three units are found over most of the area. The second formation from the top is a distinctive crystal-rich ash-flow tuff that forms a very useful marker unit over a large area, and is one of the two units traced northward from the central San Juan Mountains by Steven and Luedke. Isotopic determinations indicate age of marker bed W. R. Hansen has found the units that Olson and Hedlund described from the San Juan Mountains, Colo., as well as several other units, near the Black Canyon of the Gunnison, northwest of the Powderhom district. Preliminary potassium and argon analyses by H. H. Thomas, R. F. Marvin, and Paul Elmore of a biotite concentrate separated by Hansen from the distinctive crystal-rich ash-flow tuff mapped farther east by Olson and Hedlund, and farther south by Steven and Luedke, indicate a tentative late Oligocene or early Miocene age. This isotopic determination is being checked by additional samples, and if valid will establish a point in time that wll be widely applicable to rocks in the San Juan region. Ash-flows tuffs in Costilla Valley, N. Mex. In a preliminary investigation of silicic volcanic rocks in Costilla Valley, Taos County, N. Mex., Paul Orkild and C. L. Pillmore have distinguished two sequences of ash-flow tuffs. The older sequence, of probable Pliocene age, is exposed along the east side of the valley in a downfaulted remnant of a former widespread sheet of volcanic rocks. It consists of about 1,000 feet of vitric nonwelded to densely welded ash-flow tuffs, overlain unconformably by a rhyolitic lava flow about 200 feet thick. A younger bed of ash-flow tuff floors Costilla Valley to a depth of about 200 feet. It post-dates faulting and erosion of the older sequence, and probably was erupted in late Pliocene or early Pleistocene time. Age of tuffs from Middle Park and near Berthoud Pass Sanidine from rhyolite tuffs collected by R. B. Taylor and Glen Izett in the Fraser and Kremmling basins in Middle Park, and from intrusive rhyolite porphyry collected by P. K. Theobald at the Red Mountain volcanic center near Berthoud Pass, have been analysed for potassium and argon by H. H. Thomas, R. F. Mar- vin, and Paul Elmore. All samples yielded a late Oligocene age. Geologic mapping by Izett in the Hot Sulphur Springs area in Middle Park has shown that the late Oligocene tuffs are part of a volcanic sequence that rests unconformably on the Middle Park Formation of Cretaceous and Paleocene age, and underlies tuf-faceous intermontane basin-fill deposits. The basin-fill deposits contain a rich mammalian fauna that is classed as middle Miocene in age by G. E. Lewis. The volcanic sequence ranges from 0 to 2,000 feet in thickness and consists of a thin lower unit of alkalic olivine basalt flows and a much thicker upper unit of complexly interlayered rhyolitic to rhyodacitic tuff, tuff breccia, breccia, and welded tuff, and minor beds of conglomerate. The volcanic rocks are remnants of an extensive sheet that once covered uplands along the flanks of the Rabbit Ears Range north of Middle Park. Welded tuff northeast of Salida, Colo. Studies by M. G. Dings in the Cameron Mountain quadrangle, northeast of Salida, Colo., and the western edge of the Thirtynine Mile volcanic field, show that a widespread silicic welded tuff is older than the Antero Formation of DeVoto (1962) of Oligocene age. Previously, the tuff was thought to be contemporaneous with or younger than the Antero. The tuff extends into South Park to the north and northeast, and at one place or another it rests on an older Tertiary welded tuff, Paleozoic sedimentary rocks, and Precambrian rocks. Locally it is overlain by basalt flows younger than the Antero Formation. Intrusive dike of welded tuff in Sawatch Range Intrusive welded tuff forms a nearly vertical dike 30 to 50 feet wide and about D/i miles long near the crest of the Sawatch Range in the Mt. Harvard quadrangle, Colorado. According to M. R. Brock and Fred Barker, the rock consists of about equal parts glass shards, pumice fragments, and wallrock fragments; these materials were emplaced and welded at depths of at least 800 feet as indicated by the vertical range of exposure of the dike. The dike possibly may have been a feeder for an extrusive ash-flow tuff. Silicic intrusives of West Elk Mountains cut Wasatch Formation The West Elk Mountains in west-central Colorado are formed in part of silicic stocks, dikes, sills, and laccoliths that intrude the Wasatch Formation of Eocene age, as described by L. H. Godwin and D. L. Gaskill (P. C66-C68). The structure and composition of the igneous bodies are similar to those in comparableA98 REGIONAL GEOLOGY laccolithic intrusive centers on the Colorado Plateau to the west and southwest. Walsen lamprophyre dike R. B. Johnson (p. B69-B73) studied the Walsen dike near Walsenburg in south-central Colorado and found it to be composite, consisting of three dikes varying in composition from soda-minette to minette, each intruded at a different stage into a tension joint trending normal to the northerly strike of the sedimentary wallrocks. QUATERNARY GEOLOGY Map of bedrock geology and of Quaternary overburden in southeastern Nebraska A map showing the bedrock geology and thickness of Quaternary overburden in an area of 8,400 square miles in southeastern Nebraska has been prepared by G. E. Prichard, of the U.S. Geological Survey, and E. C. Reed, V. H. Dreeszen, and R. R. Burchett, of the Nebraska Geological Survey. The map, which includes the Lincoln 1°X2° quadrangle and the southwest part of the Nebraska City quadrangle, is the first in a series of maps being prepared in cooperation with the Conservation and Survey Division of the University of Nebraska to provide statewide coverage at a scale of 1: 250,-000. The maps are intended for general purpose use; a knowledge of bedrock geology is fundamental for many and diverse purposes; the distribution and thickness of Quaternary overburden are important to the construction industry and as a reservoir for ground water. Landslides in Golden area, Colorado Studies prompted by the rapid urbanization of the Golden quadrangle, Colorado, have disclosed many landslides in the areas underlain by the Denver and Arapahoe Formations. Most of the landslides, according to Richard Van Horn, now appear to be stable, although some of those disturbed by human activity such as excavations or irrigation have again become active. Others will likely become active in the future if similarly disturbed. Recent fault movement along Laramie Mountains Recent fault movement in the Brush Creek area along the east flank of the Laramie Mountains in southeastern Wyoming has been documented by L. W. McGrew. The fault cuts several beds of alluvium, one of which contains snail shells that have been dated by Meyer Rubin, using radioactive-carbon techniques, as 9,500±400 years. A younger alluvium unit resting unconformably across the eroded trace of the fault also contains snail shells, dated by Rubin as 1.520±300 years old. The late movement bracketed between these ages offset the alluvial deposits at least 20 feet. Pleistocene stream capture in South Platte drainage A complex history of Pleistocene drainage changes along the South Platte River is being unraveled by P. E. Soister in the Platteville, Fort Lupton, and Hudson quadrangles north of Denver. Numerous remnants of deeply weathered gravelly alluvium capping hills and underlying Beebe Draw 3 to 10 miles east of the present South Platte River in this area are believed to represent channels of the South Platte River in pre-Nebraskan (?), Nebraskan, Kansan, and most of Illi-noian time. A shift to the present course was accomplished in about latest Illinoian time by stream capture in the area between Denver and Brighton. Ash beds south of Black Canyon, Colo. In mapping the Pleistocene valley-fill deposits in Bostwick Park and Shinn Park valleys, south of the Black Canyon of the Gunnison, Colo., R. G. Dickinson has found three separate rhyolitic volcanic ash beds. The lower ash bed, as much as 4 inches thick, is at the base of the valley-fill section; the middle bed, as much as 3 feet thick, is about 35 feet above the first and over-lies a moderately developed soil zone; the upper bed, as much as 8 inches thick, is about 125 feet above the middle bed and about 4 feet above a second strong soil zone. Each of the lower two ash beds contain pheno-crysts of chevkinite, green ferroaugite, and white zircon, but refractive indices of the green ferroaugite and the surrounding glass shards in the two beds are different. The upper ash bed differs in mineralogy from the other two. The mineralogy of the middle ash bed is identical with that of the Pearlette Ash Member of the Sappa Formation of Kansan or Yarmouth age in Nebraska. The occurrence of tuff of this composition in the Bostwick Park area is the second to be reported near the Black Canyon of the Gunnison, and if the correlation with the Pearlette is valid, it is of great importance in the dating of Pleistocene events, as well as establishing further extension of this widespread ash unit. GEOPHYSICAL INVESTIGATIONS Aerial radioactivity survey of Denver area Aerial radiological measurements by Peter Popenoe have shown that the natural gamma radioactivity level within the Denver area ranges from 300 to 1,500 counts per second. The highest radioactivity was found overCOLORADO PLATEAU A99 alluvium derived from the crystalline rocks of the Front Range and occurring either as upland gravels or as recent alluvium along modern streams. The radioactivity of alluvium diminishes eastward along the South Platte River. High radioactivity was found also over arkosic sandstones and conglomerates of the upper part of the Dawson Arkose and in the Castle Rock Conglomerate both of which were derived from the crystalline rocks of the Front Range. Median levels of radioactivity were found over the Laramie, Arapahoe, and Denver Formations, the Pierre Shale, and over loess and some dune sand. Low levels of radioactivity are associated with the limestone and sandstone beds that crop out in the hogback ridges along the Front Range, and with dune sand and sandy alluvium along the South Platte River. Regional gravity low in Colorado mineral belt Geophysical investigations by J. E. Case in the headwater area of the Arkansas River have disclosed a large regional gravity low of 30 to 50 milligals that trends northeast across the Gore and Tenmile Ranges from Leadville to Breckenridge along the trend of the Colorado mineral belt. From Leadville, the same low extends southward diagnonally across the Arkansas Valley and along the Sawatch Range at least 10 miles and into the area underlain by the Twin Lakes pluton of Tertiary age. Scattered data farther south suggest that it may continue across the Mount Princeton batho-lith in the southern Sawatch Range. Gravity gradients along the flanks of the anomaly are steep, and probably reflect an intracrustal, relatively near-surface mass of lighter rock. The coincidence of the gravity low with an area containing many intrusive igneous bodies of early Tertiary age suggests that this buried mass of lighter rocks may be a batholitic body of regional proportions. Gravity low in the San Juan volcanic field A gravity survey made by D. E. Karig in and around the San Luis Valley, Colo., disclosed a gravity low over the Bonanza area in the northeastern part of the San Juan volcanic field. This anomaly is believed to reflect a caldera collapse structure related to volcanic eruptions during middle Tertiary time. Available geologic and gravity evidence suggests that the suspected caldera has an elliptical outline with axes of 8 and 10 miles, and is filled with about 8,000 feet of low-density material. Gravity low associated with the Valles caldera, New Mexico Gravity and aeromagnetic surveys by H. R. Joesting and L. E. Cordell in the Jemez and Nacimiento Mountains, New Mexico, show7 that a 35-milligal gravity low is associated with the Valles caldera. An extension of this low7 to the northeast probably reflects an earlier caldera now mostly obscured by the Valles caldera. The Valles anomaly closely resembles gravity anomalies over large volcanic calderas in Japan and the western United States, and by analogy with these, the Valles anomaly may be caused by a low-density mass more than 10,000 feet thick. The faulted western border of the Rio Grande trough can be traced beneath the Valles volcanic field, but it is difficult to separate effects of basement structure from those of near-surface volcanic rocks. Gravity and aeromagnetic data indicate segmentation of the Rio Grande trough and discontinuities of the fault boundaries of the trough, which are not evident from surface geologic mapping. A prominent northwest-trending regional magnetic anomaly which transects the Valles caldera indicates a major discontinuity in the Precambrian rocks, which is reflected in part by minor displacements in the Paleozoic rocks. The caldera thus apparently lies at the intersection of two major regional basement structures. COLORADO PLATEAU GEOPHYSICAL STUDIES Magnetic and gravity patterns in and around Uncom-pahgre uplift J. E. Case found that the 16,000 to 19,000 feet of structural relief on the Precambrian surface from the crest of the northwestern part of the Uncompahgre uplift, Colorado, southwestward to the deepest part of the Paradox Basin is reflected in a magnetic anomaly of about 300 gammas. Paradox evaporites and other Paleozoic sedimentary rock units wedge out, pinch out, or were eroded along the Uncompahgre front and therefore are in relatively sharp contact with relatively dense Precambrian quartz monzonite on the flank of the uplift. The quartz monzonite in turn is in contact with denser gneiss on the crest of the uplift. This juxtaposition of rock types of different density gives rise to a total gravity anomaly of 50 milligals or more. The combined geologic and magnetic data serve to outline in the same region unexposed bodies of quartz monzonite, many of which are concentrated in two belts.A100 REGIONAL GEOLOGY GEOLOGICAL STUDIES Regional study of Chinle Formation in northeastern Utah and northwestern Colorado F. G. Poole and J. H. Stewart reported (chapter D) on a regional synthesis of information on the Chinle Formation (Late Triassic) and related sediments in the area extending from the Continental Divide west to the Uinta Mountains. They recognize a regional angular unconformity at the base of the Chinle throughout the area and at the top of the Chinle in northwestern Colorado. Six members are recognized, only one of which extends throughout the area. Sonsela Sandstone Bed in Chinle Formation Preliminary study of subsurface information indicates to J. D. Strobell that the Sonsela Sandstone Bed in the middle of the Petrified Forest Member of the Chinle Formation is an extensive well-defined stratigraphic unit that is readily identified in the subsurface of the western San Juan Basin, N. Mex., and northeastern Arizona. It is so prominent that it has commonly in the past been miscalled Shinarump Conglomerate, thus leading to the misidentification of the underlying beds as “Moenkopi” Formation. The Sonsela appears to be physically continuous with the Poleo Sandstone Member of the Chinle in New Mexico and and the Moss Back Member in Utah. In the central part of its basin of deposition, near the Four Comers, it becomes limy, and perhaps represents deposition in a lake to which the marginal sandy and conglomerate beds were graded. Tonguing of Juana Lopez Member of Mancos Shale Detailed sections of the Juana Lopez Member of the Mancos Shale, measured by C. H. Dane and E. R. Landis, indicate that the uppermost part of the Juana Lopez in the Chama Embayment of the San Juan Basin, N. Mex., tongues out northward and is not present in the vicinity of Pagosa Springs, Colo. Coral distribution in Redwall Limestone in Arizona W. J. Sando (p. C39-C42) has analyzed the coral distribution in the Redwall Limestone of northern Arizona and found that the Horseshoe Mesa Member, highest unit of the formation in Grand Canyon, has been removed by post-Redwall, pre-Pennsylvanian erosion in most of the area south of the canyon. The Redwall coral faunas suggest an age range from Kinderhook to Meramec and permit correlation of the formation with all but the lowermost part of the Madison Group and with post-Madison Mississippian strata. Mancos Shale and Mesaverde Group west of Albuquerque A strategically located stratigraphic section of part of the Mancos Shale and Mesaverde Group in the Rio Puerco Valley, west of Albuquerque, in Sandoval and Bernalillo Counties, N. Mex., was measured photogram-metrically by A. B. Olson, using a Kelsh plotter. The outcrops in T. 11 and 12 N., R. 2 W., are the south-easternmost in the general area where this part of the section is measurable and the nearest to the corresponding rocks exposed on the east side of the Rio Grande trough. Dips are low, the section extends across several miles of exposures, and the beds are broken by numerous faults. Coral beds above Mancos Shale correlated Fossils collected by R. G. Dickinson from the upper part of the Mancos Shale in the Cerro Summit area east of Montrose, Colo., were identified by W. A. Cobban as belonging to the Didymoceras cheyennense faunal zone of the Campanian Stage. This indicates that the coal-bearing beds immediately above the fossil zone correlated with the Fruitland Formation of the San Juan Basin to the south. Restudy of Ojo Alamo Sandstone A restudy of the type Ojo Alamo Sandstone in the San Juan Basin, N. Mex., by E. H. Baltz and S. R. Ash, of the Geological Survey, and R. Y. Anderson, of the University of New Mexico, indicates that the upper conglomeratic sandstone rests on a deeply channeled erosion surface cut in the medial dinosaur-bearing shale which is a persistent unit, rather than a lens as reported by C. M. Bauer.45 The upper conglomeratic sandstone also intertongues with the Nacimiento Formation and contains a pollen assemblage identical with an assemblage from the beds of the Nacimiento that contain Puercan mammals. Thus, the upper pari of Bauer’s Ojo Alamo is Paleocene and rests unconformably on the middle part, which is Late, but not latest, Cretaceous. These facts indicate that the Ojo Alamo Sandstone should be redefined, and that concepts of the nature and stratigraphic position of the Cretaceous-Tertiary boundary in the San Juan Basin should be revised. Artifacts and tree rings date alluviation and erosion Continuing studies by M. E. Cooley of the sequence of alluviation and erosion in late Quaternary time in the central and southern parts of the Colorado Plateau 45 C. M. Bauer, 1917, Stratigraphy of a part of the Chaco River Valley : U.S. Geol. Survey Prof. Paper 98-P, p. 275, 276.BASIN AND RANGE REGION A101 indicate that during the past 1,000 years, periods of alluviation and of arroyo cutting can be compared with the centuries-long tree-ring chronologies of Schulman.46 The chronology of the geologic deposits and sequence of events have been dated mainly from associated archaeological deposits, the ages of which were determined by the tree-ring dating technique. Comparison of the alluvial-erosional sequence with the tree-ring data indicates that alluviation occurred during periods of generally excessive tree growth—before A.D. 1100 and between about A.D. 1300 and 1850; whereas arroyo cutting occurred during periods of generally deficient tree-growth—-between A.D. 1100 and 1300 and since 1850. The comparison also indicates that fluctuations of less than about 25 years duration in the tree-growth records are not recognizable in the geologic record. Mineralogy of tuff beds in Green River Formation Petrographic studies have been made by R. L. Griggs of the altered tuff beds in the Green River Formation in the southern Uinta Basin, Garfield and Rio Blanco Counties, Colo. Although none of the tuff beds contain distinctive diagnostic minerals, as does the Pear-lette Ash Member of the Sappa Formation, that would permit widespread use and ready recognition, one of the beds was recognized as a multiple ash-fall unit; this characteristic, readily observable in the field, allows extensive use of the bed as a stratigraphic marker within much of the Piceance Creek Basin. Of geochemical interest is the observation that the altered tuff beds contain more abundant analcite than albite at the rim of the basin. Conversely, in the center of the basin, analcite is absent and the tuff beds have been replaced by albite and quartz. This difference in mineralogy probably reflects increased alkalinity toward the center of the basin. 1: 250,000-scale geologic map of Shiprock quadrangle A new geologic map of the Shiprock quadrangle, New Mexico and Arizona (O’Sullivan and Beikman, 1-63), portrays the geology of an area in the heart of the Colorado Plateau covering 2° of longitude and 1° of latitude. The map consists of two sheets compiled on a scale of 1:250,000 from more than 20 sources. It is the first of 10 similar quadrangles that will, when completed, cover much of the Colorado Plateau. Block diagram of the San Rafael Group in Utah A new block diagram (Wright and Dickey, 1-63) shows the lithologic changes accompanying the grad- “ Edmund Shulman, 1956, Dendrocllmatic changes in semi-arid America : Tucson, Ariz., Arizona Univ. Press. ual thickening of the San Rafael Group westward across the ancient platform of the present Colorado Plateau portion of Utah. Also shown are the abrupt changes in lithology and thickness farther west at the margin of the ancient miogeosyncline in the present transition area between the Colorado Plateau and the Basin and Range provinces. Geologic map of area in and near Colorado National Monument Published during the year was a map by S. W. Loh-man (1-63) of an area south of Grand Junction, Colo., that includes the Colorado National Monument. An outgrowth of Lohman’s study of the geology of the area was a request by the National Park Service that he guide the preparation of interpretive geologic diagrams, explanations, and pictures of some of the significant geologic features of the monument. These illustrations, prepared by John Stacy, scientific illustrator, are now on display in the monument. BASIN AND RANGE REGION STRATIGRAPHY AND STRUCTURAL GEOLOGY NEVADA AND EASTERN CALIFORNIA Stratigraphic correlations in White and Inyo Mountains Working in Inyo County, Calif., and the contiguous part of Nye County, Nev., J. H. Stewart has revised previously accepted correlations of upper Precambrian and Lower Cambrian strata. The Reed Dolomite of the Inyo and White Mountains, which had previously been considered to be correlative with the Noonday Dolomite of the Death Valley-Spring Mountains region, is correlated instead with dolomite that develops by change of facies out of the upper part of the Stirling Quartzite of the same region. The Deep Spring Formation, which overlies the Reed Dolomite, and the Campito Formation, which in turn overlies the Deep Spring Formation, correlate with the lower and middle parts of the Wood Canyon Formation of the same region. Previously the Deep Spring Formation had been correlated by many geologists with the Johnnie Formation of the Death Valley-Spring Mountains region, and the Campito Formation had been correlated with the Stirling Quartzite. Stratigraphic attenuation along plutonic contacts in White and Inyo Mountains C. A. Nelson found that the White and Inyo Mountains contain several plutonic bodies, mainly quartzA102 REGIONAL GEOLOGY monzonite, that appear satellitic to the plutons of the Sierra Nevada. In contrast to most of the Sierra Nevada, where host rocks are moderately to highly metamorphosed and their original nature is obscure, the rocks which the White-Inyo plutons intrude are only slightly metamorphosed and can readily be recognized. This feature has made possible detailed mapping of stratigraphic units which reveals that large-scale stratigraphic attenuation (in some places the strata have lost 85 percent of their thickness) is a common feature adjacent to regionally concordant plutonic contacts. Historic faulting in western Nevada suggests regional strike-slip relations D. R. Shawe believes that the map pattern and sense and direction of movement on certain faults in western Nevada, on which ground rupture has taken place in historic time, suggest an origin related to strike-slip faulting. Surficial ruptures resulting from fault movement associated with seven major earthquakes that have occurred during the past 60 years form a coherent arcuate linear zone (the Churchill arc) which can be thought of as resulting from a stress system acting at a single instant in geologic time. The Churchill arc transects several mountain ranges, suggesting that it is a structure of higher order than the individual mountain ranges. A transition from dip-slip normal faulting at the north end of the arc to dominantly right-lateral strike-slip faulting at the south end suggests a relation to the Walker Lane at the south end. The Walker Lane is a major northwesterly trending structural zone along which significant right-lateral strike-slip displacement is believed to have occurred. A surface rupture that formed during one other historical earthquake in this part of western Nevada, in the Excelsior Mountains, is oriented northeasterly and is characterized by left-lateral strike-slip movement. The strike-slip fault in the Excelsior Mountains and the Walker Lane, taken together, may be regarded as forming an active conjugate system, paralleled in California by the San Andreas-Garlock strike-slip fault pair, and throughout Nevada by transverse lineaments, some of which show evidence of strike-slip deformation. Altogether, these elements may reflect a stress system that affects much of the Basin and Range province. Shawe suggests that the basin-ranges, exemplified by those along the Churchill arc, formed in the vicinity of large-scale strike-slip structures. Detailed orientation of ranges has been controlled by a generally north-south structural “grain” established prior to Cenozoic growth of the basin-ranges. Structural bends parallel facies boundaries in western Nevada Working in Esmeralda County, Nev., J. P. Albers (2-64) has concluded that the large horseshoe bends or oroclines marked by the Palmetto Mountains and other arcuate ranges are paralleled by the trends of at least three facies boundaries in Paleozoic and Mesozoic rocks. The facies boundaries and structure of pre-Cretaceous rocks show that the orocline marked by the Palmetto Mountains is dextrally coupled with an oro-clinal bend of similar magnitude immediately to the west; the combination of the two oroclines gives the appearance in plan of a gigantic drag structure between the Sierra Nevada and Basin and Range structural units. At least three right-lateral strike-slip faults trending northwest and having displacements ranging from 8 to 26 miles are closely associated with but slightly younger than the oroclinal bends. The main deformation occurred during Middle or Late Jurassic time, and the total indicated right-lateral shift resulting from bending and faulting is 120 to 150 miles at the latitude of Tonopah, Nev. The Basin and Range block thus appears to be shifted southward in the right-lateral sense, relative to the Sierra Nevada. Westward Mesozoic thrusting in north-central Nevada R. E. Wallace and N. J. Silberling (p. C10-C13) have re-emphasized the presence of a westward-directed movement pattern of Mesozoic age in the tectonics of north-central Nevada, in a northeast-trending belt extending from the vicinity of Lovelock, Nev., to the Hot Springs Range northeast of Winnemucca, Nev. This direction of thrusting is opposed in sense to that of the Paleozoic thrusts, such as the Roberts Mountains thrust, and to other thrusts of Late Cretaceous and early Tertiary age in the central and eastern Great Basin. The chief evidence for the westward transport of the higher structural units is the geometry of the large-scale overturned folds. Although thrust faults are involved in this movement pattern, the direction of movement of the upper plate can seldom be determined from thrust relations alone. Precambrian and Mesozoic rocks in Slate Range, Calif. G. I. Smith, of the Geological Survey, and B. W. Troxell and C. H. Gray, of the California Division of Mines and Geology, have nearly completed reconnaissance mapping of the Slate Range, east of Searles Lake, Calif. This mapping has revealed large areas of previously unreported Precambrian (?) metaplutonic rocks and lower Mesozoic(?) metavolcanic rocks. A majorBASIN AND RANGE REGION A103 fault zone trends diagonally northward through the range; it cuts rocks probably as young as late Mesozoic, but is overlapped by upper Cenozoic rocks. A large west-dipping low-angle fault crops out along the west edge; small grabens in lake gravels of early Wisconsin age are areally related to it and are thought to indicate that the major fault is a tensional feature that developed in late Pleistocene time. Lower Cambrian fossils found in Nye County, Nev. In mapping northern Nye County, Nev., Frank Kleinhampl has found fossils that demonstrate the presence of Lower Cambrian rocks in the Monitor and Toquima Ranges. This discovery will modify present ideas of the extent of the seaway that crossed in Early Cambrian time what is now Nevada. Triassic rocks mapped in Inyo Mountains, Calif. Ward C. Smith has found that Mesozoic strata crop out in a belt 25 miles long on the west slope of the southern Inyo Mountains, Calif. Two units are exposed. The lower, 2,500 feet thick, consists of marine limestone and shale of Early and Middle Triassic age; it rests unconformably on marine sedimentary rocks of Pennsylvanian to Permian age. Of the upper unit, strata about 7,000 feet thick are exposed, the top of the section being faulted away. Continental sedimentary and volcanic rocks make up this unit, which is unfossil-iferous. These units were strongly deformed, evidently prior to the intrusion of batholithic granite masses of Mesozoic age. The Lower and Middle Triassic section is one of the most complete in this region. Paleozoic plutonic rocks found in Pershing County, Nev. D. B. Tatlock, mapping in Pershing County, Nev., has found two leucogranite plutons, one at the south end of the East Range and another, smaller one near the north end of the Stillwater Range, that are equivalent to upper Paleozoic leucogranite in the Humboldt Range. These are the only Paleozoic plutonic rocks thus far found in western Nevada. WESTERN ARIZONA AND SOUTHEASTERN CALIFORNIA Metamorphic rocks of Riverside Mountains, Calif. Detailed mapping of the Riverside Mountains, Calif., by Warren Hamilton (1-64) shows that they consist of a very large recumbent isoclinal syncline of Paleozoic and lower Mesozoic(?) rocks enclosed between middle(?) Precambrian gneiss and migmatite. The Paleozoic and Mesozoic(?) rocks are pervasively deformed by bedding-plane shearing, thrust faulting, and isoclinal folding, and bedded and plutonic rocks are tectonically intercalated. Basement rocks of the lower (upright) limb are but little sheared and recrystallized, whereas basement rocks of the upper (inverted) limb are pervasively crashed; enclosed bedded rocks are metamorphosed to about the same degree as the retrograde metamorphism of the upper limb. Similar relations exist in the structurally similar Big Maria Mountains to the south. This indicates that the cause of the regional metamorphism is probably heat generated by the extreme deformation rather than heat conducted upwards into the crust. Upper Cretaceous or lower Tertiary megabreccias derived from pre-Cretaceous rocks have been broken by gravity thrust faults and by left-lateral strike-slip faults striking north-northeastward. Cyclic sedimentation of Cambrian rocks of Death Valley A. R. Palmer has found, in a study of the stratigraphy of the Carrara Formation in the Death Valley region, California, that it includes part or all of four transgressive-regressive sedimentary cycles. Each cycle is terminated by a limestone unit and these limestones intertongue to the southeast with siltstones and shales. The lowest cycle, which begins with the underlying Zabriskie Quartzite, is entirely Early Cambrian. The second cycle includes Lower Cambrian shales and silt-stones at its base and Middle Cambrian limestone at its top. The two upper cycles include early Middle Cambrian beds. Mojave block north of San Andreas fault forms part of Mesozoic batholith Geologic mapping of the pre-Tertiary crystalline rocks in the central and southern Mojave Desert and San Bernardino Mountains, Calif., by T. W. Dibblee, Jr., shows that the Mojave block north of the San Andreas fault is in effect part of a Mesozoic batholith of quartz monzonite that here contains pendant remnants of Precambrian (?) gneiss overlaid unconformably by Paleozoic metasedimentary rocks. The quartz monzonite was emplaced in at least two major waves, separated by the emplacement of masses and dikes of andesitic porphyry. Deposits of iron ore are associated with in-trusives of the first wave. In the San Bernardino Mountains the San Andreas fault splits into several branches, and displacements on all are right lateral, but only on the north, major (Mill Creek) branch is displacement of major magnitude, measurable in at least tens of miles. This is indicated by the abrupt termination caused by this branch, of the Mojave block rocks 746-002 0 - 64 -8A104 REGIONAL GEOLOGY mentioned, in which the gneiss dips regionally northwest. The adjacent southwest block is composed almost entirely of Precambrian (?) gneiss, schist, and mylonite, with a regional southward dip. Oldest rocks in Arizona exposed in a plunging diapiric anticline P. M. Blacet reports that the oldest rocks so far recognized in Arizona, the pre-Yavapai gneiss of Turkey Creek, southeast of Prescott, Ariz., are exposed in the core of a northeast-plunging diapiric anticline. Both the gneiss and the overlying Yavapai Series are cut out by intrusions of porphyritic granodiorite south of Battle Flat, thus limiting the exposed area of pre-Yavapai basement to about 10 square miles. Stratigraphy revised in southwestern Arizona L. A. Heindl and N. E. McClymonds (p. C43-C49), working in the Papago Indian Reservation of southwestern Arizona, have tentatively reclassified a well-known clastic unit, long correlated with the Troy Quartzite, of younger Precambrian age, as Bolsa (?) Quartzite, of Cambrian age. In the Vekol, Slate, and Waterman Mountains, the unit in question contains fragments of fossils, is conformable with the overlying Abrigo Formation, and rests unconformably either on rocks of the Apache Group or on Precambrian granite. EASTERN NEVADA AND UTAH Miocene and Oligocene fossils found in Humboldt Formation of eastern Nevada J. F. Smith and K. B. Ketner suggest on the basis of field studies in the Dixie Flats-Huntington Creek area south of Elko, Nev., a revision of the age of the Humboldt Formation, formerly thought to be of Miocene and Pliocene (?) age. J. A. Wolfe has identified plant fossils of probable Oligocene age from the lower part of the Humboldt, and G. E. Lewis has identified late Miocene vertebrate fossils from the upper part. Faulting in Confusion Range, Utah, dated In the Confusion Range, in Millard County, Utah, R. K. Hose has found evidence that high-angle dip-slip faults, of irregular trend, with displacements of as much as 2 miles, were formed in late Mesozoic to premiddle Tertiary time. These faults are locally overlapped by equivalents of the Needles Range(?) Formation of Mackin (1960) of late Oligocene to early Miocene age. Probably many, if not most, of the high-angle faults of the northern Confusion Range (including the Conger Range), whose relations to Tertiary units cannot be determined, were also formed during late Mesozoic to pre-middle Tertiary time. Corals suggest correlation of Pilot Shale in Utah Study of corals by Helen Duncan from the upper part of the Pilot Shale in the Confusion Range, Utah, and in the Pahranagat Range, Nev., resulted in the identification of two characteristic Carboniferous solitary rugose genera (Permia and Rhopalolasma) in association with the tabulate genus Vaughania, which is the guide fossil for the oldest Carboniferous faunal zone of Great Britain. The Pilot species of Permia is closely related to, if not identical with, the Louisiana Limestone coral previously identified as Neozaphrentis parasitica (Worthen). In the Confusion Range, the corals occur in a diversified assemblage, including productoid brachiopods and trilobites of early Carboniferous aspect, that bears a great deal of similarity to the fauna of the Louisiana Limestone of Missouri. An Early Mis-sissippian assignment for the controversial Louisiana Limestone is therefore supported by several critical groups of larger invertebrates. Tear fault inferred in East Tintic Mountains, Utah H. T. Morris and W. M. Shepard (p. C19-C21) have found evidence for a concealed tear fault of large displacement in the central East Tintic Mountains, Utah. This fault, of probable east-northeasterly trend, is believed to terminate on the south of the Oquirrh-East Tintic system of folds and the East Tintic thrust. This inferred termination is beneath the lava cover of the central part of the East Tintic Mountains. A fault that is the possible continuation of the inferred tear crops out in the southern part of West Mountain, 15 miles northeast of the central East Tintic Mountains. This fault has been previously regarded as a thrust in which the upper plate moved southward with respect to the lower plate, but the structural style of the block northwest of this fault, as well as its outcrop pattern, are more nearly consonant with the interpretation offered here. Similar late Paleozoic deposition in Nevada and Idaho suggests extension of Antler orogenic belt R. J. Roberts and M. R. Thomasson (2-64) have compared the late Paleozoic depositional history of northern Nevada and central Idaho and have found many points of resemblance, leading them to infer an extension of the Antler orogenic belt into Idaho. The major thrust thus far known is post-early Permian, but they infer earlier major thrusts.BASIN AND RANGE REGION A105 Imbricate thrust sheets in Oquirrh Mountains, Utah R. J. Roberts and E. W. Tooker, mapping in the Oquirrh Mountains of Utah, report that a synthesis of stratigraphic and structural data from the Oquirrh Mountains and reinterpretation of data from some of the surrounding ranges indicate that the rocks in the Oquirrh Mountains are involved in a series of imbricate thrust sheets in which the strata have been telescoped. Some thrusts, such as the North Oquirrh thrust, separate strata of different sedimentary facies; the great difference in facies is believed to indicate that the displacements on such thrusts may amount to tens of miles. Other thrusts, such as the Midas thrust, separate strata of the same facies; they are mappable because the structural style of the upper and lower plates is different. The use of this criterion to distinguish plates separated by thrusts is relatively newT in the eastern part of the Basin and Range province. The ore deposits at Bingham, Utah, occur in overturned, folded, faulted, and brecciated rocks, and are spatially associated with Tertiary intrusive rocks in the upper plate of the Midas thrust fault. Major middle Tertiary or younger faulting suspected in Ruby Mountains, Nev. Geologic mapping in the Jiggs quadrangle, Nevada, by C. R. Willden, has resulted in recognition of a klippe of a major thrust plate resting on the Harrison Pass quartz monzonite stock. A sample of this intrusive body collected by R. R. Coats has yielded a K-Ar age of 35 million years and a Pb-alpha age of 40 million years. If the dating of additional samples from this intrusive body, now in progress, confirms these dates as the actual age of the stock, then middle Tertiary or younger thrusting can be demonstrated in the Ruby Mountains. Late Tertiary low-angle fault in Juab County, Utah In western Juab County, Utah, near the Spor Mountain beryllium deposits, D. R. Shawe (p. B13-B15) has found a low-angle fault on which Cambrian carbonate sedimentary rocks have moved at least 1 mile over volcanic rocks of probable Miocene and Pliocene age. It is the youngest low-angle fault of this magnitude now known in the region. A tuff underlying the fault may be correlative with the tuff that contains large beryllium deposits at Spor Mountain, and therefore this fault, or others like it, may in places conceal additional beryllium deposits. Movement along thrust fault in eastern Nevada Harald Drewes reports (p. B20-B24) subsequent movement in diverse directions on an earlier thrust fault in the Schell Creek Range near Ely, Nev. These movements reflect first normal faulting, then low-angle gravity sliding, and finally renewed normal faulting, according to his interpretation. Thrusting in Park City district, Utah Mapping by C. S. Bromfield on the east side of the Park City mining district, in Wasatch and Summit Counties, Utah, shows that the Eocene(?) and Oligo-cene (?) volcanic rocks which flank the west side of the north-plunging Park City anticline were deposited on a surface of considerable relief and rest on beds ranging in age from the Pennsylvanian Weber Quartzite to the Triassic Thaynes Formation. The major movement on the Frog Valley thrust, fault which cuts the sedimentary rocks along the east side of the anticline apparently antedates the volcanic rocks. Lower Paleozoic rocks faulted over Tertiary deposits in Snake Range, Nev. D. H. Whitebread has found several small areas on the east side of the southern Snake Range, Nev., where large masses consisting of brecciated rocks of Cambrian and Ordovician age are faulted over Tertiary gravels. The fault blocks are probably gravity slides from the higher areas to the west. Although the rocks within the upper plate are extremely broken, the individual units remained virtually intact, as the several formations in the upper plate remain as mappable units. Offset of Egan Range, Nev., ascribed to faulting Geologic mapping by A. L. Brokaw and P. J. Barosh in the Giroux Wash area of the Ely and Reipetown quadrangles near Ely, Nev., indicates that the abrupt offset of the Egan Range, between the south end of Radar Ridge and the north end of Rib Hill, may be due in part to a set of east-northeast-trending transverse faults. The rocks on Radar Ridge are tightly folded into a north-trending unbroken syncline, strongly overturned to the west. To the southeast for about 3 miles, only the east limb of the fold remains and this has been broken by a succession of high- and low-angle transverse faults having a cumulative offset to the east of more than a mile. South of Rib Hill, the syncline continues unbroken for more than 2 miles. The intrusive rocks and related ore deposits are localized on the projection of the transverse fault zone,A106 REGIONAL GEOLOGY but the relation is obscured because of later northtrending normal faulting. EASTERN ARIZONA, NEW MEXICO, AND WESTERN TEXAS “Down-structure” method of tectonic analysis P. B. King (p. B1-B8) has applied the “down-structure” method of tectonic analysis to steeply plunging complex structures in the Garden Springs area of the Marathon Basin of west Texas. When the map is oriented so that the geologist views it in the direction of plunge, the outcrop pattern becomes a structure section, but in a near-horizontal plane rather than the vertical plane of conventional structure sections. By this method of analysis it can be shown that the Garden Springs area contains what was originally a low-angle thrust fault that was subsequently steeply folded. Paleozoic section studied in Whetstone Mountains, Ariz. S. C. Creasey has found in the Whetstone Mountains the most complete and relatively undisturbed section of Paleozoic rocks in southeastern Arizona. From top to bottom the section consists of the Rainvallev Formation, Concha Limestone, Scherrer Formation, Epitaph Dolomite, Colino Limestone, Abrigo Limestone, and Bolsa Quartzite. The span of time is from Permian to Cambrian, but representatives of the Silurian and Ordovician are missing. Because the rocks are well exposed, the geologic structures are simple, and the Paleozoic section is so complete that the Whetstone Mountains will serve as a “reference range” for the Paleozoic stratigraphy of southeastern Arizona. Percha Shale younger than Sly Gap Formation in New Mexico Correlations and ranges of invertebrate fossils in Devonian rocks in New Mexico have been considerably strengthened as a result of fieldwork by G. A. Cooper, U.S. National Museum, and J. T. Dutro, Jr., of the Geological Survey. A major conclusion is that the Percha Shale of western New Mexico is entirely younger than the Sly Gap Formation of Stevenson (1941) in the southeastern and south-central parts of the State. It also appears that several close similarities to the Devonian sequence of western Canada can be documented. Limestone rafted by volcanic flows in Arizona In the Huachuca Mountains, Canelo Hills, and Santa Rita Mountains of southeastern Arizona, Harald Drewes, Philip Hayes, Robert Raup, and Frank Simons have found thousands of feet of rhyolitic tuffs, flows, and associated sedimentary rocks of Triassic or Jurassic age, in which exotic blocks of Paleozoic limestone, as much as half a mile in length, are a common feature. While some of these blocks are apparently ancient landslides, others seem to have been rafted into place by thick, viscous flows. Presumably these remarkable features result from the disruption of the roof of shallow laccolithic intrusions. Quartz-vein mineralization in Santa Rita Mountains, Ariz. In the Mount Wrightson quadrangle, Santa Cruz County, Ariz., Harald Drewes has studied a system of quartz veins that carry lead, silver, and zinc, and that were emplaced, probably in Miocene time, in a system of fractures that fan out like the leaves of an opened book standing on end, and that lie athwart the major north-northwest-trending Mesozoic structures. Helmet Peak anticline of Pima district, Arizona In the Pima copper district, Arizona, large-scale mapping by J. R. Cooper substantiates that the Helmet Peak anticline is a diapir with its roots in the easttrending thrust zone of Laramide age that is mineralized at the San Xavier mine, west of the root zone of the diapir. The plunge of the fold axis and the dip of the thrust zone are to the south, having been much steepened by the late southward tilting of this part of the district. Due to the flowage of the mobile core of the diapir, Permian rocks were driven upward three-quarters of a mile in an upright isoclinal anticline less than 1,000 feet wide that pierces Mesozoic red beds and arkoses normal to their trend. CENOZOIC VOLCANISM Shape of Three Peak intrusion, Utah H. R. Blank, Jr., and J. H. Mackin report that an analysis of the magnetic anomaly produced by the Three Peak intrusion, the most easterly of the three bodies of quartz monzonite porphyry in the Iron Spring district, Iron County, Utah, shows that the intrusion must have the form of a thick plate, rather than a stock or plug. Using an effective susceptibility value of 6 X10'3 centimeters per gram per second obtained from a ground magnetometer profile, the best fit with the observed amplitude and shape of the anomaly is obtained with a model slab about 3,000 feet in thickness. The improved precision for the shape may have important economic consequences.BASIN AND RANGE REGION A107 Thick Tertiary volcanic sequence in Cady Mountains, Ariz. Mapping in the Cady Mountains of the central Mojave Desert by T. W. Dibblee, Jr., and A. H. Bassett, reveals that the Mesozoic quartz monzonite platform is overlain by volcanic piles of Tertiary andesitic and basaltic rocks that accumulated to thicknesses of m$ny thousands of feet around several vents. The volcanic sequence contains many vein deposits of manganese ore, fluorite, barite, travertine, agate, and jasper. It is overlain by a Miocene sedimentary sequence that contains lacustrine strata including deposits of celestite, lithium clay, and clinoptilolite tuff. Extensive accumulations of Pliocene and Pleistocene fanglomerate complete the sequence. Volcanic sequence subdivided near Beatty, Nev. In the general vicinity of Beatty and Goldfield, Nev., D. C. Noble, R. E. Anderson, E. B. Ekren, and J. T. O’Connor (4—64) have mapped a sequence of rhyolitic ash-flow and air-fall tuffs. These tuffs (Noble and others, 4r-64) are called the Thirsty Canyon Tuff, and have been recognized in five formal members: the Spearhead, Trail Ridge, Dry Lake, Gold Flat, and Labyrinth Canyon Members, and an unnamed upper member. Each member was deposited within a short interval of time, and cooled generally as a single unit. The several members are soda rhyolites and pantel-lerites, and apparently are comagmatic. Phenocrysts include soda-rich sanidine, pigeonite, green clinopy-roxene, fayalite, brown amphibole, and zircon. Quartz is rare. There is significant lateral and vertical variation in phenocryst, lithic-fragment, and pumice content within the individual members, which can also be distinguished one from another in general appearance and petrography. Zonal features of ash-flow sheet studied P. W. Lipman and R. L. Christiansen (p. B74—B78) have studied variations in chemical composition within an ash-flow sheet in the Piapi Canyon Formation in southern Nevada. They found that (1) the unwelded vitric tuff at the edges of the sheet had lost small amounts of silica and sodium by leaching of the glass shards; (2) the various phases of the dense welded tuff are all very similar in their composition, as crystallization from a vapor phase had no measurable effect on the bulk composition of the rocks; and (3) only a very local redistribution of the major elements and oxidation of the iron in the vapor-phase crystallization zone appear to have been involved. Structure of Timber Mountain caldera, Nevada W. J. Carr (p. B16-B19) has found that the center of Timber Mountain caldera, on the western edge of the Nevada Test Site, northeast of Beatty, is a structural dome in a thick sequence of ash-flow tuffs. These tuffs were intensely faulted in two episodes. The first resulted in an arcuate system of faults that were intruded by possible ring dikes, the surface expression of which is a group of light-colored porphyritic syenite intrusions that follow a part of the ring-fracture system. The second episode of faulting is expressed in a system of graben faults that resulted in irregular collapsed segments in the middle of the dome. CENOZOIC STRATIGRAPHY Pleistocene lake deposits subdivided around Searles Lake, Calif. G. I. Smith, mapping upper Quaternary deposits in the south part of Searles Lake Valley, now exposed at a higher level than the salt deposits of Searles Lake, has delineated deposits formed in lakes believed to be of Yarmouth (?), Illinoian (?), Sangamon (?), early Wisconsin, middle Wisconsin, late Wisconsin, and Recent ages, and has found that some of these lakes had two or more distinct maxima. The mapping has also fixed the position of one fossil soil in this sequence as being immediately pre-Wisconsin in age, and several others as being of Wisconsin and Recent ages. All indicate a significant hiatus in the sedimentary history. Although not fossil soils in the strict sense, sedimentary features interpreted as fossil desert pavements that were covered with desert varnish have also been used as an indication of an hiatus in sedimentation. Recognition of such gaps is important in the study of this sequence of beds because the gaps are the lateral equivalent of the saline layers buried in the central part of the basin. Revision of Lake Bonneville history Roger Morrison has been able to make significant revisions in the accepted history of Pleistocene Lake Bonneville, and in the stratigraphy of the deposits laid down within it, as a result of intensive studies of a huge gravel pit at Little Valley, near the southern end of Promontory Point, Box Elder County, Utah. Two earlier lake cycles, comparable in magnitude to the well-known Lake Bonneville described by G. K. Gilbert, were probably Kansan and Illinoian, respectively. Included in the early history of the Lake Bonneville were two early lake cycles (recorded by the Alpine For-A108 REGIONAL GEOLOGY mation) during which the lake rose nearly to the Bonneville (highest) shoreline, and which are correlated, principally on the basis of comparative maturity of soils, with the Bull Lake Glaciation in the Rocky Mountains. After long desiccation, there were three lake cycles in late Lake Bonneville time, all correlative with the Pinedale Glaciation. The first lake cycle nearly reached the Bonneville shoreline, the second reached this shoreline, and the third nearly reached the Provo level. Pleistocene faulting at Salt Lake City, Utah Richard Van Horn has found, in a building excavation in downtown Salt Like City, Utah, sedimentary deposits that can be attributed to the Alpine Formation, corresponding to the early lake cycles and others that are correlated with the Bonneville Formation, of late Lake Bonneville time. The latest of these formations was faulted, but the faulting occurred before the development of a soil profile by weathering in post-Bonneville time. The possibility that younger faults may exist elsewhere in the Salt Lake area is not excluded by this evidence. Pliocene and Pleistocene drainage changes in Arizona M. E. Cooley, on the basis of a study of the imbrication of pebbles and the lithology of gravels of Pliocene^) age which are faulted and tilted, has interpreted the ancestral stages of the Salt River and the development of the Tonto Basin of Arizona. In the Tonto Basin these gravels are equivalent to or underlie fine-grained sedimentary rocks containing fossils of Pliocene age. The resulting interpretation is that the ancestral Salt River entered the Tonto Basin near the course of the present Salt River, flowed westward and northwestward through the basin, and left in a valley underlain principally by schist; it flowed through the Mazatzal Mountains near the Phoenix-Payson highway. The dacite and rhyolite flows and tuffs in the Globe-Superior area formed a barrier to streams and were responsible, in part, for the establishment of the ancestral Salt River across the Mazatzal Mountains. Later, this valley was blocked by basalt flows that were erupted between Bartlett Reservoir (on the Verde River) and the Mazatzal Mountains and forced the ancestral Salt River to leave the Tonto Basin by the channel now occupied by the river. The relief of the area in late Tertiary time was not as great as it is today, although the main mountain ranges and valleys were outlined. The Tonto Basin, Mazatzal Mountain, and other nearby mountains were formed largely as a result of large-scale normal faulting, which displaced the gravels, basalts, and older rocks. GEOCHEMICAL EXPLORATION Shallow intrusive suspected near Cortez, Nev. Working in lower plate Silurian and Devonian rocks exposed in the Cortez window of the Roberts thrust about 4 miles north of Cortez, Nev., R. L. Erickson, Harold Masursky, A. P. Marranzino, LT. Oda, and W. W. Janes (p. B92-B94), have found anomalous amounts of arsenic, antimony, and tungsten in fracture fillings and jasperoid in limestone. Discontinuous alined masses of skam and abundant fine-grained quartz-bearing dike rocks in the window suggest that an intrusive mass lies at shallow depths beneath at least part of the area. The skarn consists of calcite marble with porphyroblasts of idocrase, grossularite, and scapolite (meionite) in crystals as much as 2 inches across. This is the most intense contact metamorphic aureole in the Cortez area and it suggests that the metal anomalies may be leakage haloes emanating from concealed metalliferous deposits near the contact with the postulated buried intrusive. Geochemical trends in Ruth copper district, Nevada G. B. Gott and J. H. McCarthy, Jr., who have been carrying on geochemical investigations of the Ruth porphyry copper district, Nevada, are able to show that the district is well defined by the distribution of tellurium. Relatively small amounts (0.1-1 parts per million) of tellurium are present in the area where copper has been mined, and an irregular broad tellurium halo surrounds the central copper area. Iron- and manganese-rock material contains up to 1 percent tellurium. Silver and mercury show almost identical geochemical patterns. These investigations also shows that the district is zoned in the following manner: Copper is the predominant metal in the central core; the core is surrounded by a zone in which zinc predominates, and this in turn is surrounded by a zone in which lead predominates. COLUMBIA PLATEAU AND SNAKE RIVER PLAIN Three members of Yakima Basalt in Washington K. L. Walters and J. W. Bingham have recognized the upper three members of the Yakima Basalt in eastern Franklin and Whitman Counties, southeastern Washington. Although the thickness and number of the flows in each member differ from place to place,COLUMBIA PLATEAU AND SNAKE RIVER PLAIN A109 the characteristic lithology, joint pattern, and relative stratigraphic position of the members remain consistent throughout the 175 miles between the canyon of the Yakima River and eastern Whitman County. Facies changes in Dalles Formation in Oregon Eastward from the flank of the Cascade Range in north-central Oregon, R. C. Newcomb has found a progressive change in the lithologic character of the Dalles Formation, which overlies the Columbia River Basalt. The Dallas Formation changes from coarse pumiceous agglomerate with some andesite clasts on the west to fine-grained andesine lithic-vitric tuff in the canyon of the Deschutes River. Farther east, the tuff beds iufertongue with pebble and cobble conglomerate, and at the east edge of the Wishram quadrangle the Dalles Formation resembles the Arlington Beds of Shotwell, 26 miles farther east. The middle Pliocene (Hemphillian) age assigned the Arlington Beds by Shotwell, however, is not in accord with the early Pliocene age commonly assigned to the Dalles Formation. Oldest strata of Harney basin, Oregon, dated Along the southern margin of the Harney basin, southeastern Oregon, widespread crystal-vitric and pumice-lapilli welded tuffs are interstratified with tuf-faceous sedimentary rocks that, in one place low in the sequence, contain lower Pliocene vertebrate fossils, according to G. W. Walker and C. A. Repenning. A welded tuff layer in this sequence has a K-Ar age of about 9.7 million years. Near the basin, these lower Pliocene rocks lap with slight angular discordance onto sedimentary rocks that contain upper Miocene vertebrate fossils and onto basalt flows that overlie the upper Miocene rocks. The Pliocene rocks seem to be the oldest strata deposited in the Harney basin itself. Ash from Crater Lake traced as far as Montana and British Columbia Volcanic ash from the catastrophic Mazama eruption at Crater Lake, Oreg., about 6,700 years ago, has been traced by H. A. Powers and R. E. Wilcox (1-64) across Oregon, Washington, and Idaho, into Nevada, Montana, Alberta, and British Columbia. The petrographic and chemical characteristics of the Mazama ash distinguish it from other ash deposits in the Pacific Northwest, making it a recognizable stratigraphic marker, and, because it is well dated, an ideal geologic datum. Powers and Wilcox have found that most of the ash formerly called “Glacier Peak ash” in Washington, and “Galata ash" in Montana, is from the Mazama eruption. Glacier Peak Volcano in northern Washington was the source, however, of an ash bed of very late glacial or early postglacial age found locally in Washington, Idaho, and Montana. Fault mapped along border of Snake River Plain In the Mountain City quadrangle, northern Nevada, R. R. Coats has mapped a major normal fault near the northern margin of the mountainous part of the quadrangle; the fault trends about N. 70° E. and is thrown down on the north. This fault, and other faults of probable similar trend in the Jarbidge quadrangle, are roughly parallel to the mountainous belt along the southern border of the Snake River Plain eastward as far as Salmon Falls Creek. Coats suggests that the mountains and the Snake River Plain in this region may have been outlined by faulting as early as the Miocene. Gravity survey of Arco area, Snake River Plain A reconnaissance gravity survey of the National Reactor Testing Station, Idaho, near the northern margin of the Snake River Plain shows that a gravity low extends from the south end of the valley of the Little Lost River around the east and south sides of the Arco Hills. D. R. Mabey interprets this low as indicating that a large volume of sediments of low density are interbedded with the basalt at the north edge of the plain. A gravity high over the Lost River Sinks indicates that the sediments are less abundant there. Gravity anomalies appear to correlate generally with magnetic anomalies, suggesting that both the gravity and magnetic highs are produced by dense basalt. Structural features extend beneath Snake River Plain from the north North of the National Reactor Testing Station, Idaho, roughly parallel northwest-trending fault-controlled basins and ranges intersect the Snake River Plain. Preliminary gravity and aeromagnetic profiles drawn by G. H. Chase suggest that the roots of such structures, although possibly downfaulted at the margin of the Snake River Plain, extend into the plain beneath the sequence of basalt flows and intercalated sediments. According to D. A. Morris, northwest-trending faults locally cut Quaternary basalt flows and alluvial fans north of the station. Either this faulting or intraflow lensing of sediments within the basalt has produced a barrier that materially affects the movement of ground water in the eastern part of the station.A110 REGIONAL GEOLOGY Overflow of Lake Bonneville estimated At a time of pluvial climate about 90,000 years ago, Lake Bonneville overflowed at Red Rock Pass near Preston, Idaho, and discharged 1.3 billion acre-feet of water onto the Snake River Plain. The resulting flood inundated an area of 250 square miles between Pocatello and American Falls, covered an area of 170 square miles near Rupert, and filled the canyon in the next 200 miles downstream to a depth of 300 feet. Calculations of discharge by C. T. Jenkins at constricted sections along the canyon south of Boise, determined from height of flood deposits and from hydraulic principles, indicate a maximum discharge of 15 million cubic feet per second—a flow about 5 times the estimated mean annual discharge of the Amazon. This extraordinary flood caused spectacular erosion at the canyon head near Twin Falls, where cutting of cataracts and marginal spillways removed at least 50 billion cubic feet of basalt. This rock was washed downstream and deposited in wide segments along the canyon as enormous bars of boulders and sand. Some of the bars reach 300 feet above the Snake River and are several miles long. Because of relatively tranquil flow of deep water through the wide segments (owing to constrictions downstream), virtually all of the flood debris was dropped in the 120-mile stretch below Twin Falls. The volume of gravel therefore can be equated with the amount of flood erosion. Moreover, the distribution and physiography of the flood debris give an accurate picture of the width, the profile, and the pattern of flow of this gigantic flood. Thus, geologic study and mapping contribute empirically to the hydrologic assessment of a discharge vastly beyond the range of experimental measurement. PACIFIC COAST REGION WASHINGTON Geology of Mount Rainier The geology of Mount Rainier National Park, the site of one of the most impressive volcanic edifices in the Cascade Range, is described in a report by R. S. Fiske, C. A. Hopson, and A. C. Waters (1-63). The bulk of Mount Rainier volcano, composed chiefly of pyroxene andesite flows and breccias, grew during Pleistocene time. These flows and breccias were extruded on an irregular mountainous surface underlain by a complex of altered volcanic and sedimentary rocks of Eocene to Miocene age and plutonic and hypabyssal igneous rocks of the late Miocene Tatoosh pluton. Mount Rainier probably last erupted about 500-600 years ago, but is now dormant and is clad by glaciers and snow-fields. Glacial erosion, rockfalls, and avalanches are rapidly reducing the size of the mountain. Plutons of Northern Cascade Mountains F. W. Cater, D. F. Crowder, and others have recently completed studies of the Coast Range batholith between Glacier Peak and Lake Chelan. These studies have resulted in the delineation of 20 major plutons and many smaller stocks which occur within medium-grade metamorphic rocks of the Northern Cascade Mountains. The older plutons are dominantly elongate and commonly gneissic parallel to the regional northwest trend of foliation and compositional layering in the surrounding rocks. These older plutons range in composition from tonalite, the dominant rock, to granodiorite. Radiometric age determinations suggest a Cretaceous age for the large pluton at Chelan, known as the “Chelan batholith.” Four of the older plutons are interpreted as having formed in place by granitization, whereas others may be magmatic intrusives emplaced before or during regional metamorphism. The youngest bodies, which are widely distributed and largely discordant, are massive, shallow, magmatic intrusions of late Miocene age. They range from tonalite to adamellite in composition. Recent radiometric age determinations have also distinguished a late Eocene pluton that consists largely of granodiorite, was emplaced at moderate depth, and is dominantly concordant. Structural history of eastern Olympic Mountains New data bearing upon the structural history of the eastern Olympic Mountains resulted from mapping by W. M. Cady and R. W. Tabor of large asymmetrical folds with limbs about a mile wide, west of Mount Constance. These folds plunge steeply northwest and are outlined by distinctive graywacke beds interlayered with slate in a thick sedimentary section west of and stratigraphically below the nearly vertical homoclinal sequence of volcanic rocks of the Crescent Formation. The Crescent volcanics, which encircle the Olympics on the north, east, and south, were not involved in the folding, thus indicating a strong tectonic break between the graywacke-slate sedimentary section and the volcanic rocks. Steep axes of numerous smaller folds and related cleavage-bedding intersections occur in the graywacke-slate sequence elsewhere in the eastern Olympics, and their distribution, orientation, and movement sense are under systematic study. The confinement of the steeply plunging folds to the graywacke-PACIFIC COAST REGION Alll slate sequence suggests a possible analogy with salt domes, wherein the complexly folded salt may correspond to the folded interbedded graywacke and slate, and the Crescent volcanics may correspond to the resistant caprock. Glaciation of southwestern Olympic Mountains Valleys heading on the southwestern side of the Olympic Mountains were occupied by glaciers three times during Wisconsin time, and at least once in pre-Wisconsin time, according to D. R. Crandell (p. B135-B139). During all but the last of these glaciations, the interior of the mountains probably was mantled by extensive icefields, if not by a continuous icecap above which only the highest ridges and peaks protruded. Some of the glaciers extended westward as broad lobes and reached the present Pacific shoreline. Continuing studies of urban geology in and around the city of Seattle, by D. R. Mullineaux and H. H. Waldron, have established the existence of late Pleistocene, pre-Vashon, nonglacial sediments that range in age from about 18,000 to 24,000 years, as determined by radiocarbon dating methods. In addition, the existence of previously unknown older sediments of gla-ciomarine origin has also been established. Both of these discoveries are a significant contribution toward an understanding of the sequence of events that occurred in the Pacific Northwest during the Pleistocene Epoch. OREGON Geologic mapping of Portland area A report on the geology of the Portland area by D. E. Trimble (1-63) not only contributes to the knowledge of the general geology of northwest Oregon, but also provides basic geologic data broadly applicable by the construction industry to urban development of the region. The more than 1,000 square miles in the area mapped around Portland is underlain mainly by Ce-nozoic terrestrial deposits and volcanic rocks; a small granodiorite stock crops out in the northwestern part, and the marine Scappoose Formation crops out in the northwestern part. Included in the Quaternary sediments are the products of a large-scale flood, believed to have resulted from the sudden release of water from glacial Lake Missoula; other somewhat older alluvial units consist of mudflow deposits, bouldery gravel, and loess. Most deposits older than late Pleistocene are deeply weathered. The structural instability of loess and weathered material, when wet, poses most of the foundation problems for the construction industry in this region. Eocene volcanoes of Oregon coast Geologic mapping along the central Oregon coast, by P. D. Suavely, Jr., and N. S. MacLeod, together with petrographic studies and new chemical analyses, indicates that volcanoes that erupted along the axial parts of the Oregon-Washington Tertiary eugeosyncline during early to middle Eocene time followed a life cycle somewhat similar to that of volcanoes in the Hawaiian Islands. Great volumes of saturated theoleiitic basalt were erupted onto the sea floor to form pillow flows and breccia in early Eocene time. In areas of thickest accumulation, islands were constructed and a pyroclastic phase formed thick units of tuff and tuffaceous siltstone adjacent to the islands. During the waning periods of volcanism the magma was probably contained within shallow reservoirs beneath the volcanic centers, where it differentiated to form augite-rich basalt and alkalic basalt. Surface or near-surface occurrences of these lower to middle Eocene basaltic rocks produce broad gravity highs and sharp, high-amplitude magnetic-anomaly zones. COAST RANGES AND KLAMATH MOUNTAINS OF NORTHERN CALIFORNIA AND SOUTHERN OREGON Hypothesis for distribution of ultramafic rocks Anomalous distribution of the pre-Tertiary rocks of northwestern California and southwestern Oregon may be a result of regional thrust faulting, according to an hypothesis advanced by W. P. Irwin (p. C1-C9). According to this hypothesis, extensive linear belts that crop out in the area of ultramafic rocks are the exposed edges of sheetlike intrusions that lie between the postulated thrust plates, and have root zones to the east. The ultramafic sheets intruded the rocks of the Klamath Mountains during the Late Jurassic (Nevadan orogeny), and those of the Coast Ranges probably during the Late Cretaceous. Emplacement of the principal ultramafic sheet of the Coast Ranges is thought to have been along a regional thrust fault formed prior to the development of the San Andreas fault system, and to have resulted from a different force couple than (heA112 REGIONAL GEOLOGY San Andreas. Thus, if the emplacement of the Coast Range ultramafic sheet can be accurately dated, it may indicate a limit to the maximum age of the San Andreas fault system. G. A. Thompson’s gravity investigations of large ultramafic masses in the northern Coast Ranges of California, in the Cazadero and Red Mountain areas, indicate that these bodies extend only to relatively shallow depths. The geophysical data are compatible with the suggestions of Irwin that these rocks constitute thrust plates resting on the Franciscan or Dothan Formations. Regional gravity anomalies in southwestern Oregon Data from some 2,250 gravity stations in southwestern Oregon have been reduced to simple Bouguer values in a regional study by H. R. Blank, Jr. The Bouguer gravity field in the area between the Oregon coast and the Klamath graben, just east of the Cascade Range, has a total relief of about 210 milligals. An overall east-to-west gradient of about —1 mgal per mile is closely related to an increase in average elevation toward the east, and may therefore be largely attributed to crustal thickening to the east away from the continental margin, under conditions of approximate iso-static equilibrium. Ultramafic rocks and lower Eocene volcanics, which occur along a linear gravity high, may reflect a major north-trending fracture zone in southwestern Oregon that may be an extention of the Powers fault zone, as postulated earlier by P. D. Snave-ly. According to Blank there was no residual positive anomaly associated with Klamath Mountain rocks west of the Powers fault zone in southwestern Oregon. In the Klamath Mountains province, a gravity low is associated with the north-trending belt of sedimentary rocks of the Dothan Formation, and a gravity high with the heterogeneous rocks to the east. Glaucophane schist localized along thrust faults in Coast Range In the northern Coast Ranges, R. D. Brown, Jr., has mapped a gently south-dipping, virtually tabular mass of glaucophane schist more than 8 miles long extending southeastward from Goat Mountain in the southwestern corner of the Stonyford quadrangle. The schist body appears to lie along the southern extension of a folded thrust fault. Other numerous small exotic bodies of glaucophane schist are also found along this and other thrust surfaces. The field evidence thus suggests a close relation between thrusting and the tabular body of glaucophane schist, which parallels the thrust surfaces. Metamorphic facies of Triassic rocks along Oregon border Mapping and petrographic studies by P. E. Hotz in the Condrey Mountain quadrangle, Siskiyou County, Calif., have shown a generally zonal arrangement of metamorphic facies in a regionally metamorphosed ter-rane. Rocks of the Triassic Applegate Group, which are in the greenschist facies, overlie more highly metamorphosed mafic and quartzo-feldspathic rocks, which are in the almandine-amphibolite metamorphic facies. Indications of a progressive increase in the metamorphic grade of rocks of the greenschist facies toward those of a higher grade can be seen, but the increase cannot be positively demonstrated because the two assemblages are separated by a zone of shearing along which a large sill and many small bodies of granitic rock have been emplaced. Rocks of the almandine-amphibolite facies are thrust over a central core of quartz-muscovite and albite-chlorite-epidote schists belonging to the lower part of the greenschist facies. Thrust inferred in northern Coast Ranges, Calif. R. D. Brown (1-64) has interpreted a klippe of volcanic rock covering 50 square miles in Glenn, Colusa, and Lake Counties, Calif., as evidence of a folded thrust fault that can be traced eastward into the Stony Creek fault zone. Rocks involved in the thrusting are of Late Jurassic and Cretaceous age. Sulfide deposits mapped in West Shasta district The geology of the western part of the West Shasta copper-zinc district, Shasta County, Calif., is shown on a new map of the French Gulch quadrangle by J. P. Albers, A. R. Kinkel, Jr., A. A. Drake, and W. P. Irwin (3-64). The eastern part of this map is a reinterpretation by Albers of earlier work by Kinkel and others.47 The quadrangle contains several large sulfide deposits and numerous gold deposits, none of which are being worked at present. Age data of glaucophane schist in California Isotopic age determinations of muscovite from glaucophane schist of the Franciscan Formation near Cazadero, Calif., range from 130 to 150 million years. Donald E. Lee, H. H. Thomas, R. F. Marvin, and R. G. Coleman (1-64) conclude that the 5 K-Ar ages and 1 Rb-Sr age indicate the time of recrystallization of tectonic blocks and bedrock schist during a Late Jurassic and Early Cretaceous metamorphic event. 17 A. R. Kinkel, Jr., W. E. Hall, and J. P. Albers, 1956, Geology and base-metal deposits of West Shasta copper-zinc district, Shasta County, California : U.S. Geol. Survey Prof. Paper 285, 156 p.PACIFIC COAST REGION A113 SOUTHERN CASCADE RANGE AND SIERRA NEVADA OF CALIFORNIA Volcanic history of area north of Lassen Peak Geologic mapping by G. A. Mcdonald (1-63) in the vicinity of Lassen Volcanic National Park has been carried eastward from the Manzanita Lake and Prospect Peak quadrangles through the Harvey Mountain quadrangle, thus adding to the strip extending across the southern end of the Cascade Range into the Great Basin. The rocks delineated are largely volcanics of Pleistocene and Recent age, and include some of the youngest volcanic rocks of the conterminous United States. A series of very late Pliocene (?) andesite and rhyodacite lava flows was folded along nearly east-west axes, and later broken by faults trending nearly northward and northwestward. These flows were subsequently covered by another series of volcanic rocks that range in composition from basalt to dacite. The volcanic activity of the quadrangles mapped, which do not include Lassen Peak, continued into historic time; the most recent eruption was in 1851 at Cinder Cone, northeast of Lassen Peak. Block faulting continued through early Pleistocene, but ceased before late Pleistocene time. Ages of metamorphic rocks of western Sierra Nevada Reconnaissance geologic mapping by L. D. Clark and N. K. Huber in the northern part of the western Sierra Nevada metamorphic belt has resulted in stratigraphic reassignment of large areas of rock that were previously believed to be of Paleozoic' age. Some bodies of limestone that contain late Paleozoic fossils are now recognized as slumped blocks, rather than lenses that formed in situ. The blocks were emplaced by subaqueous mudflows during the Late Jurassic. Similar slumped blocks containing Paleozoic fossils were also mapped farther south within the Jurassic Mariposa Formation in the San Andreas quadrangle by Clark, A. A. Stromquist, and D. B. Tatlock (1-63). The transported fossilifer-ous blocks were previously thought to indicate the true age of the deposits in which they are now situated. Aeromagnetic mapping in Mother Lode belt Analysis of an aeromagnetic survey in the central Mother Lode belt, by J. R. Henderson, A. A. Stromquist, and Anna Jesperson, suggests that most of the major positive magnetic anomalies are associated with ultramafic bodies. Many of these ultramafic bodies in the area are associated with major fault zones, and the trend of at least one, the Melones fault zone, is reflected by a linear belt of magnetic anomalies. An east-west elongate magnetic anomaly in the southwestern part of the Valley Springs quadrangle suggests the existence of a deeply buried ultramafic mass at the east edge of the San Joaquin Valley. This anomaly is of particular interest, as its trend is remarkably different from that correlated with structures exposed in the foothills belt. Geology of central Sierra Nevada summarized P. C. Bateman, L. I). Clark, N. K. Huber, J. G. Moore, and C. L). Rhinehart (1-63) have summarized their geologic findings along a belt across the central part of the Sierra Nevada. Emphasis in the report is on the compound nature of the Sierra Nevada batho-lith and the mode and environment of its emplacement. A geologic map, at a scale of 1:250,000, shows the distribution of individual plutons and adjacent country rock in those areas which have been mapped geologically in some detail. K-Ar and Rb-Sr age studies by R. W. Kistler, P. C. Bateman, and W. W. Brannock (1-64) indicate an age of 85 to 90 million years for the Mount Givens and Lamarck Granodiorites of the batholith. Together with the probably correlative Half Dome Quartz Monzonite, and the younger Cathedral Peak Granite of the Yosemite region, these rocks comprise a northwest-trending central belt along and just west of the Sierra Nevada crest, averaging 20 miles in width and at least 80 miles in length. Older granitic rocks on both sides of this belt yield discordant K-Ar mineral ages that have been irregularly reduced as a result of reheating of the rock at the time of intrusion of the more centrally located younger plutons. K-Ar ages of hornblendes from the Tinemaha Granodiorite, one of the older plutons, range from 150 to 180 million years and indicate that some of the plutons which make up the batholith are at least as old as Jurassic. Isotope ratios of Sierra Nevada granitic rocks Analysis of Sr^-Sr86 and Rb-Sr ratios from whole-rock samples of granitic rocks from many of the same plutons mentioned above suggests an initial Sr^-Sr86 ratio of 0.7075. Bateman, in collaboration with P. M. Hurley and others at the Massachusetts Institute of Technology (1-64), interprets this ratio as indicating that the Sierra Nevada granitic magmas were not direct simple derivatives of the typical mantle-source regions of oceanic basalt (ratio about 0.704), nor were they dominantly formed by fusion of typical marine shales of a period or two earlier age (ratio >0.710). The initial ratio is compatible with the hypothesis that theA114 REGIONAL GEOLOGY granitic magmas were formed by anatexis in a geosyncline containing much volcanic material and some terrigenous sialic detritus. It is also compatible with a magmatic derivation from a very ancient basalt. Metasedimentary rocks of the east flank of the Sierra Nevada In the Mount Morrison quadrangle, C. D. Rinehart and D. C. Ross (1-64) have studied and described a thick section of metamorphosed Paleozoic sedimentary rocks and Mesozoic volcanic rocks that are exposed in a roof pendant on the steep eastern flank of the Sierra Nevada and that together total 50,000 feet in thickness. The metasedimentary sequence, about 32,000 feet thick, is composed chiefly of pelitic and siliceous hornfels in-terbedded with subordinate amounts of calcareous rocks. Fossils indicate that the metasedimentary rocks range in age from Ordovician to Permian(?). Lithologically and faunally the pre-Pennsylvanian strata are transitional between the carbonate and detrital-volcanic assemblages of the Great Basin; the Pennsylvanian to Permian (?) strata contain a much higher proportion of clastic material than the dominantly carbonate assemblages of similar age 50 miles to the southeast. Permian volcanism in eastern Sierra Nevada Five samples from a thick unit of metavolcanic rocks, lying between fossiliferous metasedimentary rocks of Pennsylvanian and Permian (?) age and fossiliferous metavolcanic and metasedimentary rocks of Early Jurassic age, were determined by C. E. Hedge to be of Permian age (230-265 million years) by the Rb-Sr whole-rock dating technique. This metavolcanic unit, which has been mapped in the Ritter Range roof pendant by C. D. Rinehart, N. K. Huber, and R. W. Kistler, is the first evidence of pre-Mesozoic volcanism in the east-central Sierra Nevada. CENTRAL AND SOUTHWESTERN CALIFORNIA Aerial radioactivity survey of central California Compilation of data by K. G. Books from an aerial radioactivity survey in the San Francisco-Central Valley region indicates that the intensity of radioactivity in the area is moderate. It is highest in areas underlain by igneous rocks and has the greatest variation in the Coast Ranges, where rocks of diverse compositions are present. In a large part of the area a low intensity of radioactivity reflects an extensive alluvial cover, much of which has a high water content with a correspondingly strong masking effect. Upper Tertiary sequence of Salinas Valley revised Stratigraphic and paleontologic study of upper Tertiary strata in the southern Salinas Valley, Monterey and San Luis Obispo Counties, Calif., by D. L. Durham and W. O. Addicott, indicates that the upper Miocene Santa Margarita Formation intertongues with the Monterey Shale northward from the south end of the valley. Certain strata in Monterey County, previously assigned to the Santa Margarita Formation, belong instead to a newly defined Pliocene formation. Structural interpretation of Santa Monica Mountains Geologic mapping in the Santa Monica Mountains by R. H. Campbell, R. F. Yerkes, and C. M. Wentworth has resulted in a better understanding of this structurally complex area. The south flank of the Santa Monica Mountains is traversed by the east-west-trending Malibu Coast fault, which forms the boundary be-twTeen the Transverse Ranges province to the north and the Peninsular Ranges province to the south. Structural and stratigraphic evidence indicates that the Malibu Coast fault is chiefly a reverse fault, with the north block relatively upthrown. North of the fault are four major structural elements—three major thrust sheets and an autochthonous block. The superimposed thrust sheets form a sequence of tectonic layers which was subsequently folded, faulted, dilated by the intrusion of mafic igneous rock, and truncated by the Malibu Coast fault. Fossil vertebrates in Barstow Formation From a study of the fossil vertebrates in the Barstow Formation of the Mojave Desert of southern California, G. E. Lewis has concluded (1-64) that: (1) the uppermost third of the formation definitely corresponds to a zone containing a faunal assemblage usually considered to be late Miocene in age; (2) the middle third of the formation may correspond to a zone containing an assemblage usually thought to occupy a middle Miocene stratigraphic position; and (3) the lower third of the formation contains no identified fossils, and is of unknown age but not younger than Middle Miocene. Geologic mapping of San Nicolas Island The geology of San Nicolas Island, the outermost of the Channel Island group, has been described by J. G. Vedder and R. M. Norris (1-63). The stratigraphic section on the island consists of nearly 3,500 feet of folded and faulted sedimentary rocks of Eocene age which are partially concealed by surficial marine terrace deposits and dune sand of late Pleistocene and Recent age. Structurally, the rocks comprise a broad, com-ALASKA A115 plexly faulted anticline whose crest is near the southwest shoreline. The anticline roughly parallels the long dimension of the island and plunges gently southeast. ALASKA Figure 6 is an index map of Alaska showing the boundaries of the regions referred to in the following summary of scientific and economic findings of recenf geologic and geophysical sfudies. NORTHERN ALASKA Mapping in Point Hope area A traverse across the structural saddle between the Lisburne Hills and the nose of the DeLong Mountains by I. L. Tailleur completed preliminary fieldwork in the Point Hope and DeLong Mountains quadrangles of northwestern Alaska. The previously undescribed east flank of the saddle consists of a dark, fine-grained facies of the Mississippian Lisburne Group overlain by a late Paleozoic and early Mesozoic complex of chert, some of which contains oil shale. The middle Cretaceous rocks filling the saddle consist of several different gray-wacke-mudstone assemblages, none of which could be differentiated as a map unit along the traverse. Folding is intense along a northerly to northeasterly grain, but no large-scale faulting was recognized. Tiglukpuk Formation yields Lower Cretaceous fossils Stratigraphic and structural studies by Arthur Grantz and W. W. Patton, Jr., in the Tiglukpuk Creek area and study of new fossil collections by D. L. Jones indicate that the structurally complex Tiglukpuk Formation, previously assigned to Upper Jurassic, is at least in part Lower Cretaceous. The stratigraphic relations of the Tiglukpuk Formation and the possibly Figube 6.—Index map of Alaska, showing boundaries of regions referred to in discussion of Alaskan geology.A116 REGIONAL GEOLOGY correlative Lower Cretaceous Okpikruak Formation have not been determined, pending a restudy of earlier fossil collections and additional fieldwork. New fossil collections from the unnamed sequence of tuffaceous graywacke along Tiglukpuk Creek confirm the Middle Jurassic age of these beds and rule out the possibility that they may overlie the Tiglukpuk Formation, as suggested previously by W. W. Patton and I. L. Tailleur. Triassic rocks of Brooks Range Reconnaissance study of Triassic exposures along the north front of the Brooks Range by N. J. Silberling and W. W. Patton, Jr., demonstrates that the “shale member” of the Shublik Formation, as defined by Patton and I. L. Tailleur in the Killik-Itkillik region, is at least partly a temporal equivalent of the Ivishak Member of the Sadlerochit Formation, which underlies the typical Shublik Formation farther east in the Shavio-vik-Sagavanirktok region. The “shale member” was traced eastward to a point several miles south of Saga-vanirktok Lake and was found to be characterized by a middle Lower Triassic fauna including Euflemingites rormmdwi Tozer, Posidonia mimer Oeberg, and “Pseu-domonotis” boreas Oeberg. This same fauna has been collected by oil company geologists in the upper part of the Ivishak Member about 10 miles north of Sagav-anirktok Lake. As no transition occurs between the lithologically different “shale member” of the Shublik and Ivishak Member of the Sadlerochit, despite the proximity of their correlative outcrops near Sagava-nirktok Lake, they may belong to different structural units that were juxtaposed during deformation of the region. Oil-rich shales found in Nuka-Etivluk Rivers region Samples of oil shale from the Nuka-Etivluk Rivers region in northern Alaska assay 26-146 gallons of oil per ton (Tailleur, 1-64). They were collected from beds as. much as a few feet thick that are associated with beds of varicolored chert in the post-Triassic, pre-Berriasian (Cretaceous) stratigraphic interval. Similar organic shale has been found more than 100 miles to the west and to the east of the region. Too little is yet known about the deposits to judge the importance of the relatively high oil content. WEST-CENTRAL ALASKA Mapping in Kobuk-upper Koyukuk basin Investigations of the Kokub-upper Koyukuk Cretaceous basin, a possible petroleum province, were begun in the Hughes quadrangle by W. W. Patton, Jr., and T. P. Miller. Preliminary mapping indicates that the areal extent of possibly favorable basin sediments in the Hughes quadrangle is more limited than previously thought. Southeast of the Koyukuk River, large areas of the sedimentary rock have been invaded and metamorphosed by granitic intrusives, and in the eastern Lockwood Hills the basin sediments have been stripped off a broad structural high which exposes lower Cretaceous volcanic rocks. The basin sedimentary sequence consists of marine graywacke and mudstone with a narrow band of continental quartzose sandstone and conglomerate along the northern edge of the basin. The sedimentary rocks were found to be complexly folded and faulted nearly everywhere in the basin. Pleistocene history of Bering Strait area Studies of marine sediments in western Alaska by D. S. McCulloch, I). M. Hopkins, and F. S. MacNeil have resulted in the recognition of a record of seven marine transgressions since the beginning of the Pleistocene Epoch. The oldest deposits contain faunas suggestive of relatively warm-water temperatures; many of the species differ significantly from their nearest living relatives. Successively younger faunas of early and middle Pleistocene age become successively more similar to the modem faunas of adjoining waters; the rich fauna contained in the youngest of the middle Pleistocene marine sequences is identical with the modern fauna of adjoining waters. However, late Pleistocene faunas of Sangamon age, though composed mostly or entirely of living forms, contain a few species that now live only in areas farther south, indicating that sea temperatures were warmer during Sangamon time than at present. A comparison between the stratigraphy and faunas of Quaternary marine deposits in Chukotsk Peninsula (U.S.S.R.) and western Alaska indicates that no early Pleistocene marine deposits have yet been found in the Chukotsk area, although deposits representing two early Pleistocene marine transgressions are recognized in Alaska. Each middle and late Quaternary transgression is represented in the Chukotsk area by sediments containing faunas suggesting colder water temperatures than the faunas found in deposits of the same transgression in Alaska; this indicates that the present contrast in water temperatures in coastal waters of the Chukotsk Peninsula and Alaska has existed during each middle and late Pleistocene marine transgression and presumably that current systems in Bering and Chukchi Seas were similar during middle and late Pleistocene times to those at present.ALASKA A117 D. S. McCulloch found evidence on the Baldwin Peninsula for a warm late glacial to early postglacial period. This evidence is (1) a buried discontinuous wood-rich zone in a now treeless area, (2) the habitation by beaver beyond their modem range, and (3) evidence for a period when ice wedges melted. Radiocarbon dates suggest that the warm period started after 11,340±400 years ago and encompassed the interval from 9,020±350 to 7,270±350 years ago. Detailed study by C. L. Sainsbury of the deposits on the York Terrace, a marine platform of the western Seward Peninsula, has yielded information and fossils which lead to the conclusion that the terrace was uplifted to its present height of about 600 feet in post-Yarmouth, pre-Wisconsin time. Because the terrace extends west to the Bering Strait, which has been considered the most likely route of migration of plants and land animals between Siberia and Alaska, Sainsbury regards it as probable that the Bering Strait was a seaway throughout early Pleistocene time until the uplift which raised the terrace, and hence migrations by land were restricted to late Pleistocene time. Laumontitized sedimentary rocks widespread J. M. Hoare, W. H. Condon, and W. W. Patton, Jr., (p. C74-C78) outlined an area of at least 2,000 square miles in western Alaska characterized by laumontitized sedimentary rocks of Cretaceous age Most of the lau-montite is thought to have formed diagenetically through the reaction of water rich in calcium carbonate with tuffaceous material of acid or intermediate composition. SOUTHWESTERN ALASKA Biologic samples indicate ice-free biota refuge on Kodiak Island Analyses by Thor Karlstrom of biologic samples collected on Kodiak Island in 1962 by Drs. Eric Hulten, botanist, and Carl Lindroth, zoologist, of Sweden; Dr. Ball, entomologist, of Canada; and Dr. Rausch, mammal ogist, of Anchorage; have been completed. The biologic results in general support the geologic data of an ice-free area, a potential biota refuge, that persisted on the island during at least the last two major glaciations. The character of the flowering plants, invertebrate fauna, and fish of the island strongly suggest survival of some of these forms during glacial maxima in such an isolated refugium. The evidence of the mosses, lichen, algae, and mammals, however, is not so clear cut, and it is possible that many of these forms migrated to the island in postglacial time. Reconstruction of the refugium from the geologic data indicates a mountainous ice-free area with major valleys largely occupied by proglacial lakes and in all probability characterized by an austere arctic-type climate. In keeping with this reconstruction, the plants and animals that suggest persistence and survival in the refugium are all of arctic type. Ultramafic rocks found on Kodiak Island Four ultramafic bodies were discovered by G. W. Moore on the northwest coast of Kodiak Island during the course of reconnaissance mapping. The bodies occur along a line extending from Middle Cape to Broken Point, and the largest, at Middle Cape, is about 3 miles in diameter. The bodies consist of partly serpentinized dunite, pyroxenite, and banded gabbro. Ultramafic rocks had not previously been known on Kodiak Island, but these bodies are probably an extension of a belt of similar rocks on the Kenai Peninsula. Mining properties at Red Mountain and Flame Point on the Kenai Peninsula have been responsible for all of Alaska’s chromite production. EAST-CENTRAL ALASKA Dating of uplift of Alaska Range Field investigation by Clyde Wahrhaftig, J. A. Wolfe, and E. B. Leopold in the Fairbanks A-3 quadrangle disclosed a tuff bed about 50 feet thick. The tuff was erupted from some unknown but nearby source at the beginning of the time when the south-flowing drainage across the site of the Alaska Range was dammed and diverted by the rising of the mountains that constitute the present Alaska Range. The uplift of the range is recorded in the Nenana Gravel, a 4,000-foot-thick alluvial-fan accumulation, whose constituent pebbles can be traced to sources in the range. Dating the ash will put a lower limit on the rate of deformation of the Alaska Range, as the plant fossils associated with it are regarded by Wolfe as probably early Pliocene in age, and the deposition and subsequent deformation of the Nenana Gravel were completed well before the first of four distinct glacial advances in the Alaska Range. Gravity survey of Yukon Flats Gravity traverses by D. F. Barnes and R. Y. Allen along the upper Yukon, Porcupine, Chandalar, Sheen -jek, and Black Rivers indicate that Bouguer gravity anomalies in the Yukon Flats range from 0 to —30 mil-ligals, with the highest values covering a broad area in the southeastern portion of the flats. This providesA118 REGIONAL GEOLOGY additional evidence that no large sedimentary basin occurs beneath the alluvial cover of the Yukon Flats, although local sedimentary prisms may be indicated in the northern portion of the flats. Cambrian history of Tatonduk-Nation Rivers area Stratigraphically controlled collections of Cambrian fossils from the Tatonduk-Nation Rivers area by A. R. Palmer show that although the Cambrian section is probably less than 1,000 feet thick, most of the Middle and Late Cambrian faunas found in the Cordilleran sections of southern Canada and western conterminous United States are present. Striking facies and thickness changes within a few miles indicate a complicated Cambrian sedimentary history. The Early Cambrian faunas of Alaska include botli material in place and faunas from boulders in a Middle Cambrian conglomerate. The trilobites in some of these faunas include several genera known also from Siberia. No olenellids or other typical Early Cambrian trilobites of the Cordilleran area have been found. Kandik Basin proves smaller than expected Mapping by hi E. Brabb and Michael Churkin indicates that the Kandik Basin, a possible petroleum province, is smaller than originally thought but nevertheless may contain petroleum. Possible oil-bearing structures in this basin have been mapped for the first time. A small amount of bitumen has been found in Paleozoic rocks cropping out at the margins of this basin, suggesting that oil may be trapped at depth. Stratigraphy revised in Livengood and Christian quadrangles Mapping by R. M. Chapman and F. R. Weber in the Livengood quadrangle, northeast of Fairbanks, indicates that two rock units near Wickersham dome, previously mapped as Precambrian Birch Creek Schist and an undifferentiated pre-Middle Ordovician unit, and thought to be separated by a thrust fault, are gradational. The younger unit, including distinctive red and green argillaceous rocks, seems to correlate with similar rocks, described by A. H. Brooks in 1900 as the Nilkoka Group, near the junction of the Tolovana and Tanana Rivers. The differentiation of an as yet unnamed late Middle or early Upper Devonian fossiliferous gray-wacke and shale unit by Weber and Bond Taber in the central part of the quadrangle, and the discovery of extensive unmapped Devonian (?) mafic intrusive rock units by Chapman, Weber, and Taber are also of regional significance. According to W. P. Brosge and H. N. Reiser, the basic igneous rocks that cover a 1200-square-mile area in the Christian quadrangle are not Devonian volcanic rocks as previously thought. The rocks are mostly gabbro and basalt sills with only minor flows. A preliminary radioisotope age determination by M. A. Lanphere shows that the gabbro is probably Jurassic in age. The sills form a structural basin which contains remnants of sedimentary country rocks, some of which are as young as Permian or Triassic according to pollen identification by R. A. Scott. SOUTHERN ALASKA Glaciers active along southern coast since Miocene time An exceptionally long and complete record of Ceno-zoic glaciation is preserved in the Gulf of Alaska Tertiary province along the coast of southern Alaska. Seven sections of this sequence were measured in detail by George Plafker between Middleton Island and Icy Point to supplement earlier reconnaissance investigations by D. J. Miller and others. The fieldwork shows that the sequence, which contains distinctive marine conglomeratic mudstones and sandy mudstones that are interpreted as glacial debris, is at least 16,500 feet in aggregate thickness. Lithologically similar deposits of unconsolidated sandy mud and pebbly mud are now accumulating locally near tidal glaciers in southern Alaska. The fieldwork and studies of the marine mol-luscan faunas by F. S. MacNeil indicate that active tidal glaciers or an ice shelf were present along the coast intermittently during the middle and late Miocene (Astoria), and almost continuously throughout the Pliocene and early to middle Pleistocene. Mollusks of definite Pleistocene age (probably pre-Yarmouth) were identified only in collections on the Middleton Islands, from the upper part of the 3,875-foot-thick section, the top of which is not exposed. Younger deposits of Pleistocene age have not been found in outcrop, but probably are present in the subsurface and offshore on the continental shelf. Mesozoic stratigraphy of Matanuska area A stratigraphic reconnaissance by Arthur Grantz of upper Mesozoic rocks in the Kotsina-Kuskalana area, supplemented by isotopic age data by M. A. Lanphere and study of fossil mollusk collections by D. L. Jones and R. W. Imlay, indicated that the Kotsina Conglomerate is Jurassic (not Cretaceous) and showed that this conglomerate and sedimentary rocks of Late Juras-ALASKA A119 sic (Callovian?) and Early Cretaceous (Hauterivian and Albian) ages are locally present between Kotsina River and Mount Drum. The Hauterivian beds include a nearshore facies to the north which is lithologically very similar to the Nelchina Limestone and to an offshore facies to the south which has not been previously reported from beds of this age in the Matanuska geosyncline. New and revised paleontologic work by D. L. Jones and additional field stratigraphic studies by Arthur Grantz have shown that dissimilar facies in the lower part of the Matanuska Formation (Late Cretaceous) in the southern part of the Nelchina area are closely juxtaposed. The juxtaposition is apparently produced by the presence of abrupt facies changes in the formation. The abrupt facies changes may have been accentuated by a fault or fault system with a significant lateral component of displacement. Tertiary stratigraphy of Cook Inlet region Paleontologic and stratigraphic studies by J. A. Wolfe, D. M. Hopkins, and E. B. Leopold in the Cook Inlet region suggest that the ages of some early Tertiary units will require revision. A threefold zonation of the Kenai Formation has been established on the basis of fossil floras, and the pollen assemblages of each zone have been characterized, permitting refined local correlations which-should assist the active petroleum exploration presently in progress in the Cook Inlet area. The threefold zonation established in the Kenai Formation can be applied to Miocene and Pliocene rocks elsewhere in Alaska, and this assists in making regional correlations and in analyzing the late Tertiary tectonic history of Alaska. The fossil floras obtained from the Kenai Formation and from other parts of Alaska provide a record of deteriorating climate in Alaska and illuminate the evolution of the modem taiga and tundra vegetation from the mixed hardwood forest that clothed Alaska in early Miocene times. Copper ore controls in MacLaren River area The Ivathleen-Margaret (MacLaren River) copper prospect, examined by E. M. MacKevett, Jr. (p. C117-C120) explores north-striking quartz veins north of an east-striking fault zone. Only one of the quartz veins is large enough and rich enough to have encouraged much exploration. This exploration showed that the copper values, which are contained chiefly in chalcopy-rite and bornite, diminish in the vein northward from the intersection between the vein and the fault zone. SOUTHEASTERN ALASKA K—Ar ages indicate probable early Paleozoic intrusive Geochronologic studies in Alaska by M. A. Lanphere and G. D. Eberlein provide the first direct evidence suggesting emplacement of early Paleozoic intrusive granitic rocks along the western margin of the North American continent. K-Ar ages on hornblende concentrates from quartz diorite and from quartz mon-zonite near Bokan Mountain, Prince of Wales Island, are 430 million years and 445 m.y., respectively. Bio-tite from the quartz monzonite gave a lower K-Ar age of 370 m.y. The Bokan Mountain and Tenakee intrusive rocks therefore probably are among those that contributed granitic debris to the middle Paleozoic conglomerate units throughout southeastern Alaska. K—Ar ages of minerals from syenite complex Hornblende from syenite at Tenakee on Chioagof Island gave a K-Ar age of 405 million years, and coexisting hornblende and biotite from the same syenite complex at Point Hayes yielded ages of 230 and 113 m.y., respectively. Abrupt facies changes in Alexander Archipelago area Striking facies changes in Triassic, Permian, Carboniferous, and Devonian sedimentary rocks have been mapped and studied by L. J. P. Muffler for a distance of more than 6 miles across the northwest-trending structural grain in the area between Kuiu and Kuprea-nof Islands. Detailed stratigraphic studies exclude the possibility of appreciable tectonic transport during the period of deformation (late Cretaceous or Paleo-cene) and suggest further that both Triassic and Paleozoic sedimentation took place in troughs parallel to the present structural grain. Two generations of folding at Cape Fanshaw On the mainland northeast of Kupreanof Island, in the vicinity of Cape Fanshaw, two generations of folds were mapped by L. J. P. Muffler. Cleavage related to isoclinal first folds in Jurassic and Cretaceous gray-wacke and argillite is deformed into a steeply plunging second fold of large amplitude. The two inferred episodes of folding are correlated with the first and second episodes of Late Cretaceous or Paleocene folding that occurred in the Pybus-Gambier area on Admiralty Island, 20 miles to the west. 746-002 0 - 64 -9A120 REGIONAL GEOLOGY PUERTO RICO Provisional geologic map A geologic map (Briggs, 1-64) of Puerto Rico and adjacent islands shows that the central core of Puerto Rico consists of Cretaceous and lower Tertiary volcanic and sedimentary rocks cut by hundreds of faults and intruded by serpentine of Cretaceous (?) age and dioritic intrusive rocks of Cretaceous and early Tertiary age. On the northern and southern coasts these older rocks are overlain by several thousand feet of generally calcareous sedimentary rocks that dip gently seaward and by many kinds of surficial deposits mainly of Quaternary age. Deformation along south coast Conglomerate on Isla Caja de Muertos, off the south coast of Puerto Rico, about 10 miles southeast of Ponce, collected by P. H. Mattson contains Eocene larger For-aminifera in pebbles and Oligocene large Foramini-fera in the matrix, according to K. N. Sachs, Jr. The conglomerate is probably correlative with some of the Oligocene strata in the coastal plain of southern Puerto Rico. It dips about 35° SE. and is overlain uncon-formably by subhorizontal limestone also believed to be equivalent to a part of the Oligocene and Miocene coastal-plain sequence. This relation indicates that deformation occurred in this area in Oligocene or possibly Miocene time. Late Cretaceous laumontitization As a part of his study of the general geology of the Coamo area in south-central Puerto Rico, Lynn Glover is investigating the distribution, genesis, and time of formation of zeolite-bearing assemblages in the Upper Cretaceous and lower Tertiary volcaniclastic rocks. At present the zeolites clinoptilolite, stilbite, analcime, and laumontite have been identified. Laumonite is particularly abundant in the higher Upper Cretaceous rocks, where it formed most readily in the permeable plagioclase-rich crystal tuffs of the Cariblanco Formation. In the presence of water and dissolved silica, plagioclase broke down to form albite and laumonite. The reaction occurred after considerable burial because laumontite also fills cracks developed during load crushing of such nonreactive minerals as hornblende. The generation of laumontite-bearing assemblages was a regional phenomenon and in places encroached upon the earlier prehnite and epidote of contact zones around small intrusives. The intrusives have been dated geologically, and this allows some limits to be put on the age of laumontitization. On this basis the laumontite seems to be latest Cretaceous (Maestrichtian) or younger. Gravity survey of south coast basin A detailed gravity survey of a potentially petroliferous Tertiary sedimentary basin on the south coast of Puerto Rico indicated minimum simple Bouguer anomaly values at Punta Cabullon in the Playa de Ponce quadrangle. The gravity gradients indicate that even lower values must exist offshore to the south of this area. These lower values probably indicate the location of the deepest portion of the sedimentary basin. Karst phenomena Lithologic control in the development of karst topography is well illustrated in the geologic map of the Camuy quadrangle by W. H. Monroe (1-63). Deep steep-sided sinks are confined to the outcrop belt of the Aguada Limestone, which consists of alternating beds of hard and soft limestone. Mogotes or steep-sided sub-conical “haystack” hills are restricted to the outcrop belt of the Aymamon Limestone, which consists of nearly pure compact chalk that is dissolved and re-precipitated at the surface into hard dense limestone. Hard ferruginous limestone of the Camuy Formation forms long smooth ridges. Several series of long, narrow, parallel solution trenches have been discovered in north-central Puerto Rico affecting thin-bedded somewhat impure limestone. These trenches, named zanjones (Spanish zanjon= large drainage trench) by W. H. Monroe (p. B126-B129) seem to represent a persistant deepening and widening of joint cracks by action of acidic waters derived largely from decay of forest vegetation. In contrast to zanjones, the slightly similar karren or lapies form only on bare, generally pure limestone and are usually more closely spaced. The somewhat similar cutters of Tennessee form only under soil, whereas zanjones may form under a thin forest litter. ANTARTICA The U.S. Geological Survey is cooperating with the National Science Foundation and its U.S. Antarctic Research Program (USARP) in carrying out continuing geologic studies in Antarctica. Where feasible, reconnaissance geologic mapping is an integral part of the investigations. Topographic and planimetric base maps are compiled by the Topographic Division (see “Mapping in Antarctica”). Logistical support for the Antarctic field projects is provided by the U.S. Navy Operation Deep Freeze.ANTARCTICA A121 Geology of central Pensacola Mountains The Pensacola Mountains (fig. 7) are a 250- by 50-mile north-northeast-trending mountain region comprised of three main mountain groups, along the southeast margin of the Filchner Ice Shelf. Geologic mapping of the central mountain group, the Neptune Range, by D. L. Schmidt, P. L. Williams, W. H. Nelson, and J. R. Ege in the austral summer of 1963-64 has demonstrated a lengthy and complex history of sedimentation, volcanism, igneous intrusion, and deformation probably in early Paleozoic and earlier time. Three major folded sequences, each separated by angular unconformities, in the central and the southern Pensacola Mountains (the latter studied in the 1962-63 field season) have a total stratigraphic thickness of at least, several tens of thousands of feet. The lowest unit, the Patuxent Formation, believed to be of Precambrian age, consists of graywacke and slate, with locally abundant flows of basalt that are in part pillow bearing. Diabase sills and felsitic plugs intrude this unit in a few places. The middle unit consists of bedded limestone, rhyolite flows, shallow-water shale and siltstone, and volcanic sandstone and conglomerate. The rocks ha ve been intruded by hypabyssal sills and irregular crosscutting bodies of rhyolite, and are folded in open sinuous folds with moderately steep to overturned limbs. The lime- 0" Figure 7.—Index map of Antarctica. stone is fossiliferous and the unit is probably of early Paleozoic age. The upper unit consists of orogenic conglomerate, red calcareous sandstone, and conglomerate with clasts of mostly volcanic materials, red quartzose siltstone and sandstone, tan quartzose sandstone, and massive black siltstone containing scattered pebbles and cobbles. These rocks are folded in broad, sinuous folds which locally have steep or slightly overturned limbs. Fossils have not been found in the unit. Stratigraphically above the three sequences of folded rocks are nearly flat-lying quartzose siltstones and sandstones, as well as quartzites, that occur in the southernmost mountain group of the Pensacola Mountains and that appear very similar to the Beacon sedimentary rocks in other parts of the Transantarctic Mountains, according to D. L. Schmidt, A. B. Ford, J. H. Dover, and R. D. Brown (1-63). Devonian and Permian plant remains from carbonaceous interbeds have been identified by J. M. Schopf at the U.S. Geological Survey coal laboratory in Columbus, Ohio. The Permian flora has typical Gondwana characteristics. Diabase sills, probably of Jurassic age, occur in the upper Paleozoic sequence. Pensacola Mountains meteorite find A nickle-iron meteorite, the fourth meteorite yet to be discovered in Antarctica, was found by J. R. Heiser and D. C. Barnett of the Topographic Division in the central part of the Neptune Range (lat 83°15' S., long 55° W.) on February 7, 1964. The meteorite, weighing 2.4 pounds and measuring 4 by 3 by 2 inches, was found on a rock outcrop about 100 feet above the ice base of a nunatak. Evidently, it is a resistite which had been glacially transported. Glaciology of central and southern Pensacola Mountains The mean annual air temperature in the vicinity of the Geological Survey camp (lat 83°36' S., long 57° 15' W.) in the Neptune Range was determined by W. W. Boyd, Jr., to be — 25.8±0.2°C, based on firm temperature measurements in an 11-meter-deep bore hole. Stratigraphic studies and firn density measurements in several pits indicate an average annual accumulation over a 16-year period of 8 centimeters of equivalent water. Almost 80 percent of the yearly accumulation appears to be during winter, and accompanied by very little wind. Four sets of surveyed stake lines in the Neptune Range provided bases for thickness profiles by gravimetry and for accumulation and ice-movement measurements.A122 REGIONAL GEOLOGY In the Patuxent Mountains (lat 84°45' S., long 63° 59' W.), the southernmost one-third of the Pensacola Mountains, movement of local ice ranges between about 7 meters per year in a large central basin to about 15 m per year in a large glacier that enters the central basin from the east. Annual accumulation near the center of the basin ranges from 10 to 12 centimeters of equivalent water. Geology of Thiel Mountains Continued petrographic studies of cordierite-bearing hypersthene-quartz monzonite porphyry point to an origin of the porphyry, according to A. B. Ford (1-63), by the nearly complete melting of preexisting charnock-ite-like rocks such as those found throughout the shield region of East Antarctica. Numerous small lithic inclusions of hypersthene- and cordierite-bearing granu-lites scattered throughout the sill-like body of porphyry may be incompletely melted relicts of parental matter. Large corroded insets of cordierite and hypersthene in the porphyry, according to this interpretation, may be xenocrysts. Similar igneous rocks are not known to exist elsewhere in the Transantarctic Mountains. Stock-like or batholithic granitic bodies intrude the porphyry at several places and may be related to early Paleozoic plutonic activity that was widespread in the Transantarctic Mountains. Age of intrusive rocks of Thiel Mountains A late Precambrian to early Paleozoic time of formation of the igneous rock suites is indicated by radio-metric zircon age studies by T. W. Stem, Harold West-ley, I. H. Barlow, and C. S. Annell; by biotite age studies by H. H. Thomas, R. F. Marvin, Paul Elmore, and Hezekiah Smith; and by potassium feldspar and whole-rock age studies by C. E. Hedge and F. C. Walthall. A lead-alpha zircon age of 670 ±50 million years supports previously reported zircon dates of the quartz monzonite porphyry that average about 600 m.y. Bio- tite-bearing granitic rocks that intrude the porphyry yield mostly early Paleozoic radioactivity ages. Four Iv-Ar biotite ages of the intrusive rocks range from 484 to 511 m.y. Lead-alpha zircon ages of the granitic rocks are somewhat older, ranging from about 470 to 720 m.y. The early Paleozoic ages are in close agreement with most other reported ages of basement rocks elsewhere in the Transantarctic Mountains, according to J. M. Aaron and A. B. Ford (1-64). Geologic reconnaissance of Eights Coast Zircon from a sample of quartz diorite collected by A. A. Drake, Jr., from the Eights Coast region was found by T. W. Stem and H. Westley to have a lead-alpha age of 150± 20 million years. This middle Mesozoic age, according to Drake (Chapter D) confirms the previous thought that the batholithic rocks of Eights Coast and Thurston Island are older than the plutonic rocks of Andean (Cretaceous to early Tertiary) age from the Antarctic Peninsula. Biotite separated from the same sample was found by H. H. Thomas, R. F. Marvin, P. Elmore, and II. Smith to have a K-Ar age of 97± 5 million years. This age may reflect a later orogenic event perhaps associated with younger plutonic rocks that are known to intrude the quartz diorite. The younger rocks are characterized by presence of myrmekite and resemble plutonic rocks of Andean age from the Antarctic Peninsula. The biotite age is in harmony with the suggestion that Andean plutonic activity may have extended to the Eights Coast region. Antarctic paleobotany It is becoming evident, according to J. M. Schopf (1-64), that the dominant glossopterid vegetation in Antarctica w;us arborescent, seasonally deciduous, and native to a temperate climate with favorable conditions for growth.GEOLOGIC AND HYDROLOGIC INVESTIGATIONS IN OTHER COUNTRIES For more than 20 years the U.S. Geological Survey has provided technical assistance to newly developing nations in geology, hydrology, and related sciences, under the auspices of the U.S. Agency for International Development and other national and international agencies. This assistance has been directed toward the appraisal of mineral and water resources and the establishment of cadres of experienced earth scientists in the developing countries. As a result of this coordinated assistance, vigorous national geological and hydrological agencies have been established in Afghanistan, Bolivia, Chile, Indonesia, Iran, Nepal, Pakistan, Philippines, Thailand, and Turkey; earth-science programs have been strengthened in Brazil, Ghana, Jordan, Korea, Liberia, Nigeria, Taiwan, Tunisia, and Sudan, and national geological maps or summary resources reports have been issued in Ecuador, Libya, Peru, and Saudi Arabia. In two decades of technical assistance, the U.S. Geological Survey has sent 485 members of its staff on investigations and training assignments in 68 countries and has provided specialized training in the United States for 731 scientists from 68 nations. At the request of other governments, 124 specialists from the U.S. Geological Survey were assigned to 25 countries during fiscal year 1964, and geologists and engineers were brought to the United States for advanced academic or on-the-job training. The accompanying table (p. A124) summarizes the type of assistance given to each country by the Geological Survey during the year. AFGHANISTAN Surface-water studies in Helmand River basin A compilation of streamflow, meteorologic, and sediment data for the Helmand River basin was released in early 1964. This report, prepared by R. H. Brigham, covers the 10-year period prior to 1960. BRAZIL Mineral deposits in Minas Gerais From 1947 to 1962, field studies were carried on jointly by the Brazilian Departamento Nacional da Produgao Mineral and the U.S. Geological Survey in the Quadrilatero Ferrffero, an area of about 7,000 square kilometers containing exceptionally large reserves of iron ore. This region has already produced mineral products valued at some $D/£ billion and will probably surpass this past production in years to come. During fiscal year 1964, a Geological Survey Professional Paper chapter (Pomerene, 1-64) was issued covering three quadrangles in the north-central part of the Quadrilatero Ferrffero, an area containing estimated reserves of high-grade hematite ore (66 +percent iron) totalling more than 570 million tons and extending to a depth of 50 meters below lowest exposure. The hematite ore bodies are regarded as replacement deposits formed by either hypogene solutions or circulating ground water, without apparent structural control. Three other papers were published in professional journals, including one on caves in canga (ferruginous breccia or conglomerate) found on dolomitic itabirite;48 one on leucophosphite, an ammonium iron phosphate mineral caused by reaction of bat droppings with iron-formation (Simmons, 1-64); and one on the origin of high-grade hematite ore (Dorr, 1-64). Amazon flow measured for first time The first actual measurements of the flow of the Amazon River were made by a U.S. Geological Survey team consisting of R. E. Oltman (1-64), L. C. Davis, F. C. Ames, and G. R. Staeffler, in collaboration with the University of Brazil and the Brazilian Navy. Flow measurements at Obidos (above tidewater), made at high stage in July 1963, and at low stage in November 1963, indicated an average flow of 6.6 million cubic feet per second. Based on these measurements and an analysis of the hydrology of the Amazon basin flow at Obidos, the average outflow of the Amazon to the Atlantic was computed to be about 7.5 million cfs. Previous estimates have generally ranged from 3 to 5 million cfs. A 19-year record of river stage at Obidos together with the flow measurements formed the basis for rough estimates of maximum flow of 8y2 million cfs and minimum 48 G. C. Simmons, 1963, Canga caves of the Quadril&tero Ferrffero, Minas Gerais, Brazil: Nat. Speleological Soc., Bull., v. 25, pt. 2, p. 66-72. A123A124 GEOLOGIC AND HYDROLOGIC INVESTIGATIONS IN OTHER COUNTRIES Technical assistance to other countries 'provided by the U.S. Geological Survey during fiscal year 1964 USDS specialists assigned to other countries Scientists from other countries trained in the United States Country Number Type Type of activity 1 Number Field of training Latin America 2 Geologist _ _ _ A None 4 do A, C, D 2 General geology. 2 Cartographer 2 Economic geology. 1 Topographic engineer . 1 Ground-water hydrology. 4 1 Geochemistry and analytical chemistry. 3 Hydraulic engineer (SW) 2 Stratigraphy and sedimentation. 1 Paleontology. 1 Photogeology. 2 Geologist. A 1 Engineering geology. 1 Ground-water hydrology. 1 Surface-water hydrology. 1 Petrology and mineralogy. 1 Stratigraphy and sedimentation. 1 do A 1 General geology. 1 Photogeology. 2 __do_ _ B None 2 Geophysicist 1 Surface-water hydrology. 1 General geology. i Geologist _ _ C None Africa 2 Surface-water hydrology. 2 Geologist __ _ B None r 3 Hydraulic engineer (GW).. A 2 Ground-water hydrology. 1 Hydrogeologist. .. .. . 1 Quality of water. 1 Publications specialist- 1 Topographic engineer 1 Mathematician. ..... 1 Electronics specialist 1 Hydrochemist 1 Corrosion specialist .. 1 Hydrogeologist _ _ _ __ __ B None 2 Geologist. _ _ _ A 1 Surface-water hydrology. 2 Exploration. 1 Hydrogeologist B 1 Ground-water hydrology. 1 Mining geology. 5 Hydrogeologist A None 2 Hydraulic engineer (SW) None 1 Economic geology. 1 Geophysics. i Hydrogeologist _ B 2 Photogrammetry and surveying. 2 Publications. 1 Administration and supervision. Footnote at end of table.GEOLOGIC AND HYDROLOGIC INVESTIGATIONS IN OTHER COUNTRIES A125 Technical assistance to other countries provided by the U.S. Geological Survey during fiscal year 1964—Continued Country USGS specialists assigned to other countries Scientists from other countries trained in the United States Number Type Type of activity 1 Number Field of training Tunisia i i Hydraulic engineer (GW) Hydrogeologist. _ B Great Britain None Surface-water hydrology. Near East-South Asia Afghanistan 2 Hydraulic engineer (SW) Ceylon India.. None None Iran Iraq 1 Hydraulic engineer (SW) A None Israel . Jordan 1 Hydrogeochemist 1 Hydrogeologist... B None Nepal Pakistan Saudi Arabia Syria... Turkey. 1 1 15 1 1 2 2 1 1 1 1 1 5 1 8 2 2 1 1 1 1 2 None 3 1 1 1 1 Hydraulic engineer (SW)_ B .. A . _ Geophysicist. _ ___ Geochemist. Photogrammetrist Cartographer Electronics specialist Publications specialist _ A Driller . . ... Program assistant _ _ Hydrogeologist Corrosion specialist _ _ _ Geologist Geochemist Geophysicist. - Chemist .. Geodesist Photogrammetrist, Topographic engineer Program assistant Geologist C Photographer. Hydrogeologist-_ Geophysicist. _ _ Hydraulic engineer (GW) 3 Ground-water hydrology. 1 Surface-water hydrology. 1 Photogrammetry and surveying. 1 Economic geology 3 Do. 1 Engineering geology. 1 General geology. 1 Geochemistry and analytical chemistry. 1 Ground-water hydrology. 2 Do. 1 Surface-water hydrology. 2 Exploration. 1 Surface-water hydrology. 1 2 5 3 2 1 2 General geology. Economic geology. Ground-water geology. Petrology and mineralogy. Geochemistry and analytical chemistry. Paleontology. Administration and supervision. 1 Administrative and supervision. 1 Ground-water hydrology. 1 Engineering geology. 6 Ground-water hydrology. 1 Geophysics. 1 Photogrammetry and surveying. 4 Administration and supervision.A126 GEOLOGIC AND HYDROLOGIC INVESTIGATIONS IN OTHER COUNTRIES Technical, assistance to other countries provided by the U.S. Geological Survey during fiscal year 1964—Continued Country USGS specialists assigned to other countries Scientists from other countries trained in the United States Number Type Type of activity 1 Number Field of training Far East Indonesia Japan_____ Korea_____ Philippines Republic of China___ Thailand____________ Viet Nam____________ 2 Geologist B- None None 2 Geologist. A None 4 1 Geologist Driller... A, B 2 1 1 1 1 1 1 1 1 General geology. Petrology and mineralogy. Geochemistry and analytical chemistry. Geophysics. Stratigraphy and sedimentation. Marine geology. Mining geology. Exploration. Publications. 2 2 2 2 1 1 Geochemistry and analytical chemistry. Ground-water hydrology. Engineering geology. Ground-water hydrology. Quality of water. Petroleum geology. 1 Ground-water hydrology. 2 1 Ground-water hydrology. Geochemistry and analytical chemistry. 1 Hydrogeologist. B i A, Broad program of advisory help in institutional development and direct help in resources appraisal. B, Limited program of advisory help, training, and investiga-tion in selected fields. C, Advisory help or consultation, with specific training or investigational activity. D, Geological education; assistance to universities. flow of 2yz million cfs at Obidos. Even the minimum flow exceded the greatest known flood of the Mississippi, and the maximum was more than 3 times that of the Mississippi. CHILE Ground-water investigations Hydrologic investigations in collaboration with the Institute de Investigaciones Geologicas have pointed out new sources of ground water in water-short areas at the opposite ends of Chile. In northernmost Chile, W. W. Doyel (1-64) reports that an artesian aquifer underlying the coastal terrace along the Chile-Peru border offers good possibilities for additional water supply for the port city of Arica. In Tierra del Fuego in southernmost Chile, Doyel and Octavio Castillo U. (p. B169-B172) report that oil-test wells drilled in the early 1950’s indicate that water suitable for industrial and domestic use occurs in two artesian aquifers of Tertiary age which underlie a large part of the Isla Grande de Tierra del Fuego. Exploration of this artesian water will help alleviate a shortage which is handicapping further economic development of the area. COLOMBIA Mineral exploration program A new program to explore and appraise mineral resources, and to help strengthen the National Geological Service (NGS) in the Ministry of Mines and Petroleum, was started in March 1964 under the auspices of the Government of Colombia and the U.S. Agency for International Development. COSTA RICA Study of volcanic activity and related problems The current eruption of Irazu volcano northeast of San Jose, Costa Rica, which began in March 1963, has resulted in loss of life, ash accumulations over an area of more than 1,200 square miles, and damage to land, communications, and water supply. At the request of the U.S. Agency for International Development and the Government of Costa Rica, preliminary examinations of the volcano were made by K. J. Murata in September 1963 and J. P. Eaton in January 1964. In April 1964, a longer range geological and geophysical study was started to determine the characteristics of recent volcanism, to evaluate the geological conditions that constitute immediate hazards, including potential land-GEOLOGIC AND HYDROLOGIC INVESTIGATIONS IN OTHER COUNTRIES A127 slides and mudflows, and to recommend measures, to minimize the effects of future eruptions. As part of this study, a survey of heat radiation in the area around Irazu volcano was made by R. M. Moxham and S. J. Gawarecki in cooperation with the Institute of Science and Technology, University of Michigan. Other phases of the study will include mapping of surficial deposits and geological structures in and near the volcanic belt, installation of three seismic stations to monitor earthquake activity, and establishment of leveling stations on the side of the volcano to check ground movements. Information resulting from these activities is expected to provide data needed for urban protection and redevelopment as well as a better understanding of the eruptive habit of volcanoes in the circum-Pacific volcanic belt. INDONESIA Engineering geology in Tjimanuk River basin Reed Anderson of the U.S. Geological Survey and personnel of the Indonesian Geological Survey are studying the Tjimanuk River basin in West Java to develop a master plan for irrigation, flood control, hydroelectric power, and conservation. Good dam sites are scarce along the Tjimanuk River because of: (1) the youthful stage of erosion, with resulting steep, narrow stream canyons in the region of Pleistocene and recent volcanic deposits along its upper reaches; and (2) subdued topography in the region underlain by Miocene and Pliocene sediments along the lower course of the river. The entire basin is seismically unstable, and active faults are common. One potential dam site investigated but subsequently rejected was found to be cut by 6 faults, no less than 4 of which appeared to have been active since 1955. Investigations have centered on the site for Sakarwangi Dam, which is tentatively planned as a rock-fill structure about 120 meters high, resting on Pleistocene volcanic breccia and tuff, with a storage capacity of approximately 650 million cubic meters. Geologic map As part of its assistance to the Government of Indonesia, the U.S. Geological Survey is printing a new geological map of Indonesia, which has been compiled by the Indonesian Geological Survey from all available sources. The map will serve as a reference in exploration and development of the nation’s resources and as a basis for planning more detailed mapping of the country. KOREA Ground-water reconnaissance W. W. Doyel and R. J. Dingman (chapter D), reporting on a ground-water reconnaissance of the Republic of Korea, conclude that large additional supplies of ground water, now virtually untapped, can be developed from alluvial fill in river valleys and from coastal deposits. Such development will be required to meet the demands of population increase and industrialization ; the use of wells for supplemental irrigation will reduce damage to the rice crop from recurring droughts. LIBYA Geologic map A new geological map of Libya compiled by L. C. Conant and G. H. Goudarzi (1-64) was officially presented to the Government of Libya on March 3, 1964, in ceremonies at the Ministry of Industry in Tripoli. Prepared under the auspices of the U.S. Agency for International Development and the Kingdom of Libya, with the cooperation of the Petroleum Commission and Petroleum Exploration Society of Libya, the map is at a scale of 1:2,000,000. It shows 46 sedimentary and igneous rock units representing all geologic periods except the Permian. In the south and west it reveals broad outcrops of Mesozoic rocks and narrow belts of Paleozoic rocks, separated by alluvial basins and deformed by southwest-trending folds and faults. In the north, Tertiary and Quaternary units are cut by subparallel northwest-trending faults, many of which have been active during the Quaternary. PAKISTAN Geologic map An important objective of the Mineral Exploration and Development Program conducted jointly by the U.S. Geological Survey and the Geological Survey of Pakistan, under the auspices of the U.S. Agency for International Development and the Government of Pakistan, is to compile small-scale geologic, tectonic, and mineral-resources maps that will aid in the exploration and development of Pakistan’s natural resources. The first of these maps, a new geological map of Pakistan at a scale of 1:2,000,000, has been compiled and is now being prepared under the direction of R. O. Jackson, J. T. Heare, and A. J. Freda for printing by the Survey of Pakistan press in Rawal-A128 GEOLOGIC AND HYDROLOGIC INVESTIGATIONS IN OTHER COUNTRIES pindi. An important by-product of this joint activity has been the compilation of a geographic base, the first available at this scale. The various segments of reproduction copy are being prepared jointly by the Geological Survey of Pakistan in Quetta and the U.S. Geological Survey in Washington. Chromite studies, Hindubagh district Concentric circular fractures observed on aerial photographs of the ultramafic intrusive at Hindubagh, West Pakistan, are being intensively studied by Roger Van Vloten, who believes that the structures may have been caused by upward-thrusting serpentine masses piercing the overlying dunite. Specific-gravity determinations of a large number of samples reveal that the centers of the structures consist of serpentine of low density. Gravimetric studies of one of these structures by geophysicists of the Geological Survey of Pakistan, under the guidance of W. J. Dempsey, show a positive anomaly of 2 milligals, suggesting a mass of chromite near the surface. Paleozoic reef discovery in West Pakistan Fossiliferous limestone mapped by K. W. Stauffer and personnel of the Geological Survey of Pakistan has been identified by Curt Teichert as a relief belt comprising the first Paleozoic reef facies discovered in Pakistan or India. The belt contains a number of reefs 300 feet thick, or more, which crop out along a narrow easttrending ridge rising as much as 250 feet above the surrounding plain, about iy2 miles north of Nowshera and about 25 miles east of Peshawar in the northern part of West Pakistan (lat 34° N., long 72° E.). The reef limestone contains tabular and spheroidal stromatopo-roids, tabulate corals, rugose corals, brachiopods, gastropods, and large cephalopods. The age of the reef limestone is either Silurian or Devonian. Reef biotas of these two periods have many genera in common. All genera identified so far range through both periods or longer. The rugose coral, Mucophyllum, according to W. A. Oliver, Jr., is most characteristic of Silurian strata, although its range extends into the Lower and, possibly, Middle Devonian. Fossil assemblages from some other limestones less than 30 miles away seem to be correlative with those of the Nowshera reef, especially those of the Kali limestone, which is found in the Mardan district and has reef characteristics. Previously some of these limestones had been assigned to the Precambrian; all others had been considered to be Carboniferous and Permian. The presence of reefs associated with porous dolomite and fetid black limestones may be significant in the exploration for oil. Structural studies in Hazara district Geological mapping in the Hazara district of northern Pakistan by T. W. Offield, J. A. Calkins, and members of the Geological Survey of Pakistan has yielded detailed structural information for the large part of the apical area and western limb of the famous 180° “syntaxial bend” near the western end of the Himalayas. Analysis of the structural geometry by Offield indicates that this bend was formed by large-scale southward extension of rock masses on either side of an axial zone in which such movement was impeded. Folds were initially formed parallel with the principal direction of movement and were succeeded in a later phase by folds of a different type oriented perpendicular to the movement. Evidence presently available indicates that the horseshoe configuration of the “syntaxial bend” was produced by differential extension (flow) during a single orogenic event rather than by flexing of a line of preexistent structures. Sor Range—Daghari coal field A mapping and training program of the Geological Survey of Pakistan carried on between 1956 and 1963 under the guidance of J. A. Reinemund resulted in detailed mapping of Pakistan’s most productive coal field, the Sor Range-Daghari field. The coal crops out in the mountains near Quetta for a distance of nearly 20 miles. Geological maps on a scale of 1: 6,000 have already been supplied to many coal-mine operators for use in planning mine development; the maps provided guidance for driving two long adits that reached coal early in 1964 and are scheduled for production of 2,000 long tons per day. Total coal reserves in all categories in the Sor Range-Daghari field have been estimated at about 50 million long tons, about half of it presently classed as recoverable. The geological studies in this field have revealed a significant unconformity within the Eocene coal-bearing formation and a divergence between the trends of deformation in Quaternary strata and in older rocks. Water-logging and salinity control in Punjab region Currently a U.S. Geological Survey hydrologic team headed by M. J. Mundorff is evaluating the effectiveness of tubewell networks in two large salinity-control and reclamation projects located in Rechna and Chaj Doabs of the Punjab region. Since 1961, large-scale pumpingGEOLOGIC AND HYDROLOGIC INVESTIGATIONS IN OTHER COUNTRIES A129 from these wells has already lowered the water table an average of about 4 feet in the project areas. The lowering of the water table will enable large blocks of land, now out of production, to be reclaimed for agriculture. PERU Plans for central geological service At the request of the Government of Peru and the U.S. Agency for International Development, G. E. Erickson studied the problems and requirements for establishing a central geological service in Peru. His report recommends establishing a geological agency with about 80 employees to undertake a national mapping and resources-appraisal program under a 10-year assistance plan. SAUDI ARABIA Mineral exploration project started Under an agreement with the Kingdom of Saudi Arabia signed in September 1963, the U.S. Geological Survey has begun geological mapping and appraisal of mineral-resources possibilities in central and western Saudi Arabia. Sixteen members of the Survey, under the supervision of Glen Brown, have started geological, geophysical, geochemical, and topographical surveys, and are providing assistance to the Ministry of Petroleum and Mineral Resources in establishing facilities for geological and topographical work. Geochronology and photogrammetry laboratories are under construction in Jidda to support the surveys. Known mineral showings are to be evaluated with the help of geophysical exploration and drilling. Guidelines for future exploration are to be developed through the mapping of approximately 315,000 square miles in the Arabian shield. Geologic maps issued Twenty-one geological maps of Saudi Arabia on a scale of 1: 500,000 prepared by the U.S. Geological Survey and the Arabian American Oil Co. under the aus- pices of the Ministry of Petroleum and Mineral Resources have now been issued, nine within the past year (R. A. Bramkamp, 1 to 4-63; G. F. Brown, 1 to 3-63; and L. F. Ramirez, 1,2-63). In addition, separate geological and geographical maps of the entire country on a scale of 1:2,000,000 have also been published. THAILAND Mesozoic rocks of northeastern Thailand A report compiled by D. E. Ward for publication by the Royal Thai Department of Mineral Resources describes the stratigraphy of the Khorat Group in northeastern Thailand. These Mesozoic sedimentary rocks are nonmarine and are more than 12,000 feet in aggregate thickness; thick but lenticular beds of rock salt and gypsum are present in two areas in the uppermost formation of the group. Mineral exploration in northeastern Thailand C. T. Pierson, H. S. Jacobson, and personnel of the Royal Thai Department of Mineral Resources are systematically investigating mineral showings in northeastern Thailand under the auspices of the United Nations Special Fund and the Governor of Thailand. Geological, geophysical, and geochemical surveys have revealed the presence of four previously unreported iron deposits, and drilling programs have been scheduled for two promising iron deposits and one base-metal deposit. Geologic map of Phuket Island completed C. L. Hummel, U.S. Geological Survey technical advisor, and Prachuab Phawandon’ of the Royal Department of Mineral Resources have completed a map on a scale of 1:50,000 of the geology and mineral deposits of Phuket Island, South Thailand, and of adjacent parts of the mainland to the north. The map, in two sheets, Northern and Southern Phuket Island, is extensively annotated. Siltstones and shales of Cambrian age, making up the Phuket Series, are in part metamorphosed to mica schist along a northward-striking central belt. Granitic intrusives of Cretaceous age form the most widespread bedrock.INVESTIGATIONS OF PRINCIPLES AND PROCESSES A substantial part of the Geological Survey research program is primarily topical and involves the application of principles and analytical techniques largely developed in the laboratory to the elucidation of the evolution, composition, and structure of: (1) the earth as a whole, (2) its rocks and minerals, (3) its constituent elements, (4) its waters, and (5) its past and present living forms. The emphasis is upon quantitative measurements as a means of obtaining basic data having genetic significance. For the past several years the scope of the topical studies has been broadened to include investigations of the moon and of materials of extra terrestrial origin under sponsorship of the National Aeronautics and Space Agency. The program of topical studies is, by its nature, long term, but it has produced important current benefits. For example, the program has played an integral part in setting up and operating a nationwide nuclear blast and earthquake detection system, together with the eruption warning system for the island of Hawaii. Studies of the stability relations and isotopic compositions of minerals have given insight into the ore-forming processes and have provided new guides for finding ore. Many new analytical techniques and methods of wide application, with the Geological Survey and without, have been developed in the fields of wet chemistry, emission spectroscopy, mineralogy, X-ray spectrometry, and the electron microprobe. Analytical services in these fields and in the fields of paleontology and geochronology are provided for the Geological Survey as a whole. PALEONTOLOGY The activities of Geological Survey paleontologists are divided between applied paleontology, a service summarized in numerous administrative reports on fossils submitted for examination by Survey and other geologists, and paleontologic research involving biostrati-graphic, taxonomic, and ecologic studies. In more specific terms, paleontologic objectives can be grouped under four headings: (1) restudy of classic stratigraphic areas, (2) biostratigraphy, (3) evolution of major plant and animal groups, and (4) biologic oceanography and paleoecology. CLASSIC AREAS Much of the biostratigraphic framework on which general geologic and paleontologic conclusions depend was established 50-150 years ago. Many of the basic data have not been reviewed critically in the light of incurred knowledge of the present generation of geologists. Recent advances in paleontologic, stratigraphic and sedimentologic techniques require a reexamination of the fundamental framework. Studies are initiated as the opportunities arise. Bryozoans and brachiopods in the Upper Ordovician of the Cincinnati region In conjunction with the cooperative mapping program of the Kentucky Geological Survey and the U.S. Geological Survey, a restudy of the standard Upper Ordovician sequence in the Cincinnati region, Ohio, is underway. Among the early results of this program, bryozoan and brachiopod distributions have proven most useful. Preliminary studies of bryozoans from the Maysville area by O. L. Karklins indicate that two faunal breaks occur in beds of Maysville age and older. One is approximately the Eden-Maysville boundary, and the other is about at the top of the Fairview equivalent. In addition, Karklins’ bryozoan studies have enabled him to subdivide the Ordovician and Silurian genus Pachydictya into three parts, on the basis of microstructure. These differences, contrary to published reports of homogeneous microstructure, may lead to stratigraphically useful groupings of species. Statistical studies by R. J. Ross, Jr., of the Late Ordovician brachiopod Platystrophia ponderosa from beds of Maysville age in northern Kentucky indicate a consistent shape difference between two closely related forms that occur in beds previously assigned to the “Bellevue” and the “Mt. Auburn.” Perhaps a stratigraphically useful split in this widely distributed species will be documented as more data are accumulated and analysed. Silicified fossils from 29 samples collected by R. C. Greene and R. B. Neuman in the Valley View and adjacent quadrangles, Kentucky, have added significantly to our knowledge of brachiopods and other fossils in the Ordovician of Kentucky. Neuman’s studies A131A132 INVESTIGATIONS OF PRINCIPLES AND PROCESSES indicate that some genera are found in formations where they had not hitherto been known to occur, and that some newly differentiated species and genera of silicified brachiopods prove to be excellent guide fossils to several of the formations distinguished for mapping purposes. Differences in wall structure of Bryozoa From an investigation of the cryptostome Bryozoa fauna from the Decorah Shale at several localities in Minnesota, O. L. Karklins concluded that (1) study of the internal structure in Stictopora and Pachydictya species has resulted in a new interpretation of the wall structure which appears to be very promising in grouping of species and genera in the family Rhinidictyidae, and (2) a few species of Stictopora and Pachydictya, and probably the genus Egcharopora, can be used for an improved zonation of the formation. On the basis of a new interpretation of the dark lines crossing the exozone in thin sections showing the longitudinal and transverse views, it is concluded that the so-called inner walls are not formed in genus Stictopora. After reinterpreting the internal structure in genus Pachydictya, it is also concluded that genus Pachydictya consists of three, and possibly four, species groups whose geographic and stratigraphic distribution is not known at the present time. Ostracodes in the Silurian and Devonian of central New York More than twelve genera of ostracodes have been found by Jean Berdan iirthe Onondaga Limestone of central New York. Several of these have not previously been reported in beds older than Hamilton, and others have not been found in beds younger than the Camden Chert. Favulella is the only genus that appears to be restricted to the Onondaga and its equivalents. Although ostracodes have been described from the Onondaga equivalents in Pennsylvania, only five genera have been reported from the type Onondaga of New York. Drepanellina clarki has been identified by Jean Berdan in collections from the Herkimer Sandstone near Utica, N.Y., made by D. H. Zenger, Pomona College. The Silurian D. clarki zone of Maryland has been correlated by Ulrich and others with the Rochester Shale of New York. Until now, however, no specimens of Drepanellina had been reported from New York State. Because the Herkimer Sandstone is the eastern equiva- lent of the Rochester Shale, according to Gillette,4’ the correlations of earlier workers are borne out. Criteria for defining correlatives of the standard Missis-sippian series in the West As a result of detailed studies in several areas, Mackenzie Gordon, Jr., Helen Duncan, W. J. Sando, and J. T. Dutro, Jr., have agreed on criteria for recognizing approximate correlatives of the standard Mississippian series in the West. The Kinderhook-Osage boundary is considered to be the base of the Homalophyllites-V esiculophyllvm coral zone (base of Sando’s zone Ci), and the Meramec-Chester boundary is placed at the top of the Faberophyllum zone. The Osage-Meramec boundary is generally marked by the appearance of fasciculate lithostrotionoid corals (base of Sando’s zone D). The top of the Mississippian is characterized by a change is brachiopod assemblages with Diaphragmm below and Rugoclostus above. Mississippian brachiopods in the Great Basin Study of Mississippian productoid brachiopods of the eastern part of the Great Basin (in Utah) by Mackenzie Gordon, Jr. (1-64), has resulted in the recognition of 10 distinct assemblages in time sequential order. Over 60 Mississippian species are recognized; approximately 20 percent of these have been described previously. The productoid brachiopod zones have been correlated in part with the goniatite zones studied earlier by Gordon and the coral zones studied by Helen Duncan. It is now possible to recognize in the Great Basin, with close approximation, the provincial series (Kinderhook, Osage, Meramec, and Chester) of the American midcontinent. Goniatites in fhe Hale Formation in Arkansas Mackenzie Gordon studied Carboniferous fossils at the Geological Survey of Great Britain and discussed stratigraphy with British colleagues. These discussions and a comparison of cephalopod specimens have shown that the early ReticvZoceras zone (Ri) goniatites, long unrecognized in the United States, do occur in northern Arkansas in the Hale Formation, where four species can be referred to ReticvZoceras. However, nothing in the Arkansas section appears to represent the discoidal late Reticuloceras (R2) zone species. In the Bloyd Shale, which should be of R2 age, there are species of the genus Gastrioceras, unrecorded in 49 Tracey Gillette, 1947, The Clinton of western and central New York : New York State Mus. Bull. 341, 191 p.PALEONTOLOGY A133 the British Ii2 zone, but represented in Brittany by as yet undescribed species. The fauna of the Hale Formation occurs in the upper part of the Cane Hill Member and locally in the basal several feet of the Prairie Grove Member. The new Arkansas fauna, found in Washington County, contains elements representative of the lowermost part of the lower Reticuloceras (R,) zone in the British Carboniferous section. Goniatites related to lower Reticuloceras (Rx) zone species likewise occur in the upper part of the Hale Formation. The Homoceras zone, as yet unidentified in the United States, may be represented by the lower part of the Cane Hill Member that has yielded no cephalopods. The Hale Formation thus appears to be equivalent stratigraphically to at least the upper part of the Sabden Group and Kinderscout Grit group of the Midland or Central region of England. Mammalian faunal zones at Big Bone Lick State Park, Ky. A team of eleven paleontologists, geologists, and field assistants representing the University of Nebraska, the U.S. Geological Survey, and the William Behringer Memorial Museum has completed the second season of a 4-year project of excavating late Pleistocene mammals at Big Bone Lick State Park, Ky. Large excavations have been dug in 2 of the 3 terraces at the site, and 3 faunal zones have been delineated, as follows: Zone A: Deposited since the coming of the white man, as indicated by the presence of the European pig, Sus scrofa. Also contains Canis sp., Bison bison, Bos taurus, Odecoileus virginianus, and Equus caballus. Zone B: Apparently represents a period before the coming of the white man, but still within the Christian era, as shown by the discovery of an ornamental pendant ascribed to the Adena Indian culture, dating from 1,500 to 2,000 years ago. Bones of the modern buffalo, Bison bison, are very abundant. Also present are musk ox, elk, deer, and, probably reworked from older beds, bones of elephants, giant bison (B. antiquus), and extinct horse (Equus complicatus). Zone C: Contains an extinct late Pleistocene fauna, dated by the C1* method as 10,600±250 years before present. It includes Mylodon sp. (ground sloth), Mam-mut americanus (mastodon), Bison antiquus, Cervalces scotti (extinct “stag-moose”), Rangifer sp. (caribou), Equus complicatus, and Mammuthus primigenius (woolly mammoth). Most of these bones were found in a rust-colored iron-rich layer that probably is an old soil zone. A climatic contrast is presented by the woolly mammoth (cold climate) and the ground sloth (relatively warm climate), which were found at about the same level in the excavation and only about 20 feet apart. It appears that the woolly mammoth remains were buried in a stream channel cut into the deposit in which the ground sloth was found. BIOSTRATIGRAPHY Parts of the United States have had only the most general biostratigraphic reconnaissance. These areas offer a challenge to carry out pioneering stratigraphic and biologic studies that involve large-scale collecting programs, with localities carefully documented in terms of structural and stratigraphic position. Detailed descriptions of these fossils provide valuable new information on regional correlations, age relations, and geologic history. Siberian and North American faunas in the Cambrian of Alaska Two early Cambrian faunas from the Cambrian section in Alaska west of the point at which the Yukon River crosses the Canadian border are being studied by A. R. Palmer. One, from the lowest limestone member of early Cambrian age, includes trijobites entirely of Siberian aspect. The other, from an Early or early Middle Cambrian boulder in the conglomerate above the shale-sandstone section that includes the limestone, contains trilobites typical of the North American province. Middle Cambrian assemblages, including elements known in both the Asiatic and American provinces, will prove very useful for problems of regional correlation. Upper Cambrian assemblages are yet to be studied in detail. Early Middle Devonian corals from east-central Alaska are reported by W. A. Oliver, Jr., to be related to previously described faunas from the Urals and adjacent parts of the U.S.S.R. The collections from the Charlie River quadrangle, submitted by Earl Brabb and Michael Churkin, contain species of Spongo-phyllum, Xystriphyllum, ‘£ Fas ciphyl lum,’ ’ and uPachy-favosites” that are conspecific or closely similar to Russian species. Middle Pennsylvanian beds in northeastern Alaska Recognition of Pseudogastrioceras (Phaneroceras) by Mackenzie Gordon, Jr., from a collection made by H. N. Reiser in the Table Mountain region in the eastern part of the Brooks Range, establishes firmly forA134 INVESTIGATIONS OF PRINCIPLES AND PROCESSES the first time in northeastern Alaska the presence of beds of Middle Pennsylvanian (Atokan) age. Also recognized for the first time in Alaska is the discoidal nautiloid Phacoceras of Late Mississippian age, from specimens collected by I. L. Tailleur near the head of the Kukpuk River in the western part of the Brooks Range, Alaska. Atlantic and Pacific trilobite faunas reflect “mirrored” environments Silicified trilobites collected by R. J. Ross, Jr., and L. A. Wilson, in company with Jim McAllister, from the Orthidiella zone of the Pogonip Group in the Ryan quadrangle, California, are very similar to trilobites reported by H. B. Whittington from Lower Head, Newfoundland. The Newfoundland assemblage comes from a 200- X 600-foot “boulder” of white limestone. In a comparable stratigraphic position in southwestern Nevada are large white limestone bioherms described by Ross and Cornwall.50 These occurrences add to growing evidence of a remarkable mirroring of environments on opposite sides of the continent in early Paleozoic time. Upper Paleozoic corals of the Western States W. J. Sando has completed a restudy of the type specimens of upper Paleozoic coral species described in the various reports of the Federal geological surveys of the Western United States made in the last century. The study is a necessary prerequisite for description of the rich western upper Paleozoic coral faunas, which are in dire need of investigation for purposes of stratigraphic correlation and paleoecologic analysis. The classification of the corals has changed so profoundly in the last 100 years that only 1 of the 12 species considered retains the same generic name under which it was originally described. Six of the species are retained as useful taxonomic concepts. Of the remaining six, one is considered as a junior subjective synonym, three are regarded as nomina dubia, and two are rejected as a nomina oblita. Middle Triassic ostracodes from North America Triassic fossils are of interest because the beginning of the Triassic marks the extinction of a great number of organisms on the generic and higher level at the end of the Paleozoic Era and is the first record in the Mesozoic Era. Recently, I. G. Sohn found marine Middle Triassic ostracodes in Israel. As a result of his 50 R. J. Ross, Jr„ and H. R. Cornwall, 1961, Bioherms In the upper part ot the Pogonip In southern Nevada, in D.S. Geol. Survey Prof. Paper 424-B, p. B231-B233. preliminary note, he received a collection from Nevada containing the first identified Middle Triassic marine ostracodes from North America. In order to obtain comparative material from Europe, Sohn collected from Triassic sedimentary rocks in northeastern France and found there also hitherto unrecorded Middle Triassic ostracodes. Preliminary results of this study (chapter D) suggest that several of the ostracode genera considered to have become extinct at the end of the Paleozoic have species of Triassic age. Upper Triassic ammonites from Oregon Several successive upper Karnian and lower Norian (middle Upper Triassic) ammonite faunas have been identified by N. J. Silberling in collections submitted by Bruce Nolf from the northern Wallowa Mountains in northeastern Oregon. Nolf’s field studies of the Wallowa batholith wallrocks are under the supervision of W. H. Taubeneck at Oregon State University. Of particular significance is the occurrence of the lower Norian Mojsisovicsites, Malayites, and Himavatites faunas which relate to the faunal sequence recognized in northeastern British Columbia. NewOligocene Foraminifera from Guam Ruth Todd’s study of rich and well-preserved fauna of smaller Foraminifera from the Mahlac Member of the Alutom Formation of Guam shows the fauna to be unlike any so far known from the Pacific islands. It can be correlated, by means of its good assemblage of planktonic Foraminifera, with the Globigerina sellii zone of early Oligocene age in East Africa. In addition, many identical species (both planktonic and ben-thonic) indicate that it can be correlated approximately with the Vicksburg of the southeastern United States. Cool-water molluscan fauna noted in North Carolina The first occurrence of a Miocene, Calvert-type molluscan fauna south of northern Virginia is reported by T. G. Gibson. The fossils were collected from the Lee Creek phosphate pit of the Texas Gulf Sulphur Co. near Aurora, N.C., 110 feet below ground level; the fossiliferous bed does not crop out at. the surface. This find establishes a Miocene cool-water fauna south of the Cape Hatteras axis, the present barrier between cool and subtropical faunas. Smaller Foraminifera of Georgia Investigations by S. M. Herrick (1-64) of smaller Foraminifera occurring in surface and subsurface de-PALEONTOLOGY A135 posits of coastal Georgia show that these fossils are of late Miocene age and are equivalent to similar microfaunas previously reported from the Duplin Formation of Florida and the Carolinas. Except for single species belonging to the genera Archaias and Sorites, occurring in the lower Miocene of Georgia (Tampa equivalent), these Foraminifera constitute the only microfossils so far reported from the Miocene deposits of Georgia. Smaller Foraminifera occurring in the large oyster bed at Griffin Landing, Ga., are late Eocene in age and are definitely equivalent to the microfauna occurring at Shell Bluff, Ga., according to Herrick (p. C64-C65). These findings show the two faunas to be equivalent, and the Shell Bluff microfauna to be of late Eocene age. Range of oreodonts extended south to Panama Continued study of Miocene mammals of Panama by F. C. Whitmore, Jr., has established that, in addition to deerlike traguloids and rhinoceros, the fauna includes oreodonts. These primitive ruminants, the most numerous members of the population of the High Plains of North America from Oligocene to Piocene time, had not previously been known south of the Big Bend country of Texas. The range of these animals is thus extended southward about 2,000 miles. The Panama oreo-dont is a member of the subfamily Merycochoerinae and probably a member of the genus Brachycrus, a Miocene form. Information now available on the Panama fauna and compilation of information concerning other finds of early Miocene mammals in North and South America make it possible to locate with greater accuracy than before the strait that once separated the continents. The strait ran north-south in what is now western Colombia, and probably coincided with the Bolivar geosyncline. The entire Isthmus of Panama was attached to North America during at least part of the Tertiary Period, although, being a tectonically active area, it could have been at times broken up into a chain of islands. There is no evidence that the isthmus was attached to South America at any time between the Pale-ocene and the middle Pliocene. EVOLUTION Biostratigraphy, geochronology, and stratigraphic correlation are only as good as our understanding of the. geologic histories of. fossil groups. The more we learn about the evolution of major groups as a function of time, the more reasonable and accurate a picture we can paint of the changing geologic landscapes. Restudy of rugose coral Billingsastraea In North America, the compound rugose coral Billingsastraea ranges from late Early Devonian (middle Coblenzian) to latest Middle Devonian (late Givetian); it is not known, definitely, outside of North America, although it may occur in Europe and Australia. W. A. Oliver’s (3-64) recent paper indicates that the genus is composed of astraeioid, thamnostraeioid, and aphroid corals with disphyllid structure. The oldest known species, B. affinis, is redescribed. Ancestry of primitive molluscoid fossils Ellis Yochelson’s research in primitive molluscoid fossils suggests that the poorly known Upper Cambrian genus Matthevia Walcott may be the representative of an extinct class of mollusks related to, but distinct from, the Amphineura or chitons. Redefinition of pelecypod family Ambonychiidae xV detailed comparative morphological study of the early Paleozoic pelecypod family Ambonychiidae was carried out by John Pojeta, Jr. North American genera of the family are redefined and their known stratigraphic ranges are tabulated. In addition, the phylogenetic relations of the family are considered and their biostratigraphic significance analysed. Study of evolution of brachiopod genus Composita Development of the brachiopod genus Composite/, through geologic times from Late Devonian through Permian is the subject of a paper by R. S. Grinnel, Jr., Lamont Geological Observatory, and George W. Andrews (1-64). Forty-two species and varieties were accepted for the study; 9 others were considered doubtful ; and 18 wrere rejected as obsolete. Morphologic intergradation among associated, synchronous forms was analysed with the aid of frequency polygons. Lack of clear separation of the associated species indicated their dominant intergradation. These forms, previously described qualitatively, are considered typological species. Environment of Foraminifera family similar in U.S.S.R. and United States Representatives of the subfamily Tournayellinae Dain, 1953, calcareous Foraminifera first described in the U.S.S.R., have been found recently by B. A. Skipp (1-64) in Kinderhook, Osage, and Meramec rocks of North America. They are associated with endothyrid Foraminifera and are common and zonally distinctive in most Cordilleran faunas studied, but are rare in the midcontinent region. No Tournayellinae have been recovered so far from Devonian or Chester rocks in the 746-002 0 - 64 - 10A136 INVESTIGATIONS OF PRINCIPLES AND PROCESSES United States, although they are common in the Devonian of the U.S.S.R. The remarkable similarity between the tournayellid and endothyrid faunas of Mississip-pian age in the Cordilleran region and those of early Carboniferous age of the Urals suggests coeval development and like environments, possibly connecting sea ways. Septaglomospiranella Lipina, 1955, is found in the Red wall Limestone, Arizona; the Leadville Limestone, Colorado; the Madison Limestone, Wyoming; the Shun-da and Pekisko Formations, Alberta; and the Gilmore City Limestone, Iowa. Septabrunsiina Lipina, 1955, is recognized in the Redwall and Madison Limestones, and in the Livingstone and Mount Head Formations, Alberta. Toumayella Dain, 1953, and Septatoumayella Lipina, 1955, are common in (1) the Redwall Limestone, (2) beds formerly assigned to the Brazer Limestone in southeastern Idaho and northern Utah, (3) parts of the White Knob Limestone of Idaho, and (4) the Mount Head Formation, Alberta. They are rare in the Arroyo Penasco Formation, New Mexico, and the Salem Limestone, Indiana. Illustrated guide to upper Paleozoic floral zones of United States C. B. Read and S. J. Mamay provided for the first time an illustrated guide to the upper Paleozoic floral zones of the United States. They recognize 14 floral zones extending from the Early Mississippian into the Permian. This report includes photographs of key assemblages for each zone, as well as discussions of floral provinces and correlations. Utility of the report is enhanced by an annotated glossary, compiled by Grace Keroher, of all the stratigraphic terms used in the text. New data cast doubt on age of conodonts in the Cam-eroons John Huddle reports that abundant conodonts in a well-dated Triassic collection made by I. G. Sohn at Makhtesh Ramon, Israel, are the same as those reported from the Cretaceous Mungo Chalk of the Oameroons, Africa. This find casts some doubt on the age of the Cameroons occurrences, which are the only recorded Cretaceous conodonts, and suggests that they might be reworked from older strata. Evolution of two Upper Cretaceous mollusks A study of the geologic history of the Upper Cretaceous cephalopod Haresiceras, by W. A. Cobban (1-64), outlines the phylogenetic development of the genus and suggests its origin. The older species of Haresiceras are stouter than the younger species and have less complex sutures. The older species have constrictions on the early juvenile whorls, arched to nearly flat venters, and ribbing differentiated into primaries and secondaries on the adult body chamber; later species lack constrictions, possess flat to slightly concave venters, and have ribbing tending to be of uniform strength on the adult body chamber. The older species of Haresiceras have suture pattern and rib type in common with Des-moscaphites and Clioscaphites. Cobban believes the origin of Haresiceras is to be found in the Santonian scaphites of the western interior. W. A. Cobban’s investigation of the Late Cretaceous marine pelecypod Inoceramus ? fibrosus (Meek and Hayden) revealed that this “species” consists of an early form with weak radial and concentric folds, a later form (typical form) in which radial folds dominate over the concentric ones, a still later form in which radial and concentric sculpture is of about equal strength, and a final form in which the concentric sculpture dominates. These phylogenetic changes aid in correlating the uppermost part of the Pierre Shale with equivalent strata farther west. Classification, evolution, and geologic use of shrews Study of the fossil and living shrews of the world has been undertaken by C. A. Repenning in order to establish systematic groups within the family and to discover the phylogenetic history of these groups. Review of the shrews has shown that four subfamilies (two extinct) are clearly recognizable and that one of these can be broken further into three tribes. Rate and direction of evolution have varied greatly within these groups. Also, the shrews appear to be highly endemic mammals not only geographically limited in both fossil and living species but also tending to remain so throughout appreciable spans of their evolutionary histories. Therefore, their usefulness in stratigraphic correlation varies greatly with the particular lineage represented and with the detail of the known provincial history in any particular area. Nevertheless, with due respect for these qualifications, the shrews are useful in correlation on a continental scale and, to a more limited extent, are of value in intercontinental correlation of Oligocene and more recent terrestrial rocks. Areal and stratigraphic range of Desmostylians « Desmostylians, marine mammals that inhabited the nearshore areas of the North Pacific Ocean during the later Tertiary, have been studied by W. D. Mitchell withPALEONTOLOGY A137 C. A. Repenning (2-63). The most common genus, Des-mostylus, has been considered an index fossil for the middle Miocene “Temblor Stage” in the California area but actually has a range from the late Oligocene to the late Miocene, as this age is used with Pacific coast marine rocks. The genus has been found in association with primitive Hipparion and Pliohippus horses con-sidered to be early Pliocene in North American usage of terrestrial mammalian ages. Desmostylus is circum-North Pacific and is known from California, Oregon, Washington, Kamchatka, Sakhalin, and Japan. The related genus Paleoparadoxia is also circum-North Pacific and ranges in age from early to late Miocene (but also is associated with fossil horses, which are evidence of early Pliocene age in terrestrial mammalian usage). The rare genus Comwallius is known only from the early Miocene and from the eastern side of the North Pacific. Sirenians, introduced into the North Pacific from the Caribbean area, are first known from the late Miocene (but again associated with horses generally considered to be of early Pliocene age and are found with desmo-stylian remains (both Desmostylus and Poleopara-doxia). Unlike the desmostylians, the sirenians did not become extinct before the end of the Miocene, but have inhabited the North Pacific area until Recent time. The sequence of events and the presumed ecologic similarity suggests a causal relationship between the introduction of sirenians to the North Pacific and the extinction of the native desmostylians. BIOLOGIC OCEANOGRAPHY AND PALEOECOLOGY To better understand fossil assemblages in terms of inferred environments and, thereby, to reconstruct land and sea distributions during past epochs, wTe must examine present day interrelations between organisms and their environments. The findings below bear on the general subject of paleogeographic reconstructions. Use of diatoms in correlation and paleoecology Many areas of both California and the Great Basin contain diatom-bearing sediments which range in age from Late Cretaceous to Recent, according to K. E. Lohman. The diatom assemblages in these rocks contain both short-ranging species that are useful for stratigraphic correlation, and others, still represented in living assemblages elsewhere, that are useful for paleo-ecologic interpretations. Distinctive diatom assemblages are known from the Moreno Shale of Late Cre- taceous and Paleocene( ?) age and from many sedimentary formations in Eocene, Oligocene, Miocene, Pliocene, and Pleistocene rocks in California from the San Francisco Bay area southward. These assemblages from rocks of Cretaceous through Miocene age are virtually all marine. Pliocene rocks in different localities contain either marine or nonmarine diatom assemblages. Pleistocene assemblages are dominantly nonmarine. Extensive areas of Miocene, Pliocene, and Pleistocene sediments in Nevada and other parts of the Great Basin also contain distinctive nonmarine diatom assemblages. In that region, diatoms are often the only fossils present. Here also, the diatom can provide much needed paleoecological information, as the Ceno-zoic lake basins varied greatly in depth, temperature, salinity, pH, and other factors of paleoecological importance. Ranges of certain early Tertiary plant genera extended A number of petrified fruits and seeds, relatively uncommon plant fossils, were collected by R. A. Scott from a locality near Lander, Wyo. This occurrence was discovered by Richard Keefer and David Love. The fossils, of early Tertiary age, include several genera in common with the London Clay flora of England and the Clamo flora of Oregon. The Wyoming discovery establishes a wider and earlier distribution for certain paleotropical plant genera in North America than has previously been known. Large Mesozoic oyster shows unusual distribution N. F. Sohl, of the Geological Survey, and E. G. Kauffman, of the U.S. National Museum, have completed a report on two species of large oysters from the Gulf Coast and Caribbean area. One of these is the largest known ostreid from the Mesozoic of North America; the other (Arctostrea aguilarae) is the largest known species of its genus and shows an unusual distribution that transcends the boundaries between the Caribbean and the Gulf Coastal Plain faunal province of the Upper Cretaceous. It is found in Alabama, Mississippi, Texas, Mexico, and Cuba. Nonmarine snails from the islands of the open Pacific H. S. Ladd has identified two fresh-water snails (Gyraulus and Neritilia?) from the Lower Miocene of Bikini and a third genus (Melanoides) from the Neogene of Viti Levu, Fiji. Except for a single river snail (Theodoxus), previously described from Fiji by Ladd, these are the first nonmarine fossils from the islands of the open Pacific.A138 INVESTIGATIONS OF PRINCIPLES AND PROCESSES First definite nonmarine lower Paleozoic ostracodes in North America Fresh- and brackish-water ostracodes provided by J. W. Wells and studied by Jean Berdan from Middle and Upper Devonian localities in New York State are believed to be the first definitely nonmarine lower Paleozoic ostracodes found in North America. Cenozoic marine paleoecology of Pacific coast Studies of marine mollusks, by W. O. Addicott, are helping to unravel the marine paleoecology of the Pacific coast during the late Cenozoic, and are providing correlation aids for strata containing such mollusks. A systematic review of the gastropod genus Nassarius indicates that fossil species of this genus, a characteristic element of late Cenozoic molluscan faunas of the Pacific coast, are particularly useful in stratigraphic correlation of marine Tertiary and Quaternary formations. The intricate sculpture of the nassariids permits an unusual refinement in the recognition of species, many of which have a relatively restricted stratigraphic range. The genus first appears in strata of early Miocene age in California, and by middle Miocene had diversified into three subgeneric groups that have continued into Recent time as the principal nas-sariid subgenera in the northeastern Pacific Ocean. A previously unrecorded late Pleistocene invertebrate assemblage from near Point Dume, western Los Angeles County, Calif., contains a small element of warm-water mollusks that are now restricted to latitudes far to the south. Addicott notes that these species represent the most northerly occurrence of subtropical taxa in upper Pleistocene deposits of the Pacific Coast. Addicott’s work has also shown that a large and varied invertebrate fauna from the Kern River area, California, may well provide a standard of reference for the correlation of middle Miocene marine strata of the Pacific coast. In what is probably the largest known Miocene molluscan fauna from the Pacific coast, there are approximately 175 species of gastropods, about one-third of which are new and undescribed. Many of these species are closely related to modem gastropods living in the Panamic molluscan province of the tropical eastern Pacific Ocean. MARINE GEOLOGY AND HYDROLOGY Regional studies of the Atlantic continental shelf and adjacent coastal and marine areas are continuing (Emery and Schlee, 1-63), but emphasis is shifting from synthesis of existing information to collection and analyses of new data and mapping of offshore areas. ATLANTIC CONTINENTAL SHELF AND SLOPE Topography of the sea floor The Geological Survey is collaborating with the Woods Hole Oceanographic Institution and the U.S. Bureau of Commercial Fisheries Woods Hole Laboratory in a 5-year reconnaissance investigation of the Atlantic continental shelf and slope, under the direction of K. O. Emery of the Institution. To provide a base map for these investigations, Elazar Uchupi of the Institution has contoured the shelf and slope at a scale of 1:1,000,000, with contour intervals of 20 meters on the shelf and 200 meters on the slope, using data from the U.S. Coast and Geodetic Survey, the Canadian Hydro-graphic Service, and the Woods Hole Oceanographic Institution. Richard Pratt, also of the Institution, has completed preparation of a bathymetric chart of adjacent deep sea areas at a scale of 1:5,000,000. These charts will be published by the Geological Survey. Studies by Elezar Uchupi of the topography, subsurface structure, surficial sediments, and associated organic materials on the northern part of the shelf provide much new information about the development and history of the shelf. Topographically the area can be divided into seven distinct provinces: (1) Nova Scotia continental shelf—a series of basins and flat-topped banks; (2) Bay of Fundy—a shallow trough between Nova Scotia and New Brunswick; (3) Gulf of Maine— a rectangular basin with hummocky topography; (4) Georges Bank—a large shoal with northwest-southeasttrending sand ridges to the southeast of the Gulf of Maine; (5) Nantucket Shoals—a series of northeast-southwest-trending sand ridges on the shelf; (6) Continental shelf from Massachusetts to Delaware—a broad gently sloping plane with broad low swells that trend roughly east-west, lying south of New England; and (7) continental slope—a gently sloping plane cut by numerous jagged steep-walled submarine canyons. Composition of the bottom sediments J. C. Hathaway (1-63),‘ Jobst Hiilseman,51 J. S. Schlee (3-63), and J. V. A. Trumbull (1-63) have found that variations in the composition and texture of bottom sediments can be related in large part to their 51 Jobst Hiilsemann, 1964, Organic constituents: Woods Hole Oceanog. Inst. Summary of Inv. Conducted 1963, ref. 64-12, Chemistry-geology, p. 90-92.MARINE GEOLOGY AND HYDROLOGY A139 topographic setting and origins. For example, in the Gulf of Maine, currents sweeping elevated banks have produced deposits that have a relatively high content of quartz, feldspar, and rock fragments; sand fractions are characterized by poor sorting. In contrast, basins and swales generally have greater amounts of chlorite, mica, and biogenic contributions of foraminifers and spicules. Content of organic carbon, carbonate, and aminoid nitrogen is generally low in the Gulf; the organic carbon and aminoid nitrogen tend to be concentrated with the finer sediments of low areas, and the carbonate is concentrated where tests of foraminifers are common in basins or where relict shell debris is abundant on banks. In general, relict glacial sediments of the Gulf of Maine have wide distribution of grain sizes and are poorly sorted when compared to better sorting of typical sediments on the open shelf where reworking has winnowed the fine debris. Much of the sand as far south as New Jersey is probably relict and was deposited during lowered sea levels of the Pleistocene. Trumbull has found that the relict nature of the grains and lowered sea levels are indicated by a high percentage of iron-stained grains, an abundance of rock fragments near the shelf break, and patchy coarsening of the sand near the outer part of the shelf. Isolated concentrations of glauconite on the suggest local erosion of exposed Tertiary rocks. Foraminifera ratios as indicators of environment On the basis of analyses of more than 500 samples from the Gulf of Maine, Georges Bank, and the Cape Cod area, T. G. Gibson has been able to demonstrate distinct differences in formaniferal faunas of areas to the north and south of the Cape Cod-Georges Bank area. The fauna to the north has a subarctic origin and is related to fauna of Labrador and Greenland. The fauna to the south is temperate or subtropical in character, depending on the area’s proximity to the Gulf Stream. Both benthonic and planktonic Foraminifera show the provincial distribution, although some southern Gulf Stream planktonic forms are dispersed into the Gulf of Maine. Within both faunal provinces, the Foraminifera have well-defined depth zonation. In general, the abundance of tests per gram of sample and the proportions of planktonic forms increase with increasing distance from shore in areas of uniform shelf conditions. In the Gulf of Maine where the topography is irregular and currents are variable, the proportions of benthonic to planktonic forms cannot be used to determine depth or distance from shore. Structure of the Bay of Fundy interpreted from sonic profiles Sonic profiling suggests to ElazarUchupi (1-64) that (1) the Bay of Fundy is underlain by Triassic strata folded into a gentle syncline which has a thin cover of Pleistocene and post-Pleistocene deposits, (2) the Gulf of Maine is underlain by a Paleozoic (?) basement complex beneath Mesozoic to Recent sediments and glacial deposits averaging slightly less than 200 meters in thickness, and (3) Georges Bank is underlain by a thick sequence of Mesozoic and Cenozoic strata which dip very gently seaward and are covered by a thin blanket of Pleistocene sediments. Profiles of the open shelf and slope south of Martha’s Vineyard show prograding upward and outward of the sediment layers. Recovery of skeletal materials from plankton samples During the spring of 1963, K. N. Sachs, Jr., of the Geological Survey, and Richard Cifelli, of the U.S. National Museum, took part in oceanographic investigations aboard the Woods Hole Oceanographic Institution research ship Chain. In attempting to recover radiolarians and Foraminifera from plankton samples, Sachs and Cifelli have developed a new technique for removal of soft-bodied phytoplanktons and zooplanktons which would otherwise either obscure or hopelessly entangle the tests and prevent their extraction. In the new technique, the sample is first washed with a hot 10-percent solution of hydrogen peroxide to remove as much protoplasm as possible. The resulting residue is filtered and washed with the aid of a Buchner funnel. The filter paper containing the residue is then dried, placed in a crucible, and heated in a furnace at 500°C until all cellulose and chitin have been volatilized, which generally takes about 2 hours. The technique leaves a concentrate of tests including radiolarians, foraminifers, pteropods, diatoms and other calcareous and siliceous shells and skeletal material. Examination of the delicate radiolarians and foraminiferal tests shows no appreciable damage to the tests and spines when compared with comparable material from untreated samples. Whale bones indicate northward extent of Miocene Elazar Uchupi, of the Woods Hole Oceanographic Institution, secured a collection of fragmentary fossil whale bones dredged by a fisherman in 50 to 70 meters of water on Georges Bank, off the Massachusetts coast. Included were a few fragments of cetotheres, primitive* whalebone whales of the Miocene, which have beenA140 INVESTIGATIONS OF PRINCIPLES AND PROCESSES found on Martha’s Vineyard Island and in the Chesapeake Group of Maryland and Virginia, as well as in the Miocene beds of Europe. This indicates that Miocene beds, probably a nearshore facies, extended north of Cape Cod, according to F. C. Whitmore, Jr. GEOLOGIC STUDIES ON GUAM Mariana Limestone contains ancient reef facies The uplifted Mariana Limestone that forms the north half of the island of Guam contains facies of an ancient reef complex of Pliocene and Pleistocene age according to J. I. Tracey, Jr., S. O. Schlanger, J. T. Stark, D. B. Doan, and H. G. May. Coral and algae limestone of a reef facies near the present cliff-lined coast surrounds finer grained molluscan, coral, and foraminiferal limestone of lagoonal facies, and is bordered by outwarddipping detrital limestone of the outer slopes, similar to patterns of distribution found on living reefs. S. O. Schlanger recognizes diagnostic differences within thin sections of samples from the major facies of the reef complex; and he shows that comparable Miocene facies, .preserved only in scattered outcrops, and Eocene facies, preserved only as fragments in pyroclastic deposits, existed and can be distinguished on Guam. Algae in the Cenozoic limestones of Guam J. H. Johnson (1-64) reports that he has found 82 species of calcareous algae belonging to 16 genera in the Cenozoic limestones of Guam. Of these, 1 genus and 20 species are new. Mineral composition of lateritic soils as related to bedrock In a study of the mineralogy of the lateritic soils of Guam, Dorothy Carroll and J. C. Hathaway (2-63) report (1) that the principal soil type on volcanic rocks contains halloysite, goethite, and a little gibbsite; (2) that soil on very pure limestone contains gibbsite, hematite, and a little halloysite; and (3) that soil on argillaceous limestone contains halloysite, goethite, and a little gibbsite. Lateritic soil on volcanic rocks has not been found higher than the inferred former extent of the Alifan Limestone of Miocene and Pliocene age, nor lower than the shoreline of the later Mariana sea, according to Tracey and others. Apparently the period of erosion following emergence of the Alifan Limestone during deposition of the Mariana Limestone was a time of lateritic weathering. ESTUARY STUDY IN MARYLAND Biologic study of the Patuxent River estuary R. L. Cory has obtained records on the attachment organisms of the Patuxent River, which flows into Chesapeake Bay, for about iy2 years. At six sampling stations between Lower Marlboro and Solomons, Md., production of organic carbon varies considerably seasonally as well as from station to station. The period of greatest production extended from the beginning of May until the end of September. Highest values for this period were obtained at Lower Marlboro (672 grams per square meter), with continuously decreasing values downstream to Solomons (251 grams per square meter). Salinities at Lower Marlboro averaged about 6 parts per thousand, whereas average salinities at the Solomons station were about 18 ppt. More than 80 percent of the organic carbon obtained at Lower Marlboro formed during August and September and was attributable exclusively to barnacles and tube-building amphipods. The downstream stations exhibited a much larger variety of organisms and a longer period of sustained yield. The purpose of these studies is to monitor ecological changes that are anticipated with the introduction of heated water into the estuary. The quality of attachment also varied considerably and usually consisted of only 1 or 2 dominant species from any 1-month period. Generally the following succession was noted at each of the stations: tube building amphibods, barnacles, bryozoans, tube worms, hy-droids, sea squirts, and bryozoans and barnacles. ASTROGEOLOGIC STUDIES The Geological Survey is continuing its investigations in support of the space exploration program for the National Aeronautics and Space Administration. Basic investigations are being undertaken in four major fields: (1) Lunar geologic mapping by means of visual photographic and photometric studies with telescopes; (2) field and laboratory studies of terrestrial and experimental impact and cratering phenomena; (3) study of extraterrestrial materials of possible lunar origin; and (4) engineering studies designed to aid in conducting space missions. LUNAR GEOLOGIC MAPPING Geologic mapping of the earthward face of the Moon at a scale of 1:1,00,00 constitutes a major part of the Geological Survey’s program. To date, mapping ofASTROGEOLOGIC STUDIES A141 more than 1 million square miles of the 3-million-square-mile area of the lunar equatorial belt has been completed. Geologic maps of the Kepler and Letronne quadrangles have been published in color, and preliminary geologic maps of the Copernicus, the Apennine Mountains (now called Montes Apenninus), the Aristarchus, the Timocharis, the Riphaeus, the Hevelius, and the Mare Humorum quadrangles have been completed and will be published in the Survey’s quadrangle map series. Lunar stratigraphy Geologic mapping of the areas away from the central part of the Moon has led to the redefinition of the Pro-cellarian System, represented by mare and dome material, as the Procellarum Group, a rock-stratigraphic unit, within the Archimedian Series of the Imbrian System. The Procellarum Group now consists of two fundamental units, the mare material and the dome material. This change was made necessary by recognition that complex time relations may exist between the Archimedian craters and mare material. As more geologic mapping on superior lunar photographs is completed, the lunar stratigraphic sections are being revised as new units are recognized and their extent and characteristics determined. D. E. Wilhelms has recognized complex stratigraphy extending into the pre-Imbrian in his preliminary study of the Taruntius quadrangle. Of unusual interest is the material of the Palus Somni which is smooth but has higher albedo than mare material of the Procellarum Group and is partly ringed with groups of small craters along its margins. In addition, in the Procellarum Group there appear to be at least two mappable types of mare material, one type being characterized by a distinct waviness of the mare surface. On the nonwavy mare material, domes are probably more abundant than in any quadrangle studied so far. The majority of the domes have summit craters, but one has a small hill at its summit instead. Many craters on the maria seem to be alined, and there are also a number of rimless craters; Wilhelms suggests that many of these craters are of volcanic origin. R. E. Eggleton 52 and H. J. Moore 52 found during study of the Riphaeus and Aristarchus quadrangles that the material interpreted to be ejecta, derived from the Imbrium Basin during its excavation, is widespread and has been designated the Fra Mauro Formation in 52 U.S. Geological Survey, 1964, Astrogeologic studies annual progress report, August 25, 1962 to July 1, 1963 : Part A. the Apennian Series of Imbrian age. Another widespread’ unit which rests on the Fra Mauro Formation on the southern margin of the Imbrium Basin in the Montes Apenninus quadrangle has been designated the Appenine Bench Formation by R. J. Hackman. E. C. Morris has traced the distribution of the Apennian Series in the western half of the Julius Caesar quadrangle. He finds that the Apennian Series has partly filled in the southeastern portion of the pre-Imbrian crater Julius Caesar more than the northwestern part, a relation that is interpreted to be the result of deposition of the Apennian Series from low-angle ballistic trajectories originating within the Imbrium Basin. Beneath the Appennian Series there may also be a deposit of material derived from the region of Mare Serenitatis which partly fills the southern portion of Julius Caesar more than the northern. The combined result is a depositional floor sloping slightly west of north. Some of the oldest rock units were found by D. P. Elston53 during mapping of the Colombo quadrangle. The oldest unit crops out in an arc of low hills of subdued relief peripheral to the northeast part of the Nectaris Basin and is informally named the Pyrenees Formation. It is interpreted to be the remnants of a regional blanket of material around the Nectaris Basin. The next younger unit comprises a distinctive group of crater deposits, characterized by the crater Gutenberg. The plan outline of this class of craters commonly is markedly polygonal, and crater floor material consists of jumbled blocks and slivers. The next younger deposit consists of a blanket of material that forms a plateau and highlands area in the northern part of the Colombo quadrangle. This material, informally named the Censorinus Formation, overlies, wholly or in part, several Gutenberg-type craters whose forms are still distinguishable through the blanket. The Censorinus Formation is interpreted to be part of a regional blanket of material derived from an event that occurred to the north. The youngest unit in the quadrangle forms a patchy veneer of smooth material on the Censorinus Formation, and may be equivalent to other smooth materials of regional extent found peripheral to the Serenitatis and Imbrium Basins. New stratigraphic units of Imbrian-pre-Imbrian age were recognized by S. R. Titley 54 during study of the Humorum quadrangle. These are the Humorum Group composed of a rim and a bench unit and the Gas- 53 See footnote 52. 64 See footnote 52.A142 INVESTIGATIONS OF PRINCIPLES AND PROCESSES sendi Group representing the class of craters later than the Humorum but flooded by mare material of the Procellarum Group of Imbrian age. The units of the Humorum Group are abundant peripheral to the Humorum Basin, a feature 300 kilometers in diameter. Mapping of the Hevelius and Grimaldi quadrangles by J. F. McCauley 55 has led to investigation of the regional stratigraphic relations around Mare Orientale, a basin 320 kilometers in diameter, in the extreme west-central part of the visible lunar disk. Two new rock stratigraphic units of Archimedian age have been recognized in the region: (1) the Cordillera Group comprises the regional blanket that thins radially from the basin and contains two types of craters, and (2) the Cruger Group represents a class of post-Cordillera craters filled by mare material. Both units have proved useful in deciphering the structures and stratigraphy of the Hevelius quadrangle in the western part of the Moon. Geologic mapping of the Timocharis quadrangle by M. H. Carr56 has led to the recognition of features suggesting that an erosional process has occurred on the lunar surface. Study of the numerous secondary craters derived from formation of the Copernicus and Eratosthenes craters has shown that the Copernicus secondary craters have distinct and commonly cuspate outlines, and the Eratosthenes secondaries of equivalent size have indistinct, noncuspate outlines, rounded rim crests, and are less deep. Because Eratosthenes is demonstrably older than Copernicus, the Eratosthenes secondaries are thought to be a degraded form of Copernicus secondaries. Similar differences are found between the Rima La Hire I and Rim a La Hire II craters. Rima La Hire II has a distinct outline and steep walls, whereas Rima La Hire I is indistinct, has rounded walls, and is very shallow. Hence, Rima La Hire I is thought to be an older degraded rill. TERRESTRIAL AND EXPERIMENTAL IMPACT AND CRATERING PHENOMENA Study of the structure, stratigraphy, and mineral composition of the lithologic units in and around natural and manmade terrestrial craters develops data that aid in determining the origin of such features and their relation to similar lunar features. The Geological Survey program of crater investigations is aimed at acquiring this information. 65 See footnote 52, p. A141. M See footnote 52, p. A141. Stability and separation of impact polymorphs of Si02 B. J. Skinner and J. J. Fahey57 have investigated the inversion rate of stishovite from Meteor Crater, Ariz., a very dense form of Si02 in sixfold coordination, which inverts to silica glass in fourfold coordination. The inversion rate, determined at ten temperatures between 300 °C and 800°C and extrapolated to the time for total inversion of stishovite to silica glass, indicates the virtual impossibility that stishovite can be formed and preserved at the surface of the earth by any mechanism other than meteorite impact. Coesite and stishovite, the high-pressure polymorphs of silica, were recovered by J. J. Fahey58 from the shocked Coconino Sandstone at Meteor Crater by repeated treatments using hydrofluoric acid. The recovery of stishovite is quantitative because it is not attacked by hot concentrated hydrofluoric acid. Coesite is atacked by hydrofluoric acid, but much less readily than is quartz, and can be obtained by repeatedly leaching the host material with a 5-percent solution of hydrofluoric acid at 25 °C. Colloidal and suspensoidal particles of coesite can then be separated from the residual quartz by repeated shaking and decantation in water. TERRESTRIAL CRATERS AND STRUCTURES Structure of the Sierra Madera west Texas Detailed geologic mapping by E. M. Shoemaker and R. E. Eggleton59 on the east flank of the nearly circular Sierra Madera disturbance in west Texas identified three previously unrecognized units: The Tessey Formation of Permian age, a thin section of probable Bissett Formation of Triassic age, and a thin unit of claystone, probably Triassic in age. The presence of these units eliminates the need for the existence of a significant angular unconformity between the rocks of Permian and Cretaceous age. To date, detailed mapping has been confined to a zone of thrust faults and related folds that surround a central lens of megabreccia. The thrusts dip toward the center, and the upper plates are displaced outward. Within each thrust plate the beds are buckled and locally cut by subordinate thrust faults and by steeply dipping normal, reverse, and tear faults. Horse blocks of the basement sandstone of Cretaceous age occur along the thrusts and tear faults. Eastward from the center of the structure, displacement on the 67 U.S. Geological Survey, 1964, Astrogeologic studies annual progress report, August 25, 1962 to July 1, 1963 : Part B. 58 See footnote 57. 69 See footnote 57.ASTROGEOLOGIC STUDIES A143 thrust faults decreases, thrusts die out in asymmetrical anticlines with axial planes dipping back toward the center, and the intensity of buckling decreases. The additional data are compatible with the concept that the structure resulted from meteoritic impact. Impact origin of Campo del Cielo craters confirmed An expedition consisting of representatives from Lamont Geological Institute, Direction de Geologia y Mineria (Argentina), Mellon Institute, Carnegie Institute of Technology, and Daniel J. Milton 60 of the Geological Survey made the first detailed examination of the Campo del Cielo, an Argentine meteorite and crater field. The expedition confirmed the impact origin of craters, located and mapped seven craters, and acquired a newly found iron meteorite of about 3 tons for the U.S. National Museum. In addition, the number of small iron meteorites collected from this field was increased from a handful to more than 400, establishing Campo del Cielo as probably the largest known meteorite-strewn field. Excavation of the best preserved crater revealed charcoal that may represent wood buried beneath loose throwout and burned in a forest fire caused by the meteorite fall. Carbon 14 age of charcoal was determined by Wallace Broecker of Lamont Observatory as 5,800, ±200 years. Impact characteristics of a rockfall, Little Colorado River, Ariz. A group of fresh, low-velocity impact craters formed by a 950-foot rockfall of Toroweap Sandstone into the dry sand bed of the Little Colorado River, about 15 miles west of Cameron, Ariz., was studied by D. P. Elston and D. J. Milton.61 One crater, having a diameter of 5 to 7 feet and a depth of 2 feet, was formed by impact of a block of sandstone weighing about 175 pounds into a nearly level, slightly coherent sand bank. An apron of ejecta was deposited asymmetrically in a direction dominantly away from the source of the rockfall and consisted of (1) a continuous blocky sand ejecta blanket extending from the crater lip to as much as 4 feet from the crater, and (2) a discontinuous sand ejecta blanket, in part raylike, that extended to about 14 feet from the crater. The blocky blanket formed a distinct “hummocky” crater rim deposit. Geologic relations indicate that the material of the discontinuous blanket was deposited upon and beyond the crater rim deposit and was derived from the deepest part of the crater. Fragments of the impacting projectile were deposited in elongate trains traceable up the crater wall, across 00 See footnote 57, p. A142. 61 See footnote 57, p. A141. the blocky ejecta apron, and into the ray like areas, forming the roughest material in the discontinuous blanket. Craters such as this provide a good approximation of secondary impact craters, which are thought to be important features contributing to lunar topography. Origin of the Flynn Creek, Tenn., cryptoexplosion struc-ture Geologic mapping of the Flynn Creek, Tenn., cryptoexplosion structure has been completed by D. J. Roddy.62 The field studies have delimited, in an otherwise undeformed area, a circular deformed rim of Ordovician rocks, about 2.2 miles in diameter, enclosing an intensely brecciated rock consisting of rock fragments of Middle and Late Ordovician age. The upper surface of the breccia is in the form of a crater, 300 feet deep, which contains a centrally raised structure of intensely disturbed rocks of Middle Ordovician age. The structure formed in the interval that includes Late Ordovician to early Late Devonian time. A thin marine deposit of bedded breccia and an anomalously thick section of Chattanooga Shale, including a crossbedded dolomite, possibly basal-most Chattanooga, of early Late Devonian age were deposited in the crater-form structure. The character of the breccia, the presence of shatter cones, the gross structural form, and the apparent lack of gravity and magnetic anomalies obtained from detailed geophysical surveys, are compatible with a meteoritic impact origin. Experimental cratering phenomena Work has continued by M. H. Carr63 on the development of a rapid, inexpensive technique for explosively shock loading materials to permit the study of their behavior under varying pressure conditions. The most fruitful use of this technique is in shocking rock materials to known peak pressures so that the effects of known shocks on a variety of materials can be studied. This experimental technique can be used to obtain the Hugoniot curve, which relates specific volume of the rock material to pressure. It involves passing an explosively generated shock wave through an aluminum rod and then through the specimen. The time of passage of the shock wave past strain gauges on the aluminum and the specimen are measured, and the shock speeds are determined. From the two shock speeds, the shock equation of state can be determined by an impedance match solution, provided the shock wave in 62 See footnote 57, p. A142. 63 See footnote 57, p. A142.A144 INVESTIGATIONS OF PRINCIPLES AND PROCESSES the specimen is a single-step function. The technique, applied to copper, gave results that are in good agreement with the previously determined Hugoniot curve for copper. The results for Yule marble from Colorado indicate that a multiple wave structure is generated; thus an impedance match solution is invalid and no Hugoniot curve can be constructed. Results on basalt show that the measured speed of the shock wave is not pressure dependent and was virtually constant at 5.76 ±.0.28 kilometers per second over the pressure range studied. These results are similar to that found for gabbro by other workers, and may result from measurement of an elastic precursor at pressures less than 200 kilobars. EXTRATERRESTRIAL MATERIALS GEOCHEMISTRY AND PETROGRAPHY OF TEKTITES Systematic study of the mineralogy and chemistry of tektites from Australasia, southeast Asia, and the Philippine Islands strewn fields comprised a major part of the Geological Survey effort during 1963. Characteristics of different groups of tektites New analyses for major and minor elements and physical-property determinations on 6 australites and 6 javanites have been made by Frank Cuttitta, E. C. T. Chao, M. K. Carron, Janet Littler, J. D. Fletcher, and C. S. Annell.64 New minor-element analyses have also been performed on 6 indochinites, 1 additional javanite, 15 philippinites, and 2 thailandites. The new data indicate that Australasian tektites comprise at least two distinct chemical populations which are characterized by differences in (1) indices of refraction and specific gravities, (2) MgO/CaO ratios, (3) Cr, Ni, and Co contehts, and (4) Cr/Ni ratios. The analyzed australites are similar to philippintes in that both kinds of tektites have MgO/CaO less than 1 and have low Cr, Co, and Ni contents. Indochinites and javanites are characterized by MgO/CaO values greater than 1 and Cr, Co, and Ni contents that are higher, in general, than in australites and philippinites. Physical and chemical data, such as these, point toward a better understanding of the extent of intermixing of tektites within each of the various regions comprising the Australasian strewn field, and thereby, a means of reconstructing fall patterns. 64 U.S. Geological Survey, 1964, Astrogeologic studies annual progress report, August 25, 1962 to July 1, 1963 : Part C. Mineralogy and chemistry of spherules in philippinites E. C. T. Cliao, E. J. Dwornik, and Janet Littler 65 have reported new mineralogic, petrographic, and chemical data on metallic spherules present in philippinites from the Ortigas site of Mandaluyoung near Manila, Philippines, and in indochinites from Dalat, South Yiet Nam. Most of the spherules contain ka-macite, schreibersite, and troilite. Schreibersite is in-terstital to the round or elongate, fine-grained kamacite, or forms blebs in a matrix of this kamacite. Where abundant, schreibersite forms a network throughout the entire spherule. Troilite generally comprises small round inclusions in the schreibersite. The amount of schreibersite in the spherules ranges from less than 5 to about 35 modal percent, and the troilite constitutes as much as 5 modal percent. The composition of the phases present in the metallic spherules was determined by use of the electron probe. The kamacite from metallic spherules in 9 philippinites contains from 1.6 to 4.5 percent Ni. The average Ni contents of kamacite in each of 3 analyzed spherules from indochinites are 4.7, 10.0, and 12.9 percent. The average Ni contents in each of 4 schreibersite grains in a single indochinite spherule ranges from 12.1 to 15.8 percent. The spherules in the tektites are very similar to the meteoritic spheroids from Meteor Crater, Ariz., in texture and mineral assemblage. It is concluded that the spherules in the tektites were formed as molten droplets from an impacting meteoritic body which was instrumental in producing the tektite glass. Vapor pressure and fractionation in Philippine tektite melts The vapor pressure and vapor fractionation of Philippine tektite melts of approximately 70 percent Si02 have been studied by L. S. Walter and M. K. Carron. The total vapor pressure at temperatures ranging from 1500°C to 2100°C is 190±40 mm Hg at 1500°C, 450±50 mm at 1800°C, and 850±70 mm at 2100°C. Determinations were made by visually observing the temperature at which bubbles began to form at a constant low ambient pressure. By varying the ambient pressure, a boiling-point curve was constructed. This curve differs from the equilibrium vapor pressure curve due to surface-tension effects. This difference was evaluated by determining the equilibrium bubble size in the melt and calculating the pressure due to surface tension, assuming the latter to be 380 dynes/cm. “ See footnote 64.ASTROGEOLOGIC STUDIES A145 The relative volatility from tektite melts of the oxides of Na, K, Fe, Al, and Si has been determined as a function of temperature, total pressure, and oxygen fugacity. The volatility of Si02 is decreased and that of Na20 and K20 is increased in an oxygen-poor environment. Preliminary results indicate that volatilization at 2100°C under atmospheric pressure caused little or no change in the Na20 or K20 percentage. The ratio Fe+3/ Fe2 of the tektite is increased in ambient air at a pressure of 9 X 10~4 mm Hg ( = 10“7 * 09-4 atm 02, partial pressure) at 2000°C. This suggests that tektites were formed either at lower oxygen pressures or that they are a product of incomplete oxidization of parent material with a still lower ferric-ferrous ratio. Development of spectrographic methods for small amounts of extraterrestrial material The Geological Survey is conducting an extensive investigation of methods of quantitatively analyzing very small amounts of extraterrestrial materials because of the limited samples available. C. S. Annell66 has investigated the analysis of solutions by emission spectroscopy as a technique for the quantitative determination of the major constituents of tektites and meteoritic materials. Use of rotating-disc apparatus in conjunction with high-voltage spark excitation produces the characteristic spectra of many elements present in these materials. The spectral intensities can be measured and quantitatively related to known standards. Studies of experimental factors show that excellent working curves covering the elemental ranges exhibited by known tektites are obtained for aluminum, iron, magnesium, calcium, and titanium. Methods for detecting or determining other elements present in tektites are being studied. Spectrographic determination of low concentrations of Cs, Rb, and Li in tektites A spectographic method for the determination of Cs, Rb, and Li in less than 10 parts per million concentrations in tektites has also been developed by Annell (p. B148-B151), A 1-ppm analytical limit for Cs was obtained using a 3-meter concave grating spectrograph. The method was primarily designed to determine the Cs content of tektites, with adaptation to Rb and Li determinations. The precision of the method was checked by duplicate determinations of Cs, Rb, and Li in bedi-asites from Texas and tektites from Southeast Asia and Indonesia. “ See footnote 64, p. A144. Chemical determination of ferrous iron in small samples M. K. Carron 67 has developed modifications of Wilson’s 68 method for the determination of ferrous iron in milligram amounts of silicates. The modifications provide a means for high-precision determinations of ferrous iron in tektites using ordinary semimicro laboratory equipment. The method presented here employs more dilute solutions of vanadium, V, (0.00139A) than proposed by Wilson. The excess vanadium remaining in solution, after oxidation of the ferrous iron of the sample, is titrated with a 0.0139A ferrous ammonium sulfate solution, using a semimicro buret graduated to 0.02 ml. The results obtained by the proposed method show excellent agreement with those obtained spectrophotometrically. X-ray fluorescence analyses of small samples of tektites X-ray fluorescence analyses of tektites, using 50 milligram samples, have been performed by H. J. Rose, Jr., Frank Cuttitta, M. K. Carron, and Robens Brown (1-64). X-ray fluorescence spectroscopy had been applied previously in the analysis of materials of geologic interest, but larger samples had hitherto been required. Six Java tektites, representative of the range of indices of refraction and specific gravities from a large collection, were analyzed both by X-ray fluorescence and chemical methods, and the results were compared. The analyses, including those of the light elements, are closely similar. Determinations of Si02, A1203, total iron, K20, CaO, Ti02, and MnO are in agreement with those obtained by conventional chemical techniques. Partition of nickel among coexisting phases in basaltic achondrites Metallic iron, occurring as a minor constituent in the basaltic achondrites, has been investigated by M. B. Duke. New electron-probe analyses and petrographic data have been obtained from kamacite in six eucrites and one howardite. The low nickel content of kamacite in eucrites has been verified. Emission spectrographic analyses for nickel in pyroxene from several types of stony meteorites69 and new electron-probe analyses for nickel in the coexisting kamacite give a distribution factor that is in fair agreement with experimental determinations at atmospheric pressure and magmatic temperatures. The low nickel content of the metal and 07 See footnote 64, p. A144. 68 A. D. Wilson, 1960, The micro-determination of ferrous iron in silicate minerals by a volumetric and colorimetric method: The Analyst, v. 84, p. 823-827. 09 M. B. Duke, 1963, Petrology of the basaltic achondrites : California Institute of Technology, Ph. D. dissert.A146 INVESTIGATIONS OF PRINCIPLES AND PROCESSES the generally low total nickel content of the basaltic achondrites are interpreted as due to fractionation between metal and silicate phases during magmatic differentiation of the basaltic achondrites. The nickel distribution supports other mineralogical and textural evidence that these rocks formed at relatively low pressures. Iron content of metallic copper in achondrite Metallic copper from the Norton County, Kans., achondrite has been investigated by M. B. Duke in collaboration with Robin Brett, of the Carnegie Geophysical Laboratory. Electron-microprobe' analyses of the copper indicate an iron content of 4.2 weight percent (Keil and Fredriksson 70). However, phase equilibria relations from the system Cu-Fe-S (R. A. Yund, oral communication) suggest that the copper was formed below 475 ±25°C, the temperature at which iron solubility in copper is negligible. Therefore, new electron-probe microanalyses were made of copper grains (5/t to 20//.) from the chondrites. Iron contents ranging from 1.1 to 4.5 weight percent were obtained. Determinations varied within single copper grains, suggesting that analytical uncertainties were involved. In order to assess the magnitude of CuK-induced FeK radiation arising from outside the analyzed copper grains, four iron fragments were polished and given coats of metallic copper ranging from 0.8 to 3.5/* in thickness. These were analyzed using microprobes of the Applied Research Laboratory and U.S. Geological Survey. The intensity of induced FeK radiation apparently decreases exponentially with the thickness of the copper layer, but is equivalent to 3 weight percent or more for iron covered by 3.5// of copper. The lower the excitation potential or the lower the X-ray take-off angle, the smaller is the fluorescence effect. On the basis of the phase equilibria data and the experiments with copper-coated iron, it is suspected that the analyzed values of iron in copper are unreasonably high due to fluorescence effects. It is necesary, therefore, to analyze large grains or to separate the copper from the matrix in order to determine the true iron content. Electron microprobe analyses of metallic spherules in impactite Using the electron microprobe, E. J. Dwornik and R. R. Larson found that nickel content in 12 metallic spherules in impactite from Wabar, Saudi Arabia, 70 Keil,4ciauss, and Fredriksson, Kurt, 1963, The light-dark structure in the Pantar and Kapoeta stone meteorites: Geochim et Cosmoehim. Acta, v. 27, p. 717—739. ranges from 12.2 to 45.2 percent. Cobalt was noted in minor amounts in those spherules with high nickel content. In a continuing study of “cosmic particles,” the same workers analyzed qualitatively five particles from a suite collected recently by C. W. Crozier from the summits of Mt. Wittington, N. Mex. The particles ranged in size up to 80 microns. Iron was the major constituent in all particles. In one instance titanium was also found, and in another, silicon and calcium. In three particles from the San Augustine Playa deposit, only iron could be detected. Nickel was found in seven metallic spherules from tektites from the Orti-gas site, Philippines, to range from 2.2 to 4.5 percent, and from three spherules from Dalat indochinites to range from 4.7 to 12.9 percent. The analysis of nine additional metallic spherules submitted by W. D. Crozier showed only iron. Four, of the particles were collected from the atmosphere atop Mt. Wittington, N. Mex., the others from a depth of 3 feet from the San Augustine playa nearby. No differences are apparent in these two suites of spherules, suggesting that the particles are not industrial contaminants. Four additional black metallic “cosmic” spherules also analyzed again showed major Fe only. MAGNETIC SUSCEPTIBILITY AND ELECTRICAL RESISTIVITY OF TEKTITES Magnetic susceptibility of tektites Magnetic-susceptibility measurements by A. N. Thorpe and F. E. Senftle On 18 tektites from various strewn fields have shown a relatively large temperature-independent, component of the magnetic susceptibility in all tektites studied. The data indicate that this component is the result of submicroscopic iron spherules in the tektites. An investigation of the color of tektites in terms of the magnetic measurements and of the optical absorption spectra suggests that the basic color of all tektites is green or greenish blue. The brown to black coloration in some tektites appears to be due to finely dispersed Fe203 and (or) many submicroscopic metallic spherules. The magnetic properties of metallic spherules in tektites from Isabela, Philippine Islands, have been investigated by F. E. Senftle, A. N. Thorpe, and R. R. Lewis (1-64). Five metallic spherulas from a single tektite (Pi-73) were studied. They ranged from 0.02 to 0.04 cm in diameter and from 0.07 to 0.28 mg in mass. An electron-probe analysis of one spherule confirmedASTROGEOLOGIC STUDIES A147 the report of Chao and others11 that silicon, if present, is less than a few tenths of a percent. Magnetic-susceptibility measurements on the spherules were made by the Faraday method using a quartz helical spring balance. Measurements were taken at temperatures ranging from 303°K to 77°K. The susceptibility was found to be independent of temperature and approximately the same in all spherules for given field strengths up to 6,000 oersteds. Measurements of magnetic susceptibility as a function of field strength at 298°K and 77°K showed that saturation occurs at relatively high field strengths compared to the saturation of pure iron. The specific magnetization of two of the spherules is about 1.85 Bohr magnetons per atom in fields in excess of 6,000 oe. The permeability of the spherules is close to 1.38. The large field- and temperature-independent susceptibility (0.03 emu/g) is not to be expected for an iron alloy of the composition of the spherules (about 3 percent Ni and 97 percent Fe). Some Ni and low-Si iron alloys lack magnetic saturation except at high fields, as do the spherules; however, such alloys have very large permeabilities in contrast to the low permeability of the spherules. Also, the specific magnetization of the spherules is much higher than would be expected for a low-Ni iron alloy, but can be accounted for by the presence of Fe-Ni phosphides. These considerations indicate that the apparently abnormal magnetic properties of the spherules cannot be a direct result of their chemical composition. The field-independent susceptibility of the spherules, except in very high fields, indicates the absence of a magnetizing field within the spherule. Considerations of the resultant field inside a spherule as a function of the applied field, the shape of the spherule, and the saturation magnetization shows that the field- and temperature-independent susceptibility is a direct result of the shape of the spherules. The saturation of the spherules at relatively high field strengths indicates that the use of the equation of Owen 72 and Honda 73 to detect gross ferromagnetic impurities in tektites is valid only if there are no spherules present. Thus, the presence of spherules less than I/* in diameter cannot be detected by this method or by microscopic examination. 71E. C. T. Chao, J. J. Fahey, Janet Littler, and D. J. Milton, 1962, Stishovite, Si02, a very high pressure new mineral from Meteor Crater, Arizona : Jour. Geophys. Research, v. 67, p. 419-421. 72 M. Owen, 1912, Magnetochemisch Untersuchungen die thermomag-netischen Eigenschaften der Elemente, 2 : Ann. Physik, v. 37, p. 657-699. 78 K. Honda, 1910, Die thermomagnetischen Eigenschaften der Elemente : Ann. Physik, v. 32, p. 1027—1063. Senftle, Thorpe, and Lewis (1-64) have also found that measurement of magnetic susceptibility as a function of temperature is a possible technique for the detection of submicroscopic metallic spherules. The presence of a temperature-independent component of the susceptibility appears to indicate the presence of spherules. If the presence of spherules is established for tektites in general, it will give additional evidence of a meteoritic origin for tektites when combined with the known existence of relatively high phosphorus and nickel contents of the metallic spherules. Relation of electrical resistivity to viscosity of tektites The electrical resistivity of tektites is being investigated with the hope of correlating it with the viscosity. A relation has been found between the electrical resistivity and viscosity of glasses of simulated tektite composition. The average value of the activation energy for electrical resistivity has been found to be 21.3 kilocal/gram and the average activation energy for viscosity has been found to be 3.9 times this value. SPACE-FLIGHT STUDIES Method for measuring lunar slopes An increasingly important part of the Geological Survey investigations for NASA is aimed at determining those characteristics of the lunar surface that are important in designing the manned and unmanned space vehicles and attendant scientific missions. During the past year, a photometric technique for measuring the lunar slopes throughout the equatorial belt and at potential landing sites within the belt was developed by D. E. Wilhelms.74 This technique is based on the functional relation between brightness of the lunar surface, of the angle of incidence of the Sun’s rays, and the local slope of the surface. Areas of interest are traversed by a microphotometer to measure the amount of light transmitted by a lunar photograph. The record is in the form of both an inked line on a chart and a punched paper tape. With the chart, the curve which passes through horizontal segments of the lunar surface can be drawn for each albedo unit (normal albedo must be mapped in advance by other techniques using full-moon photography). The curve then serves as a comparison curve against which brightness of sloping surfaces can be matched. Angular distances in lunar longitude from the terminator, which closely correspond to the angle of elevation of the sun’s rays from the local horizontal surface, are scaled 71 U.S. Geologic Survey, 1964, Astrogeologlc studies annual progress report, August 25, 1962 to July 1, 1963 : Part D.A148 INVESTIGATIONS OF PRINCIPLES AND PROCESSES off on the chart. By measuring the difference in longitude between the segment of unknown slope and the point of equal brightness on the comparison curve, the calculation of the slope is readily made. The average slope of an area can be measured, and terrain maps showing areas of similar slope distribution can be constructed. By recording the microphotometer measurements on punched tape, the data can be transferred readily to a computer where the calculations can be performed automatically. J. F. McCauley has successfully automated the technique, including derivation of the comparison curves, and applied it to a large portion of the lunar equatorial belt, using existing telescopic photographs. In the future, when photographs obtained from spacecraft become available, it should be possible to measure slopes of smaller segments than 0.75 kilometers by refinement of the technique. Terrain maps obtained by this method are of importance in planning unmanned and manned spacecraft landings. Isotonal map of the Lansberg region R. J. Hackman has constructed an isotonal map of the Lansberg region by densitometer traverses of a high-contrast, positive transparency of a full-moon photograph. The lines of traveres were automatically plotted on a Cronopac print, simultaneously with the densitometer traverses of the transparency, and the densitometer curves also were recorded simultaneously on graph paper. The curves were divided into density units by periodic comparison with the curve for a standard density wedge. Traverse segments corresponding to each of the density units were plotted on a 1: 2,000,000 enlargement of the photograph. With these segments (along with 600 spot measurements) as control, and tonal patterns as visual aids, isotonal lines connecting points of equal density were drawn on the photograph. For the final portrayal of the map, the isotonal lines were transferred to ACIC Mercator projection lunar topographic charts by means of a Sketchmaster. Similar tone values are often a clue to correlation of lunar geologic units separated from one another. An isotonal map such as the one compiled correlates tones with greater precision than the unaided eye because the eye is influenced by surrounding tones. Also, small tonal variations that would escape the eye are detected by the densitometer. Isotonal maps are a prerequisite to the construction by photometric methods of lunar terrain maps, as described above, because effects of albedo must be separated from effects of variation in slope. Infrared emission studies of lunar material In other investigations, the properties of the lunar material are being determined from infrared emission studies being conducted by Kenneth Watson.75 Both broad-band and narrow-band emission within the two major atmospheric windows of 8-14/* and 18-24/* will be examined. The broad-band studies will provide information on the distribution of thermal properties at and near the surface, while narrow-band studies will primarily provide information on the grain-size distribution of the lunar material and possibly, in the case of bright-ray craters, a limited amount of compositional analysis. An important line of research will be the computation of models, supported by experiment and observation, to explain the infrared emission. At present, studies are being made on the use of models of the lunar photometric function to derive the variation of absorbed solar energy as a function of the inclination of the Sun’s rays. These data, coupled with model and laboratory studies, will aid in differentiating geologic units. Density of small craters on the lunar surface H. J. Moore has made calculations of the density of small (telescopically unobservable) craters on the lunar surface. The results differ significantly from extrapolations of frequencies of telescopically observable craters 1 kilometer in diameter or larger. By combining data on hypervelocity impact cratering and data on the distribution of interplanetary dust, micrometeoroids, meteoroids, and asteroids, it is calculated that a billion-year-old surface composed of rock and sand would be completely covered with primary craters of all sizes up to 1 meter across in various stages of destruction. If craters 100 meters in diameter are destroyed by erosion and infilling in a billion years, about 10 percent of such a surface could be covered by well-preserved craters between 1 and 10 meters in diameter, 10 percent by well-preserved craters between 0.1 and 1 meter, and 10 percent by wrell-preserved craters between 0.01 and 0.1 meter. The remaining surface area would be covered by primary craters 0.01 to 10 meters in diameter that are more than three-tenths destroyed, by rare larger craters, and by secondary impact craters. Higher rates of crater destruction, as might result from flow of material or burial by volcanic products, would substantially alter these predictions. A smaller crater density is expected on surfaces younger than 1 billion years. ” See footnote 74, p. A147.GEOPHYSICAL INVESTIGATIONS A149 Effect of increasing crater size on effective target strength in basalt H. J. Moore, D. E. Gault, and E. D. Heitowit have shown experimentally that there is a decrease in effective target strength in basalt with increasing size of hypervelocity impact craters. The results are consistent with defect theory, which predicts a decrease in strength with increasing size of specimens containing defects. The experiments refute predictions that the amount of mass ejected for each unit of projectile energy (corrected for the projectile-target density ratio) should be constant. Search for dust clouds near libration regions of the Moon The possible existence of dust clouds near the L4 and L5 libration regions of the moon was investigated by E. C. Morris, J. Ring, and H. G. Stephens76 from Mt. Chacaltaya, Boliva. The libration points, lying in the orbital path of the Moon 60° ahead of and behind it, are points of equilibrium where centrifugal forces balance gravitational forces. It was hoped to observe clouds of particles (“Kordylewski’s clouds”) which may be trapped at these points. From June through November 1963,17 photographic plates of L4 and 28 plates of L5 were taken with a 12-inch focal length aerial camera. Visual examination and microphotometer measurements of the plates failed to show any brightening in the region of the libration points. Further statistical analysis of. the plates is planned. In addition, photoelectric scans were made with a 6-inch-diame-ter Maksutov-Cassegrain telescope. Data from the scans are being reduced; preliminary reduction shows no indication of the presence of a cloud. With further reductions, it is hoped to place an upper limit on the possible cloud brightness, and particle density corresponding to this brightness will be calculated. Statistical analysis of microphotometer data Research in statistical analysis of microphotometer data from full-moon photographs has been continued by A. T. Miesch and C. W. Davis.77 Their results have shown that variations in albedo, textural properties of the albedo patterns, and the regional gradation of the albedo can provide statistics useful in quantifying the observations made during lunar geologic mapping. Thus, correlation between rock units is made easier, and a better understanding is achieved of the nature of the variations in reflectivity. n See footnote 74, p. A147. ” See footnote 74, p. A147. GEOPHYSICAL INVESTIGATIONS STUDIES OF THE CRUST AND UPPER MANTLE Rocky Mountains divide United States into two crustal and upper-mantle superprovinces The crust of the earth is separated from the deeper mantle by the Mohorovicic (M) discontinuity or “Moho.” Specific new results on the thickness of the crust and seismic-wave velocity in the upper mantle have been obtained by the Geological Survey in the Middle Rocky Mountains of Idaho, Utah, and Wyoming (C.R. Willden, unpublished data), the Colorado Plateaus of Arizona and Utah (Roller, 1-63), the Coastal Plain of Mississippi (Healy and others, 1-64) and the Central Lowlands of Missouri (Stewart and Stauder, 1-64). Additional information has also been obtained in areas previously studied, particularly the Basin and Range province of Nevada and Utah (Eaton and others, 2-64; Roller, 1-64). These new results, combined with previous results, permit the generalization that the conterminous United States is divided by the Rocky Mountain System into two crustal and upper-mantle superprovinces. The investigations upon which this conclusion is based were largely supported by the Advanced Research Agency, Department of Defense, as a contribution to the vela uniform Program. The western superprovince includes the Pacific Mountain System, the Intermountain Plateaus, and the Rocky Mountain System. It has the following properties: (1) The velocity of compressional waves in the upper-mantle rocks is everywhere less than 8 kilometers per second, except along the margin of the Pacific Ocean Basin, (2) the mean-crustal velocity is generally less than 6.4 km/sec, (3) the crust is generally thinner than 40 km, and (4) the crust seems to be divided into two fairly distinct layers by a boundary or velocity-transition zone that separates the upper crust with a compressional-wave velocity of about 6 km/sec from the lower crust (intermediate layer) with a compressional-wave velocity of about 7 km/sec. There are important regional variations in the thickness of crustal layers within the western superprovince, but the upper mantle seems to be fairly uniform. For example, the upper surface of the intermediate layer is less than 10 km deep in the Snake River Plain, and the thickness of the crust there is 40 or 45 km (Hill and Pakiser, 1-63), whereas the upper surface of the intermediate layer is about 15 or 20 km deep in the Middle Rocky Mountains, and the thick-A150 INVESTIGATIONS OF PRINCIPLES AND PROCESSES ness of the crust there is about 35 km (C. R. Willden, unpublished data). The eastern superprovince includes the Interior Plains, the Interior Highlands, the Appalachian Highlands, and the Coastal Plain. It has the following properties: (1) the velocity of compressional waves in the upper-mantle rocks is everywhere greater than 8 km/sec, (2) the mean-crustal velocity is generally greater than 6.4 km/sec, (3) the crust is generally thicker than 40 km, and (4) evidence for separation of the crust into distinct layers is less convincing than in the west. The velocity of compressional waves in the crust may increase continuously with depth from about 6 km/sec just beneath the veneer of sedimentary rocks to as much as 7.5 km/sec just above the M-discontinuity. As in the western superprovince, there are important regional variations in the thickness of the crust; the degree of uniformity of the upper mantle is still a matter for debate and further experimentation. One example of such regional variation is the observation that material of compressional-wave velocity 6.6-6.8 km/sec is present at depths of only 5-10 km in the Lake Superior region (Steinhart, 1-64), whereas material of this velocity is present only at depths of 20 km or more in the Great Plains Province (Jackson and others, 1-63). Laboratory measurements of density and seismic velocity, gravity measurements, and considerations of isostasy indicate that crustal and upper-mantle densities vary directly with velocity, so the western superprovince is characterized by low crustal and upper-mantle densities, and the eastern superprovince by relatively high densities. The Late Mesozoic and Cenozoic diastrophism, plutonism, and volcanism have been widespread in the western superprovince, whereas the eastern superprovince has been relatively stable and quiescent during the past 100 million years or so. The crust and upper mantle in the western superprovince can be thought of as youthful—still in the process of evolution. The crust and upper mantle in the eastern superprovince can be thought of as mature. This concept is supported bj aeromagnetic measurements analyzed by Isidore Zietz. These measurements reveal anomalies of large amplitude in the eastern superprovince and a relatively featureless magnetic field in the western superprovince, suggesting, along with the geology and observations of mean-crustal velocity and density, that the crust in the west is now receiving mafic material from the mantle, whereas the mature crust in the east has already been extensively intruded with material from the mantle. Cooperative experiments in seismology Eight Geological Survey seismic stations were among the 46 stations representing 14 U.S. and Canadian institutions that recorded seismic waves generated by 82 one-ton explosions in Lake Superior in July 1963 (Steinhart, 1-64). Geological Survey recording units provided about one-fifth of the more than 3,000 seismograms recorded in this first United States-Canadian cooperative experiment of the international upper mantle project. The Geological Survey has also cooperated extensively with St. Louis University in improving seismic traveltimes for location of earthquakes in southeast Missouri (Stauder and others, 1-64), and in studying crustal structure in Missouri (Stewart and Stauder, 1-64). The Geological Survey has cooperated with the Advanced Research Projects Agency, Air Force Technical Applications Center, California Institute of Technology, and University of California (San Diego) to make a detailed study of crustal structure in the vicinity of the Tonto Forest Seismological Observatory near Payson, Ariz., with the objective of improving the seismic identification capability of the observatory. Data processing of seismic records The Geological Survey is making extensive use of automatic and semiautomatic methods of analyzing seismic data. For example, a six-channel analog-to-digital converter that converts analog magnetic tape recordings to digital records is being used in the Survey’s Denver data-analysis laboratory for computer processing (Healy and Warrick, 2-64). Preliminary research with digital processing has been directed toward selecting processors that help the seismologist to identify events on seismograms and to measure their amplitudes and apparent velocities. A final evaluation of the usefulness of digital processing in the interpretation of refraction seismograms is not possible at this time, but the following conclusions are suggested by the preliminary work: (1) It is difficult to codify and program the function of the seismologist in seismic interpretation, and it may never be practical to remove him completely from the process of interpretation, (2) automatic processing enables the seismologist to make precisely defined and accurate measurements on many more seismograms than can be handled practically by a seismologist without automatic processing, (3) automaticGEOPHYSICAL INVESTIGATIONS A151 processing detects events on seismograms that are missed in routine interpretation by the seismologist. These advantages will probably justify the effort and expense of digital processing. A new analog system for processing magnetic-tape recordings has also been installed in the Survey’s Denver data-analysis laboratory, and it is now in use. Portable seismic recorders An intensive effort is being made by the Geological Survey to develop highly portable seismic-recording equipment for studies of small earthquakes and aftershocks. A new portable seismic-recording system developed recently permits unmanned operation for up to 10 days (Hoover, 1-64). The heart of the seismic-recording system is a tape recorder developed to meet strict performance specifications for low weight, low power, small size, long recording time, and high dynamic range. The record-only transport uses -inch-wide magnetic tape and provides up to 7 data channels and 2 edge channels. The 35-pound recorder, with a bandwidth from direct current to 17 cycles per second, operates over wide environmental conditions without need for special precautions. A prototype seismic system has been developed around the new type recorder. The Geological Survey will use 20 of these systems for studies of aftershocks and small earthquakes, and also to augment its long-offset refraction studies of the earth’s crust, particularly in remote areas. Geothermal investigations The first heat-flow determination on an island arc, excluding Japan, was made by W. H. Diment and J. D. Weaver (2-64) near Mayaguez, Puerto Rico. In addition to finding a low value of heat flow, 0.6 microcalorie per square centimeter per second, they showed that the history of land use may be important in determining the thermal regime. Curvature of the plot of temperature versus depth for the location is tentatively attributed to a 1-degree increase in temperature caused by clearing of forests for cane fields several hundred years ago. In order to provide a basis for understanding the variations in thermal conductivity of ultramafic rocks and for estimating conductivity from a knowledge of mineral composition, W. H. Diment has compiled new and published data on the thermal conductivity of serpentin-ites and minerals commonly comprising them, such as antigorite, chrysotile, olivine, pyroxene, amphibole, talc, magnesite, magnetite, and brucite. Determinations of terrestrial heat flow were obtained near Oak Ridge, Tenn. (Diment and Robertson, 1-63), and Washington, D.C. (Diment and Werre, 3-64). These measurements plus three in progress and those in the literature indicate a deviation of less than 30 percent from a mean of about 1 microcalorie per cm2 sec in eastern North America. Although the measurements are sparsely distributed, their uniformity suggests that heat flow is rather uniform throughout some regions and that the extreme range of continental heat-flow values is the result of processes occurring within the mantle or deep crust. It may thus be practicable in some large regions to estimate temperatures at depth on the basis of reasonable estimates of the thermal conductivities of its rocks and only a few heat-flow determinations. From drifting station Ice Island T-3, B. Y. Marshal], J. P. Kennelly, Jr., E. P. Smith, and A. H. Lachen-bruch have recovered cores and measured temperatures in the bottom sediments in the Arctic Ocean. This continuing study so far includes measurements at 20 locations within a region roughly 100 kilometers on a side, between lat 82° and 83° N. and between long 156° and 164° W.; half the region lies in an abyssal plain, the Canadian Basin, and" half lies on the flank of a suboceanic rise, the Alpha Rise. A preliminary interpretation by Lachenbruch and Marshall (1-64) shows a systematic change of the heat flux from 1.40 microcalories per cm2 sec, ±5 percent, in the abyssal plain (water depth, 3,740 meters) to about 0.8 microcalories per cm2 sec at the shallowest station on the rise (water depth, 2,215 m). In a study of the geologic and hydrologic factors that control local variations in heat flow, A. H. Lachenbruch, G. W. Greene, and R. J. Monroe have made temperature measurements to depths of several thousand feet in 19 holes within a 1,000-square-mile region of complex geology in southern Nevada. Preliminary results show that the thermal gradients within a single formation range from one hole to another by a factor of three. THEORETICAL AND EXPERIMENTAL GEOPHYSICS Paleomagnetism Investigators engaged in paleomagnetic studies have now acquired enough data to establish the theory of reversals of polarity of the earth’s main magnetic field and to date the intervals during the last 4 million years when the field has been “normal,” as it is now, or “reversed,” approximately opposite its present direction. 746-002 0-64-11A152 INVESTIGATIONS OF PRINCIPLES AND PROCESSES Using their extensive measurements of remanent magnetization and absolute age (by the K-Ar method) of rocks from the Hawaiian Islands, Alaska, and Western United States and data published by other workers, R. R, Doell, Allan Cox, and G. B. Dalrymple recognize four major intervals, termed “polarity epochs,” during which the magnetic field has had a single polarity: (1) reversed, from greater than 4.0 bo 3.5 million years ago, (2) normal between 3.5 and 2.5 m.y. ago, (3) reversed between 2.5 and 1.0 m.y. ago, and (4) normal from 1.0 m.y. ago to the present. Intervals of relatively short duration (about 100,000 years) have also occurred during which the polarity of the field was opposite that of the respective epoch. These intervals have been termed “polarity events,” and two are presently recognized: (1) a reversed event about 3.1 m.y. ago, and (2) a normal event about 1.9 m.y. ago. Artificial iron-formation, made by stacking magnetite-bearing and magnetite-free bakelite disks, has been found by C. E. Jahren (1-63) to have the same range of susceptibility anisotropy as natural layered samples. The anisotropy increases with increasing layer susceptibility and is largely independent of the details of layering when less than half the volume of the sample is magnetic material. Triassic diabases and contact-metamorphosed sediments from southeastern Pennsylvania show a considerable range of intensity of magnetization and of magnetic susceptibility, according to preliminary results of a study by M. E. Beck, Jr. Within diabase units the mafic facies are in general more strongly magnetic than late-stage felsic differentiates, and the ratios of remanent to induced magnetization appear to be greater for the finer grained rocks. Within the contact aureole, remanent magnetization and magnetic susceptibility range more widely, in complex relation with the composition of the original sediment, the degree of baking, and the amount of titanomagnetite introduced by hydrothermal solutions. After removal of unstable components, specimens have a “normal” direction of remanent magnetization, very nearly corresponding to the axial dipole position inferred from previous measurements on Triassic rocks of the Eastern United States. Significant deviations from the mean direction exist from one locality to another that probably indicate secular variation of the geomagnetic field; some may have resulted from undetected differences in the amount of structural deformation. Elastic properties of calcite redetermined Using improved ultrasonic pulse-echo instrumentation yielding velocities reproducible to ±0.2 percent, Louis Peselnick and R. A. Robie (1-63) have rederived the elastic constants of calcite as follows (in 1011 dynes per square centimeter) : Cn, 14.45±0.10; c33, 8.31±0.05; C44, 3.263 ±0.03; c^, 5.Vl±0.10; Cj3, 5.34±0.20; c^, — 2.05±0.06. The values of some of the constants were found to be disproportionately sensitive to errors in crystal orientation; for example, a 1-degree error in the polar angle in the YZ plane results in an error of about 1 percent in velocity but an error of about 15 percent in the elastic constant, c13. Rock deformation As a result of a review of time-dependent strain in rocks as a function of temperature, stress difference, and hydrostatic pressure, E. C. Robertson has determined that the theory of viscoelasticity is inapplicable to problems involving rocks in the crust, with the possible exception of unconsolidated water-bearing sediments. The rate of postglacial rebound in Fennos-candia and brittle fracture of salt under loading from nuclear blasts can be predicted at least qualitatively from a preliminary relation evolved. A hyperbolic sine function of stress difference fits the strain-rate data over 10 orders of magnitude for aluminum, copper, steel, and Yule marble; the temperature effect is satisfied by the negative exponential relation of the Arrhenius rate equation up to 80 percent of the melting point. Fracture follows creep as the principal mechanism of failure in metals and rocks at a critical stress near the inflection point of the curve of stress difference versus strain rate. Migration of radon isotopes A. B. Tanner has made an extensive review of the migration of radon isotopes in the ground. In all but very exceptional circumstances, radon-222 concentration undergoes hundredfold diminution by radioactive decay during migration through distances of several meters or less. The underground migration distances of the shorter-lived isotopes, radon-220 (thoron) and radon-219 (actinon), should be measured in centimeters and millimeters, respectively. Electrical properties of iron-formation F. C. Frischknecht and G. I. Evenden have tested the turam electromagnetic method over lenses of metamorphosed iron-formation in the Oakfield Hills area,GEOPHYSICAL INVESTIGATIONS A153 Smyrna Mills quadrangle, Maine. Using an insulated loop for excitation, they obtained large anomalies from which the magnetic susceptibilities and thicknesses of the lenses could be estimated. When a long grounded wire was used for excitation, the anomalies were complicated by effects of galvanic currents. Aerial infrared investigations Aerial infrared imagery was acquired of the Salton Sea, Calif., geothermal area and the Steamboat Springs hot springs area, Nevada, in cooperation with the University of Michigan Infrared Radiation Laboratories. Preliminary study of the Salton Sea area imagery by S. J. Gawarecki indicates that previously known mud pots are detectable, except for one now submerged by the sea. Infrared images of the Steamboat Springs area show a series of hot springs whose alinement suggests that they are associated with a previously mapped fault zone. Comparison of infrared imagery with conventional photography of part of the Shenandoah Valley, Va., by S. J. Gawarecki, discloses that many old drainage channels, sinkholes, and emerging subterranean streams, not readily visible on conventional aerial photography, are clearly visible on the infrared imagery. The recognition of these features suggests that infrared imagery may have particular application to ground-water and engineering-geology studies. Thick soils obscure much of the bedrock. Differences in vegetation, however, in part correspond to differences in lithology. Some differences in vegetation are visible on the imagery and assist in mapping contacts. Automatic contouring of aeromagnetic anomalies G. E. Andreason’s studies of magnetic models for interpretation of aeromagnetic anomalies have been facilitated by adoption of a U.S. Weather Bureau program for automatic contouring and curve drawing. An accurate and reproducible map can now be prepared from model data in less than 1 minute instead of the 1 to 3 days required for hand contouring. The automatic contouring system is expected to be applicable to production of magnetic and gravity maps from field data as well as from model studies. Calculation of depth of magnetic anomalies R. G. Henderson has found that the mathematical process of downward continuation, by which the magnetic field is computed for points in planes successively closer to the source of an anomaly, may be used effec- tively to estimate maximum depth to juxtaposed magnetically different rock bodies. He is also reporting improvement in surface trend analysis (fitting of polynomial surfaces by recourse to orthogonal polynomials) and is making a comparative study of this essentially statistical method with analytical methods based on potential theory. Geophysical Abstracts The Geological Survey continued publication of Geophysical Abstracts for the thirty-sixth year of the publication. Abstracts were derived from more than 500 journals in 20 languages. The staff and volunteer abstracters cover literature pertaining to physics of the solid earth, application of physical methods and techniques to geologic problems, and geophysical exploration. SOLID-STATE STUDIES Luminescence and thermoluminescence studies Basic studies of luminescence are continuing on cesium iodide. The fact that the temperatures of the thermoluminescence “glow” peaks are characteristic of the host crystal and not of the type of impurity has been firmly established. The emission spectra of the glow peaks is a function of the type of impurity. A model has been developed showing that the thermoluminescence “glow” peaks can be due to the migration of holes at characteristic temperatures. The experimental data confirm such a model for cesium iodide at low temperatures, and a preliminary report of this work has been published by Martinez, Senftle, and Page (1-64). Besides the two modes of decay previously reported 78 for “pure” cesium iodide, a third mode having a decay time of 13-15 microseconds has been found. The emission of this mode is in the ultraviolet but at a somewhat longer wavelength than the other two modes. A more precise measurement of the emission of all three modes is planned with a new fast-scan monochrometer now being built. Luminescence studies of zircon have been started, and an attempt is being made to correlate thermoluminescence with natural radiation damage. The thermoluminescence spectrum changes with, but is not consistent with, the amount of damage. 78 F. E. Senftle, P. Martinez, and V. Alekna, 1962, Temperature dependence of decay times and intensity of alpha particles in pure and thallium activated cesium iodide : Rev. Sci. Instruments, v. 33, no. 8, p. 819-822.A154 INVESTIGATIONS OF PRINCIPLES AND PROCESSES Magnetic susceptibility measurements In connection with the magnetic studies of coffinite, it was found necessary to investigate the magnetic properties of some associated compounds to aid interpretation. Magnetic susceptibility measurements have been made on U02-a?H20 for a?=1.78 to a?=2.13, and from 77°K to 375°K. As the value of x decreased, the susceptibility increased. Both these data and structural arguments imply that the formula of this compound is U(OH)4 rather than the dihydrate form. Based on this concept, the data have been corrected for diamagnetism and also for small amounts of U02 and H20 which were present. The molar susceptibility of U+4 in U(OH)4 is nearly an order of magnitude less than in other uranium compounds, and it is suggested that this is probably due to superexchange between adjacent uranium atoms through intervening oxygen atoms. The results of this study have been reported by Pankey, Senftle, and Cuttitta (1-63). A detailed study of the magnetic properties of zircon has been initiated by F. E. Senftle and R. R. Lewis. By measuring the change in magnetization as a function of the accumulated time of heating at 853 °K in a hydrogen atmosphere, it has been shown that the iron in zircon is primarily in the Fe203 form. The observed change in magnetization is due almost entirely to the reduction of surface Fe203. Magnetic susceptibility measurements have been made by A. N. Thorpe on Pd, Pd-H, and Pd-D systems from 4.2°K to 300°K. With H/Pd or D/Pd of over 0.6 the system is diamagnetic at about the same value, that is, — 0.074 X15~6 electromagnetic units per gram. In all cases the susceptibility reaches a maximum at 70°K, but if the hydrogen or deuterium is desorbed to ratios of about 0.5, the susceptibility does not pass through a maximum value. This has a significant effect on the theory of the magnetic susceptibility and is being studied in more detail. Magneto-acoustic studies The magneto-acoustic pulse-echo technique was used by A. F. Hoyte and E. V. Mielczarek to study the shape of the Fermi surface of potassium. Single crystals of potassium were grown by a modified Bridgman method using a two-section stainless steel crucible. The faces of the crystals were cut and polished flat to within 0.001 inch, and their orientations were determined by X-ray crystallographic methods. The measurements were made at a frequency of 94.7 millicycles per second and at a temperature close to 4.2°K. The high-frequency sound wave was propagated in the (111) direction—the growth direction of the single crystals. The crystals were rotated a total of 70° in the magnetic field, which was kept perpendicular to the propagation direction. This was later determined by X-ray crystallography to be a rotation from the (110) direction through the (Oil) to the (134) direction. Thus the complete symmetry of the Fermi surface perpendicular to the (111) direction was studied. One and a half oscillation periods (2 minima and 1 maximum) were observed, and from these the Fermi surface was determined to be spherical within an experimental error of 12 percent. The average value of the Fermi momentum measured was 0.97 X10'19 gram-centimeters per second, and this is in good agreement with the theory by F. S. Ham which predicts an anisotropy of about 1 percent in the Fermi surface of potassium with an average Fermi momentum of 0.87 X 10'1B gram-centimeters per second. GEOCHEMISTRY, MINERALOGY, AND PETROLOGY FIELD STUDIES IN PETROLOGY AND GEOCHEMISTRY Studies of silicic plutonic rocks In the course of a comprehensive study of approximately 250 analyses of “Laramide” igneous rocks of central and western Colorado, George Phair has found that intrusive stocks throughout the State show a strong correlation between petrochemical type and regional gravity. Calc-alkaline stocks tend to be associated with regional gravity lows, whereas alkalic stocks tend to be associated with regional highs; alkali-calcic stocks predominate in a broad area of intermediate gravity between the highs and lows. Implications of these correlations on crustal structure and the origin of magma types are under investigation. As part of an intensive study of the Sierra Nevada batholith in California and Nevada, F. C. Dodge has found that the composition of amphiboles from the various plutons of the batholith shows little variation and is independent of rock composition. The implication is that conditions within the various plutons were similar during formation of the amphiboles. R. I. Tilling (chapter D), in a similar study of the Boulder batholith in Montana, finds that, al-GEOCHEMISTRY, MINERALOGY, AND PETROLOGY A155 though numerous samples from the same pluton may consist of similar mineral species, their relative proportions may be exceedingly variable. Modal analysis of chemically analyzed specimens from the granodiorite of Rader Creek, a pluton apparently homogeneous in outcrop and hand specimen, shows that several modes from a single specimen may be more variable than single modes from specimens from different localities. Furthermore, because he finds that the average composition of any particular specimen as determined from modes may differ from that as determined from its CIPW norm, Tilling concludes that norms and modes cannot always be used interchangeably as an indication of average composition. Studies of mafic and ultramafic plutons From a detailed study of the ultramafic zone of the Stillwater complex, Montana, E. D. Jackson (1-63) finds a strong lateral change in oxidation ratio in chromites that suggests that a lateral oxidation gradient persisted in the magma during crystallization and accumulation of that zone. He also notes a vertical decrease in total iron in chromites that indicates an early reversal in the expected trend of differentiation, later followed by normal iron enrichment. T. P. Thayer (2-63) in a review of structures in alpine peridotite-gabbro complexes concludes that most layering, as well as lineation and foliation, in such complexes is formed by flowage of a semisolid crystal mush. The rarity of relict primary (stratiform) features implies that practically all the layering formed during emplacement, perhaps by mixing of predifferentiated rocks and partly by processes akin to metamorphic differentiation. Studies by F. A. Mumpton, of Union Carbide Corp., with R. G. Coleman and P. B. Hostetler, reveal that the widespread occurrence of brucite in the New Idria, Calif., serpentine body is a product of early serpentini-zation and not of late hydrothermal alteration. Studies of volcanic rocks and processes Petrologic studies of the volcanic rocks surrounding the Creede caldera, San Juan Mountains, Colo., by J. C. Ratte and T. A. Steven (1-64) reveal a progressive increase in volume of lavas relative to ash flows that is interpreted as the result of progressive devolatilization of the Creede magma chamber. Cyclic changes in phenocryst composition and abundance and in chemistry through the sequence further record magmatic reversals that are attributed to interrupted differentia- tion and to stratification of the magma chamber. Similar changes in chemistry and phenocryst abundance have been noted by D. W. Peterson and R. J. Roberts for welded tuffs in Arizona and Nevada. Studies by R. L. Smith and R. A. Bailey, in progress on the Bandelier Tuff, Jemez Mountains, N. Mex., reveal progressive changes in emplacement temperature, chemistry, and feldspar composition which also contribute to the concept that many ash-flow deposits are the stratigraphically inverted products of zoned magma chambers. Warren Hamilton (4—63) notes, on the basis of new chemical analyses of rhyolites from Yellowstone National Park, Wyo., that fluorine and chlorine are several times more abundant in lavas than in welded tuffs, and that iron, although about equally abundant in both rock types, is considerably more oxidized in welded tuffs. He suggests that the differences may aid in distinguishing lavas and welded tuffs. David Cummings (1-64) has discovered that eddy zones associated with inclusions in rhyolite flows are a definitive criterion for determination of flow di-ection. Study of the numerous mafic flows of Dome Mountain, Nev., within the moat of Timber Mountain caldera, by S. J. Luft (chapter D), indicates differentiation toward the upper flows. Upward decreases were observed in abundance of mafic minerals, color, index, and content of normative anorthite; increases were noted in content of alkalies and silica, K/Ca ratio, and differentiation index. The rocks are silica saturated. A Peacock index slightly below 56 puts the suite near the boundary of the alkalic-calcic and calc-alkalic fields. Minor-element studies of igneous rocks and minerals Investigation of the distribution of hafnium and zirconium in glassy rhyolitic volcanic rocks from the Jemez Mountains, N. Mex., is being carried on by David Gottfried. He finds that Hf/Zr ratios are greater in the glass than in associated zircon, and notes that although hafnium concentrations are higher in the zircon, a total amount of hafnium is greater in the glass, owing to the very small percentage of zircon in the rocks. A similar study by David Gottfried and C. L. Waring (p. B88-B91) on zircon from the southern California batholith shows a general increase in hafnium and Hf/Zr ratios from early gabbroic rocks to later granitic differentiates. The studies show that zircon crystallizes continuously throughout the course of magmatic differentiation and that it changes composition systematically as do the major rock-forming minerals.A156 INVESTIGATIONS OF PRINCIPLES AND PROCESSES Studies of thermal waters New isotope data from the Salton Sea, Calif., geothermal area make an igneous origin for the saline brine less likely than previously thought.79 Although the heat certainly is derived from a subjacent igneous body, oxygen and deuterium studies by Harmon Craig indicate a probable meteoric origin for the water of the brine. In addition, studies by Bruce Doe and Carl Hedge indicate that the isotopic composition of lead and strontium in the brine is similar to that in the enclosing sediments but quite unlike that in the Quaternary rhyolite domes in the area. (See also sections “Isotopic Tracer Studies,” and “Light Metals and Industrial Minerals.” A possible mode of origin for saline oil-field waters has been suggested by D. E. White. Many saline waters of sedimentary rocks probably owe their salinities and chemical characteristics to clay minerals that act as semipermeable membranes, permitting passage of water, some other charged molecules, and small, single charged cations (for example, Na+1), but not anions or doubly charged cations (Ca+2 and Mg42). Chemical and electrical balance is maintained by return flow of hydrogen ions. Consideration of Ca/Cl and Br/Cl ratios versus salinity further provides a method of distinguishing waters produced by action of semipermeable clay membranes from those produced by dissolution of evaporites. Studies of metamorphic rocks A review of the mode of occurrence and the chemical and mineralogical variations of eclogites has led R. G. Coleman and D. E. Lee to the conclusion that the eclo-gite metamorphic facies is no longer a valid subdivision in terms of the facies concept. Classifying eclogites into three types on the basis of their occurrence in (1) kimberlites, basalts, and ultramafic rocks, (2) magma-tite gneissic terranes, and (3) alpine orogenic belts, they find that group 3 eclogites have coexisting garnets and pyroxenes with Ca/Mg ratios suggesting pressure-temperature conditions characteristic of the glauco-phane schist facies. J. C. Reed (p. C69-C73) concludes from field relations and new chemical analyses that the greenstones of the Catoctin Formation in the Blue Ridge Mountains, Va., were probably derived from subareally deposited tholeiitic basalts. Their spilitic character, as indicated ™ D. E. White, E. T. Anderson and D. K. Grubbs, 1963, Geothermal brine well—mile-deep drill hole may tap ore-bearing magmatic water and rocks undergoing metamorphism: Science, v. 139, no. 3558, p. 919-922. by Na20/K20 ratios, is not due to submarine eruption, but rather to low-grade regional metamorphism. Studies of sedimentary rocks In a continuing study of the geochemistry and de-positional environments of the Pierre Shale, H. A. Tour-telot, Claude Huffman, Jr., and L. F. Rader (1-64) have discovered positive linear correlations between cadmium and zinc, sulfur, and organic carbon. Some samples relatively high in cadmium do not contain organic carbon in amounts expected from this correlation, however, and they suggested that the cadmium concentration in the sea water, rather than the presence of organic matter, may be a controlling factor. This conclusion is supported by facts that the minor-element composition of carbonaceous and noncarbon-aceous nonmarine shales does not differ appreciably, and that in a very general way the minor-element content increases from nonmarine through nearshore to offshore shale facies. Consideration of the sorption properties of humic materials and clay minerals and differences in their behavior in dilute nonmarine solutions and relatively concentrated marine solutions suggests that interaction of these factors plays an important role in determining the final composition of the sediments. Weathering of the Chattanooga Shale Results of Fischer assay of samples of Chattanooga Shale collected from outcrops, drill cores, and other subsurface sources in Kentucky and Tennessee indicated that oxidation due to weathering leads to increased yields of water and decreased yields of oil according to Andrew Brown and I. A. Breger (p. C92-C95). Decrease in oil/water ratios when plotted against water yields provides an index for evaluating the degree of weathering of the shale; low ratios are indicative of a high degree of weathering. MINERALOGIC STUDIES AND CRYSTAL CHEMISTRY Applications of the computer to mineralogical calculations A new computer program which greatly facilitates the refinement and indexing of X-ray powder diffraction data has been written and extensively tested by H. T. Evans, Jr., D. E. Appleman, and D. S. Handwerker (1-63). Starting with an initial approximation to the unit cell, the program computes the wg 4, g Order (decreasing preference) Natural Exchanger I II III IV V VI VII Mg Ca Sr Ba Mg Sr Ca Ba\ Mg Sr Ba Ca/ Mg Ba Sr Ca Ba Mg Sr Ca Ba Sr Mg Ca\ Ba Sr Ca Mg/ Kaolinite, beidellite (2d site) Silica gel, illite Kaolinite Biotite lNa alumino-boro-KaoliniteJ silicate glasses Montmorillonite, silicate glasses, feldspar, K-mica, bentonite, permutite, phosphate glass, resin, beidellite (1st site) 81R. W. Goranson, 1936, Silicate-water systems; the solubility ot water In albite-melt: Am. Geophys. Union Trans., v. 17, p. 257-259. From clay titration data, Marshall82 found that beidellite exhibits two orders of selectivity, VII at low pH, and I at high pH. The second site with a small equivalent anionic radius behaves as a weak acid, whereas the first site with a larger anionic radius behaves as a stronger acid. Christ and Truesdell (1-64) have developed a method for the interpretation of clay titration curves. Garrels and Christ83 and P. D. Blackmon84 have shown that if each II clay is considered a mixture of two distinct weak acids, then for an exchange, where X is the clay substitute, the equilibrium constant is HX+M+1=MX+H+1, [H+'][MX] Pr-HM (1) (2) [M+'][HX\ where [ ] denotes activity. In order to obtain values for iKHm and 2KHm, certain assumptions based on unsatisfactory theory were made in the evaluation of the ratio [MX\/\_HX~\. However, if the exchangeable cations form a regular solution on a clay, then (2) may be rewritten as (3) [H+1](MX) WHM(. v . Khm~[M+1](HX) ^ RT(1 2Nhx)’ where {MX) and {HX) are concentrations in the binary solution on the clay, WHm is a constant for a given clay and a given exchange, and NBx is the mole fraction of H clay remaining. These variables are readily evaluated from experimental data, and no unverified assumptions need to be made. Using the data of Marshall and others 85 86 the following numerical constants have been obtained from (3) : H clay M+* i_Whm iWhm iKhm jKhm H beidellite. . Na+1 -0. 28 -1. 5 10-31 10-7-3 K+1 -0. 65 0 10“3-4 10-M NH4+l -0. 30 0 10-S.5 10"71 H illite .. Na+1 -. 035 -0. 79 10-2.9 10-0.4 K+1 -0. 74 -1. 13 10-2.0 10-0-3 NH4+1 -0. 61 0. 10 io-3-3 10-5.9 H kaolinite. ... .. Na+1 0. 35 0 10-41 10-5.9 K+1 0 0 10"1-7 10-2.0 H bentonite. _ . K+> -1. 2 10-‘.o 88 C. E. Marshall, 1954 Multifunctional ionization as illustrated by the clay minerals, in Proceedings 2d National Clay Conference: Natl. Acad. Sci.-Nat. Resources Council Pub. 327, p. 364-384. 83 R. M. Garrels and C. L. Christ, 1956, Application of cation-exchange reactions to the beidellite of the Putnam silt loam soil: Am. Jour. Sci., v. 254, p. 372-379. 84 P. D. Blackmon, 1958, Neutralization curves and the formulation of monovalent cation exchange properties of clay minerals: Am. Jour. Sci., v. 256, p. 733-743. 88 C. E. Marshall and W. E. Bergman, 1942, The electrochemical properties of mineral membrane: Jour. Phys. Chemistry, v. 46, p. 52-61. 88 C. E. Marshall and C. A. Krinbill, 1942, The clays as colloidal electrolytes : Jour. Phys. Chemistry, v. 46, p. 1077-1090.GEOCHEMISTRY, MINERALOGY, AND PETROLOGY A161 Truesdell and A. M. Pommer (1-63) have investigated the alkaline-earth ionic selectivity of a phosphate glass as part of a general study of electrode properties. The composition of the glass is (in weight percent): Si02, 3.1; A1203, 5.6; total iron as Fe203, 16.0; Na20, 6.1; K20, 0.09; H20, 0.19; P205, 66.7; and the order of selectivity is 2H+1>Ba+2>Sr+2>Ca+2>2K+I>2Na+1> Mg*2. The use of electrodes in field measurements of Nan in lacustrine closed basins in California and Oregon was accomplished by Truesdell, B. F. Jones, and A. S. Van Denburgh. These waters range from 10 to 120,000 parts per million Na+1 and contain variable amounts and ratios of Cl-1, CO.r2, HCO3*1 and S04"2. The Na+1 concentrations are obtained from Na+l activities by means of a dilution technique and agree well with flame photometric measurements. Variation in H20 and C02 activities in Searles Lake, Calif. H. P. Eugster, of Johns Hopkins University, and G. I. Smith have investigated the relation between the chemical activities of HaO and C02 in the brines of Searles Lake and the evaporite minerals that are in contact with those brines. Fifteen of the 21 known evaporite minerals can be considered as simultaneous and occupy 28 different a«2o=aco2 fields. All observed suites (several thousand) are in agreement and show both stratigraphic and lateral independent variations in ffln2o and aco2 values which reflect either depositional conditions or postdepositional events. Gypsum-anhydrite equilibria E-an Zen, in an extended laboratory and theoretical study of the system CaS04-NaCl-H20, has reexamined the available thermochemical data, including more recent heat-capacity data for anhydrite (CaS04), and revised the temperature of the gypsum-anhydrite—H20 assemblage from 40°C to 46°C at 1 atmosphere pressure. The change of 6°C is significant in terms of evaporite precipitation from sea water, and makes the precipitation of anhydrite from sea water an unlikely event even if equilibrium conditions were realized. In the laboratory, Zen has been unable to crystallize anhydrite from aqueous solutions containing variable amounts of NaCl at 35°, 50°, and 70°C; although he was able to precipitate it from a saturated CaCl2 solution at 70°C. At temperatures where anhydrite should be stable, it converts to gypsum in 3 months, although in runs of 18 months, no gypsum formed, and the anhydrite appeared to be recrystallized. The preparation of starting materials, identification of products, seeding, length of runs, and approaches to reversibility influence the results, and much existing experimental work on the system is internally inconsistent. The precipitation of anhydrite is apparently controlled in part by kinetics, and the origin of sedimentary anhydrite beds remains open to question. Studies of time-dependent processes H. R. Shaw has measured viscosities of synthetically hydrated obsidian, using the falling-sphere technique, at pressures of 1,000 and 2,000 bars and temperatures between 700°C and 900°C. The effect of pressure on the viscosity is found to be so slight that the results can be expressed as a function of H20 content and temperature alone. At 4.3 percent H20, by weight, the common logarithm of the viscosity, in poises, ranges from 6.51 at 800° to 5.88 at 900°C, and at 6.2 percent H20 from 6.54 at 700°C to 5.25 at 850°C. These data and the data of Friedman, Long, and Smith (2-63) on rhyolite glass, at H20 contents of as much as 1.25 percent have been interpreted in the light of the discrete-ion theory of silicate melts,87 and a generalized graph has been constructed which permits approximate predictions of viscosities of framework silicate H20 melts for H20 contents to about 10 percent by weight at temperatures between 500°C and 1200°C (H.R. Shaw 1-63). Shaw has also measured the rate at which H20 is absorbed by obsidian at 850°C and 2,000 bars fluid pressure. A linear relation between weight increase of obsidian, due to sorption, and the square root of time was found to hold until the obsidian is more than two-thirds saturated. Extrapolation to vanishing time gives an intercept at an H20 content between 1.5 and 2.0 percent by weight (saturation under these conditions is 5.9 ±0.2 percent). This demonstrates that there is some mechanism of rapid hydration near the surface of the sample before the slower diffusion-controlled mechanism of hydration takes place. Using the intercept at vanishing time as the initial H20 content, the average diffusion coefficient under these conditions was determined to lie between 10'7 and 10‘8 cm2sec'1. B. J. Skinner has demonstrated that the monotropic inversion pyrite —> marcasite is a zero-order kinetic reaction at 1 atmosphere pressure, between 300°C and 500°C. The host marcasite phase acts as a template for the orientation of the daughter pyrite phase, and experiments are proceeding to establish the crystallographic relations of this epitaxic relation. 87 J. D. Mackenzie, 1957, The discrete ion theory and viscous flow in liquid silicates : Faraday Soc., Trans., v. 53, p. 1488-1493.A162 INVESTIGATIONS OF PRINCIPLES AND PROCESSES Simple systems have been selected for study to further elucidate kinetic mechanisms controlling polymorphic inversions in ore minerals. Two such systems presently under study are a-domeykite (Cu3As) —> algodonite (Cu(8-*) As+/3-domeykite (Cu(3_ir)As) in the temperature range 115°C-250°C, and dense tetragonal Cu2S-» chalcocite in the temperature range 25°C to 100°C and over the pressure range of 1 to 2,000 atmospheres. Thermodynamic properties E. A. Eobie has constructed and placed in routine operation a vacuum-jacketed hydrofluoric acid solution calorimeter having very low thermal leakage. From it has been obtained a heat of solution of KC1 in water at 25°C and infinite dilution of 4,116±11 calories, within 0.05 percent of the most accurate determinations by other laboratories. Eeproducible preliminary results have been obtained with KAlSi308 (microcline) in 20-percent HF at 60°C. Fluid inclusions Edwin Eoedder, in a continuing study of fluid inclusions, has found that liquid C02 inclusions commonly occur in the olivine and other minerals of olivine nodules in alkali basalts. The inclusions apparently represent droplets of a dense C02 phase, immiscible with the magma, trapped by the growing crystals at a depth of 8-16 kilometers. Their existence implies that the olivine crystals 10 percent H20. When the known or estimated geologic age of the samples in each cate- gory was examined, 81 of the 91 samples agreed with the following tabulation: Percent H2Q Age, in yean 0__________________________________ <10* <10________________________________ 104-10e >10________________________________ >10” There are many uncontrolled variables that make further refinement as an “age method” doubtful, and even preclude its use in some localities, but the method is quick and simple and applicable to time spans difficult to measure by other geochronological techniques. GEOCHEMICAL DATA The collection and synthesis of geochemical data are important parts of the program of the Geological Survey. Some types of collections, such as the “Data of Geochemistry” are of immediate value as reference works, not only to geologists but to workers in other scientific fields as well. Other collections, commonly those resulting from fieldwork, provide background for studies of geologic processes, environmental effects on animal and human health, or for programs in economic geology such as geochemical prospecting. Uranium and thorium in igneous rocks Z. E. Peterman has completed a draft report on the geochemistry of uranium and thorium in igneous rocks. Of interest are the uranium and thorium contents of the major classes of nonalkalic igneous rocks. These are median values based on nearly 1,000 uranium analyses representing almost 7,000 samples, and approximately 500 thorium analyses representing almost 3,000 samples. The following estimates are made: mafic igneous rocks (gabbros and basalts), 0.5 parts per million uranium and 1.6 ppm thorium; diorites and quartz diorites, 1.7 ppm uranium and 7.0 ppm thorium; granodiorites, 2.3 ppm uranium and 9.0 ppm thorium ; granites and quartz monzonites and fine-grained equivalents, 3.9 ppm uranium and 16 ppm thorium. Estimates for the exposed continental crust are 2.4 ppm uranium and 10 ppm thorium. Assuming a basaltic oceanic crust, and a basaltic layer beneath the continental crust, the uranium and thorium contents of the total earth crust are estimated to be 1.5 ppm uranium and 5.8 ppm thorium. The major uncertainty in these estimates is the poor knowledge of the relative abundance of igneous rock types in the crust. Minor-element contents of Paleozoic black shales Beds of metal-rich black shale, characterized by concentration of at least 500 parts per million vanadium,GEOCHEMISTRY, MINERALOGY, AND PETROLOGY A163 and variable concentrations of barium, boron, chromium, copper, lanthanum, molybdenum, nickel, lead, silver, yttrium, and zinc are now known from formations in every system of the Paleozoic at one or more localities in the conterminous United States. J. D. Vine has assembled data that indicates that these beds were deposited in geologic environments ranging from the abyssal sea waters of the western eugeosyncline to transgressive brackish-water beds that overlie coal in the Eastern Interior coal cyclothems, and the black-shale facies associated with evaporite deposits. Ordovician graptolitic black shale marginal to and within the western eugeosyncline is locally metal rich at widely scattered localities extending from Mono County, Calif., and Esmeralda County, Nev., on the south, to British Columbia on the north, and including localities in central and northern Nevada, central Idaho, and northeastern Washington. • Fluorine content of silicic volcanic glass R. R. Coats, W. D. Goss, and L. F. Rader have found in an investigation of more than 170 samples of silicic glassy volcanic rocks a marked regional variation in fluorine content. Fluorine content of the samples ranges from 20 to 4,900 parts per million; the median value is 520 ppm, and the 90th percentile is 1,820 ppm. The frequency distribution of fluorine contents closely approaches a log-normal one. The highest values are predominantly from a belt in central Colorado, and west-central New Mexico, from the Big Bend region of Texas, and from southeastern Idaho, western Utah, and northeastern Nevada. The distribution of fluorine in the rocks corresponds closely with the distribution of fluorspar deposits, and somewhat less closely with areas where volcanic rocks are prevalent, and where ground waters carry large amounts of fluorine. Minor elements in metallic ore minerals M. S. Toulmin has completed compilation of 2,800 published analyses of minor elements in sulfide and other metallic ore minerals on punch cards, together with geologic and geographic data of mineral occurrence. Analysis of spectrographic data on Entrada Sandstone P. L. Williams has continued study of the Entrada Sandstone in the Moab 1:250,000 quadrangle, Colorado and Utah, and has had a statistical analysis of spectrographic data on Entrada samples made by the Geological Survey computer. The analysis shows that elemental abundance is about the same in altered and unaltered rock. This is interpreted to mean, in the absence of sample bias, that some minerals were destroyed during alteration. The data further indicate that their chemical constitutents were not removed, but formed new minerals or were sorbed in remaining minerals. For example, barium is about four times as abundant in the heavy minerals of altered sandstone as it is in heavy minerals in unaltered sandstone. This suggests that barium possibly was originally present in cement, or was sorbed in the clay fraction of unaltered sandstone recrystallized during alteration into larger grains of barite. Aluminum, sodium, nickel, lead, yttrium and ytterbium, silver, beryllium, cobalt, molybdenum, columbium, lithium, scandium, uranium, and vanadium are more abundant in altered sandstone than in unaltered standstone. Manganese nodules from sea show high tellurium content D. F. Davidson and H. W. Lakin report that tellurium is much more abundant in manganese oxide nodules from the ocean floor than in other types of manganese oxide occurrence. Highest content of tellurium, as much as 125 parts per million Te, was found in nodules from the Pacific Ocean. These nodules are the first discovered point of strong concentration of tellurium in the sedimentary cycle so far as is known. Computer simulation applied to sampling methods and data analysis A. T. Miesch and J. J. Connor (1-64) in cooperation with R. N. Eicher have been investigating methods of sampling and data analysis using the technique of computer simulation. A computer program has been devised which enables one to “sample” mathematical models of rock bodies using various sampling schemes, and then to analyze the sample data in order to recover the built-in parameters of the model. The advantage of this approach is chiefly in the fact that the parameters are known, whereas in field problems, one can seldom be certain of the accuracy of his statistical estimates. A two-stage method of sampling in geochemical prospecting has been proposed on the basis of studies of this type. GEOCHEMISTRY OF WATER Investigations of the geochemistry of water by the U.S. Geological Survey are directed mainly toward understanding the interrelations of the chemical character of water to the geologic and hydrologic environment. Some of the topics under study include the source of dissolved constituents in precipitation, theA164 INVESTIGATIONS OF PRINCIPLES AND PROCESSES chemical content of stream waters, the relation of the chemistry of ground waters to the mineralogy of aquifers, the effects of local hydrology on the chemistry of lake sediments, and the use of isotopes in hydrologic investigations. Studies of thermal waters are treated in the sections “Light Metals and Industrial Minerals,” “Field Studies in Petrology and Geochemistry,” and “Isotopic Tracer Studies.” STUDIES OF ATMOSPHERIC PRECIPITATION Chemical composition of precipitation Utilizing the precipitation sampling network established in the summer of 1962, A. W. Gambell, Jr., has obtained detailed data for a complete year on the chemical composition of rainfall over a 34,000-square-mile area in North Carolina and Virginia. Over the network as a whole, month-to-month variation in rainfall composition appears to follow seasonal patterns. An increased oceanic influence during the winter months was evident. The range of monthly average concentrations for some of the individual constituents is as follows: SOr2, 1.1 part per million to 3.2 ppm; Cl*1, 0.1 ppm to 1.2 ppm; Ca+2, 0.2 ppm to 1.2 ppm. Studies by A. W. Gambell, Jr., and D. W. Fisher at Prince William National Forest Park, Va., suggest that much of the SOr2 in rainfall results from the catalytic oxidation of S02 in cloud droplets. Atmospheric N02 is indicated as an important catalyst in this reaction. Samples from a number of thunderstorms suggest that, contrary to widespead belief, lightning is relatively unimportant as a source of N03~2 in thunderstorm rainfall. Tritium in precipitation and stream water Tritium rainout has increased considerably since the first nuclear bombs were exploded in 1952, and, due to weather phenomena, a tritium rainout peak occurs sometime during the spring and early summer period. G. L. Stewart, C. M. Hoffman, and T. A. Wyerman observed particularly sharp increases in tritium rainout during late spring and early summer of 1963 when tritium levels in precipitation reached about 7,000 tritium units at Palmer, Alaska, 4,100 T.U. at Lincoln, Nebr., and 1,700 T.U. at Menlo Park, Calif. Other sample collection stations showed similar increases. The same sharp increase in tritium level has occurred in stream water. In 1962, some stream-water samples had peak values of 300 T.U., compared to tritium levels for these same streams of over 2,000 T.U. during the summer of 1963. STUDIES OF SPRINGS, STREAMS, AND LAKES Thermal springs in Upper Colorado River basin In the Upper Colorado River basin, thermal springs discharge to the streams about 59,100 acre-feet of water and 541,600 tons of dissolved solids annually, according to the calculation of W. V. Ioms, C. H. Hembree, and G. L. Oakland. Hot springs along the 17-mile reach of the Colorado River between the Eagle River and the Shoshone powerplant in Colorado contribute about 182,600 tons of dissolved solids to the river each year; of this, about 160,700 tons is sodium chloride. Computations show that thermal springs along the banks and in the bed of the Colorado River between the Shoshone powerplant and Cameo, Colo., add an additional 252,000 tons of sodium chloride annually. Uranium in stream water In a study of the quantity of radioelements being transported by surface waters, E. C. Mallory has calculated that the minimal load of uranium contributed yearly by major rivers of the conterminous United States to the Atlantic Ocean, Gulf of Mexico, and Pacific Ocean is 58,000, 771,000, and 361,000 pounds, respectively. GROUND-WATER STUDIES Methane gas in a fresh-water aquifer in Louisiana Studies by A. L. Hodges, Jr., S. M. Rogers, and A. H. Harder (1-63) of salt-water encroachment in the Chicot aquifer in the heavily pumped Lake Charles area in southwestern Louisiana have revealed the presence of methane gas in the water in some localities. Techniques developed there for estimating the quantity of gas and the rate of movement of the gaseous water can be used elsewhere. There appears to be no relation between gas content and high chloride content. Freeze-thaw effects on chemistry of ground water In northwestern Alaska, marked increases in mineralization of ground water during the colder months are accounted for by simple concentration by freezing, and by reduction in recharge of low mineral content during winter, according to A. J. Feulner and R. G. Schupp (3-63). Fluoride in Florida ground water Mapping of the natural fluoride content of ground water in Florida by L. G. Toler shows concentrations as high as 13 parts per million in coastal areas of theGEOCHEMISTRY, MINERALOGY, AND PETROLOGY A165 Florida panhandle. Insoluble residues of well cuttings from limestones in peninsular Florida disclose previously unreported fluorite at depths which coincide with zones of high fluoride content in ground water. Other known minerals in Florida that contain fluoride are phosphate minerals and mica. Arsenic-rich ground water in Oregon Work by A. S. Van Denburgh has helped to delineate the areal extent, probable geologic associations, and geochemical character of arsenic-rich ground water in central Cane County, western Oregon. The water that contains appreciable arsenic—as much as 1.6 parts per million—apparently is restricted to aquifers within the Fisher Formation, an accumulation of pyroclastic debris of Eocene and Oligocene age. Sodium and bicarbonate are the principal dissolved constituents; the calcium and magnesium contents are characteristically low; the boron and orthophosphate contents are unusually high for Oregon ground waters. Arsenic and boron probably were trace components of the airborne volcanic debris that accumulated to form rocks of the Fisher Formation. After deposition, the glassy portions and certain mineral constituents of the debris were altered hydrochemically and converted to clays and, perhaps, to zeolites. The resulting interstitial water probably was naturally softened and was alkaline. It evidently contained arsenic and boron extracted from the glassy volcanic debris during the course of the same diagenetic reactions that produced the mineralogic changes. CHEMICAL EQUILIBRIUM STUDIES Geochemistry of closed lacustrine basins Study of layered salt crusts at Deep Spring Lake, Calif., by B. F. Jones (1-64) has shown that in spite of bulk chemical differences the saline minerals follow the same sequence, from bottom to top, of nahcolite, thenardite, burkeite, trona, halite, in both the main playa and a nearby fault-trough pond. Thenardite is dominant on the playa, while trona is dominant in the pond. The mineral layering reflects the original sequence of precipitation, adjustments to local equilibrium with interstitial solutions, and an upward decrease of the pressure of C02. Examination of the clay fractions from alluvial-fan materials, former beach deposits, and modem playa sediments in Deep Spring Valley suggests that expand- able-lattice clays have undergone alteration in contact with the waters of an alkaline lake, which is related to the increase in salinity accompanying the evaporative recession of the lake. Dehydration of gypsum in Na2S04 solution Experiments by L. A. Hardie in the system Na2S04-CaS04-H20 have determined reversibly the dehydration of gypsum to anhydrite in saturated Na2S04 solution at 47°±2°C with approximately 12-month runs. This can be extrapolated to about 50° C in pure CaS04 solutions, as compared to 46°±25° C calculated from the most recent thermodynamic data of Kelley (1960). A system has been devised for measurement of the activity of water reproducibly to 0.005, and solid-phase transition temperatures are being studied utilizing the method. Five double salts have been found in the ternary system, all metastable with respect to glauberite (Na2S04-CaS04) above 25° C; at least one has been found in the efflorescenses in Saline Valley, Calif. Mechanism of acid generation in coal-mining areas Ivan Barnes and F. E. Clarke (3-64) reported on an early phase of a fundamental study of water chemistry in relation to generation of acid mine wastes and other contaminants. They inferred that reactions between water, rock minerals, and organic matter result in an acid, strongly reduced solution containing iron and sulfate. These reactions may be able to take place in an anaerobic environment, and, as a result, could have an important bearing on methods selected for preventing or controlling generation of acid mine wastes. Manganese concentrations in water J. D. Hem (1-64) has found that manganese is adsorbed somewhat more strongly than calcium on the surfaces of feldspar grains. The concentration of manganese in ground waiter could be altered by changes in adsorption equilibria accompanying changes in concentration of predominant dissolved cations. A study by E. T. Oborn (1-64) showed that aquatic vegetation in general contained larger percentages of manganese than did land plants. Very dilute solutions of gallic acid can bring manganese into solution from manganese dioxide, and such solutions are relatively stable in contact with air. The dissolved manganese is in a reduced form but is not fully complexed with organic molecules.A166 INVESTIGATIONS OF PRINCIPLES AND PROCESSES ISOTOPIC STUDIES IN HYDROLOGY Preparation of water samples for C14 analysis A simple system for the field preparation of water samples for C14 analysis'has been devised by H. R. Feltz and B. B. Hanshaw (1-63) and tested under field conditions. By use of this technique the total dissolved carbonate species can be stripped from a large water sample and reduced to a small volume. Source of salt-water contamination at Brunswick, Ga. A study of saline water contaminating ground water at Brunswick, Ga., was made by B. B. Hanshaw, William Back, and Meyer Rubin (1-64). C14 analysis indicated that the contaminant was ancient ground water and not nearby modem ocean water. Tritium fractionation in porous media Because the physical and chemical properties are different for the various hydrogen and oxygen isotopes, observations of isotopic fractionation may lead to quantitative techniques for ascertaining processes that occur in nature. Laboratory investigations conducted by G. L. Stewart, C. M. Hoffman, and T. A. Wyerman show that tritium fractionation occurs during the diffusion of water through porous materials. Tritiated water held at low tensions (saturated conditions) contained about 15 percent more tritium than water held at 35 atmospheres tension. INVESTIGATIONS AT THE HAWAIIAN VOLCANO OBSERVATORY Volcanic events, 1963 Tiltmeter surveys indicated a rapid buildup of magma within the summit complex during March and April. Discharge of magma into the Koae-southwest rift systems followed during May 9-11. This discharge was accompanied (1) by many earthquakes that could be felt, (2) by much harmonic tremor centering about the junction of the two rift systems, and (3) by the opening of a larger number of cracks in a zone about 3 miles long and as much as a quarter mile wide. Coincidentally, the tiltmeters indicated rapid collapse of the summit area and inflation under the rift zone centered on the area of seismic and crack activity. The cycle reversed on May 12, when the tilt-instrument system indicated a rapid resumption of inflation under the summit that continued until June 30. Violent seismic activity that centered along the upper east rift zone of Kilauea began on July 1 and initiated a new period of deflation. Later, a new zone of cracks developed for a distance of about 4 miles, trending N 60°-70° E to a point in the area of Devil’s Throat and Aloi crater. Long-base tiltmeter readings and precise levelling indicated an absolute uplift in the center of the zone of almost 3 feet, coupled with downdrop along the margins of nearly half a foot. Coincident rapid detumescence of the Kilauea summit region approximately equalled that which accompanied the December 1962 eruption near Aloi crater. A rapid return to summit inflation was interrupted by outpouring of a million cubic yards of lava at Alae pit crater on the upper east rift zone during August 21-23. An estimated maximum rate of extrusion of 150 cubic yards an hour was reached in the 4th hour of activity. The laval lake reached its maximum thickness in 12 hours of activity. Though some fountaining continued for another 36 hours, the level of the lake actually receded, presumably as a result of drain and (or) degassing back. Beginning 4 days after the close of eruption, the volcano observatory staff began a systematic study of the cooling history of the Alae lava lake. Six weeks later, on October 5, about 10 million cubic yards of lava poured from the floor of Napau pit crater several miles farther east along the same rift zone. Eruption was accompanied by marked deflation of the Kilauea summit, by shallow quakes and strong harmonic tremor, and by a particularly sharply felt earthquake which probably signalled the actual opening of the Napau rift. About 8 hours later, additional outbreaks took place to the east, 3 to 6 miles farther down the rift zone, but from the glow under the heavy rain clouds it appeared that most activity had ceased by 4 a.m. on October 6. This October activity completely erased all the inflation gained earlier in the year. Studies in Alae lava lake The eruption of August 21-23, 1963, left a lava lake of olivine-poor tholeiitic basalt 800 feet wide by 1,000 feet long and as much as 50 feet deep in the bottom of Alae pit crater. Field studies of the cooling lava lake will provide data supplemental to that being obtained from the larger, deeper Kilauea Iki lake. The studies include (1) periodic surface mapping to follow changes in crack pattern and sublimate deposition; (2) repeated surface leveling; (3) periodic observations, on a close net, of the intensity of vertical component of magnetic field; and (4) repeated core drilling for sampling and temperature measurement, starting with a crust thickness of only 3.4 feet. The temperature atISOTOPIC AND NUCLEAR STUDIES A167 the base of the crystalline crust was found to be 1067°C at Alae, compared with 1065°C at Kilauea Iki, and the rate of crustal thickening is similar in both lava lakes (D. L. Peck and others, chapter D). The maximum temperature at Alae, 1135°C, was measured 7.6 feet below the base of the crust. Fountain temperatures did not exceed 1140°C. The surface of the lava lake first fell at a rate of 0.50 foot per month, but thereafter it began a slow steady rise at rates ranging from 0.05 to 0.08 foot per month, presumably because of vesiculation of the lava caused by exsolution of gas. Since late September 1963 the edge of the lake has risen at a moderate rate, and the doughnut-shaped area between the center and edge has risen at a higher rate. Vertical magnetic-intensity measurements at 25 stations showed an elongate magnetic high that is parallel to, but slightly south of, the east-west centerline of the lake and that increased in amplitude by as much as 600 gammas from September 11, 1963, to January 28, 1964. Apparently the position of the anomaly is controlled by the extreme topographic relief of Alae crater; also, its changing amplitude reflects the thickening of the magnetic crust on the lava lake. Petrology of submarine basalts in southeastern Hawaii In October 1962, dredge samples of submarine lava were collected from depths of 1,400 to 17,000 feet along the submerged part of the east rift zone of Kilauea Volcano and from seamounts near the island of Hawaii. Chemical and petrographic study of these unique samples by J. G. Moore shows a systematic change in the character of the vesicles, whose volume and size decrease with depth. These changes can provide a scale by which the depth of eruption of ancient lavas may be estimated. The glassy crust of the east rift zone lavas is closely similar in chemical composition to the more highly crystallized interior of the flows and also to subaerial lava flows of the same rift zone. This indicates that chemical exchange does not take place between sea water and the surface of the deep-sea basalt at the time of eruption. In the material studied there is no evidence that spilite forms at the time of extrusion of submarine lavas. Magmatic differentiation at Kilauea Chemical and mineralogic studies by K. J. Murata and D. H. Richter on lavas of the 1959-60 eruption of Kilauea Volcano point to the involvement of three different magmas. The 1959 summit magma, represent- ing the earliest stage of differentiation, was characterized by the crystallization and gravitative separation of olivine. During the early part of the 1960 flank eruption, a more differentiated magma, probably remnant from the 1955 flank eruption, was expelled. Its differentiation was controlled by separation of plagioclase, clinopyroxene, and olivine. Later, during the 1960 flank eruption, magma separating only clinopyroxene and olivine was erupted. The lavas abundantly illustrate the mechanism of fractional crystallization for differentiation of basaltic magmas as long propounded by N. L. Bowen. Large submarine landslides on Hawaiian Ridge A large area of irregular topography on the slope of the Hawaiian Ridge is interpreted by J. G. Moore (chapter D) as submarine landsliding on a large scale. He describes 2 slides 50 kilometers long that moved down a slope having an overall gradient of about 2°. A concave escarpment marks the head of the slides, and flat-topped tilted blocky seamounts occur on the middle and lower parts. United States-Japan cooperative program A team of seismologists with portable equipment, from Japan, under the leadership of Professor Mina-kami, head of the Earthquake Research Institute, Tokyo University, spent 6 months recording earthquakes, artificial shots, and eruption tremors from different triangulation areas around the dome of Kilauea Volcano. This investigation is a part of the program of the United States-Japan Committee on Scientific Cooperation. A number of episodes of seismic activity took place during this time and were recorded simultaneously at various locations by instruments of the United States and Japanese groups. As part of the cooperative program, an offshore area about 30 by 35 kilometers across, south of Kilauea caldera, was surveyed by 600 kilometers of echo-sounding traverses made by the Japanese training ship Kagoshima Maru, under the command of Captain S. Ueda. Position was controlled by a combination of radar from the ship and three transit stations on shore making simultaneous sightings every 10 minutes, timed by radio signal. ISOTOPIC AND NUCLEAR STUDIES The expanding program in geochronology strongly emphasizes the application of two or more methods of age determination to most geologic problems. Data obtained through a combination of isotopic methods are 746-002 0-64-12A168 INVESTIGATIONS OF PRINCIPLES AND PROCESSES often useful in penetrating the barriers of metamorphic processes and permit insight into other history. Extension of isotopic techniques developed first for geochronology opens new fields of investigation in which lead and strontium isotopes are used as tracers to obtain new information on the origin and source of volcanic and plutonic rocks. Some applications of the study of lead and strontium isotopes are given in the sections that follow on geochronology, isotopic studies of crustal evolution, and isotopic tracer studies. GEOCHRONOLOGY Basement rock age investigations Rb-Sr age determinations by Z. E. Peterman and C. E. Hedge (1-64) of basement samples obtained from drill holes in the Williston basin of North Dakota and adjacent areas confirm subsurface extensions of the Churchill and Superior provinces of the Canadian Shield. The boundary between the Churchill (1.7 billion years) and the Superior (2.5 b.y.) provinces trends southward through western North Dakota. Isotopic ages (Rb-Sr and K-Ar) of core and well cuttings from basement tests in the midcontinent region of North America, reported by W. R. Muehlberger and S. S. Goldich (1-63), show broad areas of relatively uniform ages. Subsurface extensions of the age provinces of the Canadian Shield, the Churchill and the Superior, are recognized in North Dakota and South Dakota. In general the age of the basement rocks decreases to the south. Whole-rock Rb-Sr ages for granite and rhyolite from northeastern Oklahoma give consistent ages of 1,200 million years. Several cores from Kansas, to the northwest, are dated at 1,400 m.y., similar to published ages for some rocks from Missouri. Cores of rhyolite and of trachyte from the Wichita Mountains area of southwestern Oklahoma are dated at approximately 500 m.y. The basement terrane of northwestern Texas and eastern New Mexico ranges in age from 1,300 to 1,400 m.y. and is overlain by a major volcanic sequence that is approximately 1,200 m.y. old. South of this area the crystalline basement rocks of Texas give ages of about 1,000 m.y., similar to ages of rocks in the Llano uplift of central Texas. Central Texas Geochronologic investigations of the rocks of the Llano uplift in central Texas have been continued by R. E. Zartman. Four whole-rock samples of the Valley Spring Gneiss give a Rb-Sr isochron age of 1,120 ± 25 million years and an initial Sr87/Sr86 ratio of 0.706 ± 0.002. This age is significantly older than the age of l, 000-1,050 m.y. of the granites of the area. Isochron plots for minerals of the individual gneiss samples yield an age of metamorphism of 1,000 ±15 m. y., in good agreement with the time of major igneous activity. The strontium in the minerals of the older metamorphic rocks was isotopically homogenized at this time, with Sr^/S86 ratios ranging from 0.716 to 0.775. From these data it is concluded that the plutons (Sr87/ Sr86=0.706) could not have obtained their strontium from the surrounding metamorphic rocks unless some special mechanism operated to remove excess radiogenic strontium. Black Hills, S. Dak. A granite gneiss in the Black Hills, S. Dak., is approximately 2.5 billion years old as shown by preliminary Rb-Sr determinations of whole-rock samples by R. E. Zartman and an isotopic U-Pb age determination of zircon by T. W. Stern. The study of this ancient gneiss and related rocks is being continued by Zartman, Stern, and J. J. Norton. The gneiss provides a link between areas of lower Precambrian rocks in western Wyoming, eastern North Dakota and South Dakota, and western Minnesota. The new work in the Black Hills suggests that lower Precambrian rocks may have covered an extensive area in the north-central United States and that they were not necessarily restricted to several small nuclei. Alkalic rocks of the midcontinent R. E. Zartman and R. F. Marvin in cooperation with Allen Heyl and Maurice Brock have obtained K-Ar and Rb-Sr ages on biotites from a number of the mafic alkalic intrusions of the midcontinent region of the United States. These rocks are not all of the same age but appear to represent several different periods of emplacements. Dikes near Avon in southeast Missouri give an Early to Middle Devonian age; dikes, sills, and explosion breccia from the Rosiclaire fluorite district in Illinois and Kentucky yield an Early Permian age; and isolated dikes in western Pennsylvania, New York, and Vermont may be Jurassic or Early Cretaceous in age. Of special interest in this investigation was the discovery of biotite phenocrysts in rocks from the Pennsylvania and New York localities which contain excess radiogenic argon and yield ages greater than can be inferred from stratigraphic relations. This suggestsISOTOPIC AND NUCLEAR STUDIES A169 that the biotites may be xenocrysts derived from older basement rocks. Minnesota River valley Continuing the work started by E. J. Catanzaro 88 on the granitic gneiss at Morton, Minn., T. W. Stern (1-64) has analyzed 5 additional zircon concentrates and 1 allanite sample. The isotopic ages are discordant. The discordia curve age is 3,600 million years. The allanite ages form a reversed sequence (Pb 206/U 238>Pb 207/ U 235>Pb 207/Pb 206). Three size fractions of the quartz diorite gneiss zircon at Granite Falls, Minn., have practically concordant ages, with a Pb 207/Pb206 age of 2,650 m.y. The zircon from the Sacred Heart Granite of Minnesota is also about 2,650 m.y., but not all samples of zircon from this granite are concordant. Carbon-14 studies Carbon-14 determinations have indirect applications in addition to their use in dating an event in time. A study by A. A. Rosen, U.S. Public Health Service, and Meyer Rubin, Geological Survey, (1-64) makes use of carbon-14 measurements to show that the contamination of the Kanawha River at Nitro, W. Va., is due almost entirely to chemical industrial wastes. 88 E. J. Catanzaro, 1963, Zircon ages in southwestern Minnesota : Jour. Geophys. Research, v. 68, p. 2041-2048. Because of the increase in the use of shells for carbon-14 age determinations, measurements were made of the natural carbon-14 activity of shells from living clams and snails collected from a variety of environments. Meyer Rubin and D. W. Taylor (1-63) conclude that shellfish living in lime-rich waters can metabolize shells having a built-in age of 3,000 years. As a continuing study on changes of sea level, samples of organic material from borings for the Connecticut Turnpike Bridge over the Quinnipiac River in New Haven were taken from depths of 30 to 38 feet below mean sea level. J. E. Upson, E. B. Leopold, and Meyer Rubin (1-64) report that a sample from a thin bed of peat at about 31 feet, dated at 5,900± 2,000 years, represents a position of sea level not lower than 35 to 40 feet below present level. Computations based on this date suggest an average relative rise of sea level of between 1.7 and about 2 millimeters per year. List of age determinations A considerable part of the work of the Geological Survey geochronology laboratory is carried on in cooperation with Survey field geologists. Results of such service investigations throw light on local geologic problems and are reported under the appropriate headings in the section “Regional Geology”. A list of these determinations for use in cross reference follows: Regional Reference Atlantic Coastal Plain. Do. New England and Eastern New York. Do. Do. Appalachian Region. Northern Rocky Mountains and Plains. Southern Rocky Mountains and Plains. Do. Do. Do. Basin and Range Region. Columbia Plateau and Snake River Plain. Pacific Coast Region. Do. Do. Alaska (west central). Alaska (southeastern). Do. Do. Antarctica. Do. Samples dated State Mica schist______________________________________ New Jersey Basement gneiss_______________________________________ do____ Berkshire Schist_________________________________ Massachusetts. Ayer Granite__________________________________________ do________ Canterbury Gneiss________________________________ Connecticut_____ Crystal-lithic tuff______________________________ North Carolina. Glauconite, Hoadley Formation____________________ Montana_________ Boulder Creek batholith__________________________ Colorado________ Crystal-rich ash-flow tuff____________________________ do________ Rhyolite tuffs________________________________________ do________ Snail shells_____________________________________ Wyoming_________ Quartz monzonite_________________________________ Nevada__________ Welded tuff________________________________________ Oregon________ Glaucophane schist_______________________________ California______ Intrusives, Sierra Nevada_____________________________ do________ Metavolcanics, Sierra Nevada__________________________ do________ Wood, Baldwin Peninsula___________________________ Alaska_________ Intrusives, Prince of Wales Island____________________ do________ Intrusive, Talkeetna Mountains__________.-_______ _____do_________ Intrusive, Chickagof Island___________________________ do________ Intrusive, Thiel Mountains____________________________ do________ Intrusive, Eights Coast_______________________________ do________A170 INVESTIGATIONS OF PRINCIPLES AND PROCESSES LIGHT STABLE ISOTOPES Fluid inclusions A detailed study of the chemical composition and relative deuterium concentration of primary fluid inclusions in ore and gangue minerals from the Cave-in-Rock, 111., and the Upper Mississippi Valley districts was reported by W. E. Hall and Irving Friedman (1-63). The fluid inclusions in the early ore minerals are nearly saturated sodium-calcium chloride brines. Fluid inclusions in late minerals are less concentrated and have a lower deuterium concentration. In the Cave-in-Rock fluorite district the composition of primary fluid inclusions in yellow fluorite, the earliest ore mineral) is similar to that of connate water in the Illinois basin in the same strata as the ore deposits. The change in composition of fluid inclusions in the later quartz and sulfide minerals indicates that water of different origin, possibly magmatic, was introduced. Connate and possible magmatic waters were largely flushed out during deposition of the gangue minerals in the last stages of mineralization, and the composition of the fluid inclusions in these gangue minerals trends toward that of meteoritic water. In the Wisconsin-Illinois-Iowa district, the fluid inclusions in the ore minerals are highly concentrated sodium-calcium chloride brines that have a high relative deuterium concentration; whereas the inclusion fluid in late gangue minerals contains less deuterium and is relatively dilute. Irving Friedman, Thorbjorn Sigurgeirsson, and Orn Garbarsson (3-63) determined the deuterium content of 159 samples of waters of all types in Iceland. On the basis of the deuterium analyses, the water from boreholes near Reykjavik does not appear to originate from local precipitation. The variations suggest that deuterium values can be used to determine the time of travel of recharge water as well as the surface recharge area. A review paper by Irving Friedman, A. C. Redfield, Beatrice Schoen, and Joseph Harris (3-64) summarizes more than 1,000 analyses of the distribution of deuterium in waters of the North American continent and the surface waters of oceans contiguous to the continent. The various possible causes for deuterium fractionation are considered, and the regional characteristics of the surface waters of North America are described and interpreted as reflecting the history of the water in the course of the hydrologic cycle. NATURAL RADIOACTIVE DISEQUILIBRIUM STUDIES Natural fractionation of uranium isotopes The mechanism of uranium-isotope fractionation in uranium ore deposits was studied by J. N. Rosholt (p. B84-B87), of the Geological Survey, and E. L. Garner and W. R. Shields, of the National Bureau of Standards. It is suggested that the U234 in a given sample may be contributed in two ways. Atoms generated in place from the radioactive disintegration of U238 (au-thigenic U234) are subject to differential migration with respect to U238. Those atoms that have been transported and mixed with U238 and U235 (allogenic U234) will remain with these two isotopes and are not subject to further preferential leaching. Pattern of uranium fractionation in soils The isotopic composition of uranium has been determined by mass-spectrometric measurements in four soil profiles: (1) a brunizem soil derived from glacial till in Mower County, Minn., (2) a gray-brown podzolic soil derived from loess in Fillmore County, Minn., (3) a brown podzolic soil derived from Cretaceous shale in the La Sal Mountains, Utah, and (4) a brown soil derived from trachyte and volcanic tuff in the Buell Mountain area, Apache County, Ariz. Soil profiles include continuous sampling of the A, B, and C horizons. The uranium content ranges from 2 to 3.5 parts per million in the glacial soils to 6 ppm in the shale soil. A very regular pattern exists for the variation of the U235/U234 ratios with depth. In each profile the ratio increases with depth, and the U234 is most deficient in the C horizon. The C horizon in the Arizona profile has the greatest variation where U234 is 42 percent deficient with respect to the amount required for radioactive equilibrium with the parent U238. These results indicate that U234 is preferentially leached to the greatest degree in the least weathered material in the profile Soluble uranium with U234 in excess of equilbrium requirements migrates upward in the profile and continually exchanges with uranium contained in the A and B horizons to produce an isotopic composition in the upper horizons which is less deficient in U234. This interpretation is in agreement with the suggested mechanism of uranium-isotope fractionation. The C horizons in soil profiles contain the greatest proportion of authigenic U234 , whereas the proportion of allogenic U234 increases upward in the soil profile.ISOTOPIC AND NUCLEAR STUDIES A171 ISOTOPIC TRACER STUDIES Hydrothermal brines near Niland, Calif. Studies of the isotopic composition of lead in the hydrothermal brine and in rocks in the vicinity of Niland. Calif., have been continued in a cooperative study by B. R. Doe, C. E. Hedge, and D. E. White (1-63). The lead isotopic composition varies little in analyzed samples, which have a range in Pb20(5/Pb207 ratios of 1.215 to 1.222, and the composition is distinctly different from that of two samples of obsidian from the area, which have ratios of 1.207 and 1.210. The lead isotopic composition of the brine is unlike that of lead in ocean water, judging from the available analyses of lead isotopes in pelagic sediments and manganese nodules from the Pacific Ocean. The brine lead, however, resembles that of sediments of the region and of the Gulf of Mexico (Pb206,/Pb207^ 1.208-1.222). The value of SP7/Sr86 in samples of the brine is uniform at about 0.711, which is also distinctly different from that of a sample of obsidian from the area (Sr87/Sr86=0.705) and of ocean water (approximately 0.708). Samples of the sediments from the area have values for Sr87/Sr86 in the range of 0.713 to 0.718, distinctly greater than that of brine. Strontium leached from a sample of sediments, however, had a ratio Sr87/Sr86=0.710, and a similar value was found for Salton Sea water. These observations suggest that the host sediments of the area may have been the source of the strontium of the brine and of the Salton Sea water. (See also sections “Field Studies in Petrology and Geochemistry” and “Light Metals and Industrial Minerals.”) Isotopic composition of ore lead from Nevada A. P. Pierce and M. H. Delevaux have investigated the isotopic composition of galena from a series of ore deposits and prospects in Nevada. The samples were taken along a 40-mile sector of the trend of intrusive stocks that cut across the Paleozoic thrust belt of central Nevada. The samples of ore lead are of similar isotopic composition, with a range in Pb206/Pb207 of 1.211 to 1.239, and are somewhat enriched in radiogenic lead. Samples from the upper plate of the Roberts thrust do not differ measurably from those from the lower plate. The results obtained to date support the idea, favored by geologists working in this area, of a northwest-trending mineral belt of cogenetic ore deposits. Ore lead1 in the Colorado Rockies Lead-isotope analyses of 70 galena samples from the Colorado Rockies have been completed by M. H. Delevaux in a study of ore lead with J. C. Antweiler, A. P. Pierce, R. S. Cannon, Jr., and K. L. Buck. Within the Colorado mineral belt, where there is strong geologic evidence of major mineralization cogenetic with Lara-mide igneous activity, a well-defined family of ore lead generally deficient in uranium-derived lead (B-type of anomaly) is found. Galena from deposits outside the mineral belt shows considerable variety, and tentatively three types are recognized which suggest three different episodes of mineralization from Precambrian to Tertiary. Low-temperature deposits in Paleozoic rocks on the fringe of the Leadville, Colo., district, which are similar in many ways to the lead-zinc deposits of the Mississippi Valley, show anomalous excesses of uranium- and thorium-derived leads and hence are J-type leads similar in isotopic composition to the anomalous J-type lead of the Mississippi Valley. Tri-state zoned galena crystal Significant differences in isotopic composition of lead in successive growth zones of a large crystal of galena from Picher, Okla., were found by R. S. Cannon, A. P. Pierce, Jr., and M. H. Delevaux (1-63). A range in the ratio of Pb206/Pb204 from 21.97 to 22.92 was found. The variations within the single crystal are roughly one-fifth of the overall variation of Mississippi Valley J-lead. Reference lead sample In connection with analyses of lead for isotopic abundance ratios a reference sample is included at regular intervals as a means of monitoring the performance of the mass spectrometer. Data on lead reference sample GS-4 are given by M. H. Delevaux (1-63). Copper isotopes The variations of Cu63/Cu65 in approximately 100 natural samples were investigated by S. S. Goldich in collaboration with W. R. Shields, E. L. Gamer, and T. J. Murphy of the National Bureau of Standards (Shields and others, 1-63). No variations larger than the analytical error were found for chalcopyrite and for two meteorites. Two samples, one of bomite and one of chalcocite, showed about 0.5 per mil enrichment in Cu63. A number of secondary copper minerals show enrichment in Cu65. The maximum variation wasA172 INVESTIGATIONS OF PRINCIPLES AND PROCESSES found for a sample of aurichalcite with an enrichment of approximately 1 percent in Cu65. ISOTOPIC STUDIES OF CRUSTAL EVOLUTION Isotopic variation of lead in granitic rocks Isotopic analyses by B. R. Doe (1-64) of lead from granitic rocks and potassium feldspars from granites in several selected parts of the United States suggest that the oldest Precambrian rocks contain lead with isotopic rock compositions that fit fairly well the models of derivation of the lead from an “infinite reservoir.” Such lead commonly is called normal lead. The lead of younger rocks generally departs from the “infinite reservoir” model in a manner suggesting regional or provincial differences. In the Eastern United States the lead in granitic Pocks approximately 1,000 million years old and younger tends to be more radiogenic than expected, giving rise to a negative anomaly. The negative anomaly for Pb206/Pb207 is generally greater than for Pb2°yPb20\ Lead of Tertiary obsidian in the Pacific coast region also shows negative anomalies, but the anomalies are about equal for Pb206/Pb207 and for Pb208/Pb207. In the Rocky Mountain region, however, Pb206/Pb207 in Cretaceous and Tertiary granitic rocks tends to be less radiogenic than expected, producing a positive anomaly; whereas Pb^/Pb204, in general, appears to fit the model and is about as radiogenic as expected. The Precambrian granitic rocks tend to have the more common negative anomaly. The lead-isotope ratios tend to be more erratic in Cretaceous and Tertiary granitic complexes intruded into Precambrian ter-ranes. This erratic behavior is extreme in the Rocky Mountain region, particularly among units of the Boulder batholith. The granitic rocks of the Eastern United States appear to contain normal lead. The isotopic composition of lead in separates of microcline from igneous and metamorphic rocks of the Llano Uplift has been determined by R. E. Zartman (1-64). All the microcline from the igneous rocks has a similar lead isotopic composition (Pb206/Pb204=16.6-17.0; Pb207/Pb204= 15.4-15.5; Pb208/Pb204=36.4—36.7) which yields model ages close to the determined Rb-Sr age of 1,000-1,100 m.y. In contrast with the granitic rocks, the microcline samples from the Valley Spring Gneiss show a wide range in isotopic composition (Pb206/Pb204=17.1-19.4; Pb207/Pb204=15.5-15.8; Pb208/Pb204=36.8-38.2), which is suggestive of a more complex history. It is probable that the plutonic igneous rocks obtained most of their lead from a rather uniform source, possibly deep crustal or upper mantle layers which may also be the reservoir of so-called “conformable” ore lead or normal leads. The presently exposed metamorphic host rocks could have contributed a significant portion of the lead to the igneous rocks only through the operation of some special mobilization and mixing mechanism. The Pb206/Pb204 ratios in whole-rock samples of two igneous rocks were determined and calculated as a function of time, by use of the presently observed U/Pb ratio in the rocks. The ratios became equal to those of the microcline in the samples at approximately 1,100 m.y. ago, suggesting an initial lead homogeneity and subsequent closed-system conditions. The microcline and the total rock from four metamorphic rocks, however, were calculated to have equal lead isotopic compositions at times other than the time reasonably attributable to some tectonic event. Uranium and lead migration and initial lead inhomogeneity in these rocks are considered as possible causes of this discrepancy. Isotopic variation of lead and strontium in volcanic rocks The isotopic composition of lead in basaltic rocks of Japan, Iwo Jima, and the Hawaiian Islands has been determined by M. Tatsumoto (2-64). The volcanic rocks of Japan contain lead in near agreement with models of derivation from an “infinite reservoir” but tend to have small negative anomalies, whereas the sample from Iwo Jima has a much larger negative anomaly. Hawaiian Island volcanic rocks contain lead less radiogenic than expected from the “infinite reservoir” model (positive anomaly), and in addition have smaller values of Pb207/Pb204 than the rocks from Japan and Iwo Jima. This is indicative of a derivation of the Hawaiian volcanic rocks from a different source which has had a distinctly lower value of U/Pb for billions of years. Thus significant differences in lead isotopic composition exist in the sources of oceanic basalt, and are not solely found in rocks of undoubted continental origin. G. R. Tilton, P. W. Gast, and C. E. Hedge (1-64) have investigated Pb and Sr isotopic variations in volcanic rocks from Ascension and Gough Islands on the mid-Atlantic ridge, and in the Columbia River and Snake River flows of the Northwestern United States. Neither the oceanic nor the continental rocks have lead or strontium of uniform isotopic composition. The Pb206/Pb204 ratios range from 18.35 to 19.55;HYDRAULIC AND HYDROLOGIC STUDIES A173 the Pb208/Pb204 ratios range from 38.9 to 39.2. The Pb2°8/pb204 ratios, much restricted in their range compared to the Pb206/Pb204 ratios, in all the basalts agree well with those from young conformable galena deposits; however, only the Columbia River Basalt has Pb206/Pb204 ratios similar to the galena samples. The lead from the Gough Island and from the Snake River flows is apparently deficient in Pb206, whereas the Ascension Island rocks appear to be enriched in radiogenic Pb200. Although Pb206 is more radiogenic at Ascension than at Gough, the Sr87 is less radiogenic at Ascension. On the basis of data presently available, it appears that the Columbia River Basalt has higher Pb206/Pb240 ratios and lower Sr87/Sr86 ratios than the basalt of the Snake River Group. Analyses by C. E. Hedge (1-64) of strontium-isotope abundances in approximately 100 volcanic rocks reveal significant variations in the ratios of Sr87/Sr86 at the time of eruption. The range of 0.7025 to 0.7065 for ScySr86 for oceanic samples is small, but nevertheless it is analytically significant and suggests that the upper mantle beneath the oceans is not entirely homogeneous with respect to the Rb/Sr ratio. Continental volcanic rocks show a wider range in their initial Sr87/Sr86 ratio, 0.7025 to 0.7110, than do oceanic volcanic rocks. Incorporation of relatively radiogenic crustal materials may be a cause of the wider range in initial Sr87/Sr86 of continental compared to oceanic volcanic rocks; however, contamination does not appear wholly adequate as a single process to explain all the data. In several rocks series which might be attributed to magmatic differentiation, variations in initial Sr87/Sr86 with rock type were observed. The variations in Sr87/Sr86 suggest that the members of the rock series could not be derived from a single parent magma through magmatic differentiation within short periods of time. HYDRAULIC AND HYDROLOGIC STUDIES SURFACE WATER Hydraulic studies of surface water have helped show how differences in bed material, temperature, and shape of channel affect the flow of water in laboratory flumes and natural channels. Hydrologic studies have helped show how the amount of flow is affected by natural or manmade features upstream and how the areal and time distribution of streamflow can be related to topographic or hydrologic parameters. Stream-channel underflow C. W. Sullivan found that the 40 cubic feet per second of streamflow that disappears in the gravel streambed upstream from the stream-gaging station on Spavinaw Creek in northeastern Oklahoma reappears 2y2 miles downstream. The fact that it took only 21 hours for fluorescein dye to travel this distance indicates that the underground flow is largely through solution channels. Diurnal fluctuation produced by hydraulic changes F. F. LeFever reports that in midautumn and midspring the flow of the upper reaches of the Middle Loup River in Nebraska varies about 200 cubic feet per second during the day, which is a variation of about 25 percent. He tentatively attributes this variation in flow to storage and release of water in response to changes in bed regime resulting from changes in the ability of water to transport sediment as the viscosity changes with a change in water temperature through a critical range. Flow through contractions K. V. Wilson has found that discharge computed by the U.S. Geological Survey procedures for contracted sections downstream from wide flood plains agrees well with discharge measured by current meter where the flood plains are relatively clear of trees and brush. At sites with heavily wooded flood plains, however, the computed discharge tends to be higher than the measured discharge. These comparisons were made at 60 sites to test the applicability of methods based largely on laboratory experiments. Longitudinal dispersion of a solute By numerical solutions of a dispersion equation, Nobuhiro Yotsukura, G. F. Smoot, and D. I. Cahal show that the longitudinal-distribution coefficient of a solute is almost a linear function of the Reynolds number. By analysis of experimental data, however, they show that in steady rectangular flow the coefficient is proportional to the nine-tenths power of the Reynolds number. Tracer studies in natural streams show greater dispersion than given by an extrapolation of the experimental relation to Reynolds number. Shape of vertical-velocity profiles N. C. Matalas and W. J. Conover have found that the statistical model of turbulence for two-dimensional flow in open channels based on random transfer of momentum gives vertical-velocity profiles that are defined by a three-parameter hyperbolic cosine func-A174 INVESTIGATIONS OF PRINCIPLES AND PROCESSES tion in which two parameters reflect the effect of bed roughness and fluid viscosity and the third is the mean velocity in the vertical. To test the applicability of the theoretical results, they fitted curves to vertical-velocity data for water in natural channels and in a laboratory flume and for air in a wind tunnel and found that the hyperbolic cosine function provides a somewhat better fit to the observed data than does a logarithmic function. Relation of bed material and open-channel flow By collecting and studying information on bed-material size at 60 stream sites where the value of Manning’s n had previously been determined, Jacob Davidian, E. V. Giusti, and R. H. Walker found that for streambeds formed of gravel or coarser material the value of n is related to the relative roughness times the square of the bed-material sorting coefficient. They also found that the Wolman areal pebble-count method of determining bed-material grain-size distribution gives results compatible with those obtained by wet sieving, in that for grain sizes where both methods are feasible the results agree. Flow in open chonnels H. J. Tracy, C. M. Lester, and W. W. Emmett found from studies in a laboratory flume that the resistance a smooth channel offers to the flow depends as much on the waviness of the channel walls as it does on the texture of the walls. They also found that near the sidewalls the vertical-velocity profiles are not logarithmic in shape as they are farther away from the walls. By measuring six components of turbulent stress in airflow in a rectangular closed conduit and by measuring the secondary motion in the comer region, H. J. Tracy obtained data from which he shows that the secondary motion can be explained by the lateral and vertical components of the turbulence through use of Navier-Stokes equations. D. G. Anderson finds that the best mean conveyance to use in computing channel-roughness losses varies with the type of channel. In some types of channel the geometric mean of the conveyance at the ends of the reaches gives the best results, but in other types of channel the arithmetic, harmonic, or quadratic means give better results. To minimize the effect of the uncertainty as to which mean to use, enough sections should be chosen so that the conveyance at one end of the reach does not differ from that at the other by more than 40 percent. Flow in alluvial channels According to D. B. Simons and E. V. Richardson, the velocity of flow in straight alluvial channels with sand beds can be determined from the Chezy equation if the measured depth is corrected to account for separation zones downstream from roughness elements such as dunes. The depth correction is related to depth and slope for each form of bed roughness for a limited range of size of bed material. The value of the Chezy coefficient is related to the ratio of the depth correction and the depth, and to the shear-velocity Reynolds number. Oscillations in the water surface of reservoirs G. L. Haynes, Jr. (p. B158-B162) shows that data from a single wreather station provide only a general indication of the effect of wind and barometric pressure on the oscillations in water surface of Elephant Butte Reservoir in New Mexico. Analysis of the causes and characteristics of setups and seiches does, however, aid in selecting the optimum location for reservoir gages and in interpreting the records of stage. Relation of annual runoff to meteorological factors According to M. W. Busby (p. C188-C189) annual runoff is significantly related to seven meteorological factors. Using annual runoff for 68 widely scattered stream-gaging stations and records from first-order weather stations, he obtained a relation by multiple regression that has a standard error of estimate of 30 percent. Comparison of departures in annual runoff In order to compare the severity of streamflow deficiencies during the 1942-56 drought in the southwest, J. S. Gatewood and others (1-64) developed a procedure for reducing annual runoff for all gaging stations to a comparable basis regardless of differences in variability. With this procedure, which involves expressing the annual departure in terms of an index of variability, the departures from normal for a station with a wide range in annual discharge are more easily compared with those for a station with a narrow range than when the departures are expressed in the customary way. Relations of monthly discharge and precipitation H. C. Riggs (P. C185-C187) shows that for two pairs of stream-gaging stations in Tennessee, better estimates of monthly discharge can be obtained by including monthly precipitation in the regression analysis of monthly discharge than by using discharge alone. TheHYDRAULIC AND HYDROLOGIC STUDIES A175 basins for one pair of stations are adjacent and for the other are 100 miles apart. Improved regression estimates N. C. Matalas has found that the mean and variance of a short-term sequence of hydrologic events can be improved by relating the events to concurrent events in a long-term sequence if the coefficient of correlation exceeds 0.5 and if “noise” is added to each estimated event. The noise is a random variate with zero mean and with variance equal to the variance of the observations for the short sequence about the line of regression. If noise is not added, a coefficient of correlation of at least 0.8 would be required to give improved estimates. Variation in seepage from Crater Lake Hydrologic evaluation of monthly and yearly fluctuations in the level of Crater Lake, Oreg., by K. N. Phillips shows that the average loss by evaporation is 28 inches a year, and that the seepage ranges from 87 cubic feet per second to 107 cfs depending on the level of the lake. The fact that the seepage increases as the level of the lake rises acts as a governor on the level of the lake and explains why the fluctuation in lake level during the past 70 years has been only about 16 feet despite rather extended sequences of wet or of dry years. Annual precipitation on the lake is deduced to be about 7 percent greater than that observed at the Crater Lake Post Office. Lake-volume formula for Indiana The surface area (A) and the maximum depth (Di{) of lakes are more often available than is the volume (V) of water in the lake. M. D. Hale found that the relation A= 1.82^-^j— ^ 1 based on surveys of 85 natural lakes in Indiana could be used to estimate the volume of 89 other Indiana lakes with a maximum error of 40 percent. In the formula, A is expressed in acres, V in acre-feet, and DM in feet. For two-thirds of the 39 lakes the estimated volume was within 10 percent of the value based on lake surveys. Low-flow relations in Delaware River basin For streams in the Delaware River basin, A. G. Hely and F. H. Olmsted (2-63) found that in part of the basin low flows could be related to geology by analyzing the ratios of discharge exceeded 90 percent of the time to mean discharge and by assigning a ratio to each of 10 geologic classifications. For two-thirds of the 19 basins studied, basin ratios weighted according to geology check the observed ratios within 13 percent. For the same area, C. H. Hardison and R. O. R. Martin (2- 63) found that storage-draft relations can be estimated from the median annual 7-day low-flow and size of drainage area. They suggest a method for estimating the median annual low flow for an ungaged stream that requires discharge measurements at times when the flow is not affected by surface runoff from current rainfall. Relation of characteristic flows and drainage area H. C. Riggs (p. B165-B168) used gaging-station records and other flow information in the Rappahannock River basin in Virginia to establish relations between discharge and drainage area for various concurrent events. The results may be used to estimate flows of comparable frequency on the smaller streams in the basin. Low-flow relations in Ohio In a study of annual low flows for durations of 1 day to 12 months, W. P. Cross (1-63) has related the pattern of duration, frequency, and annual minimum rates of flow to the mean annual discharge and to the median 7-day annual minimum as an index. Storage-draft relations by probability routing C. H. Hardison (1-64) defines relations between storage, draft, and variability of annual discharge for streams in which the annual discharges have a lognormal distribution. The variability is defined by the standard deviation of the logarithms of the annual discharge, and the storage requirements are based on solutions of probability-routing equations by an electronic computer. Effect of reservoirs on water yield In arid and semiarid climates, part of the flood waters retained by flood-retarding reservoirs is lost to evaporation, thus decreasing the total amount of flow downstream. For the Sandstone Creek watershed upstream from Cheyenne, Okla., F. W. Kennon found that reservoirs controlling 75 percent of the 85.4 square miles of drainage area decreased the flow during 2 years of above-normal precipitation (1959 and 1960) by 20 percent. Effect of swamps on streamflow E. G. Miller reports that during the summer months the flow out of Great Swamp in New Jersey is sometimes considerably less than the inflow. The decrease on one day in July was measured as 4.2 cubic feet per second or nearly three-quarters of the inflow to this swamp of about 10 square miles.A176 INVESTIGATIONS OF PRINCIPLES AND PROCESSES Effects of upstream use on channel width R. W. Lichty attributes the decrease in channel width of the North Platte River in western Nebraska to the decrease in flow that has resulted from change in upstream water use during the past 60 years. The mean flow has decreased to one-third and the mean annual peak flow to one-quarter of their former values. The channel width has decreased from about 2,800 feet to about 500 feet. Optimum stream discharge for salmon spawning S. E. Rantz (2-64) found that for streams in the northern California Coast Ranges the discharge most preferred by king salmon for spawning is related to the mean discharge of the stream and to the ratio of stream width to drainage-area size. Effect on change in density of rain gages S. P. Sauer found that areal storm rainfall computed from 10 rain gages on the 70-square-mile Mukewater Creek study area in west-central Texas agreed very well with that computed from 19 gages in the same area. For two-thirds of the 121 storms studied, the difference was within 3 percent, which is small in comparison with the standard error of estimate of the rainfall-runoff relation for which the rainfall data were used. GROUND WATER Ground-water research in the Geological Survey was accelerated substantially during the year in response to the growing need for basic information on principles of occurrence, movement, and chemistry of water beneath the land surface. Such information is needed to handle national water problems. Research in borehole geophysics was undertaken to develop techniques of extracting more and better information from costly test holes. Water flow in clay, the principal factor controlling gross movement of water in complex sedimentary systems, was subjected to intensive analysis to explain deviations from so-called Darcy’s-law flow. Work was begun on hydrologic applications of various “remote-sensing” methods including infrared and radar imagery as related, for example, to mapping of aquifers and reconnaissance of areas of ground-water recharge and discharge. Emphasis on geochemical principles was increased, in view of their application to problems of ground-water replenishment, flow, and discharge, and of generation, movement, and disposal of contaminants in the subsurface. Emphasis was also increased on laboratory study of both saturated and un- saturated flow, and on both laboratory and field methods of measuring specific yield and the storage coefficient. Major research projects were undertaken (a) on the fundamental controls of sediment deposition and, hence, on permeability distribution in the Atlantic Coastal Plain hydrologic system; and (b) on the occurrence and discharge of brine in the Permian basin, which spoils large quantities of otherwise usable water. Permeability distribution in sedimentary basins Studies by R. R. Bennett and J. D. Bredehoeft (chapter D) of core analyses and sonic and neutron logs indicate that the permeability of the Tensleep Sandstone in the. Bighorn Basin, Wyo., decreases rapidly from the margins to the center of the basin. Permeability was estimated from an empirical correlation with porosity, a correlation developed from the core analyses and bore-hole logs. Vertical permeability, transmissibility, and storage coefficients from water-level data Work by E. P. Weeks (chapter D) at Madison, Wis., has resulted in methods for analyzing aquifer-test data by finite-difference techniques and by means of a type curve to produce quantitative information on vertical permeability, and on the ratio of horizontal to vertical permeability, in the vicinity of a partially penetrating well. Weeks (p. B181-B184) has also developed a technique for analyzing the recession curve of water level in an observation well after a period of recharge in terms of the transmissibility and storage coefficients of the glacial outwash penetrated by the well. Analysis of drillers' descriptions in terms of permeability values Results of 9 aquifer (pumping) tests and 500 specific-capacity tests made on wells penetrating arkosic deposits of the Kern River alluvial fan in the San Joaquin Valley, Calif., were used by R. H. Dale in developing techniques for relating drillers’ descriptions of texture to definite ranges of permeability values. The term “gravel” was found to indicate permeabilities of 1,000 to 10,000 meinzer units (gallons per day per square foot); “coarse to medium sand,” 100 to 1,000; “fine sand to silt,” 0.01 to 100; “clay,” 0.001 or less; and “gravel to clay,” 10 to 100. Reanalysis of California aquifer tests Earlier data on aquifer tests in California were selectively reexamined by E. J. McClelland, using the method of Hantush.89 The reanalysis gave more con- 90 M. S. Hantush, 1960, Modification of the theory of leaky aquifers : Jour. Geophys. Research, v. 65, no. 11, p. 3713-3725.HYDRAULIC AND HYDROLOGIC STUDIES A177 sistent results and significantly lower values of trans-missibility than those obtained by use of the unmodified Theis equation. Research on permeability and specific yield Several studies of permeability and specific yield of porous media are underway at the hydrologic laboratory in Denver, under the direction of A. I. Johnson. Studies by Johnson and Benjamin Reyes of the effect on laboratory permeability determinations of variables such as entrapped air, particle size, porosity, and hydraulic gradient have shown, among other things, good correlation between permeability and particle size if both particle-size distribution and dominant particle size are treated statistically. Quantitative data on the decrease of permeability that occurs in the zone of aeration with a reduction in moisture content have been obtained in a study just completed by Johnson and R. C. Prill. Johnson, Prill, and D. A. Morris showed that the effect of temperature on centrifuge moisture equivalent (which can be correlated with specific yield) was sufficient to require establishment of a standard temperature for centrifuging; also, that relative humidity must be maintained near 100 percent. In the same report, the authors showed the length of time required for “complete” drainage of columns of various materials to establish specific yield and specific retention. Johnson, W. K. Kulp, and W. E. Teasdale, using a nuclear soil-moisture meter in three areas of changing ground-water levels in California, showed that specific yield depends not only on the texture but on the thickness of the material, the time of drainage, and the texture of overlying and underlying materials. Departures from Darcy’s law in water movement in clay Laboratory work by H. W. Olsen has established that so-called non-Newtonian liquid movement (departures from Darcy’s law of flow in exact proportion to hydraulic gradient) in fine-grained material, reported in the literature as due to clay-water interaction, can be explained in part by the effects of atmospheric contamination on air-water menisci and air bubbles in capillary tubes. It is thought that textural, or fabric, changes are responsible, in a way not yet explained, for remaining deviations from Darcy’s law. Analog models show rate at which aquifers can be flushed of contained fluids J. M. Cahill, in the hydrologic laboratory at Phoenix, used hydraulic sand models as analog “computers” to determine the rate at which the native fluid in an aquifer system could be displaced by another fluid entering as recharge from the land surface. The several models simulated aquifers in which the horizontal permeability exceeded the vertical permeability by specified ratios. The recharge fluid was “tagged” with radioactive phosphorus (P32), and the effluent was monitored for the changing concentration of this radioisotope. The data were plotted to show the proportion of native aquifer fluid appearing in the effluent versus the volume of fluid recharged. Within the range of permeability ratios that was selected, the results can readily be converted into the rates at which similar aquifers can be flushed of their contained fluid. Indirect recharge of Dakota Sandstone in South Dakota F. A. Swenson, in a study of the hydrology and geochemistry of limestone and other soluble rocks, has obtained significant information on recharge to the important artesian aquifer in South Dakota known by the general name Dakota Sandstone. Water enters the Mississippian Pahasapa Limestone on the flanks of the Black Hills and moves eastward in that formation and its subsurface equivalents, well below the Dakota Sandstone. East of the middle of South Dakota, where the intervening strata were eroded away in pre-Dakota time, the limestone lies directly below the Dakota and recharges it. West of the zone of recharge, water in the Dakota is virtually stagnant and has a high dissolved solids content, principally sodium chloride. In the zone of recharge the water is of the calcium sulfate type and is less mineralized. To the east, the water “splits” around the Sioux Quartzite ridge; the water is of the sodium sulfate type to the north where circulation is poor, and of the calcium sulfate type to the south where circulation is better. Well tests in permeable limestone terrane As part of the construction of a hydrologic model of the Roswell, N. Mex., ground-water basin, J. L. Kunkler supervised “packer isolation” tests on four water wells. The tests indicate that certain zones of the San Andres Limestone and the Grayburg Formation have very high transmissibility locally, and transmit effects of discharge from nearby flowing wells very rapidly. Substantial but as yet unexplained differences in artesian pressure between zones were noted in one well. Structural control of water in crystalline rocks Studies at the Georgia Nuclear Laboratory in Dawson County, Ga., of the movement of water through the Precambrian Ashland Mica Schist in relation to movement and adsorption of radioactive contaminants (J. W. Stewart, 1-64) have yielded useful informationA178 INVESTIGATIONS OF PRINCIPLES AND PROCESSES on the occurrence of water in crystalline rocks. C. W. Sever (chapter D) has shown that the courses of streams that drain the Ashland terrane are governed primarily by joints, but the direction of ground-water flow toward the stream is controlled instead by the strike of bedding, schistosity, and axial-plane cleavage. Effect of earthquakes on ground-water levels L. D. Carswell noted earthquake-caused fluctuations of water levels in three observation wells in the Martins-burg Shale in Dauphin County, Pa. These and wells in 4 other counties showed fluctuations resulting from 7 separate earthquakes in August-November 1963, when ground-water levels were at seasonal lows; earthquakes of similar magnitude did not produce fluctuations at other times of the year. The fluctuations appear to be greatest in wells within the cone of depression of pumping of nearby wells. All the wells are in areas where the ground water has an upward component of flow. The fluctuations seem to have no relation to depth of well or to aquifer characteristics as revealed by pumping tests. The March 27,1964, earthquake in Alaska (see section “Alaskan Earthquake”) was unusual in that it produced water-level fluctuations in wells in the upland areas of the Martinsburg Shale, where ground water has a large downward component of flow, in addition to wells in lowland areas where the ground water has a large upward component of flow. In the areas of downward ground-water flow the amplitude of the water-level fluctuation was approximately proportional to the depth that the wells penetrated the aquifer. The deepest well (400 ft) had the largest fluctuation (0.8 ft) and a net lowering of water level of 0.35 foot after the passage of the earthquake. In a nearby well in a valley, where the ground water has an upward component of flow, the total water-level fluctuation exceeded 1 foot but could not be determined more precisely because of overlap in the recording instrument. There was a net rise of water level in the well of more than 0.8 foot after the passage of the earthquake. Water levels in wells respond to sonic booms Water levels in two wells in the Spokane, Wash., area have been affected by sonic booms, according to D. R. Cline. The level in one well, 11 miles north of Spokane, fluctuated 0.06 foot, 0.05 foot below and 0.01 foot above the normal water level, coincident with a sonic boom just north of Spokane. In another well 13 miles east of Spokane, the level fluctuated 0.09 foot, 0.08 foot below and 0.01 foot above the normal water level due to a sonic boom in that area. Temperature fluctuations in shallow ground water Daily temperature measurements were made by R. C. Heath at 5 depths from land surface to 18 feet at Albany, N.Y., over a period of 18 months. His results (3-64) show that temperature waves originating at land surface due to changes of air temperature are nearly dampened out within the soil zone and upper few feet of the zone of saturation. The range in monthly average temperature of the soil at a depth of 1.5 feet was 43°F, compared to 3.6°F in ground water at 17.7 feet. Creation of artesian conditions by soil freezing In a pumping test made during cold weather at Great Smoky Mountains National Park, Tenn., J. H. Criner and R. H. Bingham noted apparent artesian conditions in what was thought to be a water-table area. A second test in warm weather indicated water-table conditions. Temporary artesian conditions due to freezing of soil have been noted previously in more northerly States, but this is the first such situation noted in Tennessee, and one of the first to provide quantitative data on the effect. Correlation of water-level records Statistical methods of linear regression, long used to correlate streamflows in nearby basins so as to enable estimation of flow during periods of missing record in one of the basins, have been applied by H. G. Healy (chapter D) to water-level fluctuations in observation wells in Madison and Duval Counties, Fla. It was found possible to correlate records in wells as much as 17 miles apart. In addition to estimates of fluctuations during periods of missing record, the method enables identifying wells that show representative areal trends of fluctuation and those that do not. Technique for anticipating well clogging In a study at the Bryce State Hospital, Tuscaloosa County, Ala., K. D. Wahl discovered that precipitation of iron compounds, in part as a result of activities of “iron bacteria,” was responsible for decreases in yield of the well supplying most of the water. The construction of the well and water system was such that the plugging was not discovered until the well was almost useless and extensive acidification operations were necessary to restore yield. Now a recorder on a nearby well is used to detect incipient plugging; when the drawdown in the recorder well caused by pumping the supply well decreases, plugging is known to have begun and the yield of the supply well is restored by a relatively minor procedure.HYDRAULIC AND HYDROLOGIC STUDIES A179 Correlation of spring discharge and precipitation A time-series analysis by A. O. Westfall (2-63) of the discharge of Byrds Mill Spring near Fittstown, Okla., shows that fluctuations in discharge can be accurately correlated with fluctuations in precipitation at Ada, Okla., some 10 miles away. The seasonal peaks and troughs in precipitation are reflected at the spring 7 to 8 months later. GROUND-WATER-SURFACE-WATER RELATIONS Because the principles governing the movement and occurrence of surface water and ground water differ in many respects, the methods by which they are investigated likewise differ. For this reason they are commonly studied separately. In many areas, however, water in streams and lakes and water underground are closely related and interdependent. Included in the Survey’s hydrologic investigations, therefore, are studies of (a) the magnitude and source of ground-water contributions to streamflow, (b) methods of forecasting the low flow of streams by use of ground-water levels and aquifer characteristics, (c) the effects of changes in the stage of streams and surface impoundments on ground-water levels and (d) other subjects concerning the relations of water in the two environments. Low flow of streams related to ground-water storage by use of basin constants Research on ground-water storage and its relation to low flow of streams by M. I. Rorabaugh and W. D. Simons led to derivation of basin constants by recession analyses for streams in western Montana. The basin constant, a combination (a) of distance to divide, (b) of storage coefficient, and (c) of transmissibility, is descriptive of the geometry and hydrologic characteristics of the basin. When plotted on a map, these constants form patterns which delineate areas of different hydrologic characteristics from which future outflow can be calculated. Equations and type curves have been prepared by M. I. Rorabaugh for ground-water outflow (a) from a finite aquifer for the conditions of recharge and constant downward leakage, and (b) for rectangular and circular aquifers for conditions of sudden or gradual recharge or sudden or gradual changes in river level. Base flow computed from flow-duration data R. W. Stallman has found that flow-duration data for streams having negligible delays in flow caused by sur- face storage can be analyzed to find the average annual base flow. Base flow computed from flow-duration data is markedly smaller than base flow computed by the usual hydrograph analysis. Dissimilarity between the two estimates of base flow is believed to be due to inadequate treatment of bank-storage effects in the hydrograph analysis. Ground-water recharge and discharge in Wisconsin Studies of ground-water levels and streamflow in the Little Plover River basin, Portage County, Wis., by E. P. Weeks and D. W. Ericson, indicate that most of the recharge to the glacial outwash and morainal deposits comprising the ground-water reservoir occurs in the spring. During the summer the discharge from the aquifers by phreatophytes and by irrigation wells may exceed recharge. During periods of extreme cold in the winter, water may be lost from the water table to the frost zone by vapor transfer. Streamflow characteristics related to geology and topography in northern Michigan G. E. Hendrickson has shown that in glacial-drift terrains in Michigan, streamflow characteristics can be related to the geology and topography of the watersheds. For example, in the Manistee River above Grayling, which has a drainage basin of 159 square miles consisting of 60 percent sandy glacial-outwash plains and 40 percent hilly moraines of silty glacial till, the ratio of maximum to minimum flows was only 2.1 in the 1962 water year. In contrast, this ratio was as much as 165 in the same water year in the Au Gres River above National City, which has a drainage area of 169 square miles consisting of only 20 percent sandy lake plains and 80 percent hilly moraines. A low ratio of maximum to minimum flow indicates that the ground-water component of the streamflow is relatively large. A large ground-water component causes the water to have a low temperature and a high dissolved-oxygen content during the summer, conditions favorable to trout fishing. Relations of surface water to principal artesian aquifer in Florida and southeastern Georgia V. T. Stringfield (p. C164-C169) points out that the principal artesian aquifer of Florida and southeastern Georgia is the source of some of the largest springs known and the chief source of some surface streams where the aquifer is at or near the surface on two major geologic structures in Florida, and where it crops out in Georgia.A180 INVESTIGATIONS OF PRINCIPLES AND PROCESSES On the other hand, the surface hydrology is unrelated to the aquifer where the aquifer is far below the land surface in southeastern Georgia and in northeastern, southern, and western Florida. The surface streams there have a dendritic pattern with many tributaries in areas where they are independent of the aquifer, except on coastal Pleistocene terraces where the drainage pattern is influenced by topography left by the sea. Where recharge or discharge of the aquifer is sufficient to affect detectably the water table in the limestone or the piezometric surface, the streams have few tributaries, as in the Suwannee and Santa Fe basins in Florida. Stream-induced ground water fluctuations A method for analysis of ground-water fluctuations induced by irregular surface-water fluctuations has been developed by M. S. Bedinger and J. E. Heed (p. B177-B180). The method permits the estimation of the diffusivity (the ratio of transmissibility to coefficient of storage) where water-level fluctuations are caused mostly by changes in river stage. If the hydraulic characteristics of the aquifer are known, the methods can be an aid in the analysis of complex hydrographs where changes in river stag3 are one of several factors causing water-level fluctuations. Base flow and stage related to seepage into reservoirs J. F. Turner has evaluated interacting effects of lake stage and water-table elevation (as indicated by the base flow of a small stream) by developing linear relations between these factors and deviations from a mass-transfer calibration curve. The linear mass-transfer calibration was developed for Lake Michie, N.C., by relating the product of wind speed and difference between saturated and existing vapor pressure with the change in lake stage, adjusted for net outflow. The adjusted change in the lake stage is a measure of the combined rates of evaporation and seepage. The y-intercept of the calibration curve indicates the amount of seepage into the lake to be about 2.4 cubic feet per second. When the flow of Dial Creek near Bahama (drainage area, 4.71 sq mi) is zero, the seepage into the lake is about 2.2 cfs less than when the flow of the creek is 2 cfs. When the lake stage is 333 feet, the seepage is about 1.4 cfs less than when the lake stage is 340 feet. Ground-water contributions to streamflow in Lake Erie— Niagara River basins Study of the groundwater discharge into streams of the Lake Erie-Niagara River basins, New York, by A. M. LaSala, Jr., W. E. Harding, and R. J. Archer (1-64) indicated that streams crossing glacial sand and gravel deposits received the largest ground-water contributions. Also, streams crossing the Salina Group of Silurian age received large ground-water contributions. A gain of 3 cubic feet per second per mile of stream length was the largest observed. The poorest contributors were till, glacial-lake deposits, Silurian and Devonian carbonate rocks, and Devonian shale. Differentiating sources of base flow G. R. Kunkle, and E. C. Pogge have found that in Four Mile Creek basin, Iowa, the source of the base flow, which is derived from limestone and a sandy valley fill, can be differentiated by measurements of specific conductance of the streamflow. Locks and dams on Ohio River increase yield of wells Gerald Meyer reports that a rise in ground-water level during 1963 in alluvial deposits adjacent to the Ohio River at Kenova, in southwestern West Virginia, probably was caused by a rise in the navigation-pool stage of the river after the installation of the Greenup Lock and Dam by the Army Corps of Engineers several miles downstream in Kentucky. The water level in an observation well at Kenova rose 6 to 8 feet above normal levels. Also, the yields of public-supply wells at Ceredo, which adjoins Kenova, are reported to have increased after Greenup Dam was installed. Flow of large springs in Florida computed from pressure in artesian well Richard C. Heath reports the use of an artesian-pressure-discharge relation to compute the daily discharge for Silver Springs in central Florida. Artesian pressure is measured in a well tapping the Floridan aquifer, 4.2 miles southeast of Silver Springs, and discharge is measured in Silver Springs Run, 2% miles downstream from the head of the springs. Records of artesian pressure from this same well were used to define a pressure-discharge relation for Rainbow Springs, 27% miles west of the well. Measurements of the discharge of Rainbow Springs have been made at bimonthly intervals since 1931. By use of the pressure-discharge relation and correlation with discharge records for Silver Springs, mean monthly discharges for Rainbow Springs have been extended back to 1932, when the record of mean monthly discharges for Silver Springs begins. Aquifer system provides flow to Muddy River, Nev. Studies of the flow of Muddy River Springs, the principal source of flow of the Muddy River, a tribu-HYDRAULIC AND HYDROLOGIC STUDIES A181 tary of the Colorado in southeastern Nevada, indicate to T. E. Eakin and D. O. Moore (chapter D) that the spring flow represents the discharge from a regional aquifer system in Paleozoic carbonate rocks. They estimate the extent of the system at 7,700 square miles and conclude that 13 topographic basins in eastern and southeastern Nevada contribute ground water to the system. Preliminary analysis of minor long-term variations suggests a 15- to 20-year lag in response to recharge from precipitation. SOIL MOISTURE AND EVAPOTRANSPIRATION Evapotranspiration accounts for over 95 percent of the precipitation in arid regions, and even in the humid zone over half of the available moisture generally is removed in the vapor phase. Part of this moisture is used in the production of agricultural crops, trees, and forage; however, a significant portion is wasted as direct evaporation or in the growth of nonbeneficial vegetation. Studies of evapotranspiration are necessary to achieve a complete understanding of hydrology and to design and evaluate the effectiveness of watershed-management techniques. The soil serves an important function in the hydrologic cycle both as a moisture-storage reservoir and as a conveyance medium for the movement of water, either up for evapotranspiration or down for ground-water recharge. Evapotranspiration and soil moisture are sufficiently interrelated to require that both be considered in most evaluations of either. Mathematical and analog analysis of soil moisture Analysis of hysteresis-affected soil-moisture redistribution occurring after the cessation of rain was investigated by Jacob Rubin and resulted in a proposal for an empirical equation describing the pertinent hysteresis-affected relations of moisture content and suction. A digital computer program was prepared for predicting the moisture redistribution. Semianalytical mathematical methods developed in 1963 for estimating the lower bounds of rainwater uptakes at incipient ponding were extended to include the estimation of the upper bounds. This extended analysis also made it possible to make computations for soils having significant air intake. R. W. Stallman developed an electric analog of steady flow in the unsaturated zone to compute the effect of depth to the water table on evapotranspiration loss from homogeneous media. The results show that evapotranspiration rates are highly dependent on depth to water table. The depth to the water table is regulated chiefly by the balance between recharge and evapotranspiration loss in extensive aquifers with low hydraulic relief. Measurement of water flow through tree trunks A new method has been developed by C. R. Daum for determining water use in large trees. The method is applied under almost natural conditions and is nondestructive. The procedure involves head, flow, and temperature measurements within the trunk. Hourly water use up to 4.4 gallons has been measured in a cottonwood tree in Arizona. He found an inverse relation between hourly water use and the diurnal variations in trunk radius as recorded on a dendrograph. Evaporation from free water and transpiration by aquatic vegetation In studies of the hydrology of prairie potholes in North Dakota, W. S. Eisenlohr found that the mass-transfer coefficient N described by G. E. Harbeck90 included the effect of transpiration by emergent aquatic vegetation when present, and because of this the coefficient varied throughout the season in a pattern similar to one representing the amount of vegetative growth. J. B. Shjeflo in studying the water losses from prairie potholes found that there is very little difference in the amount of water used by a pond covered with emergent aquatic plants and one clear of vegetation. The reduction in evaporation from a pond covered with vegetation, due to shading and lower wind speed, is nearly counterbalanced by the transpiration of vegetation. Evaporation from Lake Helene, a small lake in central Florida, amounted to 53.1 inches in 1962 and 51.3 inches in 1963, according to studies by R. B. Stone, Jr. The monthly rate of evaporation varied from 2.3 to 6.2 inches during the 2-year period. The mass-transfer theory was the basis for these determinations. Monthly mean temperatures of the water surface were always higher than the monthly mean air temperatures, even during the summer. Evapotranspirometer studies Intensive study of evapotranspiration by various types of vegetation under different climatic conditions were made by use of large soil-filled tanks or evapo-transpirometers. During 1964, this method was continued at three sites to measure water use by phreato-phytes. 90 G. E. Harbeck, 1962, A practical field technique for measuring reservoir evaporation utilizing mass-transfer theory : U.S. Geol. Survey Prof. Paper 272-E.A182 INVESTIGATIONS OF PRINCIPLES AND PROCESSES On the lower Colorado River flood plain near Yuma, Ariz., 15 tanks were used to measure water loss by phreatophytes typical of the area. C. C. McDonald and G. H. Hughes report annual use of 106 inches by cattail (Typha latifolia) and 77 inches by arrowweed (Plwchea sericea). In 6 evapotranspirometers, planted to saltcedar near Buckeye, Ariz., T. E. A. van Hylckama (1-64) found that a 50-percent drop in water use reported for July of 1962 did not occur again until August in 1963. This drop in water use could not be explained by the salinity of the water, carbon dioxide content of the air, or evaporation potential. Additional tanks were placed in operation in April 1963. It was possible in these tanks to measure water use by the hour. During hot weather, evaporation rate from bare tanks is reduced during the middle of the day. Two peaks were noted in the evaporation-rate curves, one in the early morning and one late in the afternoon. Measurements of water use by four woody phreatophytes—willow, rabbitbrush, greasewood, and wild-rose—grown in evapotranspiration tanks near Winne-mucca, Nev., were continued by T. W. Robinson during the 1963 growing season (May through October). With the water level in all of the tanks maintained at 5 feet below the surface of the tank, willow (Salix) used the most water, followed by rabbitbrush (Chrysothmrmus viscidiftorus), greasewood (Sarcobatus vermicvlatios), and wildrose (Rosa). The use by willow, 4 acre-feet per acre, was nearly twice that of rabbitbrush and about 3 times that of greasewood and wildrose. It was found that willow used 50 inches, about the same amount of water as evaporated from a Weather Bureau class A pan and more than 5 times the 9 inches evaporated from a bare soil tank in which the water level stood 2.5 feet below the surface. Cover density in the willow tanks was about 90 percent, in the rabbitbrush and greasewood tanks about 50 percent, and in the wildrose tanks about 70 percent. Evapotranspiration by riparian vegetation Studies in the Piedmont province of Georgia by W. H. Norris indicate that diurnal fluctuations of stream-flow due to variation in evapotranspiration rate may be detected in streams with flows up to 100 cubic feet per second. The magnitudes of the maximum fluctuations were found to be related to the magnitudes of the concurrent daily minimum flows. This relation may be used to estimate diurnal variations likely to occur at sites on streams where special equipment has been in- stalled for the purpose of indicating minimum flows. It was also found that the time of occurrence of the minimum flows of the diurnal cycles is related to size of drainage area, magnitude of daily mean flow, and time of year. The larger the drainage area and the smaller the daily mean flow of a specific stream, the later in the day the minimum flow tends to occur. Also, the minimum flow tends to occur progressively later in the day as the season progresses during the year. Evapotranspiration by phreatophytes on the Gila River flood plain, San Carlos Indian Reservation, Ariz., is being measured by a water-budget study. R. C. Culler and R. M. Myrick found that during the dry months of May, June, and July, the water table was lowered an average of 2.5 feet. For this period the change in water storage within the saturated and unsaturated zone, as measured by neutron soil-moisture meters, ranged from 12 to 18 inches. During the summer storm period, August and September, the depletion of the surface flow of the Gila River to evapotranspiration and ground-water recharge was about 8,000 acre-feet. Depth to the ground-water table on the area of phreatophytes ranges from 6 to 45 feet. For all soil profiles having a depth to water table greater than 10 feet, the change in moisture storage during the summer was confined to 2 strata: the surface 2 feet representing the moisture received from precipitation, and a zone 5 feet thick where roots deplete the water in the capillary and saturated zone. Water savings by modification of riparian vegetation were measured in Cottonwood Wash, Mohave County, Ariz., by J. E. Bowie and William Kam. Measurements of streamflow, ground-water levels, vegetation, and meteorological phenomena obtained in a subdivided (2.6 and 1.5 miles) 4.1-mile reach of the channel and flood plain defined the use of water by riparian vegetation under natural hydrologic conditions. Subsequent defoliation and eradication of the vegetation in the lower subreach permitted the determination of the change in water use as a result of the modification. The computed average loss in the lower subreach for the 8-month growing season before modification was 80 acre-feet, which represented about 18 percent of the average flow entering the reach. The average loss after modification was 42 acre-feet, which represented about 12 percent of the average flow entering the reach. Evapotranspiration from the low terraces and flood plain along the middle part of the Big Sandy Creek valley, Colorado, is greater than 94 thousand acre-feet per year. D. L. Coffin reports that this is 4 percent ofSEDIMENTATION A183 the average annual precipitation on the entire basin. Even though this is a relatively large part of the available water supply, there has been no permanent lowering of the water table. F. W. Kennon reports that a 48-hour study of water losses from a small flood-retarding reservoir in central Texas indicated that evapotranspiration losses from reservoir borders was inducing an outward seepage equal in amount to water loss from evaporation at the free water surface of the reservoir. Areal application of soil-moisture studies Studies of soil moisture by W. H. Norris in a small basin in the Piedmont province of Georgia indicates that during periods of average rainfall, water requires several months to percolate through the zone of aeration to the zone of saturation beneath the ridges on the perimeter of the basin. The water table beneath these ridges is about 30 feet below the surface. During rainless periods, the loss of stored water in the soil due to evapotranspiration and percolation may constitute the largest transfer of water in the basin. For example, the calculated decrease in soil moisture stored above the zone of saturation during a 2 week period of base-flow recession in October 1963 was 5 times as great as the concurrent discharge of the stream draining this basin. Overbank flooding and soil moisture The influence of increased channel capacity on soil moisture and associated range-forage plants on flood-plain soils was studied by R. F. Miller, F. A. Branson, K. R. Melin, and I. S. McQueen. Periodic observations near Fort Peck, Mont., have been made since 1947 in the Willow Creek valley, which is underlain by alluvium derived from shale. Rapid advances by a series of headcuts up a previously small channel and widening of the resulting trench were observed. Channel conveyance is increased by erosion, and the frequency of overbank flooding decreases; the resulting changes in depth, degree, and frequency of soil wetting induce changes in soil chemistry and structure, as well as quantities and species of plants present. Individual soil characteristics were found to assert more influence on soil-water-plant relations as the effect of flooding diminished. Accumulation of boron by phreatophytes In the course of studies of water use by woody phreatophytes near Winnemucca, Nev., T. W. Robinson found that greasewood (Sarcobatus vermiculatus) was responsible for yearly enrichment of soluble boron salts in the surface and near surface soils. Chemical analysis of samples of the soils and leaves indicates that this was accomplished by absorption of the boron through the roots and by translocation to and concentration in the leaves; the boron is released later on the surface of the soil, as the fallen leaves decay. The soluble boron content in the soil profile was greatest in the first 2 feet, ranging from 13 to 32 parts per million, then decreasing rapidly to less than 1 ppm in the 5- to 8-foot depth. Boron content in the leaves increased rapidly in the early part of the growing season from 22 ppm in mid-May to 130 ppm in mid-July. The areal distribution of boron in the top 3 inches of soil, in the vicinity of a mature plant with a crown diameter of 2 feet, was greatest near the main stem. At a distance of 1 foot it was 15 ppm, decreasing to 11 ppm at 6 feet and to essentially zero at 8 feet. SEDIMENTATION The area of investigation termed “sedimentation” includes the sequence of events which begins with the separation of particles from parent rock and concludes with their consolidation into another rock. Sedimentation, therefore, involves consideration of sediment sources; of the erosion, transportation and deposition of sediments; and of environments of deposition and sedimentary deposits. The subject is of special interest to engineers who are primarily concerned with problems of erosion, transportation, and deposition of sediments, and to geologists who are concerned with interpreting the origin of sedimentary rocks and the origin and modification of landforms. Two reports published during fiscal year 1964 illustrate these two approaches. The first, “Fluvial Sediments—A Summary of Source, Transportation, Deposition, and Measurement of Sediment Discharge,” by B. R. Colby (1-63), is largely a summary of the engineering literature on sediment transport in rivers. The other, “A Tentative Classification of Alluvial River Channels,” by S. A. Schumm (1-63), is an attempt to classify river channels on the basis of sediment load and channel stability; it is mainly a geologic approach to the problem. The background and interests of those engaged in sedimentation research are reflected in the diversity of the results reported by scientists of the Geological Survey. These results are presented under the following major subdivisions of the subject: erosion, transportation, and deposition. 746-002 0 - 64 - 13A184 INVESTIGATIONS OF PRINCIPLES AND PROCESSES EROSION The extent and rate of erosion within a drainage basin can be estimated by measurement of the sediment transported by the streams draining the area. However, to gain some understanding of the progress of erosion on a hillslope or in a channel, repeated measurements are necessary. For example, surveys made by R. K. Fahne-stock along the Wynoochee River in Washington show that cutbank migration of from 10 to 20 feet and alteration of the form of point bars were the results of a single flood of relatively small magnitude. Repeated measurements in an ephemeral stream channel near Santa Fe, N. Mex., by L. B. Leopold and W. W. Emmett, indicate a general balance between erosional and depositional processes in the channel. Although the measurements show an average of 0.10 to 0.20 feet of aggradation during 6 years of observation, annual scour, which temporarily deepens the channel as much as 1.5 feet, may occur during flash floods. Five years of experimentation with painted cobbles in the same channel show that a close spacing of particles makes them less easily moved than when they are spaced far apart. W. B. Langbein has checked these observations experimentally by the use of glass beads in a small flume. TRANSPORTATION Predicting sediment loads of rivers One of the primary goals of those concerned with the movement of sediments through river channels is the development of criteria whereby the total sediment load can be estimated either on a short- or long-term basis. Measurements of total sediment load on Five-mile Creek, Wyo., were used by D. C. Dial to relate total sediment load to measured load using the modified Einstein procedure. Individual measurements show considerable variation in the ratio between total load and measured load; however, at high sediment concentrations, it was found that lower ratios between total load and measured load occur. This happens because the unmeasured portion of the sediment load generally is a smaller percentage of the total load when the concentration is high. A weighted-mean ratio based on concentration or measured load should improve the prediction of total loads. C. F. Nordin, Jr., J. P. Beverage, and J. K. Culbertson, after applying sediment-transport formulas to field data for the Rio Grande in New Mexico, conclude that, although no proposed relation is satisfactory in all respects, several methods give reasonably reliable results for shallow flow in sand-bed streams. In general, the formulas which relate sediment transport to the total shear stress on the bed are unsatisfactory, because they indicate a constant concentration of bed material in transport. The formulas which relate transport to effective shear stresses yield transport rates which are low at low shear stresses and are too high at high shear stresses. These discrepancies are due to experimental conditions under which the relations were derived and to some of the basic assumptions adopted in the derivations of the formulas. H. P. Guy and D. B. Simons (2-64) conclude from flume studies that velocity and sediment-concentration distributions in a cross section can be predicted only within crude limits. Sediment discharge in a stream should be computed from a velocity-weighted concentration obtained by sampling at several points or verticals in the stream cross section. Spatial sediment concentration should be measured when information on either the actual load or amount of sediment exerting pressure on the bed is required. Theoretical and measured differences between spatial and velocity-weighted concentrations show that spatial concentrations are normally greater. H. E. Reeder has found through analysis of records collected for 11 years on the Yadkin River, N.C., that annual sediment yields in tons per square mile can be estimated for the basin above Yadkin College if annual water discharge is multiplied by 4.15 X10~4. He reports that the estimates are sufficiently accurate for design and planning purposes. Computing sediment yield from geomorphic parameters A means of estimating long-term sediment yields in the absence of hydrologic data is through a quantitative geomorphic approach. L. K. Lustig (1-64) has used this method to estimate the sediment yield from the Cas-taic watershed in California. Using six drainage basins in the San Gabriel Mountains for which long-term sediment-yield data are available, he established significant relations between sediment-yield and the following geomorphic parameters: drainage area, mean-ground slope, total stream length, bifurcation ratio, stream frequency, and channel-slope ratios. On the basis of these relations, Lustig estimated the sediment yield of the Castaic watershed to be about 250 acre-feet per year.SEDIMENTATION A185 Dissolved and suspended load in United States rivers Analysis of records of dissolved load in rivers of the United States lead W. B. Langbein and D. R. Dawdy to conclude (chapter D) that the dissolved load carried by rivers increases directly with the amount of runoff only up to about 3 inches of runoff. The load increases less rapidly in those rivers whose runoff exceeds 3 inches, and it attains a generalized maximum of 150 tons per square mile per year in rivers having a runoff in excess of 10 inches. The dissolved load carried by rivers is commonly less than the suspended load, but the proportion increases with the humidity of the climate. In dry climates, less than 10 percent of the total load may be carried in solution, whereas in humid climates the percentage may be 50 percent or more. VARIABILITY OF SEDIMENT LOADS IN RIVER The difficulties in obtaining accurate prediction of sediment loads can best be understood by considering those rivers for wThich sediment loads have been measured under different conditions. Sediment load1 in Columbia basin Obviously sediment loads will vary greatly depending on water discharge through the channel. For example, W. L. Haushild, H. H. Stevens, Jr., and G. R. Dempster, Jr., report from studies in the Columbia basin that in the Columbia River in Washington and Oregon most sediment is transported as suspended load and that suspended sediment loads ranged generally from 1 to 20 parts per million, during low and medium flow, and from 50 to 90 ppm, during high discharge. Peak concentrations as high as 2,700 ppm have been measured, following storms, in the Snake River basin. It is interesting to note, however, that the particle-size distributions of bed material did not change significantly with time or discharge at the cross sections where measurements were made. Appreciable amounts of bed material are transported only periodically in much of the area because the streams are not capable of coarse-sediment transport except during high flows. Rapid snow melt produces great load The sediment loads of rivers can show marked fluctuations depending on the antecedent moisture conditions or prewetting of the soil. An example is reported by B. E. Mapes and P. R. Boucher from Washington. On February 2,1963, the ground in eastern Washington was covered with 4 to 8 inches of snow, and was frozen. On February 4, the temperature had increased to about 60°F, and some rain fell during the period. Rapid melting of the snow occurred on February 3 and 4, and additional rain, as much as 1 inch, fell on February 4. The soil, although still frozen at depth, was saturated at the surface, and severe erosion and flooding resulted. The sediment yield following the short but intensive rainfall was 150 to 200 percent greater than that during the previous 2-day period, yet it was removed by 10 to 16 percent less runoff. The Palouse River at Hooper, Wash., transported 2.1 million tons of sediment in 31,100 acre-feet of runoff on February 5, whereas only 672,000 tons was transported by 47,300 acre-feet of runoff on February 4. Urbanization and sediment load The effects of urbanization on the sediment load of a river are clearly demonstrated in a study of the urban hydrology of the Northwest Branch of the Anacostia River in Maryland by F. J. Keller, D. H. Carpenter, and C. A. Richardson. They report that prior to the urban development in the basin the highest measured suspended-sediment concentration was 6,500 parts per million, whereas concentrations in excess of 40,000 ppm are now measured. The high sediment concentrations precede the peaks of water discharge by several hours. Timber downfall produces high sediment load P. A. Glancy reports an excessively high sediment yield from streams of the Chehalis River basin in eastern Washington. About one-quarter million tons of suspended sediment was transported from the basin by about 394,000 acre feet of discharge during 5 days, during and following the storm of November 19 and 20, 1962. The Satsop and Wynoochee Rivers contributed only 45 percent of the runoff but 88 percent of the sediment. The excessive sediment yields were attributable in part to an abnormal amount of timber downfall, resulting from a violent windstorm on October 12, 1962. Effect of confining banks on transport Sediment transport is also influenced by other variables such as channel dimensions and water temperature. Bed-material transport relations at 6 sediment stations, along a 110-mile reach of the Rio Grande in New Mexico, were investigated by C. F. Nordin, Jr., and J. P. Beverage, who found that the transport relations fell into two groups. One group represented stations with confining, or partially confining banks, and the other group represented stations without lateral restrictions. At low flows there was greater bed-material discharge at the confined sections, while at high flows there was greater bed-material discharge at the uncon-A186 INVESTIGATIONS OF PRINCIPLES AND PROCESSES fined sections. Flow characteristics were compared between pool-and-riffle and sand-bed channels. For the pool-and-riffle channel, the depth, water-surface slope, bed-shear stress, flow resistance, and median bed-material size increased with increasing water discharge. For the sand-bed channel, water-surface slope and bed-material characteristics were approximately constant, while flow resistance decreased and bed-shear stress increased conservatively with increasing discharge. Sediment transport in Sierra Nevada Sediment transport studies by R. J. Janda indicate that little sediment is currently supplied to the Middle Fork of the San Joaquin River above 5,000 feet altitude because most of the runoff results from snowmelt. Most of the gravel observed on the streambed evidently is a lag deposit. Below 5,000 feet altitude, differences in the character of the flood flows, coupled with the normal downstream increase in mean velocity, result in higher flow velocities and increased stream competence. In these reaches, boulders up to 400 mm in intermediate diameter are found in splay deposits lying on root-masses of willows. DEPOSITION It is difficult to determine in which category some of the results of sedimentation research belong. Investigation of ripples, dunes, and similar bed features are here classified as depositional studies, even though the materials involved may be in transport when the features are studied. Mathematical model to predict ripple index J. F. Kennedy (1-64) has used a mathematic model, developed during an analysis of the stability of the fluid-channel-bed interface, to predict the velocity, amplitude, and wave length of ripples formed in closed rectangular conduits and in the desert. Good agreement was also found between predicted and observed values of ripple index (ratio of length to height). Large-scale study of dunes Three types of modem dunes—barchan, parabolic, and transverse—were studied on a large scale by E. D. McKee by cutting two trenches through a typical dime of each type with bulldozers. The details of the stratification were recorded with photographs, grid plotting, and latex peels. Comparisons should ultimately be possible between the dune structures examined and the cross strata in various ancient formations, such as the Navajo and Coconino Sandstones. Wave-tank studies of ripple marks In another study reported by E. D. McKee, a wave tank was used to investigate climbing ripple marks. The results demonstrate a close interrelation between various structure types, which are commonly interpreted from well cores as resulting from different environments and contrasting processes. The following conclusions were obtained: (1) The amount of ripple climbing is controlled by the rate of sediment feeding, (2) the range in form and shape of ripple marks is determined by differences in water depth, wave length, wave speed, and grain size, and (3) the evolution of ripple type in both vertical and lateral position, within a sequence of deposits, is controlled by progressive changes in factors that determine the variety of ripple mark. Suspended sediment and fish-egg survival Studies by A. R. Gustafson of the U.S. Geological Survey and D. R. Bianchi of the Montana Fish and Game Department show that suspended-sediment discharge, stream discharge, velocity through the bed gravel, and dissolved oxygen are important factors in affecting survival of rainbow and cutthroat trout eggs. Sediment settling into a redd or spawning ground caused decreases in the permeability of the gravel and the velocity of the interstitial water. When the suspended-sediment passing over a redd reached an accumulated total of 60 or more tons, the seepage velocity showed a perceptible decrease. As the accumulated total suspended-sediment load increased progressively beyond this level, there was a corresponding decrease in the seepage velocity. Redds exposed to an accumulated load of 290 tons of suspended sediment had the highest egg mortality. Redds with the lowest suspended-sediment load, highest seepage velocity, and the highest dis-solved-oxygen concentration had the greatest egg survival. Upstream effect of barrier structures When a structure is placed in a stream channel, downstream effects can be expected, but commonly upstream effects can be measured also. G. C. Eusby reports that 3 years after construction of a barrier dam across the channel of Sheep Creek, Utah, to decrease the sediment contributed to the Paria River, no material smaller than sand was being deposited in the reservoir, and that material larger than sand was being deposited at the upstream end of the reservoir above spillway level. At the end of 1962 the dam had caused deposition of 128.9SEDIMENTATION A187 acre-feet of sediment, 32 percent of which was above spillway level. Before the dam was built, the channel gradient was about 1.63 percent. After construction, the gradient on the upper end of the sediment deposit was 0.93 percent. Storage of fine material in islands and point bars C. F. Nordin, Jr., and J. P. Beverage (3-64) find that the islands and point bars in the channel of the Rio Grande contain as much as 20 percent surficial sediment finer than 0.062 mm, which is deposited during receding flows. They conclude that temporary storage of this fine sediment, which is flushed during high flows, accounts for some of the scatter noted in discharge-sediment-transport relations. Sedimentation in Mammoth Cave C. R. Collier and Russell F. Flint (1-64) resurveyed 13 lines across passageways in Mammoth Cave, Ky., that are subject to flooding from the Green River. They determined that numerous low flows had deposited 0.5 foot of sediment in the lowest levels. However, three subsequent higher flows removed this sediment but at the same time caused thinner deposits to form at higher levels. Bedforms under varying flow conditions As the hydraulic character of flowing water changes, a significant change also occurs in the type of sedimentary features to be found on the bed of a stream. For example, R. K. Fahnestock and Thomas Maddock, Jr. (p. B140-B142) report that their studies in two 1,600-foot reaches of the Rio Grande near El Paso, Tex., show that bedforms range from dunes to a plane bed in a 100-foot-wide reach, whereas under the same discharge, dunes and prominent bars were always present in a 200-foot-wide reach. Investigation in March and August showed that the change in water temperature of about 35°F significantly affected the hydraulics of flow and bedforms. For example, at similar discharges, mean velocity was greater in March, and in the 100-foot-wide reach the bed was plane; whereas mean velocity was less in August, and large dunes developed in the 100-foot-wide reach. Flume studies of bed configuration Laboratory-flume studies by J. F. Kennedy showred that the bed configuration changed from ripples to dunes in the relatively narrow range of shear velocity of from 0.12 to 0.14 feet per second—independent of the median particle size of bed material and depth of flow. Stratification in streambed deposits Observations of fluvial stratification made in shallow trenches cut through bars near El Paso, Tex., led R. K. Fahnestock and J. C. Harms (Marathon Oil Co.) to conclude that large-scale trough cross-stratification is related to dune migration; small-scale cross-stratification is related to ripple migration; and tabular cross-stratification is related to migration of bars. All types formed in the lower flow regime. However, horizontal stratification, related to plane-bed sediment transport, is formed in the upper-flow regimes. The most significant point illustrated by their study is that stratification is the product of many complexly interrelated variables, and, for this reason, interpretations of environment from stratification in terms of single variables, such as depth, velocity, or slope are unrealistic and misleading. Regional heavy-mineral trends in Colorado Plateau R. D. Cadigan found that the regional linear trends in ratios of abundance of specific heavy minerals in the Morrison Formation of the Colorado Plateau region are controlled by three main factors, namely, (1) the size and areal distribution of source areas, (2) rate of burial of the minerals, and (3) relative rate of attrition of the minerals. Trends of decreasing abundance of certain minerals are the effects of relative rates of deposition of the minerals and the effects of losses of certain minerals, due to chemical attack by interstra-tal solutions during diagenesis. The effects of the losses may be conveniently combined in the term “attrition.” The overall effect of differential attrition on regional trends of mineral ratios is to produce reverse trends for the more resistant minerals. Loss by attrition of nonopaque heavy minerals in the Morrison Formation sediments is evidently greater for the minerals garnet and staurolite than for zircon, tourmaline, rutile, and apatite. Garnet and staurolite grains show much evidence of volume loss by solution action (etched and characteristically embayed surfaces) . The other minerals show only effects of abrasion. Although there are complicating factors of different sources, garnet and staurolite ratios show linear trend surfaces which dip northward and eastward, the “downstream” direction, which is almost opposite to trend surfaces of zircon and rutile ratios which slope southward and westward. The regional trends of the ratios of durable minerals are thus mathematically dependent on the degree of differential attrition in the less durable minerals and may, as in this instance, tend to slope upstream instead of downstream.A188 INVESTIGATIONS OF PRINCIPLES AND PROCESSES Beach and eolian sands indistinguishable at Cape Cod Studies of suites of beach and eolian sands of Cape Cod, Mass., by John Schlee, Elazar Uchupi, and J. V. A. Trumbull (chapter D) indicate that these environments cannot be distinguished locally on the basis of grain-size parameters. Evidently, factors relating to original source, in this case glacial debris, overshadow the effects of local sorting by the transporting medium. Estimating glacial-drift lithology from pebble measurements C. S. Denny and A. W. Postel (p. B143-B145) have developed a rapid method of estimating glacial-drift lithology or the proportion and size of stones of various rock types in the coarse fraction of glacial drift. One hundred pebbles are selected at intervals along a measuring tape laid on the surface of an outcrop. Surface samples selected in this manner and bulk samples of the same deposit yield generally similar results. Denny and Postel conclude that a surface sample collected by this method characterizes the stones on the surface of the till, and, provided that the proportions of the various rock types do not change at depth, the sample will be representative of glacial drift lithology. Shape factor for gravel-size fragments A new shape factor for gravel-size sedimentary particles has been developed by G. It. Alger. This factor includes the effect of surface area, which was measured using fluorometer equipment. Using this parameter, one can more acceptably model the behavior of freely falling particles of sediment. LIMNOLOGY Limnological investigations of lakes and streams contribute to an understanding of the factors controlling water composition, processes involved in transport and deposition of materials, and the use of aquatic organisms as hydrologic indicators. Data from the fields of physics, chemistry, geology, biology, and meteorology are synthesized to interpret conditions observed in natural waters. Laboratory studies, conducted under controlled conditions, also are being employed for the solution of hydrologic problems. Temperature, chemistry, and algal growth in a lake In studies of Pretty Lake, LaGrange County, Ind., J. F. Ficke and R. G. Lipscomb found a close relation between water temperature, chemical character, and algal growth. From the free-circulation condition which existed after ice breakup in 1963, the lake quickly became thermally stratified owing to rapid surface heating. Wind action erased the early stratification, and a permanent thermocline was established 3 days later. As a result, the temperature of the lake’s deepest point (82 feet) during the summer of 1963 was about 2°C higher than it would have been if the original stratification had remained. Surface temperatures ranged as high as 28°C in July and August 1963; the bottom-water temperature never rose above 8°C (in November). Specific-conductance values of 280 micromhos in the upper water and 320 at the lower level, and bicarbonate increases from 140 parts per million to 176 ppm, respectively, indicate the degree to which thermal stratification influenced chemical distribution. Silica concentrations measured in October increased with depth from 1.4 ppm at the surface to 3.7 ppm at 42 feet, with a maximum of 5.5 ppm at 67 feet, corresponding to differences in diatom growth rates at different levels in the lake. In late August when the temperature profile showed marked stratification from 22°C in the top 20 feet to less than 12° C below a 35-foot depth, with a transition zone between, algal counts were about 37,000 cells per liter, and dissolved-oxygen concentration was about 8 ppm in the warmer water. In the transition region, dissolved oxygen decreased rapidly (3.6 ppm at a 25-foot depth to zero at 30 feet), while the algal population was unusually high (92,000 cells per liter) at 25 feet and decreased to 30,000 cells per liter at 30 feet. Among the diatoms and the bluegreen algae, Cydotella (d.) and Aphanizomenon (b.g.) were the dominant forms during August. By late October the association had changed to Asterionella (d.), Gomphosphaeria (b.g.) and Aphanizomenon. At the time of the fall overturn, Cyclotella, Andbaena (b.g.) and Aphanizomenon had become the dominant forms. After the autumn circulation of water in the lake, total algae measured about 15,000 cells per liter, and the dissolved oxygen was about 8 ppm throughout the water column. Vertical density currents in Lake Zurich From published reports on the algae and varved sediments in Lake Zurich, Switzerland, and from laboratory experiments, W. H. Bradley has established that vertical density currents exist and have properties which help explain processes observed in the Swiss lake. Vertical density currents are new to hydrodynamics. Experiments show that such currents are capable of moving fine particles or microorganisms from the surface waters of lakes to the bottom as much as 55 times faster than if the particles settled accord-LIMNOLOGY A189 ing to Stokes’ law. The difference in rate of fall between those indicated by Stokes’ law and those moved by vertical density currents probably depends on the population density of the particles. Water quality of western Lake Erie Studies in western Lake Erie by G. W. Whetstone during August and September 1963, showed nearly isothermal conditions with little vertical stratification of major solutes. However, a north-south difference in solute concentration was noted in the 30-mile reach from Colchester, Ontario, to Toledo, Ohio. Dissolved-solids content ranged from 140 to 200 parts per million, with the lowest concentrations on the Canadian side. Similarly, chloride values ranged from 13 to 26 ppm with high concentrations extending over a distance of 13 miles from Toledo, and low concentrations occurring near the Canadian shore. Phosphate increased from 0.1 ppm at Colchester to 0.2 ppm at a point 12 miles from Colchester, to 0.4 ppm at Toledo. Nitrate concentrations of the lake water ranged from 0.8 to 1.5 ppm, with higher concentrations observed near the center of the lake and in Maumee Bay near Toledo. The dissolved-oxygen content of the lake water was remarkably uniform, ranging from 8.2 to 9.4 ppm. Dissolved-mineral inflow to Great Salt Lake About 2 million tons of dissolved salts are discharged by streams, canals, drains and springs to Great Salt Lake, Utah, each year. A study by D. C. Hahl and R. H. Langford confirmed results of a preliminary report by Diaz91, which revised upward the earlier estimates of dissolved-mineral inflow to the lake, and established that this annual inflow is equal to about 0.05 percent of the 4.4 billion tons of salts dissolved in the lake brine. Although this load delivered by surface streams does not take into account the mineral matter contributed by ground water, it is believed to represent about 80 percent of the total dissolved load contributed to the lake. Most of the average annual inflow of 1.9 million tons for the water years 1960 and 1961 was contributed by the Bear River and by drains and sewage canals around the lake. The Weber and Jordan Rivers and streams draining the intervening mountain front together contributed about one-fifth of the load. Springs around the lake contributed slightly more than one-sixth of the mineral load. Great Salt Lake brine contained about 24 to 28 percent by weight of dissolved solids during the 2-year “ A. M. Diaz, 1963, Dissolved-salt contribution to Great Salt Lake, Utah : U.S. Geol. Survey Prof. Paper 450-E, p. E163-E165. study (1959-61). During the last century the dis-solved-solids concentration of the brine has ranged from about 15 percent in the 1870’s when the lake stage was high, to about 28 percent in the early 1900’s and 1960’s when the lake was very low. Despite the fluctuation in concentration, the chemical character of the solution has remained practically constant over the years. Mineral transport in Great Salt Lake In the late 1950’s a causeway of permeable, quarry-run, rock fill was constructed separating the northern one-third of Great Salt Lake from the main body of brine. The fill has two culverts, each 15 feet in width, which allow free flow of brine in about the upper 10 feet of the 25-foot-deep lake. Because about 95 percent of the total inflow (about 2 million acre-feet) enters the southern two-thirds of the lake, expected brine movement should be from the southern to the northern arm. Inflow is at a peak during the spring and is relatively small during the summer months when evaporation is the greatest. Therefore, after the spring inflow has equalized between the two arms of the lake, flow through the culverts should be small during calm weather. During the fall of 1963, observations by D. C. Hahl, M. T. Wilson, and R. H. Langford showed that the upper 4 feet of water in the culverts was flowing northward, while the lower 5 feet was flowing southward. It is tentatively concluded that density differences coupled with small head differences can cause opposing flows to occur simultaneously through the fill. The study of mineral transport in Great Salt Lake is further complicated by recent observations that tributary waters and local precipitation tend to spread out on the surface for long distances before mixing with the brine. Distinctive chemical character of three lakes in Oregon Goose, Summer, and Abert Lakes, in south-central Oregon, form a chemical sequence of distinctive character, according to A. S. Van Den burgh. The three lakes occupy topographically enclosed basins and serve as long-term accumulation sumps. The dissolved-solids content of water from each of the three averages 1,000 parts per million, 7,000 ppm, and 50,000 ppm, respectively, and consists chiefly of sodium, carbonate-bicarbonate, and chloride. Calcium and magnesium, two normally abundant constituents in water, are nearly absent; only sodium, chloride, and bromide undergo long-term enrichment in the lakes. During long-term salt accumulation within the lake, most constituents of surface inflow are depleted through precip-A190 INVESTIGATIONS OF PRINCIPLES AND PROCESSES itation, alteration, biologic utilization, or other processes. The shallowness of the lakes allows thorough mixing and homogenization so that the dissolved-solids content is consistent throughout each of the three. Hence, the concentration of the water is related to the depth of water in the lakes inasmuch as the total dissolved load remains nearly constant over short periods. Effect of tree leaves on water quality In a study of the effects of tree leaves on water quality, K. V. Slack found that masses of leaf-litter in pools during low flow of autumn resulted in higher solute concentrations and greatly increased water color in the North Fork Quantico Creek, Va. Although low silicate concentrations in some pools resulted from diatom uptake, most dissolved minerals increased markedly after leaf-fall began in late September. The greatest increases occurred during October, and maximum effects were observed in pools containing the largest amounts of decaying organic material. For example, between October 3 and 27, the station with the heaviest organic load showed the following changes: calcium and bicarbonate concentrations tripled, free C02 doubled, total iron increased fivefold to 2.7 parts per million, and manganese soared from 0.1 to 4.8 ppm. Dissolved-oxygen concentrations decreased to near-zero values, resulting in a partial fish kill. Sulfate concentrations decreased during October but increased sharply when flow was restored by a rise in early November. Thereafter, manganese dropped to around 0.02 ppm, total iron to about 0.5 ppm, and sulfate to 7 ppm. These observations help explain the occurrence of a black manganese- and iron-rich coating on the rocks in this stream. The deposit occurs as a narrow band only along the center of the channel, indicating that it is a low-flow phenomenon. Leaching of manganese and iron from tree litter in shallow pools can now be assigned a major role in development of the black coating, which is not removed by subsequent high flows. Water quality related to leaves of five tree species Laboratory studies by K. V. Slack and H. R. Feltz of the effects of five different species of tree leaves on composition of natural waters indicate that maple-leaf cultures developed the greatest color and beech the least. At the end of three weeks, the following color intensities were measured: Maple, 650; tulip poplar, 600; scarlet oak, 500; dogwood, 300; beech, 50; compared with the blank which remained at 20 units. Significant changes in dissolved mineral content occurred in some species within the first 24 hours. Oak is apparently the most resistant species to the leaching effects of water, exhibiting a maximum change of 5 micromhos in 3 weeks. Both iron and manganese increased in all cultures. Total-iron concentrations were lowest in beech and highest in oak and tulip poplar cultures. Manganese was lowest in beech and dogwood and highest in oak and maple cultures. Major contributors to increased solute content are calcium and magnesium bicarbonate and sodium and potassium bicarbonate. Dissolved oxygen decreased rapidly to values near zero in all leaf cultures. Biological control of minor-element concentration In a recently completed survey of the minor-element content of waters of California, W. D. Silvey found that the percentage of minor elements was fairly uniform, even for waters draining different lithologic environments. However, as biological activity increased, the concentration of minor elements decreased, reaching a minimum in sea water. When duckweed (Lemna) was allowed to decompose in samples of American River water in the laboratory, the concentrations of aluminum, iron, manganese, and titanium increased by an average factor of 382,000. Concentrations of cobalt, copper, nickel, and vanadium increased by an average factor of 33,000 over the amounts present in the original wTater. Failure to observe large increases in minor-element concentration in natural water following seasonal die-off of aquatic plants is attributed to sinking of dead organic material, resulting in concentration of minor elements in bottom sediments, and the existence of an equilibrium between biological processes and available nutrients. It is tentatively concluded that additional nutrients released by decay increases productivity until a new equilibrium is established. Effect of forest fire on stream water Water samples from streams and springs in and near the burn area were collected immediately after a fire on about 39,500 acres in Tahoe National Forest, Calif. Contrary to expectations, no significant changes in percentages of dissolved constituents were found by C. E. Roberson and J. H. Feth, who conducted the study in cooperation with the Pacific Southwest Forest and Range Experiment Station. They concluded that future evaluation of the effects of burning on forested areas should include careful prior planning and possibly use of controlled fires on study plots.PLANT ECOLOGY A191 GEOMORPHOLOGY Paleohydrologic studies at Russell Cave, Ala. The rock shelter at Eussell Cave National Monument has been studied by J. T. Hack during reexcavation. An exposed stratigraphic series indicates a cold climate prior to 9000 before present, followed by deposition of flood deposits ending in 5500 B. P. which were rich in cultural remains. From that date to the Columbian period, roof disintegration provided an upper fill, the climatic implications of which are still being studied. Erosion rates and processes The exposure of roots of long-lived trees in the White Mountains, Calif., has been interpreted by V. C. LaMarche, Jr., (1-63) in terms of rate of slope denudation. Significant differences in denudation rate of contrasting slope types on the same lithology cannot be entirely explained by differences in slope angle. Rates and processes of hillslope erosion studied by S. A. Schumm and R. J. Chorley provide some indication of the rate of cliff retreat in the Colorado Plateau. The general scarcity of talus at the foot of major scarps appears to be caused by the relatively rapid disintegration of the fallen rock rather than by the cessation of scarp retreat in post-Pleistocene time. In a related study, R. F. Hadley has shown that slope aspect is one of the determinants of the frequency of freezing and thawing. The freeze-thaw events were 2y2 times more frequent on a south-facing slope in an area studied near Denver, Colo. This greater frequency appears to make the south-facing slope more susceptible to sheet erosion than slopes having other exposure. Slope development Various mathematical models of slope development investigated by A. E. Scheidegger appear to support the thermodynamic analogy proposed by Leopold and Lang-bein.92 Morphology of stream channels W. B. Langbein (p. B119-B122), drawing an analog from thermodynamic entropy postulates that river-channel equilibrium represents the most probable condition between two opposing tendencies. There is on the one hand the tendency for minimum total work in the stream-channel network, and there is also an opposing tendency for uniform distribution of work rate in all parts of the system. These considerations allow a 92 L. B. Leopold and W. B. Langbein, 1962, The concept of entropy in landscape evolution : U.S. Geol. Survey Prof. Paper 500-A. theoretical derivation of the exponents of the hydraulic geometry not only for the downstream case but for the at-a-station case as well in natural rivers. It further allowed the derivation of the Lacy equations for stable irrigation canals with self-formed cross sections (Langbein, 1-64). A detailed study of braided channels carrying glacial-outwash gravel has been published by R. K. Fahnestock (1-63). Hitherto unmeasured details of channel change in a braided gravel-bearing stream emphasize the rapidity of channel alterations. These alterations have both seasonal and daily fluctuations associated with changes of rate of glacial melt. PLANT ECOLOGY Plants and the hydrologic and physical environment are intimately related—plants intercept water, use it, modify its quality and its movement to streams and oceans, and affect geomorphic processes. The hydro-logic and physical environments in turn have a marked influence on the distribution and behavior of plants. Unraveling these complex interrelations will provide a better understanding of man’s environment and the processes that affect it. The role of plants as consumers of water is discussed under “Soil Moisture and Evapo-transpiration,” and of aquatic plants in hydrology, under “Limnology.” Relation between tree form and disposition of precipitation A randomly stratified sampling experiment is being conducted by M. R. Collings and R. M. Myrick to determine rainfall interception in a juniper (Juniperus osteosperma) and piny on (Pinus edttlis) woodland at Cibecue Ridge, Ariz. Using the Latin square and three-way analysis of variance as statistical techniques, the direction of the gage under the tree, distance of the gage from the center of the tree, tree species, size of the tree, size of the storm, and respective interactions were tested at the 5-percent level for significance. Their findings indicate that the compass direction of the gage from the tree trunk is highly significant, while species of juniper and piny on is not significant. A single precipitation versus interception regression may be used for both juniper and pinyon. Scrub oak (Quercus tur-binetta) and tree oak (Q. arizonica) intercept more rainfall than do juniper and pinyon trees. In vegetation-modification studies on Cibecue Ridge, Collings and Myrick found that the percent of stemflow from juniper (Juniperus osteosperma) and pinyon (Pinus edulis) trees is inversely related to tree diameter.A192 INVESTIGATIONS OF PRINCIPLES AND PROCESSES Relation of plants to soil-moisture storage An investigation by F. A. Branson, R. F. Miller, I. S. McQueen, R. S. Aro, and K. W. Ratzlaff of seven contiguous plant communities on soils derived from Bearpaw Shale in northeastern Montana revealed that differences in quantities of moisture stored and used from the different soils were related to differences of kinds and quantities of plants present. The study site is a west-facing hillslope on which the soils differ in texture, chemical composition, and degree of weathering. Plant species which characterize the communities exhibit a variety of adaptations to soil conditions. These include halophytic Nuttall saltbush, xerophytic big sagebrush, and gypsophytic wild buckwheat. Plant sampling at 2-inch intervals by the all-contacts point quadrat method across the contiguous plant communities (1,150 feet) supports the classical concept that plant communities are discrete entities. Relation of tree species to geology and hydrology Preliminary results of mapping vegetation near Washington, D.C., by R. S. Sigafoos, show that certain trees have a restricted distribution related to geology and hydrology. Some species, such as black oak, scarlet oak, and mockernut hickory, predominate in areas underlain by a schistose granitic-appearing gneiss. Other species, namely, southern red oak, post oak, and mountain laurel, are common on sites underlain by Wis-sahickon Formation but are not present on comparable sites underlain by the gneiss. Even on the flood plain of the Potomac River, where the predominant environmental influence on plants is flooding and sedimentation, certain species are limited to certain reaches. Shumard oak grows only in deep, fine-grained alluvium upstream from the tidal estuary. Shagbark hickory, which is common on flood plains and low terraces in Pennsylvania and on upland sites in the Appalachian Mountains in Virginia, is exceedingly rare along the Potomac River. Size and abundance of trees affected by flooding Quantitative studies of vegetation along a 2-mile reach of the Potomac River by R. S. Sigafoos show a high correlation between the mean size of trees and flooding. The mean basal area (cross-sectional area of the trunks) of trees not damaged by the 1948 ice jam is significantly larger than that of trees damaged by the ice and of trees that are frequently flooded. Although the mean basal area of trees that were damaged by the ice, but flooded only once in 2 years on the average, is larger than that of trees flooded more frequently, the difference is not significant. Statistical studies of vegetation mapping The percentage of sites at which a species grows (frequency) was found by J. C. Goodlett, in studies of low flow of streams in Georgia, to be related to the percent maximum basal area for that species within the region. High correlation coefficients between frequency and percent maximum basal area for tree species were computed also by R. S. Sigafoos in his quantitative studies along the Potomac River. Similar high correlations were found between the percent basal area and the percent number of stems in a plot for several tree species. Approximately 75 percent of the differences in basal area of some species is the result of differences in frequency, suggesting that mapping of vegetation based on the presence or absence of species is valid and contains a measurable error. Historic changes in vegetation patterns in the Southwest Channel area along one 5-mile reach of the Gila River in central Arizona has decreased by a factor of about nine since 1914. R. M. Turner has found that during the same period batamote (Baccharis glutinosa) has virtually disappeared from the area; it is no longer dominant at any site and occurs mainly as a narrow fringe along the edge of the channel. Seed weed (Suaeda tor-reyana) has declined by a factor of about two. The areas formerly occupied by these declining species and the areas abandoned by the channel are now covered by a dense growth of saltcedar (Tamarix pentandra), a species that apparently invaded the region after 1914. Changes in vegetation and erosion in the arid Southwest in the past 80 years are attributed by J. R. Hastings, Institute of Atmospheric Physics, University of Arizona, and R. M. Turner to be due primarily to change in climate. Historical, biological, and photographic studies show that the distributional ranges of certain species below 5,000 feet altitude are higher in elevation than formerly. The abundance of some species, notably mesquite, has increased near the center of their altitudinal range. Overgrazing by cattle is believed to be of secondary importance in explaining the changes, and fire suppression and increased jackrabbit density are considered to be insignificant factors. Growth rates of trees related to hydrologic and climatic variables Radial growth studies of trees by R. L. Phipps have shown that in discontinuous tree rings, areas of growthGLACIOLOGY A193 are arranged spirally around the trunk, and that the degree of spiralling differs both between rings and vertically within any given ring. Patterns of discontinuous or “missing” rings at various vertical levels within a tree may be correlated with certain hydrologic variables on a subseasonal basis. Vertical distribution of ring volume, even in species that do not exhibit discontinuous rings, may also be correlated with variations in certain hydrologic parameters. Preliminary analysis of data from a rich deciduous forest of southeastern Ohio suggests that ring volume of any given tree may be correlated with only certain ranges of environmental variables, and that the correlative range may vary from tree to tree. Correlation of ring widths, as measured on radial increment cores of coniferous trees, with annual precipitation has been shown by W. J. Schneider and W. J. Conover (p. B185-B188) to be of little value in inferring past precipitation in central New York. The two variables, however, are not completely independent. GLACIOLOGY Traditionally, glacial deposits in the geologic record have been used as prim a facie evidence of paleoclimates. Recent theoretical and field investigations, however, suggest that the quantitative relation between glaciers and climate is complex, and that simple generalizations are often incorrect. In order to better understand the meaning of glacier variations in terms of climatic events, studies are underway on the climatic influences on existing glaciers (expressed as the mass budget), the dynamics of flow of these glaciers, their recent variations in length and thickness, and glacier variations of the recent past. Mass budget studies of South Cascade Glacier Recent studies of the net mass budget of South Cascade Glacier, Wash., by M. F. Meier and W. V. Tang-born demonstrate that the net budget shows little relation to the traditionally used parameters of climate. Mean annual temperatures and precipitation for the budget (or hydrologic) years 1962 and 1963 were almost identical, but South Cascade Glacier showed a slightly positive net budget (+ 0.5 feet of water equivalent averaged over the glacier surface) in 1962, and a strongly negative net budget (—4.3 feet) in 1963. The difference was due to consistent differences in freezing-level altitudes during times of winter precipitation, and a period of high energy income in the fall of 1963. The two effects combined to produce marked differences in the persistency of low-albedo conditions in the two summer melt seasons. Thus it appears that glacier growth and decline is not related in any obvious way to winter precipitation and summer temperature, nor is it related to mean annual precipitation and temperature. Studies of glacier flow at Blue and Nisqually Glaciers An International Geophysical Year project on the flow of the lower Blue Glacier, Wash., by a team under the direction of R. P. Sharp, California Institute of Technology, has been continued in order to collect data averaged over several years. M. F. Meier, of the U.S. Geological Survey, a member of that team, has completed an analysis of the surface velocity and strain-rate data. This analysis clearly shows the effect of the valley walls and the curving channel on the flow pattern. Components of velocity normal to the surface relate to the net mass budget and the rate of glacier thickening or thinning. Orientations and magnitudes of the components of the strain-rate tensor agree with theoretical expectations arising from the net mass budget, the changing surface slope, and the curving flow. Analysis of a hypothetical stream sheet, of narrow width but extending from the surface of the glacier to the bed, yielded fresh insight into several problems regarding subglacial slip, englacial flow, and the general applicability of empirical flow laws. A large amount of data, spanning several decades, collected by Arthur Johnson and G. C. Giles on Nisqually Glacier, Wash., is being analysed by M. F. Meier and J. N. Johnson to determine the mode of flow of this interesting glacier, and to answer several pressing questions about the theory of glacier flow. One of these questions concerns the relation of ice velocity at a given cross section to the surface slope and the ice thickness. The Nisqually results indicate that a single-valued fiuic-tional relation does exist, but that it is not the power-law relation expected from the simple analysis used in all existing theories of glacier flow. Another pressing question concerns the velocity of slip on the bed. Indirect calculations suggest that the slip velocity is not a single-valued function of the shear stress, at least not when the shear stress is calculated by conventional formulae. Recent glacier variations Comparison of mapping of Teton Glacier, Wyo., in 1963 by J. C. Reed, Jr., (p. C147-C151) with earlier maps, ground photographs, and a map constructed from aerial photographs taken in 1954 indicates that the rate of retreat of the terminus has diminished, and that theA194 INVESTIGATIONS OF PRINCIPLES AND PROCESSES thickness of the upper part of the glacier has increased since 1954. These observations suggest that the terminus of the glacier may begin to advance within the next few years. Studies of the maximum ages of the first trees to grow on modern moraines on Mt. Rainier, Wash., by R. S. Sigafoos, E. L. Hendricks, and D. R. Crandell (D. R. Crandell and R. D. Miller, chapter D) indicate that these glaciers have been active since early in the 13th century Many glaciers have receded from a maximum advance in the last 125 years; others reached maximum extents at times ranging to as early as the middle 14th century. These advances began after deposition of an ash layer from Mt. St. Helens between 3,000 and 3,500 years ago. Presence of an ash layer more than 8,800 years old in areas just beyond the 13th-to 19th-century moraines indicates that the glaciers of Mt. Rainier were larger during the last 700 years than at any time since the end of the Wisconsin Glaciation, according to Crandell. Ages of a few trees growing in Little Ice Age cirques in the Sierra Nevada, Calif., were found by R. S. Sigafoos and R. J. Janda to be more than 300 years. This suggests that ice has not been in the cirques for at least that length of time, and that recent glacial activity in California was not contemporaneous with that on Mt. Rainier. PERMAFROST Studies of permanently frozen ground in Alaska centered around ground-water conditions below the permafrost zone and on thermal characteristics of the soil in and above the permafrost zone. Preliminary analysis of data gathered in the Copper River Basin, Alaska, since 1955 shows that permafrost in this area is in equilibrium or is aggrading under present climatic conditions. This trend is in line with observations from many other Arctic areas. T. L. Pewe (1-64), continuing his study on the distribution of ice wedges in Alaska, has classified ice wedges into three categories (active, inactive, fossil) which reflect their degree of present growth. The classification has been related to the climatic conditions of an area in which a specific category of ice wedges occurs, and it was observed that growing ice wedges are confined to areas with a mean annual air temperature of — 6° to — 8°C. or colder. J. R. Williams has completed a report (1-63) on the relation of permafrost to the occurrence of ground wTater, based on a 4-year study of published reports and on unpublished data relating to subsurface conditions. He notes that permafrost forms an impermeable barrier to recharge, discharge, and lateral circulation of ground water in Alaska north of the mountains along the Pacific Coast. Its greatest effect on ground water is in the area draining to the Arctic Ocean, where permafrost is present nearly everywhere to depths ranging from 500 to 1,330 feet. In this area, ground water in bedrock beneath permafrost in the foothills of the Brooks Range and the Arctic coastal plain is brackish or saline. In the Brooks Range, however, potable water is discharged from springs along faults cutting limestone of the Lisburne Group. Unfrozen zones in alluvium beneath large rivers are potential sources of large supplies of ground water. Even though the alluvium beneath small streams may be perennially frozen, it is possible to develop a year-round aquifer in the alluvium by thawing the permafrost and by retarding the penetration of seasonal frost. Methods of developing a shallow alluvial aquifer beneath Selin Creek near Cape Lisburne include stripping the vegetation and upper few feet of alluvium, circulating water warmed in a reservoir through the alluvium by pumping infiltration galleries downstream, and erecting snow fences to retard penetration of winter frost. In the area between the Brooks Range and the Pacific coast ranges, even though permafrost is as much as 600 feet thick, it is broken by unfrozen zones through which ground water can circulate and be recharged and discharged. Ground water is readily available in alluvial deposits of flood plains, low terraces, and alluvial fans, and to a lesser extent in glacial deposits, beaches, and bedrock. Salinity of the water is a problem in coastal plains and in the Copper River lowland. Permafrost in this region is generally less important than the geologic factors which affect the occurrence of water. Studies of the water well drilled in the Kuskokwim delta near Bethel, Alaska, which obtained potable water beneath 603 feet of permafrost, were continued by A. J. Feulner and R. G. Schupp (chapter D). This is the greatest thickness of permafrost known to be penetrated by a producing water well in Alaska. At the time of temperature determinations the water averaged — 0.1°C. within the disturbed portion of permafrost and 0.7°C. in the water-bearing zone beneath permafrost. Similarity of this water to that from the Kuskokwim River suggests that at least part of the recharge may come from the river. A fragment of wood presumed to have come from just below the base of permafrost at a depth of 603 feet has been dated as older than 34,000 years by the C14 method.LABORATORY AND FIELD METHODS ANALYTICAL CHEMISTRY Manual of systematic analysis of silicate rocks L. C. Peck (1-64) has prepared a manual that presents complete directions for systematic analysis of silicate rocks and minerals by conventional methods. Many refinements of the classical methods of rock analysis and solutions of special problems have been included, based on 20 years of experience in making precise analyses on a production-line basis. Particular emphasis has been given to illustrations and descriptions of special equipment. These should aid those chemists who are involved in establishing a similar operation in this specialized field. Clay membrane electrodes Clay minerals such as montmorillonite and illite can be compacted with pressure into cation-sensitive membrane electrodes which are analogous electrochemically to glass electrodes. Details for the construction of a clay compaction press and the use of clay membrane electrodes in ion-exchange studies were presented by B. B. Hanshaw. The electrical potential developed between a clay membrane electrode and a reference electrode in contact with certain solutions of monovalent and divalent ions is given by an adaptation of the Nemst equation. From measurements of the electrical potential, the free energy of reactions or exchange constants for a series of reactions between various cation species were obtained. These determinations indicate that compacted clays prefer monovalent over divalent cations. An arsenazo-lll method for trace amounts of thorium A new spectrophotometric reagent for thorium, ar-senazo-III, developed by the Russian chemist, S. B. Savvin, was applied by Lillie Jenkins and Irving May to determine thorium in rocks and minerals in the parts-per-million range. They have modified the method by the addition of separations to take care of interferences by zirconium, titanium, niobium, calcium and the rare-earth elements. Employing arsenazo-III instead of the conventional reagent, thoron, increases sensitivity 5 to 6 fold and at the same time cuts analysis time by half. The increased sensitivity enables the analyis of smaller samples than was possible previously. Results on 37 determinations on granite, sample G-l, average 52 parts per million, the same value as for the conventional thoron method; 14 determinations on diabase, sample W-l, average 2.6 ppm, compared to 2.4 ppm by thoron. Use of the statistic chi-squared in evaluating analyses F. J. Flanagan (p. C157-C158) suggests the use of x2 for evaluating objectively the results of a chemical analysis if there is available a well-analyzed sample like G-l whose population means and standard deviations are known. The differences between the analyst’s values and the means of the analyzed sample are divided by the standard deviation to form standardized normal deviates. The sums of the squares of these deviates follow the x2 distribution. This enables one to use published tables of x2 at a specified probability for the objective evaluation. The technique is useful in any field for which the data on a well-analyzed standard are available. Determination of fluorine in silicate rocks Fluorine determinations on silicate rocks, once rarities, are now routine. To meet increased demands, L. C. Peck and V. C. Smith have developed a faster and more accurate spectrophotometric method. Difficulties with previous methods based on fluoride bleaching of thorium or zirconium lakes, such as instability of the lakes and the necessity for close control of pH, were eliminated by using a water-soluble chelate system, Zr-SPADNS, at an acidity high enough for the system to be insensitive to appreciable changes in acid concentration. The sample is sintered with a flux consisting of Na2C03, ZnO, and MgC03. After leaching the melt and filtering to remove the alumina and silica retained in the insoluble, fluorine is separated from the filtrate by distillation from sulfuric acid solution at 135°C. The Zr-SPADNS reagent is then added to an aliquot of the distillate to prepare the color system for spectrophotometric measurement. The range of concentration covered is from 0.005 to 2.0 percent fluorine. Oxygen sheath for flame photometry An oxygen-sheathed burner for flame photometry produces a hotter and more stable flame than does the A195A196 LABORATORY AND FIELD METHODS normal burner, resulting in increased sensitivity and higher precision for some elements. Irving May, J. I. Dinnin, and Fred Rosenbaum (p. C152-C153) have constructed and tested an oxygen sheath for the atomizer-burner of the Beckman flame photometer. This unit is simpler, more convenient, and very much less expensive than the sheath which is currently available commercially. Of the elements tested (K, Li, Rb, Cs, Mg, Ca, Ba, and Mn), increased sensitivity by factors of 2 to 5 were obtained for Ca, Li, Mn, and Ba. Pierre Shale analyses L. F. Rader and associates have completed an analytical study of 151 samples of Pierre Shale submitted by H. A. Tourtelot. The average content of various elements determined is as follows: Total carbon is 1.17 percent (consisting of mineral carbon, 0.42 percent, and organic carbon, 0.68 percent). Trace metals, in parts per million, are: V, 114; Cu, 22; Zn, 81; Pb, 24; As, 8; Mo, 2; and Se, 0.8. Sulfur content of samples G-l and W-l I. C. Frost and J. A. Thomas determined total sulfur in granite, sample G-l, and diabase, sample W-l, using the Leco high-temperature induction furnace and automatic titration method. The average of 17 runs on 3 different bottles of G-l is 74 parts per million S, with a median value of 78 ppm S. For W-l the average for 15 runs on 3 different bottles of sample is 124 ppm S, with a median value of 130 ppm S. The value for G-l agrees with that reported by Ricke but that for W-l is almost 100 ppm less than his value. Microdetermination of platinum metals and gold A combination of conventional fire assay, ion exchange, and emission spectrographic techniques was developed by Dwight Skinner, P. R. Barnett, Claude Huffman, and L. B. Riley for the separation, concentration, and quantitative determination of micro amounts of platinum, palladium, rhodium, and gold in rocks and mineralized samples. The silver bead produced by a conventional fire assay is dissolved, and its content of precious metals collected onto an anion-exchange resin. A small amount of silica is added to the resin and the mixture is ignited. The resulting siliceous residue is then spectrographed. Routine limits of detection are 0.001 ounces per ton (0.03 parts per million) for Pt, Au, and Rh, and of 0.0003 oz per ton (0.001 ppm) for Pd. Replicate analyses of an oxidized copper ore and a chromite-dunite ore indicate acceptable reproducibility. Semimicro procedure for ferrous iron The detailed procedure of a semimicrovolumetric method for determining ferrous iron in nonrefractory minerals was published by Robert Meyrowitz.93 The sample (25-100 milligrams) is decomposed by heating with hydrofluoric and sulfuric acids, and the decomposition mixture is added to excess standard potassium dichromate. The excess dichromate is titrated with standard ferrous ammonium sulfate in the presence of phosphoric acid, using sodium diphenylaminesulfonate as indicator. Determinations of the FeO content of various silicate minerals by this semimicroprocedure are in satisfactory agreement with those by standard macroprocedures. Ion-exchange separation of tin from silicate rocks Claude Huffman, Jr., and A. J. Bartel (chapter D) have developed an ion-exchange separation of microgram amounts of tin from silicate rocks, which reduces the separating time by a factor of about four as compared to the familiar hydrobromic-hydrochloric acid distillation procedure. Tin is absorbed on an oxalate-form, anion-exchange resin from a hydrochloric-oxalic acid solution and is eluted with 1M H2S04. The tin in the eluted solution is concentrated by a carbonate-chloroform extraction and oxidized to bring it into water solution by wet-ashing with HN03, H2S04, and HC104. The tin is then determined fluorimetri-cally with flavanol. Using a 2-gram sample, the lower limit of detection of tin is about 2 parts per million. Microdetermination of magnesium Robert Meyrowitz (1-64) completed work on the direct spectrophotometric microdetermination of large amounts of magnesium with Clayton yellow, in small samples of silicate minerals. The precision of duplicate determinations is about 3 percent of the amount present, about the same as that given by other microprocedures. The common rock-forming elements do not interfere. It is feasible to determine, without separations, as little as 0.5 percent MgO on 2 milligrams of sample. High-temperature and high-pressure decomposition of refractory minerals High-temperature, high-pressure acid decomposition of refractory minerals is of particular value for determining alkali elements and for decomposition in non- 93 Robert Meyrowitz, 1963, A semimicroprocedure for the determination of ferrous iron in nonrefractory silicate minerals : Am. Mineralogist, v. 48, nos. 3-4, p. 340-347.OPTICAL SPECTROSCOPY A197 oxidizing atmospheres, as in determining ferrous iron. The efficiency of high-temperature attack of refractory minerals with hydrofluoric acid has been studied by others using teflon-lined bombs. Irving May, J. J. Rowe, and J. F. Abell designed a platinum-lined Morey bomb which was built by R. E. Letner. The bomb has a removable nichrome-cased S^-milliliter platinum crucible and has been used with no failures of the seals at temperatures up to 450°C and pressures estimated at 6,000 pounds per square inch. Complete decomposition by hydrofluoric acid was obtained with garnet, beryl, chrysoberyl, phenacite, sapphirine, and kyanite. Samples with a high aluminum content formed difficultly soluble aluminum fluoride precipitates. Studies are being made on determining silica spectrophotometri-cally after a hydrofluoric acid decomposition in the bomb. Analysis of new or unusual minerals R. E. Stevens, in collaboration with R. J. P. Lyons, Stanford Research Institute, deduced from infrared absorption spectra that some beryl contains hydroxyl groups, contrary to previous understanding. Hydroxy end members comprise less than 10 percent of the composition of 12 beryl samples analyzed by Stevens. Inclusion of the hydroxy end members in the formulation accounts completely for the composition of the analyzed beryls. A microchemical analysis of a new vanadium garnet with the unusually high vanadium content of 18.3 percent. V203 was made by Robert Meyrowitz. A new hydrated copper-iron arsenate from Majuba Hill, Nev., was also analyzed by Meyrowitz. Unusual minerals analyzed by B. L. Ingram include: a new rare-earth carbonate, mckelveyite; a rare-earth calcium titano-silicate; a new uranium arsenate; and a leucophosphite from Brazil with a low potassium content (0.75 percent KzO) and a high ammonium content (2.4 percent (NH4)20). An interesting chromite was analyzed chemically by J. I. Dinnin. A summation of less than 100 percent was first obtained, indicating the presence of some element not looked for. H. W. Worthing found more than 5 percent zinc spectrographically, and this was corroborated by quantitative X-ray fluorescence analysis by H. J. Rose, Jr. Four samples of the new mineral, mcallisterite, 2MgO-6B203-15H20, from Furnace Creek, Calif, were analyzed by Angeline Ylisidis. Posnjakite, a new basic copper sulfate, Cu4S04 (OH)e H20, was analyzed by Laura Reichen. Also analyzed by her was a hydrous magnesium borate, preobrazhonskite, from the Inder Deposit, U.S.S.R. A semimicroanalysis by Robert Meyrowitz, in collaboration with Mary Mrose, established the composition of the mineral kolbeckite to be ScP04'2H20. Kolbeckite was originally reported by others to be a hydrated silicate-phosphate of aluminum, beryllium, and calcium. Mrose thought the major cation to be scandium instead of aluminum. By experimentally testing the 8-quinolinol procedure used by the original authors, Meyrowitz also proved that if one were not aware of the presence of scandium, its behavior in the analysis would lead this element to be reported as aluminum and beryllium in the same ratio as originally postulated. OPTICAL SPECTROSCOPY Determination of rare-earth elements In a study of allanites from Mt. Wheeler, Nev., by D. E. Lee and Harry Bastron, rare-earth analyses give supporting evidence that a satisfactory complete analysis can be made with spectrographic methods. Some interesting rare-earth data were obtained on the allanites, pointing to an astonishingly complex history of fractional crystallization. That fractional precipitation plays a dominant role in determining the concentration of the rare-earth elements was suggested by Murata and others,94 95 who proposed as a numerical index of the stage of fractionation, sigma, the quantity (La + Ce + Pa) expressed in atomic percent of total rare-earth elements. In samples from various localities they found sigma to range from 58 to 87 in monazite (26 samples), 61 to 87 in allanite (3 samples), 63 to 82 in cerite (3 samples), and 81 to 95 in bastnaesite (8 samples). The range of 62 to 81 for sigma, found by Bastron, for allanites from Mt. Wheeler shows an extremely wide variation in the extent of fractionation for a single location. The highest sigma values were obtained where limestone instead of quartzite is the country rock. Determination of lithium by direct-reading spectroscopy The direct-reading spectrometer was used by Sol Berman to determine lithium in biotite, feldspar, hornblende, plagioclase, and quartz. The Li 6707.84A line was the only one strong enough to record directly in the 94 K. J. Murata, H. J. Rose, Jr., and M. K. Carron, 1953, Systematic variation of rare earths in monzonite : Geochem. et Cosmochim. Acta, v. 4, p. 292-300. 05 K. J. Murata, H. J. Rose, Jr., M. K. Carron, and J. J. Glass, 1957, Systematic variation of rare-earth elements in cerium-earth minerals : Geochem. et Cosmochin. Acta, v. 11, p. 141-161.A198 LABORATORY AND FIELD METHODS concentration range required. The strong reversal of this line with increasing lithium concentration, which has always been a problem with photographic methods, is also a special problem for direct reading. Such reversal is easily recognized on a plate and is corrected for by resorting to a line-width measurement rather than a line-blackness measurement. For direct-reading analysis with the customary 0.1-mm exit-slit width set dead center on the line, there is at first an increase in integrated line intensity and then a decrease as the concentration of lithium increases. Thus the same value of integrated-line intensity can be obtained from two very different lithium concentrations. By replacing the exit slit with one that is much wider, 1 mm, the entire broadened line can be measured. With an IP28 photomultiplier tube used as the detector, an analytical curve was obtained having integrated values continuously increasing from 0.0001 to 2 percent lithium. The slope between 0.02 and 0.4 percent is poor, but it is close to unity above 0.4 and below 0.02. Lithium can be determined with excellent precision between 0.0001 and 0.02 percent with assurance that a sample high in lithium content will not be misinterpreted as one in the low range. X-RAY FLUORESCENCE ANALYSIS Determination of major elements H. J. Rose and Frank Cuttitta continued the development in Washington, D.C., of combined X-ray-fluorescence-chemical methods for the total analysis of rocks and minerals. Two objectives have been stressed in the X-ray fluorescence work—determinations that are time consuming or unusually difficult to perform by chemical methods, and determinations to be made on samples limited to semimicro size. To date, columbite, tantalite, allanite, epidote, microlite, rutile, ilmenite, magnetite, sphene, amphibole, mica, and tektites have been analyzed successfully with sample sizes of 25 to 50 milligrams. In a special application, 21 sulfides were completely analyzed for the elements Cu, Ag, Fe, Sb, As, and S on only 15-mg samples. A similar X-ray fluorescence laboratory has also been set up in Menlo Park, Calif., by W. W. Brannock, who with A1 Bettiga and Leoniece Beatty, have analyzed olivine, garnet, amphibole, pyroxene, pumpellyite, and omphacite. Determination of Rb/Sr ratios A simple method for determining Rb/Sr ratios useful for guiding geochronologists in the selection of samples likely to yield meaningful data for age calculations was developed by H. J. Rose. Determinations can be made in approximately a 3-minute scan of the ground materials. No effort is made to control particle size, and a simple measurement of peak heights is all that is required. The X-ray method seems potentially useful down to at least 10 parts per million, and with refinements, perhaps to 1 ppm. Comparison of X-ray determinations with those of the isotope-dilution technique shows surprisingly good agreement, as indicated below, when the simplicity of the X-ray method is considered. Rb/Sr, Rb/Sr, by by X-ray isotope-dilution technique technique Shale___________________________ 0. 8 0. 76 Do__________________________ .5 .65 Graywacke_______________________ .3 .22 Do................................17 .14 Slate.................................10 .08 Do-......................... 5. 6 6. 0 Determination of Cl, Br, and I Because of similarities in chemical properties, Cl, Br, and I are very difficult to determine chemically in a sample containing all three elements, especially if the available sample is small. H. J. Rose had devised a simple X-ray fluorescence method that allows determination of as little as 0.05 percent of each element in a single 10-milligram sample. Samples and standards are ground to a fine powder and spread as thin layers on scotch tape before X-ray excitation. Excluding the time required for the preparation of standards, the 3 halogens were determined in 6 tourmaline samples in about 30 minutes. Several weeks would have been required to make these analyses by chemical methods. Routine rock analysis for major elements With the establishment by Isadore Adler, H. J. Rose, and Francis Flanagan of the basic X-ray fluorescence method for determining major elements in rocks and with the acquisition of a 10-channel X-ray quantometer, X-ray methods have largely replaced or supplemented wet methods for rapid rock analysis. Experience indicates that about 350 determinations per man per week are realized by the X-ray method, compared to about 100 determinations per man per week by “rapid” chemical means. Na, H204, C02, and state of oxidation of iron must still be determined by wet chemical methods at present. By substituting cerium oxide for lanthanum oxide as a heavy absorber, Leonard Shapiro has modified the preparation of pellets for X-ray fluorescence analysis so that magnesium can be determined with better ac-PETROGRAPHIC TECHNIQUES A199 curacy than was previously possible. The lower solubility of cerium oxide in the lithium borate melt requires that the melt be ground and remelted. The extra fusion step results in a more uniform powder than with a single fusion and is well suited to routine handling, as less care is required for a satisfactory pellet. Several other improvements in the method were made in the course of adapting the procedure to the quantometer. An attachment was added to convert automatically the chart intensities to printed concentrations. A recycle timer was also added to allow the quantometer to repeat its integration cycle and print the results as often as desired according to a pre-set schedule. New detectors were installed to replace gas-flow types previously used, without sacrificing sensitivity or stability. The manner in which a powdered sample is spread on a bed of boric acid prior to pelletization influences the results, and this source of variation was minimized by a simple sample spreader designed by Shapiro. A 50-milligram sample in y2 gram of fusion mixture can now be spread uniformly to yield satisfactory replicate analyses. ELECTRON MICROPROBE STUDIES Pyrrhotite-sphalerite phase studies The application of the electron microprobe by Isadore Adler to analytical problems in phase studies by P. B. Barton (Adler and Barton, 1-64) has aided in making a nearly complete extraction of useful information from earlier pyrrhotite-sphalerite runs in the Fe-Zn-S system for temperatures between 580°C and 850°C. The microprobe performance has exceeded expectations to the extent that the results are considered equal to, or better than, X-ray diffraction for determining the FeS content of sphalerite. The microprobe precision is about 2 percent of the absolute Fe content (but no runs less than 10 percent FeS have been evaluated). There is good agreement between the X-ray and microprobe results up to 30 percent FeS. Because of third-dimensional uncertainties in samples with higher FeS content it is often necessary to measure 10 or more grains in each section to rule out unwarranted values. Mineral analysis Cynthia Mead analyzed three minerals for Mary Mrose: gerstleyite from the Kramer borate deposit, Kern County, Calif., a pulszkyite-like mineral from Salida, Colo., and a yellow-green monoclinic mineral from Majuba Hill, Nev. Probe analysis showed the gerstleyite to contain more than 50 percent Sb, major S, and a small amount of Ag; the pulszkyrite, major Zn and Cu, and probably a small amount of S; and the yellow-green mineral, Fe, Cu, and As. The latter also contained numerous angular inclusions of quartz. A strontium-bearing barite from Richelsdorf, Germay, contained 11 percent SrO. A preliminary eleotronprobe analysis by Cynthia Mead of a possible new strontium-niobium mineral was reported. The sample, a small veinlet in a pyrochlore crystal from the Museum zone, Mbeya carbonatite, Tanganyika, is characterized by a higher reflectivity and a lower polishing hardness than the adjacent pyrochlore. It has a locally zoned texture and is nearly colorless. Its powder pattern does not match any known mineral. Quantitative electron probe analysis indicated 52 percent Nb and 14 percent Sr. Mineralization of blood vessels Some very interesting work has been carried on by A. J. Tousimis, of George Washington University, using the Geological Survey electronprobe and some of the experimental facilities at the Walter Reed Institute of Research. Among other things, Tousimis has been studying the hardening and mineralization of blood vessels. Examination of electron-opaque deposits found in the elastica of the vessel walls revealed a periodic deposition of both calcium and phosphorus within the vessel wall and specifically in the elastica. Quantitative electronprobe analysis revealed a Ca/P weight ratio of 2.18 within the mineralized portion of the blood vessel, suggesting the presence of apatite. This was confirmed by X-ray and electron diffraction. Hydroxyapatite was also found in the experimentally mineralized rat aorta, in a malignant tumor of the human eye (retino-blastoma), and in bones of a normally growing guinea pig. PETROGRAPHIC TECHNIQUES Hexanol as a wetting agent in mineral separations Theodore Botinelly has developed a useful technique, using hexanol for separating some sulfides and native metals from admixed silicates with comparable densities. Apparently the sulfides are wetted by hexanol and other alcohols, whereas the silicates are not. The higher alcohols are immiscible with, and lighter than water. A 1 to 9 mixture of hexonol and water is vigorously shaken with the silicate-sulfide mixture. Hexanol coats and wets the sulfide grains, giving a composite body which has a density less than water and which then floats to the hexanol-water interface. The 746-002 0-64-14A200 LABORATORY AND FIELD METHODS method requires further development for general use but has already been successfully employed on many common sulfides and on native copper and iron. Use of centrifuge in heavy-liquid separations Robert Schoen and D. E. Lee (p. B154-B157) have developed a laboratory procedure whereby routine separations of mineral particles as small as 10 microns are possible. The method, which is applicable to finegrained igneous rocks, hydrothermally altered rocks, and sedimentary rocks not ammenable to treatment by normal separation methods, depends on the centrifuging of fine fractions in heavy liquids. The flocculation which normally hinders or prevents satisfactory sink-float. methods of mineral separation in fine-grained materials is avoided by very rapid application of centrifugal force before flocculation occurs. Inexpensive fruit dye used to stain plagioclase R. V. Laniz, R. E. Stevens, and M. B. Norman (p. B152-B153) have successfully developed new procedures for sequentially staining K-feldspar yellow with cobaltinitrite, and plagioclase red with the inexpensive fruit dye F. I), and C. No. 2 (amaranth). The method is applicable to rock slabs, thin sections, and mounted sand grains. Although the amaranth strain is not specific for plagioclase it may be used conveniently, as other minerals can be distinguished by the hue and depth of the stain. The new staining technique has a distinct advantage over the potassium rhodizonate method in that, the fruit dye is inexpensive and can be obtained from many dyestuff distributors. GEOCHEMICAL AND GEOBOTANICAL EXPLORATION Mercury detector developed Instrumentation has been developed by W. W. Vaughn and J. H. McCarthy, Jr., (chapter D) for the determination of submicrogram amounts of mercury in rocks, soils, and gas. The technique is based on the principle of atomic absorption spectroscopy. An analog signal, produced by absorption of ultraviolet light by mercury vapor, is converted to digital form, resulting in a very sensitive and reliable means of measuring mercury vapor. Although the method is very simple in theory, elimination of interfering substances such as particulate matter and organic gases that also absorb ultraviolet light has been a difficult problem. In practice, mercury is volatilized by heating a rock or soil sample, and the mercury vapor separated from interfering constituents by selective absorption on gold. Heat- ing of the gold releases the absorbed mercury, which then passes through the sensing chamber where it is measured. About 5 nanograms (0.005 micrograms) of mercury can be reliably measured; thus 5 parts per billion of mercury can be determined using a 1-gram sample. New method for determining mercury in vegetation F. N. Ward and J. B. McHugh have developed a spectrophotometric technique (chapter D) for determining small amounts of mercury in vegetation. The method is based on the reaction of mercury with dithi-zone after sample dissolution by wet ignition under reflux. The technique is useful for determinating as little as 0.4 part per million of mercury in dry vegetation, which is sufficiently precise for biogeochemical prospecting. Metal content of stream sediments in west-central Maine E. V. Post has studied, by means of colorimetric and spectrographic analyses, stream sediments from 5,000 square miles of glaciated terrane in west-central Maine. The metal content of the stream sediments reflects the metal content of underlying bedrock that ranges from granite to gabbro, and from politic slate to meta-volcanic rocks. Data obtained suggest that the southwestern part of the Katahdin granite batholith is relatively rich in metals such as Mg, Fe, Co, Cu, Zn, Ni, and V as compared to the remainder of the pluton. On the whole, samples of stream sediment collected over granites in west-central Maine are deficient in Ca, Cu, and V, and contain more than average amounts of Co, Cr, and Pb when compared with abundances of these elements in granites of the earth’s crust. Similarly, sediments collected over politic slates of Devonian age are deficient in Ca, Mg, Co, Cu, Pb, Ni, and V, and are above average only in Cr. Sediments collected in terrane underlain by Ordovician metasedimentary and metavolcanic rocks contain about average amounts of Cu, above average amounts of Cr and Pb, and are deficient in Ca, Mg, Co, Ni, and V. Metals in bedrock, soils, and plants in Idaho In a geochemical prospecting investigation in southeastern Idaho, F. B. Lotspeich and E. L. Markward (1-63) studied the interrelations among the metal content of (1) bedrock (Phosphoria Formation), (2) an overlying colluvial soil of extraneous origin, and (3) vegetation growing in the soil. Iodine content of Spanish-moss studied Spanish-moss plants growing at varying distances from the ocean were sampled by H. T. Shacklette, andANALYSIS OF WATER A201 their iodine content was determined by M. E. Cuthbert. As these plants have no soil connections, they must get all their elements from the atmosphere, yet they have about the same range in iodine content as do typical soil-rooted plants in Wisconsin. This relation raises the question of just how much of the iodine content of soil-rooted plants comes from the soil and how much is obtained from the air. This matter of source of iodine is an important consideration where vegetation analysis is used to outline regions of iodine deficiencies and also in attempting to relate iodine content of bedrock to the iodine content of the soils derived therefrom. Variations in blueberries growing over uranium deposits Field observations made by H. T. Shacklette®6 of fruit variation on low blueberry plants (Vacciniurn uliginomm L.) which grew over uranium (pitchblende) deposits in the Northwest Territories, Canada, suggested that whole plant populations varied greatly from the normal in fruit size and shape. The areal extent of this variation intensity was confined to the ore outcrops or suboutcrops. Comparisons with fruit morphology of this species grown in widely separated arctic and subarctic Alaskan locations showed these described fruit variations to be rare elsewhere. It was the areal intensity of the aberrant variations, not individual variations themselves, that was of the greater significance in delineating the underlying ore bodies. Chemical analysis of tree rings dates major soil changes Field studies by H. T. Shacklette (1-63), in the lead-zinc district of Grant County, Wis., of American elm trees flooded by mine and mill tailings showed that increased zinc and phosphorus in the wood marked the year when this flooding occurred. The date when the tailings settling basin causing the flooding was put in use was known, and portions of wood that were formed both before and after this date (as determined by treering count) were sampled and analyzed chemically. Chemical analysis of tree rings may be a useful technique in dating a pronounced change in the chemical nature of the soil. In geochemical prospecting it is important to know if a soil chemical anomaly is caused by a naturally occurring element concentration or by manmade soil contamination; if the date of this increase in element content can be fixed, it may be possible to determine the source. Use of citiate-soluble cobalt in prospecting F. C. Canney reports that patterns of citrate-soluble 06 H. T. Shacklette, 1963, Field observations of variation in Vacciniurn uliginosum L. : The Canadian Field-Naturalist, v. 76, p. 162-167. cobalt in stream sediment in Maine appear to be a useful guide in prospecting for ore deposits associated with mafic intrusive rocks. Fern bush found to have high antimony content A collection of 13 samples of fern bush (Chamae-batiaria, millefolium [Torr.] Maxim.) from the Egan, White Pine, and Schell Creek Ranges, Nevada, has been analyzed for antimony and other constituents. The antimony ranges from 8 to 200 parts per million in the plant (not ash). The distribution of this and related plants, which are widespread from the Sierra Nevada to the Great Basin in the Transition zone, suggests that analyses of antimony in this plant may be useful in prospecting. ANALYSIS OF WATER The growing importance of pesticides and other organic compounds as water pollutants is reflected by the increased attention given to development of methods for their identification and quantitative determination. Analysis of organic pesticides An extremely sensitive method for determining organic pesticides developed by Garland Stratton makes possible the measurement of concentrations on the order of 1 part per billion. The pesticide materials are extracted from 5 to 10 liters of water with an equi-volume mixture of ethyl ether, petroleum ether, and benzene. After “clean up,” the extracting solvents are evaporated and the residue is redissolved in 1 milliliter of acetone to make a sample concentrate. Microliter aliquots of the concentrate are then spotted on chromatographic paper, and organophosphates, chlorinated compounds, ureas, triazines, and carbamates subsequently are identified by a series of chromogenic reagents. After group identification, individual compounds within each group are determined from Rf values obtained by inverted-phase paper chromatography. Quantitative estimates are based on a comparison of the densities of spots from samples and from standard pesticide solutions. Although the method is very sensitive, the precision is inadequate for many purposes. A multichamber apparatus for the continuous liquid-liquid extraction and concentration of pesticides, including aldrin, dieldrin, and endrin, was reported by C. H. Wayman and Lloyd Kahn. The multichamber arrangement permits evaluation of extraction efficiencies of individual components.A202 LABORATORY AND FIELD METHODS New effluent collector for use in gas chromatography Certain extracted organic pollutants may be separated by gas chromatography. In collecting gas chromatographic samples, however, contamination of one component by another can occur in the effluent line and at the effluent port, particularly if several closeboiling components are involved. The substrate from the analytical column may also condense and accumulate in the effluent line. To avoid these difficulties, D. F. Goerlitz and W. L. Lamar (1-64) have designed a special effluent collector which permits isolation of pure gas chromatographic samples. The apparatus provides an individually complete assembly for the collection of each component very near the end of the analytical column. The collector is always maintained in its own heat sink. The condensing surface can readily be washed with a small amount of solvent, and a thickened glass section magnifies and pockets the sample. The collector can be completely sealed to prevent contamination by moisture during cool-down or waiting periods. The apparatus also enhances an analytical technique, developd by the authors, wherein the components are individually collected and reinjected into a different chromatographic column to obtain two characteristic retention volumes for each component. Organic carbon The total organic-carbon content of certain surface-water samples has been measured by Eugene Brown and Y. A. Nishioka by complete combustion of 20 microliters of the sample in a stream of oxygen and measurement with an infrared analyzer of the carbon dioxide formed. Solid glass pH electrodes A solid glass hydrogen-ion-sensitive electrode capable of withstanding high hydrostatic pressures has been fabricated by B. B. Hanshaw. A self-pressurizing reference electrode has also been developed. (See also “Experimental Geochemistry, Ion-Exchange Phenomena.”) HYDROLOGIC MEASUREMENTS AND INSTRUMENTATION During the year, further adaptations of the digital water-stage recorder were made for the recording of hydrologic data other than stage data; progress was also made on adapting it to multi-parameter recording. Instrumentation for recording data at remote locations was developed. Much progress was made on improving existing equipment for better field-data collection. Digital recorders are now installed at more than 1,500 gaging stations. Digital-punch gage applications R. M. Myrick and M. R. Collings have adapted the Fisher-Porter digital-punch recorder for recording rainfall concurrently with stream stage on small drainage areas in Arizona. Digital-punch gages are worked in pairs from the same clock modified to furnish 1-min-ute punching impulses. The precipitation gage uses a 12-inch catchment funnel and 6-inch stilling well with the gear train modified to punch to the nearest 0.01 inch of rain. The streamflow recorders work from a prerated critical-depth flume equipped with a 6-inch well. E. B. Boyd has also used pairs of digital-punch recorders for concurrent recording of stream stage and rainfall on an urban runoff project in Tennessee. H. C. Beaber reports the successful use of a pair of digital-punch gages for recording river stage at ends of a slope reach on the Nolin River, Ky. Use of digital records and the digital computer eases the task of computing discharge on the basis of river slope and river stage. A design for a battery-operated conductivity and water-temperature digital-punch recorder has been completed by G. F. Smoot. A selected number of conductivity cells and temperature probes may be automatically sequentially switched to a servo-balanced alternating-current bridge, which, as it comes to null, also positions the digital recorder. Battery life is longer than in conventional conductivity recorders, since no current flows except immediately preceding and during the punch-out cycle. Digital recorders and computer techniques The techniques for automatic recording and processing of basic streamflow data using paper-tape punching devices at gaging stations and a digital computer for processing of the data have undergone important improvements in the last 3 years, according to W. L. Isher-wood. These improvements have been mostly in the processing technique; the field instrumentation has undergone only minor refinement. Translation of the paper tapes punched by digital recorders from parallel-coded form into serially coded form for acceptance by the digital computer is now done by an offline paper-tape to magnetic-tape translator rather than by a paper-tape to paper-tape translator. This allows speeding up the rate of data input to the computer by a factor of 20. Computation of mean daily discharges is now doneHYDROLOGIC MEASUREMENTS AND INSTRUMENTATION A203 for each day at the time the gage-height data first enters the computer, rather than at the end of the year. Data for a given station are submitted at about 3-month intervals. At the time the initial computation of daily discharges is done, a summary of the data for each day is printed for use by the field office operating the station. This summary lists maximum, minimum, and mean gage heights, effective mean gage height, mean discharge, corrections used, and bihourly gage heights for each day. The list of bihourly gage heights, previously unavailable without considerable manual work, has been found very useful for making detailed studies of the pattern of stage changes. Printing of tables of daily discharge on the computer for use as camera copy for publication is now fully operational. Sediment sampling The U.S. Atomic Energy Commission has contracted with Parametrics, Inc., to develop a nuclear device for sensing the concentration of suspended sediment in streams, and preliminary studies and some flume tests have been completed on an experimental model. B. C. Colby designed a protecting body in which Parametrics, Inc., is to mount the cadmium-109 source, a reference cell, a detector, and a preamplifying system. The remainder of the system can be installed on a bridge or streambank. B. C. Colby designed a 200-pound U.S. P-63 suspended-sediment sampler, now in production, that will accommodate either pint or quart sample bottles and enable samples to be taken in deeper and swifter streams than can be done with the P-61 sampler. Experimental power-hoisting equipment for depth-integrated sampling of suspended sediment was developed by J. V. Skinner, B. C. Colby, and T. F. Beckers. Uniform rates of raising and lowering sediment samplers can be maintained in the range 0.5 to 2 feet per second with 4-wheeled crane and B-3 reel. On other cranes and reels, samplers up to 100 pounds can be raised uniformly in a speed range of from 1 to 4 feet per second. V. C. Kennedy has experimented with a freezing probe for collecting samples of unconsolidated sediments. Alcohol at — 50 °C to — 60 °C is circulated through the probe which has been inserted to the desired depth in the sediment. The thickness of the core which freezes to the probe depends on the length of time the probe is left in place and on the insulation on the alcohol-supply line. Accuracy of current-meter measurements Wave action has long been known to affect the registration of the Price current meter when suspended from the bow of a boat, but until the past year the errors had not been evaluated in the field. N. A. Kallio tested the Price, Ott, and Vane-type current meters at a field location where controlled amounts of periodic vertical motion similar to the motion of a boat’s bow in wavy water could be applied to the meter and the affect on the registration could be measured accurately. The tests showed that the registrations of the Price, Ott, and Vane-type meters are all significantly affected by vertical motion such as is encountered during discharge measurements made from boats on windy days. G. L. Bodhaine and John Savini recorded simultaneous velocities for 66 minutes at 10 points spaced at intervals of 10 percent of the total depth in a vertical in the measuring section on the Columbia River below Priest Rapids Dam. The mean velocity in the vertical based on the entire period was 3.28 feet per second, while the mean velocities in the vertical based on 1-minute observations ranged from 2.76 to 3.71 feet per second. Study of the variation of velocities at individual points in the vertical showed that the maximum standard deviation occurred near the streambed and decreased curvilinearly to a minimum near the surface. The mean velocity in vertical equalled the velocity at 61 percent of depth and also equalled the average of velocities taken at 26 and 80 percent of depth. Special measurements made at 5 gaging stations on the Columbia River by John Savini, G. L. Bodhaine, and others confirm that the standard Geological Survey method of computing discharge by using the average of observations at 20 and 80 percent of depth for mean velocity is as satisfactory as computing by the more elaborate method of determining the mean velocity in the vertical graphically from a curve fitted through 10 equal-spaced observations in the vertical. Artificial stream controls F. A. Kirkpatrick is studying artificial steam controls to evaluate the economics and effectiveness of three principal types: precalibrated critical-depth flumes, double-sheet piling, compound weirs, and broad-crested low-rubble fills. Glass electrode for use under high pressures F. C. Koopman and J. L. Kunkler have developed a glass electrode and reference electrode for a deep-well chemical survey instrument called UNELAN (uNder-water Electronic ANalyzer). Preliminary tests indi-A204 LABORATORY AND FIELD METHODS cate that the electrodes are about as sensitive as conventional laboratory electrodes and will withstand pressures as high as 400 pounds per square inch for more than 28 hours without damage or change in calibration. Computer contours permeability data J. D. Bredehoeft (chapter D) reported preliminary results of a study of the Tensleep Sandstone in the Big Horn Basin, Wyo., in which a three-dimensional polynominal surface was fitted to the data by the method of least squares. The surface coordinates are automatically contoured on an X-Y plotter using, as input, the magnetic tape prepared by the digital computer. Petrologic miscroscope automated to measure sand-grain orientation R. R. Bennett and J. D. Bredehoeft have developed a petrologic microscope for automatically measuring the statistical orientation of sandstone grains. Recent studies by other investigators indicate the possibility of relating the microscopic fabric of sediments to prevailing energy conditions in the sedimentary basin at time of deposition. If the possibility materializes, a good understanding of regional changes in permeability can be achieved. Multifunction geophysical logger A new multifunction geophysical logger has been developed under the direction of W. S. Keys. All probes are 2 inches or less in diameter, and logs can be made to a depth of 6,000 feet. The following logs may be made simultaneously: Natural gamma and neutron-epithermal neutron or neutron-gamma or gamma-gamma; caliper and any single radiation log; fluid resistivity and temperature; and spontaneous potential and single-point resistivity. The equipment facilitates research on aquifer and fluid characteristics in cased or uncased wells. Storm patterns measured with radar A modified M-33 military radar unit has proven highly successful in measuring the occurrence, extent, and intensity of convective storms in Arizona. Alfonso Wilson conducted trials during the summer of 1963 in a 300-square-mile basin instrumented with rain gages at each section corner. A general correlation was found between intensity and extent of storm and thermal characteristics of the rock outcrops. Areas with rocks having high solar-induced temperatures at depth appear to have more severe thunderstorms than do surrounding areas. D. D. Knochenmus is analyzing 16-mm movie films taken of the oscilloscope face on the U.S. Weather Bureau WSR-57 radar set to determine if the radar echoes from precipitation over a rain gage will correlate with the rain-gage catch. Periscope for borehole inspection F. W. Trainer and J. E. Eddy (chapter D) have developed a lightweight, portable periscope that permits observation of the rock face or condition of casing in drill holes up to 42 feet deep. With the periscope they were able to determine the number, location, and attitude of fractures and, in one hole, could observe inflow of water from a fracture above the water level. The periscope is useful also for examining inaccessible crevasses. Cooler and humidifier for centrifuge moisture-equivalent test I. S. McQueen and R. F. Miller (2-63) have developed and tested a low-cost, evaporative cooler-humidifier, which maintains required temperature and humidity for the centrifuge moisture-equivalent test. U.S. Patent 3,109,972 has been granted for the cooler-humidifier. Ultrasonic agitation in sample preparation R. P. Moston and A. I. Johnson (p. C159-C160) reported on ultrasonic agitation for disaggregating samples of sedimentary deposits preparatory to size analysis. A 15-minute agitation by ultrasonic energy appears optimum. A sample treated by ultrasonic agitation contained less silt and more clay than the identical sample treated by the standard disaggregation procedures. Continuous water-temperature recorder A battery-powered continuous water-temperature recorder has been developed for remote locations by using a clockwork-drive recording milliammeter, wheatstone-bridge circuitry, and thermistor-type water-temperature probes. R. L. Cory reports successful operation with weekly servicing to wind the chart drive. The equipment will operate in an air temperature range from + 10°F to 140°F and record water temperatures ranging from — 2°C to +40°C. Flow-through water analyzer J. F. Ficke has assembled and used a flow-through system for making repeated measurements of dissolved oxygen, specific conductance, pH, and alkalinity. The system incorporates a 12-volt submersible pump, 100 feet of hose, chambers for the dissolved oxygen andHYDROLOGIC MEASUREMENTS AND INSTRUMENTATION A205 specific-conductance electrodes, a temperature bath for pH buffers, and taps for the withdrawal of samples. Tests have shown that the system does not modify the quality characteristics of the water flowing through it. Automation of water-quality computations M. D. Edwards has developed a program for the digital computer that computes daily, monthly, and annual sediment discharges for stations where stage is recorded digitally. The data input consists of sediment concentrations sampled at given times and the previously computed record of discharge based on the digital gage records. Drag-wire probe The drag-wire probe, originally developed by Sharp in 1962, has been improved by H. P. Guy, D. B. Simons, and ,T. B. Bole and is being used to study boundary-layer flows and the lift and drag on particles immersed in the flow. Velocities can be measured within 0.002 inch of a rigid boundary. Velocity profiles measured with the probe confirm theoretical concepts. Antifouling experiment A. L. Higer tested plates of different common metals, some of which were treated with antifouling compounds or electrical charges to determine the optimum surface or treatment for preventing growth of marine organisms on hydrologic equipment in brackish and salt waters of southern Florida. Copper plate was best among the untreated metals. The best antifouling paints provided only a short period of antifouling protection. A periodic electrical charge resulted in formation of a calcium or magnesium chloride residue which sloughed off, thereby discouraging marine organisms.iTOPOGRAPHIC SURVEYS AND MAPPING MAPPING ACCOMPLISHMENTS Objectives of National Topographic Mapping Program The major function of the Topographic Division of the U.S. Geological Survey is to prepare and maintain maps of the National Topographic Map Series covering the United States and other areas under the sovereignty of the United States of America. The individual ser-ries, at various scales, constitute a fundamental part of the background information needed to inventory, develop, and manage the natural resources of the country. Other Division functions include the production of special maps and research and development in techniques and instrumentation. In addition to the maps described below, the Topographic Division prepares shaded-relief maps, United States base maps, special maps, and also a few plani-metric maps. Procedures for obtaining copies of the maps and map products of the Survey are given in the section “How To Obtain Geological Survey Publications.” Series and scales All topographic surveys, except those in Alaska, conform to standards of accuracy and content required for publication at the scale of 1:24,000. Initial publication scale may be either 1:24,000 or 1:62,500, depending on the need. If 1:62,500-scale maps are published initially, the 1:24,000-scale surveys, in the form of photogrammetric compilation sheets, are available as advance prints and for future publication at the larger scale. For Alaskan maps, the publication scale is 1: 63,360 or “inch-to-the-mile.” Coverage of the Nation Approximately 60 percent of the total area of the 50 States, Puerto Rico, and the Virgin Islands (fig. 8) is covered by published standard quadrangle maps at scales of 1:20,000 (Puerto Rico only), 1:24,000, 1:62,-500, and 1:63,360 (Alaska only). An additional 9 percent of the total area is covered by topographic surveys, which are available as advance prints at these scales. During fiscal 1964, 1,232 maps were published cov- ering previously unmapped areas equivalent to 3 percent of the total area. In addition, 511 new maps at the scale of 1:24,000, equivalent to 1 percent of the total area, were published to replace 15-minute quadrangle maps (scale 1:62,500) not meeting present needs. For the extent and location of map coverage, see figure 9. Map revision and maintenance During fiscal 1964, about 68.0 square miles of 7y2-minute mapping was added to the growing backlog of maps needing revision. Concurrently, the backlog was diminished by revising about 14,000 square miles of mapping, leaving about 372,000 square miles of 7%-minute mapping needing revision at the end of the year (fig. 10). 1:250,000-scale series The 48 conterminous States and Hawaii are 99 percent covered by 1:250,000-scale maps originally prepared as military editions by the U.S. Army Map Service. As these maps are completed, certain changes and additions are incorporated to make them more suitable for civil use. This series of maps is being revised and maintained by the Topographic Division. Maps of Alaska at this scale are prepared and published by the Geological Survey. Coverage of the 50 States, Puerto Rico, and the Virgin Islands by 1:250,000-scale maps and the work in progress are shown on figure 11. State maps State maps are published at scales of 1:500,000 and 1:1,000,000, except for Alaska, which is covered by base maps published at scales of 1:1,584,000 and 1: 2,500,000, and Hawaii, which is not yet covered by any of these types of maps. Twenty-nine maps covering 33 States and the District of Columbia, compiled to modern standards, have been published in a new series comprising as many as four editions: base; base and highways; base, highways, and contours; and shaded relief on a modified base. As shown on figure 12, other conterminous States are covered by an earlier series. Metropolitan areas Metropolitan-area maps are prepared by combining on one or more sheets the 7i/^-minute quadrangles that A207A208 TOPOGRAPHIC SURVEYS AND MAPPING 15 MINUTE SERIES 7H MINUTE SERIES REPLACEMENT, 7% MINUTE SERIES :l5.MINUTE SERIES (PRE 1947): MINUTE SERIES (PRE 1947). PERCENT MAPPED -100 80 |________ Mapping of the 50 States, Puerto Rico, and Virgin Islands is included; also, mapping prepared in part by other agencies * Replacement of 15-minute series with 7>$-minute series * * 15-minute series at 7>$-minute standards _J-------1— 194/ FISCAL YEAR Figure 8.—Progress of 7%- and 15-minute quadrangle mapping. cover a metropolitan area. Maps of 58 metropolitan areas have been published, including 1 new map and 1 revised map that were completed during fiscal 1964. Work in progress includes 1 new map and the revision of 4 others. Maps in the metropolitan-area series include: PUBLISHED Albuquerque, N. Mex. Atlanta, Ga. Austin, Tex. Baton Rouge, La. Boston, Mass. Bridgeport, Oonn. Buffalo, N.Y. Champaign-Urbana, 111. Chattanooga, Tenn. Chicago, 111. (3 sheets) Cincinnati, Ohio Cleveland, Ohio Columbus, Ohio Davenport-Rock Island-Moline, Iowa-Ill. Dayton, Ohio Denver, Colo. Detroit, Mich. (2 sheets) Duluth-Superior, Minn.-Wis. Fort Worth, Tex. Gary, Ind. Hartford-New Britain, Conn. Honolulu, Hawaii Houston, Tex. Indianapolis, Ind. Juneau, Alaska Knoxville, Tenn. Little Rock, Ark. Long Beach, Calif. Los Angeles, Calif. (2 sheets) Louisville, Ky. Madison, Wia Milwaukee, Wis. Minneapolis-St. Paul, Minn. New Haven, Conn. New Orleans, La. New York, N.Y. (8 sheets) Norfolk-Portsmouth-Newport News, Va. Oakland, Calif. Peoria, 111.t MAPPING ACCOMPLISHMENTS A209 Philadelphia, Pa. (2 sheets) Pittsburgh, Pa. Portland-Vancouver, Oreg.-Wash. Rochester, N.Y. Salt Lake City, Utah San Diego, Calif. San Francisco, Calif. San Juan, P.R. Seattle, Wash. Shreveport, La. Spokane, Wash. Tacoma, Wash. Toledo, Ohio Washington, D.C. Wichita, Kans. Wilkes-Barre-Pittston, Pa. Wilmington, Del. Worcester, Mass. Youngstown, Ohio Anchorage, Alaska Cincinnati, Ohio Little Rock, Ark. Louisville, Ky. Washington, D.C. IN PROGRESS New Maps Revision National Park maps Maps of 40 of the 201 national parks, monuments, historic sites, and other areas administered by the National Park Service have been published and are available for distribution. These usually are made by combining all existing quadrangle maps of the area into one map sheet, but occasionally surveys are made covering only the park area. Most of the other parks, monuments, and historic sites are shown on maps of the standard quadrangle series. Published maps in the National Park series include: Acadia National Park, Maine Bandelier National Monument, N. Mex. Black Canyon of the Gunnison National Monument, Colo. Bryce Canyon National Park, Utah Canyon de Chelly National Monument, Ariz. Carlsbad Caverns National Park, N. Mex. Cedar Breaks National Monument, Utah Colonial National Historical Park (Yorktown), Va. Colorado National Monument, Colo. Crater Lake National Park, Oreg. Craters of the Moon National Monument, Idaho Custer Battlefield, Mont. Devils Tower National Monument, Wyo. Dinosaur National Monument, Colo.-Utah Franklin D. Roosevelt National Historic Site, N.Y. Glacier National Park, Mont. Grand Canyon National Monument, Ariz. Grand Canyon National Park, Ariz. (2 sheets) Grand Teton National Park, Wyo. Great Sand Dunes National Monument, Colo. Great Smoky Mountains National Park, N.C.-Tenn. (2 sheets) Isle Royale National Park, Mich. Lassen Volcanic National Park, Calif. Mammoth Cave National Park, Ky. Mesa Verde National Park, Colo. Mount McKinley National Park, Alaska Mount Rainier National Park, Wash. Olympic National Park, Wash. Petrified Forest National Monument, Ariz. Rocky Mountain National Park, Colo. Million-scale maps The worldwide million-scale series of topographic quadrangle maps was originally sponsored by the International Geographical Union and designated the International Map of the World on the Millionth Scale (IMW). The conterminous United States will be covered by 53 maps, 17 of which were produced before 1955. At that time the Army Map Service began a military series at 1:1,000,000 scale. Eventually this military series will be modified slightly and published in the IMW series (fig. 13). Three of the maps, Hudson River, Mississippi Delta, and San Francisco Bay, are no longer available as IMW maps, but the areas are covered by maps in the military series. Both the IMW and military series are available for Boston, Chesapeake Bay, Hatteras, Mount Shasta, and Point Conception. In addition, the American Geographical Society has published the Sonora, Chihuahua, and Monterrey maps; and Canada, the Regina and Montreal maps. Puerto Rico is covered by two maps, compiled by the American Geographical Society and published by both the Society and the Army Map Service. Some maps of the military series have been modified for broader civil use by changing them to conform to the IMW sheet lines and sheet numbering system, but they do not meet IMW specifications in all respects. These maps are recognized by the United Nations Cartographic Office as provisional editions in the IMW series. Work in progress includes two new maps, Lake Superior and Pikes Peak. Scotts Bluff National Monument, Nebr. Sequoia and Kings Canyon National Parks, Calif. Shenandoah National Park, Va. (2 sheets) Vanderbilt Mansion National Historic Site, N.Y. Vicksburg National Military Park, Miss. Wind Cave National Park, S. Dak. Yellowstone National Park, Wyo.-Mont.-Idaho Yosemite National Park, Calif. Yosemite Valley, Calif. Zion National Park (Kolob Section), Utah Zion National Park (Zion Canyon Section), UtahFigure 9.—Status of 7Mr and 15-minute quadrangle mapping. A210 TOPOGRAPHIC SURVEYS AND MAPPING% MAPPING ACCOMPLISHMENTS A211---- JUNE 30. 1964 Published Maps □ Best quality In need of revision Reconnaissance series (Alaska) Mapping In Progress □ Army Map Service □ U S-Geological Survey PUERTO RICO AND VIRGIN ISLANDS ALASKA ALEUTIAN ISLANDS 1 HAWAII Figure 11.—Status of 1: 250,000-scale mapping. A212 TOPOGRAPHIC SURVEYS AND MAPPINGN£* c h^psH'r£ JUNE 30, 1964 Published Maps m New Series “(contour and planimetric) Q New Series (planimetric only) □ Earlier Series (planimetric only) Mapping in Progress pa New Series “3 (contour and planimetric) H New Series (Contour only) Note: State maps are available at scales of 1: 500,000 and 1:1,000,000 except for Alaska, Maps of Alaska are available at scales of 1:1,584,000 and 1:2,500,000 Figure 12.—Status of State maps. MAPPING ACCOMPLISHMENTS A213Figure 13.—Status of 1:1,000,000-scale topographic mapping. A214 TOPOGRAPHIC SURVEYS AND MAPPINGRESEARCH AND DEVELOPMENT A215 MAPPING IN ANTARCTICA The topographic mapping of Antarctica, conducted as a part of the TJ.S. Antarctic Research Program (USARP) of the National Science Foundation, was continued during fiscal 1964. Five topographic engineers went to Antarctica during the austral summer of 1963-64 to obtain geodetic control for the topographic mapping program and to execute surveys in support of other scientific disciplines. Also, a specialist in aerial photography was again assigned to Christchurch, New Zealand, for photographic liaison duty with the U.S. Navy. Topographic field operations D. C. Barnett and J. R. Heiser accompanied 4 geologists and 1 glaciologist of the Geological Survey to the Neptune Range of the Pensacola Mountains and executed 250 miles of electronic-distance traverse to control the Neptune Range for topographic mapping. These engineers also established a geodetic tie between control nets in the Patuxent Mountains and the Neptune Range, including a 45-mile electronic-distance measurement across an intervening glacier. In addition, they obtained 15 stellar and 5 solar observations at the previously established Patuxent Camp astronomic station. Additional mapping control was established in the Ellsworth Mountains by Alfred Zavis. Supported by a TJ.S. Army helicopter detachment and assisted by geologists of the University of Minnesota, Zavis extended a previously established electronic-distance control net through the Heritage Range of the Ellsworth Mountains. The Camp Gould astronomic station, established during the 1962-63 field season, was strengthened by 18 additional stellar observations. R. E. Kenfield and K. S. McLean established a precise ice-strain net originating at New Byrd Station and extending approximately 60 miles eastward toward the divide between the Filchner Ice Shelf and the Ross Ice Shelf. To obtain the required surveying accuracy of 1 part in 60,000, the engineers used theodolites for measuring angles and electronic equipment for measuring distances. A large-scale topographic map of a portion of the Cape Hallett penguin rookery was also completed. Control previously established by the U.S. Navy was extended by using theodolites and electronic instruments. Two-foot contours were sketched by planetable methods. Aerial photography U.S. Navy Air Development Squadron 6 (VX-6) obtained aerial photographs for mapping in accordance 746-002 0 - 64 - 15 with Geological Survey specifications. W. R. MacDonald was assigned to the U.S. Navy Photographic Laboratory at Christchurch, New Zealand, to advise on the quality of developed photographs and to assist with further planning and necessary reflights. In addition, MacDonald also served as visual navigator on all aerial photographic mapping missions over the Antarctic continent. The aerial photography program was severly hampered by the lack of aircraft with suitable operational capabilities. LP-2J Neptune airplanes, previously used in Antarctica to photograph 400,000 square miles, were eliminated from the U.S. Naval aircraft inventory in 1963. Therefore, photographic missions had to be flown in a C-121J Constellation limited to operations from the ice runway at McMurdo. Final analysis of the season’s photography indicates that areas totaling about 14,700 square miles were photographed acceptably for use in the Geological Survey mapping program. Cartographic activities Four 1:250,000-scale topographic maps of the Hor-lick Mountains were published in shaded-relief editions, making a total of 13 sheets at this scale now available. Mapping at the same scale is in progress for 12 sheets in the Queen Maud Range, 8 in the Queen Alexandra Range, 6 in the Britannia Range, 6 in the McMurdo area, and 19 in Victoria Land (fig. 14). In support of biological studies by Johns Hopkins University, a topographic map of the Cape Crozier penguin rookery was photogrammetrically compiled at 1: 2,400 scale, with contour intervals of 3 and 10 meters. Work is underway on a 1:500,000-scale shaded-relief map of northern Victoria Land, encompassing the area north of lat. 73° S., and between long. 158° and 171° E. Antarctic relief model The two-layer, multicolored plastic relief model of Antarctica, at the scale of 1:10,000,000, with a vertical exaggeration of 25:1, was completed, and 180 copies were distributed to individuals and organizations closely allied with scientific investigations in the Antarctic. In cooperation with the National Science Foundation, negotiations are underway to produce additional copies of the model for sale. RESEARCH AND DEVELOPMENT To support the Geological Survey program of topographic mapping, continuing research and development are needed to improve techniques, instruments, and media. The chief objectives are to improve the quality A216 TOPOGRAPHIC SURVEYS AND MAPPING 0 JUNE 30, 1964 PUBLISHED TOPOGRAPHIC MAPS MAPPING IN PROGRESS □ |: 250,000 scale 1 1 1:250,000 scale n I: 500,000 scale ^ AERIAL PHOTOGRAPHY (fixed mount) Hi Mapping quality PLANIMETRIC MANUSCRIPTS Marginal quality i ! Various scales lijflflll Exploratory Figure 14.—Index map of Antarctica, showing status of topographic mapping by the U.S. Geological Survey as of June 30, 1964. RESEARCH AND DEVELOPMENT A217 and the usability of the maps produced and to reduce the cost of producing them. As a part of this research, the Survey has tested a representative 10 percent of the quadrangles mapped, for two purposes: (1) to assure compliance with National Map Accuracy Standards and (2) to test the effectiveness of new methods and procedures. In 1964, as a result of recent developments, the accuracy-testing program was reviewed and separated into its two basic parts. Henceforth, the area production offices will be responsible for planning and executing routine tests intended to supply data on compliance with National Map Accuracy Standards. Tests for evaluating new techniques and instrumentation will be planned specially and carried out on a prepared test site for which adequate control is available, thereby reducing variables to a minimum. Major research projects in topographic surveying and mapping require a group effort by engineers and cartographers with different backgrounds and talents to achieve useful and meaningful results. Some of the results of projects carried out in 1964 are summarized below. FIELD SURVEYS Improvements in leveling The evaluation of precise leveling instruments is a continuing program, started in 1962, in which new instruments are included as they become available. In 1963 the program was expanded to include a comprehensive study of errors in leveling and procedural techniques to reduce or eliminate them. The results of the error study have been discussed in a special report distributed to fieldmen of the Topographic Division and summarized in a paper given by R. J. Karren before the American Congress on Surveying and Mapping in March 1964. These reports recommend several modifications in observing and recording procedures that will effectively reduce or eliminate systematic errors. Other means now being studied for improving the accuracy of leveling are more precise methods of graduating and calibrating level rods and applying corrections to the field observations. A photographic process for graduating rods appears promising and is being investigated in detail. A comparator has been modified for calibrating level rods, and its precision for that purpose is now being tested. ABC survey system Further research-production tests of the AirBorne Control (ABC) system were carried out in Maine in the fall of 1963. In this project, horizontal and vertical control stations were established on two 15-minute quandrangles consisting of densely wooded terrain. Towers were needed at all base stations, and for these the Survey portable aluminum towers gave excellent service. Despite unfavorable weather, nearly 200 control points were established in less than a month. In this project, the helicopter was used for the first time as a target for photoidentifying control points. As the helicopter hovered over a point, a photographer in a light airplane flying at 2,000 feet obtained overlapping pictures. These stereoscopic photographs permit photogrammetrists in the office to relate control points precisely to the mapping photographs. Antarctic astronomic position observations Procedures for observing stars in daylight in Antarctica were improved significantly during the past season by star-finding charts constructed for the 16 brightest southern stars. From these the observer could quickly obtain time, direction, and altitude for crossings of the meridian and the prime vertical. By setting the theodolite to values scaled from the charts, observations could be completed without loss of time, an important consideration in cold weather. An additional advantage was improved accuracy of results based on balanced sets of observations, confined to the cardinal directions. Most positions were determined from at least 4 observations in each of the 4 cardinal directions, or a total of 16 star observations. PHOTOGRAMMETRY Super-wide-angle photogrammetric systems Investigations of super-wide-angle photogrammetric mapping systems are continuing with evaluations of the resolution and flatness of stereomodels projected by the Wild B8 stereoplotter, Wild WH6 projectors, and Bausch and Lomb Balplex super-wide-angle projectors. Super-wide-angle photographs have been obtained over a test mapping area in Oklahoma and are being tested operationally in all these instruments. The Kern PG-2 plotter and the newly designed UDP-153 stereoplotter are scheduled for delivery in time to be included in the operational study. Field checks over the entire test area will be used to determine the planimetric and contouring capabilities of each super-wide-angle stereoplotting instrument. Visual factors in stereoplotting Under a research contract recently completed, Wendell E. Bryan, O.D., investigated the eye-fatigue andA218 TOPOGRAPHIC SURVEYS AND MAPPING vision problems of a representative group of 60 employees operating anaglyphic double-projection stereoplotters. On the basis of optometric and medical examinations, the participants were furnished with prescription-ground anaglyphic glasses for stereocompilation, regular prescription glasses for normal activities, and special clip-on binocular loupes for scribing. An experimental stereoplotting room large enough for 17 plotting instruments was designed and constructed to determine the effects of a carefully controlled environment on morale, efficiency, and visual fatigue. Participants expressed a decided preference for the controlled-environment room over conventional isolated stereoplotting booths. The work output of the group increased by more than 15 percent shortly after the introduction of optometric aids and an additional 8 percent when moved into the large, specially designed stereoplotting room. Of particular significance was the finding that, with proper optometric care, the visual capabilities of older stereocompilers can be maintained at a level which will permit continued efficient productive use of their experience and skill. Operational tests of modified Kelsh plotter Operational tests of a modified Kelsh plotter have been completed. This plotter has lenses that provide an optimum projection distance of 550 mm rather than the standard 760 mm. The tests confirmed the expected advantages of smaller model scales, more favorable pantograph reduction ratios, and a 20-percent increase in illumination, as compared with the standard Kelsh plotter. Optical performance of the prototype lenses was tested by resolution readings, grid-flatness tests, and operational tests. Subsequent investigation showed that it is feasible to combine the capabilities of the modified Kelsh plotter with those of the new super-wide-angle Kelsh plotter (projection distance, 440 mm) by means of interchangeable projector cones and lenses. These capabilities have been incorporated in the design of the new UDP-153 stereoplotter. Mapping in dense evergreen timber In a recent research study involving 18 photogram-metric compilers, James Halliday (p. C190-C194) determined the consistency of contouring in areas of dense evergreen timber for various combinations of photo-grammetric parameters. With optimum conditions (that is, early spring photographic season, a C-factor of 700, no leaves on any deciduous trees in the area, and light snow cover on the ground) the vertical accuracy of the compilations was consistently high. No significant relation was found between the vertical accuracy attained and the contouring techniques used. Because of the recurring difficulty of obtaining photographs under optimum conditions in these areas, studies are being continued to find new techniques for assisting the photogrammetrist in compilation. The ABC system is being evaluated as a means of providing more reliable photocontrol data for an area of dense evergreen woods in Maine. Airborne infrared sensors are also being investigated as a means of penetrating the foliage canopy and recording the ground data essential to topographic mapping. Analytical aerotriangulation A computer program has been written, for the Burroughs 220 computer, to establish map-coordinate positions for horizontal and vertical pass points used for orienting stereomodels in topographic map compilation. Input for the computer program consists of x and y photocoordinates measured with a precise comparator, horizontal and vertical ground-control data, and estimates of camera orientation and space position. Difficulties in the approximately 70 subroutines of the program have been checked and eliminated separately, and elimination of difficulties in the entire program is now in progress. This program will solve aerotriangulation problems in 22-photograph blocks. Switches in the program permit a problem to be solved either in a true least-squares adjustment or, for speed and expediency, in a less rigorous least-squares solution. A supplementary adjustment permits contiguous 22-photograph blocks to be fitted together after they have been solved and adjusted internally. Analytical adjustment of horizontal pass points Several methods of mathematically establishing the map coordinates of horizontal pass points from stereomodel position data are being tested. In one method, pass points obtained from Kelsh-plotter stereomodels are joined analytically to form strips coinciding with the flight strips, and then cross strips transverse to the flight strips are formed by linking together sections from adjacent flights. That is, a section of the second strip is joined to an adjoining section in the first strip, an adjoining section in the third strip is joined to the section of the second strip, and so on. After the desired number of cross strips have been formed, each is adjusted to ground control, the regular strips are adjusted to the cross strips, and the resulting block is adjusted to all ground control. The data are computedRESEARCH AND DEVELOPMENT A219 and adjusted on an RPC—4000 electronic computer. In the second method, the transformation factors needed to fit the pass points of one strip to those of an adjoining strip are computed. These factors are based on a comparison of the various combinations of corresponding line lengths and line azimuths formed from as many as 20 tie points common to two adjoining strips. After all strips are joined, the resulting block is adjusted to ground control by using the same approach as for the tie points between strips—that is, by comparing the observed line lengths and azimuths defined by the plotted and adjusted control points with the true line lengths and azimuths as determined by geodetic positions. In the third method, the horizontal projection of the stereomodel is considered the basic unit being adjusted in a simultaneous least-squares block solution. The computer program will be flexible in that models, sections, strips, or blocks can be adjusted simultaneously in either linear or nonlinear conformal transformations. Analytical vertical adjustment of a block of vertically bridged strips of aerial photographs A prototype computer program for an analytical method of adjusting photogrammetrically determined elevations has been devised and tested. Input data were obtained from a stereoscopic vertical bridge of aerial photographs, using anaglyphic projectors. In this method, a vertical-error surface, linear in y and of second degree in a?, is determined for each strip of a block in a least-squares solution, and the strips are fitted to each other and to control in an iterated adjustment. Although in the initial test the accuracy of the adjusted elevations did not meet the standards specified for field-surveyed photocontrol elevations, the results are sufficiently promising to warrant further investigation. Rapid planimetric mapping A research project to investigate a rapid method for compiling planimetric maps of unmapped areas in the conterminous United States, using readily available source materials, was completed. The project utilized high-altitude, wide-angle, 1:60,000-scale Army Map Service photographs and low-altitude, 8%-inch Department of Agriculture photographs. Control was extended over a 30-minute-square area by means of a stereotemplet assembly at 1: 24,000 scale, based on horizontal control at 10- to 15-minute intervals around the perimeter of the area. The stereotemplets were plotted from the AMS photographs. The root mean square error of 92 test points was 12.7 feet. Skeletal frameworks of readily interpretable planimetry were compiled for two 7i/f>-minute quadrangles, using the AMS photographs in Kelsh plotters. Root mean square errors for these compilations were 13 and 15 feet, and all points tested were accurate within 40 feet. The rest of the main map details were added to the manuscripts by monoscopic transfer from the Department of Agriculture photographs. Completeness of content of the final manuscripts was evaluated by comparing them with published 71/£-minute topographic maps. This comparison showed that, for example, 89 percent of the buildings on the published maps had been plotted on the map made by the rapid compilation method. Two additional test projects in other areas are now being planned to determine whether the favorable results of the first project can be obtained consistently. CARTOGRAPHY Cartographic treatment of orthophotomosaics Experiments are continuing in the development of cartographic treatment of orthophotomosaics for publication as orthophotomaps. An orthophotomap covering the 71/£-minute Cave Creek 2 SE, Ariz., quadrangle is in preparation. The experimental printing will illustrate the use of photographic imagery, in color, combined with the overprinted information to portray a sparsely settled arid area. An earlier experimental map covered the urban area including Roanoke, Ya. (M. B. Scher, chapter D). This form of map presentation appears to be particularly advantageous in these two kinds of areas. Processing geographic names Applications of electronic data-processing systems to storage and retrieval of geographic names is being investigated. The objective is a system that will store cumulative pertinent data on official standard names and Board on Geographic Names decisions and will print out, on call, geographic information in selected categories or listings. This capability will greatly facilitate publication of Decision Lists reflecting actions by the Board on Geographic Names, compilation of gazetteers of place names for the individual States, replies to correspondence, and other uses of the stored data.COOPERATING AGENCIES FOR FISCAL YEAR 1964 FEDERAL AGENCIES Agency for International Development Air Force: Cambridge Research Center Special Weapons Center Technical Application Center Army: U.S. Army—Europe Corps of Engineers, Waterways Experiment Station Atomic Energy Commission: Division of Military Application Division of Peaceful Nuclear Explosives Division of Raw Materials Division of Reactor Development Nevada Operations Office Research Division San Francisco Operations Office Department of Agriculture: Forest Service Soil Conservation Service Department of Commerce: Bureau of Public Roads Bureau of Standards Department of Defense: Advanced Research Projects Agency Defense Atomic Support Agency Defense Intelligence Agency Office of Scientific Research STATE, COUNTY, AND Alabama: Geological Survey of Alabama Alabama Highway Department Department of Conservation Water Improvement Commission Calhoun County Board of Revenue City of Huntsville City of Mobile Alaska: Department of Highways City of Anchorage Arizona: Arizona Highway Department State Land Department Regents of the University of Arizona Superior Court, County of Apache Maricopa County Flood Control District Maricopa County Municipal Water Conservation District No. 1 Navajo Tribal Council City of Flagstaff Department of Health, Education, and Welfare: Public Health Service Department of the Interior: Bonneville Power Administration Bureau of Commercial Fisheries Bureau of Indian Affairs Bureau of Land Management Bureau of Mines Bureau of Reclamation Bureau of Sport Fisheries and Wildlife National Park Service Office of Minerals Exploration The Alaska Railroad Department of Justice Department of State District of Columbia Executive Office of the President—Office of Emergency Planning Federal Power Commission Navy: Bureau of Yards and Docks Office of Naval Research National Aeronautics and Space Administration National Science Foundation Tenessee Valley Authority Veterans Administration MUNICIPAL AGENCIES Arizona—Continued City of Prescott City of Tucson City of Williams Buckeye Irrigation Company Gila Valley Irrigation District Salt River Valley Water Users Association San Carlos Irrigation and Drainage District Arkansas: Arkansas Geological and Conservation Commission Arkansas Game and Fish Commission Arkansas State Highway Commission University of Arkansas—Agricultural Experiment Station California: Department of Conservation, Division of Mines and Geology State Department of-Water Resources State Department of Fish and Game State Department of Parks and Recreation State Water Pollution Control Board Alameda County Flood Control and Water Conservation District A221A222 COOPERATING AGENCIES FOR FISCAL YEAR 1964 California—Continued Alameda County Water District Calaveras County Water District Contra Costa County Flood Control and Water Conservation District County of Los Angeles Department of County Engineers Lake County Flood Control and Water Conservation District Montecito County Water District Monterrey County Flood Control and Water Conservation District Orange County Flood Control District Sacramento County San Bernardino County Flood Control District San Francisco City and County Public Utilities Commission San Luis Obispo County Flood Control and Water Conservation District Santa Barbara County Water Agency Santa Clara County Flood Control and Water Conservation District Santa Cruz County Flood Control and Water Conservation District City of Areata City of San Diego San Francisco Water Department Santa Barbara Water Department East Bay Municipal Utility District Georgetown Divide Public Utility District Antelope Valley—East Kern Water Agency Imperial Irrigation District Metropolitan Water District of Southern California Palo Verde Irrigation District San Bernardino Valley Water Conservation District Santa Maria Valley Water Conservation District Ventura River Municipal Water District Western Municipal Water District of Riverside County Colorado: Colorado State Metal Mining Fund Board Colorado Water Conservation Board Office of State Engineer, Division of Water Resources Colorado State University Agricultural Experiment Station Colorado Springs—Department of Public Utilities Denver Board of Water Commissioners City of Westminster Arkansas River Compact Administration Costilla Creek Compact Commission Rio Grande Compact Commission Southeastern Colorado Water Conservancy District Connecticut: Connecticut Geologic and Natural History Survey Highway Department State Water Resources Commission Greater Hartford Flood Commission Hartford Department of Public Works New Britain Board of Water Commissioners City of Torrington—Engineering Department Delaware: Delaware Geological Survey State Highway Department District of Columbia: District of Columbia Department of Sanitary Engineering Florida: Florida Geological Survey State Board of Parks and Historic Memorials State Road Department Broward County—Board of County Commissioners Collier County—Board of County Commissioners Dade County—Board of County Commissioners Hillsborough County—Board of County Commissioners Orange County—Board of County Commissioners Pinellas County—Board of County Commissioners Polk County—Board of County Commissioners City of Boca Raton City of Deerfield Beach City of Fort Lauderdale City of Jacksonville—City Commission City of Jacksonville—Office of the City Engineer City of Miami—Department of Water and Sewerage City of Miami Beach City of Naples City of Perry City of Pompano Beach City of Tallahassee Central and Southern Florida Flood Control District Southwest Florida Water Management District Trustees of Internal Improvement Fund Georgia: Department of Mines, Mining and Geology, Division of Conservation State Highway Department Hawaii: State Department of Land and Natural Resources Honolulu, City and County of Idaho: Idaho Department of Reclamation Idaho Department of Highways Idaho Department of Fish and Game Illinois: State Department of Public Works and Buildings: Division of Highways Division of Waterways State Department of Registration and Education Fountain Head Drainage District Metropolitan Sanitary District of Greater Chicago Northeastern Illinois Metropolitan Area Planning Commission Sanitary District of Bloom Township (Cook County) Indiana: State Department of Conservation Division of Water Resources State Highway Commission Flood Control and Water Resources Commission Board of Health Iowa: Iowa Geological Survey Iowa State Conservation Commission Iowa State Highway Commission Iowa Institute of Hydraulic Research Iowa State University—Agricultural Experiment Station Linn County—Board of Supervisors City of Cedar Rapids City of Fort Dodge—Department of UtilitiesIOWA-NEW YORK A223 Iowa—Continued City of Iowa City City of Muscatine Kansas: Kansas State Geological Survey State Water Resources Board State Department of Health—Environmental Health Services State Highway Commission State Board of Agriculture, Division of Water Resources City of Wichita—Department of Public Works Kentucky: Kentucky Geological Survey Louisiana: State Department of Public Works State Department of Conservation State Department of Highways Sabine River Compact Commission Maine: Department of Public Works Maine Public Utilities Commission State Highway Commission Maryland: Maryland Geological Survey State Department of Health State Planning Department State Roads Commission Baltimore County—Department of Public Works City of Baltimore City of Salisbury Washington Suburban Sanitary Commission Massachusetts: Massachusetts Department of Public Works: Division of Highways Division of Waterways Massachusetts Water Resources Commission Boston Metropolitan District Commission Michigan: State Water Resource Commission Michigan Department of Conservation, Geological Survey Division State Highway Department Minnesota: Minnesota Geological Survey State Department of Conservation: Division of Waters Department of Conservation State of Minnesota Department of Highways Department of Iron Range Resources and Rehabilitation Board of County Commissioners of Hennepin County Mississippi: Mississippi Board of Water Commissioners Mississippi State Highway Department Mississippi Industrial and Technological Research Commission Harrison County—Board of Supervisors and Development Commission Jackson County—Port Authority City of Jackson Pearl River Valley Water Supply District Missouri: Division of Geological Survey and Water Resources State Highway Commission Water Pollution Control Board Curators of the University of Missouri Montana: Montana Bureau of Mines and Geology State Engineer State Fish and Game Commission State Highway Commission State Water Conservation Board Montana State College—Endowment and Research Foundation Nebraska: Department of Water Resources Department of Roads University of Nebraska—Conservation and Survey Division Nebraska Mid-State Reclamation District Nevada: Nevada Bureau of Mines Department of Conservation and Natural Resources Department of Highways New Hampshire: New Hampshire Water Resources Board New Jersey: Department of Conservation and Economic Development Division of Water Policy and Supply Division of Fish and Game Department of Health Department of Agriculture Rutgers University, the State University of New Jersey Camden County Planning Board North Jersey District Water Supply Commission Passaic Valley Water Commission Delaware River Basin Commission New Mexico: State Engineer State Highway Department State Game and Fish Commission State Bureau of Mines and Mineral Resources Division, New Mexico Institute of Mining and Technology Interstate Stream Commission Pecos River Commission Pecos Valley Artesian Conservancy District Rio Grande Compact Commission Costilla Creek Compact Commission City of Ruidoso New York: State Conservation Department: Division of Lands and Forests Division of Water Resources State Department of Commerce State Department of Health State Department of Public Works New York Water Resources Commission Office of Atomic Development Board of Hudson River—Black River Regulating District Dutchess County Board of Supervisors Nassau County Department of Public Works Onondaga County Department of Public WorksA224 COOPERATING AGENCIES FOR FISCAL YEAR 1964 New York—Continued Onondaga County Water Authority Suffolk County Board of Supervisors Suffolk County Water Authority Westchester County Department of Public Works City of Albany—Department of Water and Water Supply City of Auburn—Water Department New York City Board of Water Supply New York City Department of Water Supply, Gas and Electricity Village of Nyack—Board of Water Commissioners Brighton Sewer District No. 2 Oswegatchie River—Cranberry Reservoir Commission North Carolina: North Carolina Department of Conservation and Development, Division of Mineral Resources State Department of Water Resources State Highway Commission Pitt County Board of Commissioners City of Asheville CSty of Burlington City of Charlotte City of Durham City of Greensboro Town of Waynesville North Dakota: State Water Conservation Commission North Dakota Geological Survey State Highway Department Ohio: Ohio Department of Natural Resources—Division of Water Ohio Department of Health Ohio Department of Highways City of Columbus—Department of Public Service Miami Conservancy District Ohio River Valley Water Sanitation Commission Scioto Conservancy District Oklahoma: Oklahoma Water Resource Board Oklahoma Department of Highways Oklahoma Geological Survey Oklahoma State Department of Health Oklahoma City Water Department Oregon: State Engineer State Highway Department Board of Higher Education State Game Commission County of Coos—Board of Commissioners County Court of Douglas County County Court of Lane County County Court of Morrow County City of Dallas City of Dalles City City of Eugene—Water and Electric Board City of McMinnville—Water and Light Department City of Portland—Bureau of Water Works City of Toledo Coos Bay—North Bed Water Board Burnt River Irrigation District Mosier Irrigation District Oregon—Continued Talent Irrigation District Vale Irrigation District Pennsylvania: Pennsylvania Bureau of Topographic and Geologic Survey State Department of Forests and Waters State Department of Agriculture State Department of Health City of Bethlehem City of Harrisburg City of Philadelphia Conestoga Valley Association, Inc. Rhode Island: Rhode Island Water Resources Coordinating Board Department of Public Works—Division of Harbors and Rivers South Carolina: State Development Board State Highway Department State Public Service Authority State Water Pollution Control Authority City of Spartanburg—Public Works Department South Dakota: South Dakota Geological Survey South Dakota Water Resources Commission South Dakota Department of Highways Tennessee: Tennessee Department of Conservation: Division of Water Resources Division of Geology Tennessee Department of Highways Tennessee Department of Public Health Tennessee Game and Fish Commission City of Chattanooga City of Murfreesboro—Water and Sewer Department Memphis Board of Light, Gas, and Water Commissioners— Water Division Metropolitan Government of Nashville and Davidson County—Department of Public Works Texas: Texas Water Commission Pecos River Commission Rio Grande Compact Commission Sabine River Compact Administration City of Dallas City of Houston Utah: Utah Geological and Mineralogical Survey Utah State Engineer Utah Water and Power Board State Road Commission of Utah Salt Lake County Bear River Compact Commission Vermont: Vermont Geological Survey State Water Resources Board Department of Highways Virginia: Department of Conservation and Development—Division of Mineral Resources Department of HighwaysVIRGINIA-VIRGIN ISLANDS OF THE UNITED STATES A225 V irginia—Continued Division of Industrial Development and Planning County of Chesterfield County of Fairfax City of Alexandria City of Charlottesville City of Newport News-Department of Public Utilities City of Norfolk—Division of Water Supply City of Roanoke City of Staunton Washington: State Department of Conservation: Division of Mines and Geology Division of Water Resources State Department of Fisheries State Department of Game State Department of Highways State Pollution Control Commission King County Board of Commissiohers Municipality of Metropolitan Seattle City of Seattle City of Tacoma: Department of Public Utilities Department of Public Works West Virginia: State Department of Natural Resources State Geological and Economic Survey West Virginia—Continued State Road Commission Clarksburg Water Board Wisconsin: University of Wisconsin—Geological and Natural History Survey Public Service Commission of Wisconsin State Committee on Water Pollution State Highway Commission Madison Metropolitan Sewerage District Southeastern Wisconsin Regional Planning Commission Wyoming: Geological Survey of Wyoming State Engineer Wyoming Highway Department Wyoming Natural Resource Board City of Cheyenne—Board of Public Utilities Commonwealth of Puerto Rico: Water Resources Authority Department of Public Works American Samoa: Government of American Samoa Guam: Government of Guam Virgin Islands of the United States: Government of the Virgin IslandsU.S. GEOLOGICAL SURVEY OFFICES MAIN CENTERS Main Office: General Services Building, 18th and F Streets NW., Washington, D.C. 20242; 343-1100 Rocky Mountain Center: Federal Center, Denver, Colo. 80225; BElmont 3-3611 Pacific Coast Center: 345 Middlefield Road, Menlo Park, Calif. 94025; DAvenport 5-6761 Location Alaska, Anchorage, 99501_______ California, Los Angeles, 90014 San Francisco, 94111______ Colorado, Denver, 80202________ Utah, Salt Lake City, 84111... Texas, Dallas, 75202........... Washington, Spokane, 99204.. PUBLIC INQUIRIES OFFICES Official in charge and telephone number Margaret I. Erwin (BRoadway 2-8791)____________ Lucy E. Birdsall (688-2850)____________________ Jean V. Molleskog (556-5627)___________________ Lorene C. Young (297-4169)_____________________ Maurine Clifford (524-5652)____________________ Mary E. Reid (Riverside 8-5611, ext. 3230)_____ Eva M. Raymond (TEmple 8-2084, ext. 30)________ Address 108 Skyline Bldg., 508 2d Ave. 1031 Bartlett Bldg., 215 West 7th St. 504 Custom House, 555 Battery St. 468 New Custom House. 8102 Federal Office Bldg., 125 South State St. 602 Thomas Bldg., 1314 Wood St. South 157 Howard St. SELECTED FIELD OFFICES IN THE UNITED STATES AND PUERTO RICO [Temporary offices not included; list current as of September 1964. Correspondence to the following offices should be addressed to the Post Office Box, if one is given] CONSERVATION DIVISION Location Alaska, Anchorage, 99501 California, Los Angeles, 90014. Sacramento, 95814_________ Taft, 93268............... Colorado, Denver, 80202________ Denver, 80225_____________ Denver, 80202_____________ Durango, 81302____________ Louisiana, New Orleans, 70113 Lafayette, 70501__________ Montana, Billings, 59101______ Great Falls, 59401________ Official in charge* and telephone number LeoH. Saarela (m) (BRoadway 7-3883), Alexander A. Wanek (c) (BRoadway 2-8262), and Merwin H. Soyster (o) (BRoadway 2-8262). Russell G. Wayland (c) (688-2849) and D. W. Solonas (o) (688-2846). Richard N. Doolittle (w) (449-2203)............. Harry Lee Wolf (o) (ROger 5-4234) and E. E. Richardson (c) (ROger 5-4234). G. G. Frazier (o) (534-4151, ext. 356) and H. B. Lindeman (m) (534-4151, ext. 278). George H. Horn (c) (233-3611, ext. 8168)________ Wm. C. Senkpiel (w) (534-4151, ext. 1389)_______ Jerry W. Long (o) (247-5144)___________________ Admiral D. Acuff (o) (527-6543)_________________ Robert M. Bennett (b) (CEnter 4-1637).......... Ray M. Bottomley (m) (252-2280) and Hillary A. Oden (o) (252-2880). Andrew F. Bateman (c) (452-2008)................ John A. Fraher (o) (453-6901)___________________ Address P.O. Box 259; 62, 12 (or 15), and 13 Federal Bldg. 1012 Bartlett Bldg., 215 West 7th St. 8030 Federal Bldg., 650 Capitol Ave. P.O. Box CC. 448 and 456 New Custom House. Federal Center. 816 University Bldg., 910 16th St. P.O. Box 1809; Jarvis Bldg., 125 West 10th St. T-6009 Federal Bldg., 701 Loyola Ave. P.O. Box 3884; 301 Federal Bldg., Jefferson and Main Sts. P.O. Box 2250; 323 and 327 Federal Bldg. P.O. Box 2265; 510 First Ave. North. P.O. Box 1215; 510 First Ave. North. ♦The small letter in parentheses following each official’s name denotes branch affiliation in the Conservation Division as follows: b—Branch of Connally Act Compliance, c—Branch of Mineral Classification, m—Branch of Mining Operations, o—Branch of Oil and Gas Operations, w—Branch of Waterpower Classification. A227A228 U.S. GEOLOGICAL SURVEY OFFICES Location New Mexico, Artesia, 88210.. Carlsbad, 88220_________ Farmington, 87401________ Hobbs, 88240............ Roswell, 88201__________ Oklahoma, Holdenville, 74848 McAlester, 74502_________ Miami, 75354_____________ Oklahoma City, 73102_____ Tulsa, 74103............ Oregon, Portland, 97208_______ Texas, Kilgore, 75662________ Midland, 79701.......... Victoria, 77901__________ Utah, Salt Lake City, 84111.. Washington, Tacoma, 98402 Wyoming, Casper, 82602_____ Newcastle, 82701______ Rock Springs, 82901___ Thermopolis, 82443____ Official in charge• and telephone number James A. Knauf (o) (746-4841)___________________ Robert S. Fulton (m) and Bruno R. Alto (c) (TUxedo 5-6454). Phillip T. McGrath (o) and J. E. Fassett (c) (325-4572). Arthur R. Brown (o) (EXpress 3-3612)____________ J. A. Anderson (o) and T. F. Stipp (c) (622-1332). Gerhardt H. W. Schuster (o) (Franklin 9-3840).. A. M. Dinsmore (m) (GArden 3-5030)______________ Andrew V. Bailey (m) (Kimball 2-9481)___________ Charley W. Nease (o) (CEntral 6-2311)___________ Edward L. Johnson (c) and N. Orvis Frederick (o) (LUther 4-7161, ext. 638). Loyd L. Young (w) (226-3361, ext. 1252)_________ Warren W. Mankin (b) (5564).____________________ Everett H. Patterson (b) (Mutual 4-6741)________ John I. Watson (b) (Hlllcrest 5-1841)___________ Ernest Blessing (m) (524-5646), Harry McAndrews (c) (524-5650), and Rodney A. Smith (o) (524-5650). Gordon C. Giles (w) (MArket 7-1271)_____________ J. R. Schwabrow (o) and Donald M. Van Sickle (c) (237-2561). Glenn E. Worden (o) (746-4554)__________________ John Duletsky (o) (362-6422) and Arne A. Mattila (m) (362-7350). Charles P. Clifford (o) (864-3477).............. Addreei Drawer U; 210 Carper Bldg., 105 South 4th St. P.O. Box 1716; 504A North Canal St. P.O. Box 959; 409 Petroleum Club Plaza Bldg., 3535 East 30th St. Box 1157; 205 North Linam St. P.O. Drawer 1857; Farnsworth Bldg., 120 West 2d St. P.O. Box 789; 5 Federal Bldg. 509 South 3d St. P.O. Box 509; 205 Federal Bldg. 4321 Federal Court House and Office Bldg., 220 N.W. 4th St. 521 Wright Bldg., 115 West 3d St. P.O. Box 3087; 319 Post Office Bldg. P.O. Box 1230; Rader Bldg., 901-903 Broadway Blvd. P.O. Box 1830; 805 Petroleum Life Bldg., Texas and Colorado Sts. P.O. Box 2550; 228 Federal Bldg., Main and Church Sts. 420, 450, and 416 Empire Bldg., 231 East 4th St. P.O. Box 1152; 244 Federal Bldg. P.O. Box 400; 305 Federal Bldg. P.O. Box 231; 611 South Summit St. P.O. Box 1170; 201 and 219 First Security Bldg., 502 South Front St. P.O. Box 590; 202 Federal Bldg. Location Alaska, College, 99735_____________________ Arizona, Flagstaff, 86002__________________ California, Los Angeles 90424______________ Hawaii, Hawaii National Park, 96718________ Kansas, Lawrence, 66044____________________ Kentucky, Lexington, 40503_________________ Maryland, Beltsville, 20705________________ GEOLOGIC DIVISION Geologist in charge and telephone number Robert M. Chapman (479-6725)____________ Eugene M. Shoemaker (774-5081)__________ John T. McGill (GRanite 3-0971, ext. 9881) Howard A. Powers (678-485)_______________ Windsor L. Adkison (Viking 3-2700)______ Paul W. Richards (4-2473)............... Louis Pavlides (GRanite 4-4800, ext. 468) Massachusetts, Boston, 02116____________ Lincoln R. Page (KEnmore 6-1444)____________ New Mexico, Albuquerque, 87100__________ Charles B. Read (CHapel 7-0311, ext. 483) Ohio, Columbus, 43200___________________ James M. Schopf (AXminister 4-1810)_________ Pennsylvania, Mt. Carmel, 17851_________ Jacques F. Robertson (339-4390)_____________ Puerto Rico, Roosevelt, 00927___________ Watson H. Monroe (San Juan 6-5340)__________ •See footnote, p. A227. Address P.O. Box 580; Brooks Memorial Bldg. P.O. Box 1906. Geology Bldg., Univ. of California. Hawaiian Volcano Observatory. c/o State Geological Survey, Lindley Hall, Univ. of Kansas. 496 Southland Drive. U.S. Geological Survey Bldg., Dept, of Agriculture Research Center. 270 Dartmouth St., Rm. 1. P.O. Box 4083, Station A; Geology Bldg., Univ. of New Mexico. Orton Hall, Ohio State Univ., 155 Oval Drive. P.O. Box 366; 56 West 2d St. P.O. Box 803.SELECTED FIELD OFFICES IN THE UNITED STATES AND PUERTO RICO A229 Location Tennessee, Knoxville, 37902_ Texas, Austin, 78705_______ Houston, 77030________ Utah, Salt Lake City, 84111. Washington, Spokane, 99204 Wisconsin, Madison, 53706.. Wyoming, Laramie, 82070.. Otologist in charge and telephone number Robert A. Laurence (2-7787)____________ D. Hoye Eargle (HObart 5-6501)_________ A. L. Chidester (774-5081)............. Lowell S. Hilpert (524-5640)___________ Albert E. Weissenborn (TEmple 8-2084) Carl E. Dutton (262-1854)______________ J. David Love (FRanklin 5-4495)________ Address 11 Post Office Bldg. P.O. Box 189; Balcones Research Center, Route 4. P.O. Box 1906; Flagstaff, Ariz. 86002. 8426 Federal Bldg. South 157 Howard St. 222 Science Hall, Univ. of Wisconsin. Geology Hall, Univ. of Wyoming. Location California, Menlo Park, 94025 Colorado, Denver, 80225_________ Missouri, Rolla, 65401__________ Virginia, Arlington, 22201______ TOPOGRAPHIC DIVISION Engineer in charge and telephone number Robert O. Davis (415 325-6761, ext. 411).. Roland H. Moore (303 233-3611, ext. 8551) Daniel Kennedy (314 364-3680)_________ Charles F. Fuechsel (703 JAckson 5-7550).. Address 345 Middlefield Rd. Federal Center Bldg. 25. P.O. Box 133; 9th and Elm Sts. 1109 N. Highland St. Location Atlantic Coast Area__________ Arlington, Va., 20242. Midcontinent Area____________ St. Louis, Mo., 63103. Rocky Mountain Area_________ Denver, Colo., 80225. Pacific Coast Area___________ Menlo Park, Calif., 94025. WATER RESOURCES DIVISION Official in charge* and telephone number Address Area Offices George E. Ferguson, Division Hydrologist (202 343-4840). Harry D. Wilson, Jr., Division Hydrologist (314 622-4361). Sherman K. Jackson, Division Hydrologist (303 233-3611). Warren W. Hastings, Division Hydrologist (415 325-6761). George Washington Bldg., Arlington Towers, 1011 Arlington Blvd. 1252 Federal Bldg., 1520 Market St. Federal Center, Bldg. 25. 345 Middlefield Rd. Alabama, University, 35486. Alaska, Anchorage, 99501____ Juneau, 99801__________ Palmer, 99645__________ Arizona, Tucson, 85717______ Arkansas, Little Rock, 72201 California, Menlo Park, 94025 Sacramento, 95814________________ Colorado, Denver, 80215_____ Denver, 80225___________ Connecticut, Hartford, 06101 Middletown, 06458_______ Delaware, Dover, 19901______ Florida, Ocala, 32670_______ Tallahassee, 32304______ District Offices William J. Powell (g) and Lamar E. Carroon (s) (205 752-8105). Melvin V. Marcher (g) (Broadway 2-8333)_______ Ralph E. Marsh (s) (907 586-2815)_____________ Robert G. Schupp (q) (907 745-3115)__________ Horace M. Babcock (w) (602 623-7731, ext. 291 and 294). Richard T. Sniegocki (g) (501 372-4361, ext. 270), John H. Hubble (q) (501 372-4361, ext. 219), and Ivan D. Yost (s) (501 372-4361, ext. 706). Walter Hofmann (s) (415 325-6761)_____________ Fred Kunkel (g) (916 449-2563) and Stanley F. Kapustka (q) (916 449-3174). John W. Odell (s) (303 233-3611, ext. 6444)___ Leonard A. Wood (g) (303 233-3611, ext. 546)... John Horton (s) (203 527-3281, ext. 257)______ John A. Baker (g) (203 346-6986)______________ Philip P. Fannebecker (s) (302 734-2506)______ Kenneth A. MacKichan (q) and Archibald O. Patterson (s) (305 622-6513). Clyde S. Conover (g) (305 224-1202 and 1203)__ P.O. Box V; Oil and Gas Board Bldg., Univ. of Alabama. P.O. Box 393; 311 Federal Bldg. P.O. Box 2659; 203 Simpson Bldg., 222 Seward St. P.O. Box 36; Wright Bldg. P.O. Box 4070; Geology Bldg., Univ. of Arizona Campus. 2307, 2007, and 2301 Federal Bldg. 345 Middlefield Rd. 8024 and 8042 Federal Bldg. & U.S. Court House, 650 Capitol Ave. Rm. 22, 1455 Ammons St. Federal Center, Bldg. 25. P.O. Box 715; 203 Federal Bldg. 204 Post Office Bldg. P.O. Box 707; 604 Fairview Ave. 244 Federal Bldg. P.O. Box 2315; Gunter Bldg. (Tennessee and Woodward Sts.). ♦The small letters in parentheses following each official’s name signifies his affiliation in the Water Resources Division, as follows: g—Ground Water Branch; q—Quality of Water Branch; s-Surface Water Branch; w—Water Resources Division.A230 U.S. GEOLOGICAL SURVEY OFFICES Location Georgia, Atlanta, 30303_______ Atlanta, 30323____________ Hawaii, Honolulu, 96814_______ Idaho, Boise, 83702____________ Illinois, Champaign, 61820____ Indiana, Indianapolis, 46204.. Iowa, Iowa City, 52241_________ Iowa City, 52240__________ Kansas, Lawrence, 66045________ Topeka, 66601_____________ Kentucky, Louisville, 40202____ Louisiana, Baton Rouge, 70806 Baton Rouge, 70803________ Maine, Augusta, 04330______ Maryland, Baltimore, 21218. College Park, 20740________ Rockville, 20850________ Massachusetts, Boston, 02110 Michigan, Lansing, 48933_____ Minnesota, St. Paul, 55101__ Mississippi, Jackson, 39205 Missouri, Rolla, 65401 Montana, Billings, 59601. Helena, 59601________ Nebraska, Lincoln, 68508 Nevada, Carson City, 89701______ New Jersey, Trenton, 08605______ Trenton, 08607______________ New Mexico, Albuquerque, 87106. Santa Fe, 87501............. New York, Albany, 12201_________ North Carolina, Raleigh, 27602__ Official in charge* and telephone number District Offices—Continued Harlan B. Counts (g) (404 688-5996)_____________ Albert N. Cameron (s) (404 876-3311, ext. 5218). Dan A. Davis (g) (588-111, ext. 694, 695) and Mearle M. Miller (s) (588-111 ext. 692, 693). Wayne I. Travis (s) (208 342-2711, ext. 531) and Herbert A. Waite (g) (208 342-2711, ext. 539). William D. Mitchell (s) (217 356-5221)__________ Malcolm D. Hale (s) (317 633-7389) and Claude M. Roberts (g) (317 633-7382). Vernal R. Bennion (s) (319 337-9345)_____________ Walter L. Steinhilber (g) (319 338-1173)________ Robert J. Dingman (g) (913 864-3001)____________ Edward J. Kennedy (s) (913 233-0521)____________ Robert V. Cushman (g) and Floyd F. Schrader (s) (502 582-5241). Mack R. Stewart (s) and Russel M. McAvoy (q) (504 924-4215). Rex R. Meyer (g) (504 343-2873)_________________ Gordon S. Hayes (s) and Glenn C. Prescott (g) (207 623-4511, ext. 250). Edmond G. Otton (g) (301 235-0771)............. William E. Forrest (s) (301 277-6270)........ John W. Wark (q) (301 762-2885)________________ Richard G. Peterson (g) (617 223-2822) and Charles E. Knox (s) (617 223-2824). Arlington D. Ash (s) (517 489-2431) and Gerth E. Hendrickson (g) (517 489-7913). David B. Anderson (s) (612 222-8011, ext. 265) and Richmond H. Brown (g) (612 222-8011, ext. 260). Joe W. Lang (g) (601 354-3881, ext. 328) and William H. Robinson (s) (601 354-3881, ext. 326). Anthony Homyk, Jr. (s) (314 364-1599)_________ Edward J. Harvey (g) (314 364-1752, ext 16.)___ Charles W. Lane (g) (406 259-2412)............. Frank Stermitz (s) (406 442-4890)______________ Don M. Culbertson (q), Charles K. Keech (g), and Floyd F. Lefever (s) (402 435-3273, ext. 346, 323, and 328). George F. Worts, Jr. (w) (702 472-1388)........ John E. McCall (s) (609 394-5301, ext. 214).... Allen Sinnott (g) (609 394-5301, ext. 213)_____ Samuel W. West (g) and Jay M. Stow (q) (505 247-0311, ext. 2248 and 2249). Wilbur L. Heckler (s) (505 982-1921)___________ Ralph C. Heath (g), Donald F. Dougherty (s), Felix H. Pauszek (q) (518 463-5581). Robert A. Krieger (q), Granville G. Wyrick (g), (919 828-4345), Edward B. Rice (s) "(919 834-6429). Address Rm. 416, 19 Hunter St., Southwest. Rm. 164, Peachtree Seventh Bldg. 332 and 330 First Insurance Bldg., 1100 Ward Ave. Rms. 215 and 205, 914 Jefferson St. 605 South Neil St. Rm. 407, 611 North Park Ave. 508 Hydraulic Laboratory. Geological Survey Bldg. c/o Univ. of Kansas. P.O. Box 856; 403 Federal Bldg. 310 Center Bldg., 522 West Jefferson St. 215 and 201 Prudential Bldg., 6554 Florida Blvd. P.O. Box GS, University Station; 43 Atkinson Hall, Louisiana State Univ. Vickery Hill Bldg., Court St. 103 Latrobe Hall, The Johns Hopkins Univ. P.O. Box 37; 106 Engineering Classroom Bldg., Univ. of Maryland. 3 Abbey Bldg., 3 North Perry St. Rms. 206, 205, 211 Congress St. 407 Capitol Savings and Loan Bldg. 1610 and 1002 New Post Office Bldg. P.O. Box 2052; 302 U.S. Post Office Bldg. P.O. Box 138; 900 Pine St. P.O. Box 138; c/o Missouri Geological Survey and Water Resources, Buehler Park. P.O. Box 1818; Bell Bldg., 2 South 7th St. West. P.O. Box 1696; 409 Federal Bldg. 125 Nebraska Hall, 901 North 17th St. 222 E. Washington St. P.O. Box 967; 433 Federal Bldg. P.O. Box 1238; 432 Federal Bldg. P.O. Box 4217; Geology Bldg., Univ. of New Mexico. P.O. Box 1750; Greer Bldg., 113 Washington Ave. P.O. Box 948; Rms. 342, 343, 348 Federal Bldg. P.O. Box 2857; 4th Floor, Federal Bldg. 'See footnote p. A229.OFFICES IN OTHER COUNTRIES A231 Location North Dakota, Bismarck, 58502__. Ohio, Columbus, 43212___________ Columbus, 43209____________ Columbus, 43215____________ Oklahoma, Oklahoma City, 73102 Oklahoma City, 73109 Oregon, Portland, 97208____ Pennsylvania, Harrisburg, 17104. Philadelphia, 19106_________ Puerto Rico, Hato Rey, 00918____ Rhode Island, Providence, 02903 South Carolina, Columbia, 29201 Columbia, 29205___________ South Dakota, Huron, 57350__. Pierre, 57501_____________ Tennessee, Chattanooga, 37402 Texas, Austin, 78701__________ Utah, Salt Lake City, 84111___ Virginia, Charlottesville, 22903.. Washington, Tacoma, 98409______ West Virginia, Charleston, 25301 Morgantown, 26506_________ Wisconsin, Madison, 53706______ Madison, 53705____________ Wyoming, Cheyenne, 82002_______ Worland, 82401____________ Location Bolivia, La Paz______________ •See footnote, p. A229. Official in charge' and telephone number District Offices—Continued Harlan M. Erskine (s) (701 223-3525) and Delbert W. Brown (g) (701 255-0191). John J. Molloy (s) (614 221-6411, ext. 113)_____ George W. Whetstone (q) (614 221-6411, ext. 118) _ Stanley E. Norris (g) (614-221-6411, ext. 281)__ Alvin R. Leonard (g) 405 236-2311, ext. 412) and Alexander A. Fischback, Jr. (s) (405 236-2311, ext. 257). Richard P. Orth (q) (405 677-5022)______________ Roy B. Sanderson (s) and Eugene R. Hampton (g) (503 226-3361, ext. 1246, 1248). Leslie B. Laird (q) (503 234-3361, ext. 241)___ Joseph E. Barcley (g) (717 238-4925)____________ Robert E. Steacy (s) (717 787-3305)_____________ Norman H. Beamer (q) (215 627-6000, ext. 274) _ _ Dean B. Bogart (w) (766-3310)___________________ William B. Allen (g) (401 331-9312)_____________ Albert E. Johnson (s) (803 252-2449)____________ George E. Siple (g) (803 253-7478)_____________ John E. Powell (g) (605 352-8584)______________ John E. Wagar (s) (605 224-7856)_______________ Joseph S. Cragwall, Jr. (w) (615 266-2725)_____ Charles H. Hembree (q), Allen G. Winslow (g), and Trigg Twichell (s) (512 476-6411). Russell H. Langford (q) (801 524-5661 and 5622), Ted Arnow (g) (801 524-5654 and 5655), and Milton T. Wilson (s) (801 524-5663, 5664, and 5665). James W. Gambrell (s) (703 293-2127)___________ Arthur A. Garrett (g) (206 474-4261)________ Fred M. Veatch (s) (206 383-1491)__________- William C. Griffin (s) (304 343-6181, ext. 311)_ Porter E. Ward (g) (304 542-8103)___________ Charles R. Holt, Jr. (g) (608 262-2488)_________ Kenneth B. Young (s) (608 233-0195)_________ Ellis D. Gordon (g) and Leon A. Wiard (s) (307 634-2731, ext. 37 and 23). Thomas F. Hanley (q) (307 347-2181)_____________ OFFICES IN OTHER COUNTRIES GEOLOGIC DIVISION Official in charge Charles M. Tschanz_______________________________ Address P.O. Box 750; 7and 17 Eltinge Bldg., 202% 3d St. 1509 Hess St. 554 U.S. Post Office Bldg.; 2822 East Main St. 85 Marconi Blvd. 4011 and 4301 Federal Bldg., 200 Northwest 4th St. P.O. Box 4355; 2800 South Eastern. P.O. Box 3418; 415 and 419 Old Post Office Bldg., 511 NW. Broadway. P.O. Box 3202; 416 Old Post Office Bldg., 511 NW. Broadway. 100 North Cameron St. 1224 Mulberry St. 1302 U.S. Custom House, 2d and Chestnut Sts. 12 Arroyo St. 401-2 Federal Bldg, and U.S. Post Office. 121 Veterans Administration Regional Office Bldg., 1801 Assembly St. P.O. Box 5314; 627 Bull St. P.O. Box 1412; 231 Federal Bldg. P.O. Box 216; 207 Federal Bldg. 823 Edney Bldg. Vaughn Bldg., 807 Brazos St. 305, 125 and 130 Empire Bldg., 231 East 4th South. P.O. Box 3327, University Station; Natural Resources Bldg., McCormick Rd. 3020 South 38th St. 207 Federal Bldg. 3303 New Federal Office Bldg., 500 Quarrier St. East. 405 Mineral Industries Bldg., Univ. of West Virginia. 175 Science Hall, Univ. of Wisconsin. 5001 University Ave. P.O. Box 177, Frangos Bldg., 2123 Carey Ave. 1214 Big Horn Ave. Address U.S. Geological Survey, U.S. AID/ Bolivia, c/o American Embassy, La Paz, Bolivia. 746-002 0 - 64 - 16A232 U.S. GEOLOGICAL SURVEY OFFICES Locution Official in charge Address Brazil, Rio de Janeiro------------------ Alfred J. Bodenlos__________________________________ U.S. Geological Survey, U.S. AID/ Rio, APO 676, New York, N.Y. Colombia, Bogota------------------------ Earl M. Irving______________________________________ U.S. Geological Survey, U.S. AID/ American Embassy, Bogota, Colombia. Dahomey, Cotonou------------------------ Jules A. MacKallor__________________________________ U.S. Geological Survey, U.S. AID/ Cotonou, U.S. Department of State, Washington, D.C. 20523. Germany, Heidelberg--------------------- Jerald M. Goldberg__________________________________ U.S. Geological Survey Team Rep- resentative (Europe), USAREUR Engineer Intelligence Center, APO 403, New York, N.Y. Indonesia, Bandung---------------------- Reed J. Anderson____________________________________ U.S. Geological Survey, U.S. AID/ American Embassy, APO 156, San Francisco, Calif. Liberia, Monrovia----------------------- Darwin L. Rossman___________________________________ U.S. Geological Survey, U.S. AID/ Monrovia, U.S. Department of State, Washington, D.C. 20523. Pakistan, Quetta------------------------ Max G. White________________________________________ U.S. Geological Survey, U.S. AID/ American Embassy, APO 271 New York, N.Y. Philippines, Manila--------------------- Joseph F. Harrington________________________________ U.S. Geological Survey, c/o Ameri- can Embassy, APO 928, San Francisco, Calif. Saudi Arabia, Jidda--------------------- Glen F. Brown_______________________________________ U.S. Geological Survey, c/o Ameri- can Embassy, APO 697, New York, N.Y. Thailand, Bangkok----------------------- Charles T. Pierson__________________________________ U.S. Geological Survey/UN, c/o American Embassy, APO 146, San Francisco, Calif. WATER RESOURCES DIVISION Location Official in charge Address Afghanistan, Kabul_____________________ Arthur 0. Westfall________________________________ U.S. Geological Survey, U.S. AID/ Kabul, U.S. Department of State, Washington, D.C. 20523. Brazil, Recife_________________________ Stuart L. Schoff (g) and Leonard J. Snell (s)_____ U.S. Geological Survey, U.S. AID/ Brazil (Recife), APO 676, New York, N.Y. Nepal, Katmandu________________________ Woodrow W. Evett________________________________ U.S. Geological Survey, U.S. AID/N (Box KAT), APO 959, San Francisco, Calif. Nigeria, Kaduna________________________ David A. Phoenix__________________________________ U.S. Geological Survey, U.S. AID/ Lagos (Kaduna), U.S. Department of State, Washington, D.C. 20523. Pakistan, Lahore_______________________ Maurice J. Mundorff_______________________________ U.S. Geological Survey, U-S- AID/ Pakistan, APO 271, New York, N.Y. Tunisia, Tunis_________________________ Vinton C. Fishel__________________________________ U.S. Geological Survey, c/o U.S. AID/Tunis, U.S. Dept, of State, Washington, D.C. 20523. Turkey, Ankara_________________________ C. Richard Murray_________________________________ U.S. Geological Survey, U.S. Eco- nomic Coordinator/Ankara, APO 254, New York, N.Y. United Arab Republic, Egypt, Cairo_____ Robert L. Cushman_______________________________ U.S. Geological Survey, U.S. AID/ Cairo, U.S. Dept, of State, Washington, D.C. 20523.INVESTIGATIONS IN PROGRESS IN THE GEOLOGIC, WATER RESOURCES, AND CONSERVATION DIVISIONS Investigations in progress during fiscal year 1964 are listed below, together with the names and headquarters of the individuals in charge of each. Headquarters at main centers are indicated by (W) for Washington, D.C., (D) for Denver, Colo., and (M) for Menlo Park, Calif. Headquarters in other cities are indicated by name; see list of offices (p. A227) for addresses. Inquiries regarding projects for which no address is given in the list of offices should be directed to the appropriate Division of the Geological Survey, Washington, D.C. 20242. Lowercase letter following the name of the project leader shows the division technical responsibility: c, Conservation Division; w, Water Resources Division (g, Ground Water Branch; s, Surface Water Branch; q, Quality of Water Branch; h, General Hydrology Branch); no letter, Geologic Division. The projects are classified by principal topic. Most geologic-mapping projects involve special studies of stratigraphy, petrology, geologic structure, or mineral deposits, but are listed only under Geologic Mapping unless a special topic or commodity are the primary justification for the project. A reader interested in investigations of volcanology, for example, should look under the heading Geologic Mapping for projects in areas of volcanic rocks, as well as under the heading Volcanology. Likewise, most water-resources investigations involve special studies of several aspects of hydrology and geology, but are listed only under Water Resources unless the special topic—such as floods or sedimentation—is the primary justification for the project. Areal geologic mapping is subdivided into mapping at scales smaller than 1 inch to 1 mile (for example, 1:250,000), and mapping at scales of 1 inch to 1 mile, or larger (1: 62,500; 1: 24,000). Analytical chemistry: Analytical methods—water chemistry (M. W. Skougstad, q, D) Analytical services and research (I. May, W; L. F. Rader, Jr., D; R. E. Stevens, M) Organic geochemistry and infrared analysis (I. A. Breger, W) Organic substances in water (W. L. Lamar, q, M) Physical chemistry of radioelements (K. W. Edwards, q, D) Rock and mineral chemical analysis (J. J. Fahey, W) Rock chemical analysis: general (L. C. Peck, D) rapid (L. Shapiro W) Trace analysis methods: development (H. W. Lakin, D) research (F. N. Ward, D) Trace analysis service (F. N. Ward, D) See also Spectroscopy. Artificial recharge: Basalt aquifers, Salem Heights, Oreg. (B. L. Foxworthy, g, Portland) Basalt aquifers, The Dalles, Oreg. (B. L. Foxworthy, g, Portland) Experimental recharge basin—surface water (R. M. Sawyer, s, Albany, N.Y.) Grand Prairie region, Arkansas (R. T. Sniegocki, g, Little Rock) Artificial recharge—Continued High Plains, N. Mex. (J. S. Havens, g, Albuquerque) Kalamazoo, Mich. (J. E. Reed, g, Lansing) Water application and use on a range water spreader, northeast Montana (F. A. Branson, w, D) Asbestos: Arizona, McFadden Peak and Blue House quadrangles (A. F. Shride, D) Southeastern United States, ultramafic rocks (D. M. Lar-rabee, W) Vermont, north-central (W. M. Cady, D) Barite: Arkansas (D. A. Brobst, D) Base metals: Colorado: Tenmile Range and Kokomo mining district (M. H. Bergendahl, D) Wet Mountains (M. R. Brock, D) Montana, Philipsburg area (W. C. Prinz, W) Nevada, Antler Peak quadrangle (R. J. Roberts, M) Utah, San Francisco Mountains (D. M. Lemmon, M) See also base-metal names. Bauxite: Hawaii, Kauai (S. H. Patterson, W) Southeastern United States (E. F. Overstreet, W) Beryllium: Alaska, Lost River mining district (C. L. Sainsbury, D) A233A234 INVESTIGATIONS IN PROGRESS IN THE GEOLOGIC, WATER RESOURCES, AND CONSERVATION DIVISIONS Beryllium—Continued Colorado: Lake George district (C. C. Hawley, D) Mt. Antero (W. N. Sharp, D) Nevada, Mt. Wheeler mine area (D. E. Lee, D) Utah, Thomas and Dugway Ranges (M. H. Staatz, D) Western United States, volcanic and associated rocks (D. R. Shawe, D) Bibliographies and abstracts: Alaskan geology, index of literature (E. H. Cobb, M) Bibliography of hydrology (J. R. Randolph, w, W) Geochemical exploration abstracts (E. L. Markward, D) Geophysical abstracts (J. W. Clarke, W) North American geology, bibliography (M. Cooper, W) Vanadium, geology and resources, bibliography (J. P. Ohl, D) Borates: Borate marshes of California, Oregon, and Nevada (W. C. Smith, M) California: Furnace Creek area (J. F. McAllister, M) Searles Lake area (G. I. Smith, M) Chromite. See Ferro-alloy metals. Clay-water relations: Liquid movement in clays (H. W. Olsen, h, W) Solubility of kaolinite (W. L. Polzer, q, M) Clays: Colorado Plateau (L. G. Schultz, D) Florida and Georgia, Attapulgus-Thomasville fuller’s earth deposits (S. H. Patterson, W) Idaho, Greenacres quadrangle (P. L. Weis, W) Maryland, statewide studies (M. M. Knechtel, W) Washington: Eastern (J. W. Hosterman, W) Greenacres quadrangle (P. L. Weis, W) Coal: Minor elements in coal (P. Zubovic, W) Alabama: Resources of State (W. C. Culbertson, D) Warrior quadrangle (W. C. Culbertson, D) Alaska: Bering River coal field (A. A. Wanek, c, Anchorage) Beluga-Yentna area (F. F. Barnes, M) Matanuska, stratigraphic studies (A. Grantz, M) Nenana, coal investigations (C. Wahrhaftig, M) Arizona, Navajo Reservation, fuels potential (R. B. O’Sullivan, D) Arkansas: Arkansas Basin investigations (B. R. Haley, D) Ft. Smith district (T. A. Hendricks, D) California, SW% Priest Valley quadrangle (E. E. Richardson, c, Taft) Colorado: Animas River area (H. Barnes, D) Anthracite NE and NW, and Snowmass SW quadrangles (D. L. Gaskill, c, D) Carbondale coal field (J. R. Donnell, D) Elk Springs quadrangle (J. R. Dyni, c, D) Fort Lupton, Hundson, Platteville, Hanover NW and Corral Bluff quadrangles (P. E. Soister, c, D) Coal—Continued Colorado—Continued Hot Sulphur Springs and Kremmling quadrangles (G. A. Izett, c, D) Montrose 1 SW, 1 SE, 4 NE, and Cerro Summit quadrangles (R. G. Dickinson, c, D) Placita, SE quadrangle (L. D. Godwin, c, D) Trinidad coal field (R. B. Johnson, D) Iowa, resources of State (E. R. Landis, D) Kentucky: Eastern part of State (K. J. Englund, W) Jellieo West and Ketchen quadrangles (K. J. Englund, W) Montana: Anaconda 3 NW quadrangle (A. A. Wanek, c, Anchorage, Alaska) Black Butte and Hedstrom quadrangles (A. W. Bateman, c, Great Falls) Gardiner SW quadrangle (G. D. Fraser, c, D) Girard coal field (G. E. Prichard, D) Jordan quadrangle (G. D. Mowat, c, Great Falls) Montaqua quadrangle (E. D. Patterson, c, W) Powder River coal fields (N. W. Bass, D) Rocky Reef and Hardy quadrangles (K. S. Soward, c. Great Falls) New Mexico: Animas River area (H. Barnes, D) Johnson Trading Post quadrangle (J. S. Hinds, c, Farmington) Mesa Portales quadrangle (J. E. Fassett, c, Farming-ton) Raton coal basin, eastern (G. H. Dixon, D) Raton coal basin, western (C. L. Pillmore, D) San Juan Basin, east side (C. H. Dane, W) San Juan basin, withdrawn coal area (J. E. Fassett, c, Farmington) North Dakota: Dengate and Heart Butte NW quadrangles (E. V. Stephens, c, D) Glen Ullin quadrangle (C. S. V. Barclay, c, D) New Salem 2 SW and North Altmont quadrangles (H. L. Smith, c,D) Oklahoma, Ft. Smith district (T. A. Hendricks, D) Oregon, Bandon SE and Coquille SW quadrangles (E. M. Baldwin, c, Los Angeles, Calif.) Pennsylvania: Anthracite-mine drainage projects, geology in vicinity of (J. F. Robertson, Mt. Carmel) Anthracite region, flood control (M. J. Bergin, Mt. Carmel) Bituminous coal resources of State (E. D. Patterson, W) Southern anthracite field (G. H. Wood, Jr., W) Washington County (B. H. Kent, D) Western Middle anthracite field (H. Arndt, W) South Dakota, Harding County and adjacent areas (G. N. Pipiringos, D) Tennessee: Ivydell and Pioneer quadrangles (K. J. Englund, W) Jellieo West and Ketchen quadrangles (K. J. Englund, W)COAL—CONTAMINATION, WATER A235 Coal—Continued Utah: Gunsight Butte quadrangle (Fred Peterson, c, D) Hurricane fault (southwestern Utah) (P. Averitt, D) Kaiparowits Peak 4 quadrangle (H. D. Zeller, c, D) Kolob Terrace coal field, southern (W. B. Cashion, D) Navajo Reservation, fuels potential (R. B. O’Sullivan, D) Nipple Butte quadrangle (H. A. Waldrop, c, D) Ogden 4 quadrangles (T. A. Mullens, c, D) Wyoming: Adam Weiss Peak quadrangle (W. L. Rohrer, c, D) Carbon and Northern Laramie basins (H. J. Hyden, c, D) Ferris quadrangle (R. L. Rioux, c, D) Fish Lake and Kissinger Lakes quadrangles (W. L. Rohrer, c, D) Jackson 30-minute quadrangle (D. A. Jobin, c, D) Oregon Buttes area (H. D. Zeller, c, D) Sheep Mountain and Tatman Mountain quadrangles (W. L. Rohrer, c, D) Virginia, Big Stone Gap district (R. L. Miller, W) Washington, Maple Valley, Hobart and Cumberland quadrangles (J. D. Vine, M) Construction and terrain problems : Deformation research (D. J. Vames, D) Ground-movement inventory (A. S. Allen, W) Lunar terrain studies (C. R. Warren, W) Miscellaneous site studies (D. J. Vames, D) . Mudflow studies (D. R. Crandell, D) Project bilby, close-in aquifer response to a nuclear detonation (W. E. Hale, D) Project dogsled, selection of sandstone site for nuclear cratering experiment (W. S. Twenhlofel, D) Project perris wheel, selection of carbonate rock sites for nuclear experiments (R. E. Davis, D) Project schooner, selection of granite site for nuclear cratering experiment (W. S. Twenhofel, D) Sino-Soviet terrain atlas (M. M. Elias, W) Water-resources development, potential applications of nuclear explosives (A. M. Piper, M, and F. W. Stead, D) Alaska: Mt. Hayes D-3 and D^4 quadrangles (T. L. P6w£, College) Northeastern Alaska coastal plain and foothills (C. R. Lewis, W) Origin and stratigraphy of ground ice in central Alaska (T. L. Pdw6, College) Project chariot (harbor construction) (G. D. Eber-lein, M) Surficial and engineering geology : Anchorage-Matanuska Glacier area (T. N. V. Karl- strom, W) Bristol Bay area (E. H. Muller, Ithaca, N.Y.) Construction-materials sources (T. L. P6wd, College) Copper River Basin, northeastern (O. J. Ferrians, Jr., W) Construction and terrain problems—Continued Alaska—Continued Surficial and engineering geology—Continued Copper River Basin, southeastern (D. R. Nichols, W) Copper River basin, southwestern (J. R. Williams, W) Eastern Denali Highway (D. R. Nichols, W) Johnson River district (H. L. Foster, W) Kenai lowland (T. N. V. Karlstrom, W) Kobuk River valley (A. T. Femald, W) Lower Chitina Valley (L. A. Yehle, W) Mt. Chamberlain area (C. R. Lewis, W) Seward-Portage Railroad (T. N. V. Karlstrom, W) Slana-Tok area (H. R. Sehmoll, W) Steese Highway area (W. E. Davies, W) Taylor Highway area (H. L. Foster, W) Upper Tanana River (A. T. Femald, W) Valdez-Tiekel belt (H. W. Coulter, W) Yukon-Koyukuk lowland (F. R. Weber, College) California, Bodega Head reactor site (J. Schlocker, M) Colorado: Air Force Academy (D. J. Vames, D) Black Canyon of the Gunnison River (W. R. Hansen, D) Cheyenne Mountain, electrical properties (J. H. Scott, D) Roberts Tunnel (C. S. Robinson, D) Straight Creek tunnel (C. S. Robinson) Upper Green River valley (W. R. Hansen, D) Greenland, terrain studies (W. E. Davies, W) Massachusetts: Application of geology and seismology to public works planning (C. R. Tuttle and R. N. Oldale, Boston) Sea-cliff erosion studies (C. A. Kaye, Boston) Montana: Wolf Point area (R. B. Colton, W) Nebraska: Franklin, Webster, and Nuckolls Counties (R. D. Miller, D) Valley County (R. D. Miller, D) Nevada: Nevada Test Site, Pahute Mesa (F. N. Houser, D) Nevada Test Site, site studies (R. E. Davis, D) New Mexico, Nash Draw quadrangle (L. M. Gard, D) South Dakota, Fort Randall Reservoir area (D. J. Varnes, D) Utah: Coal-mine bumps (F. W. Osterwald, D) Oak City area (D. J. Vames, D) Upper Green River valley (W. R. Hansen, D) Virginia, Herndon quadrangle (R. E. Eggleton, Flagstaff, Ariz.) See also Urban geology. Contamination, water: Cadmium-chromium and detergent contamination in ground water, Nassau County N.Y. (N. M. Perlmutter, g, Albany) Determination of pesticides and insecticides in water (G. Stratton, q, Columbus, Ohio)A236 INVESTIGATIONS IN PROGRESS IN THE GEOLOGIC, WATER RESOURCES, AND CONSERVATION DIVISIONS Contamination, water—Continued Ground-water contamination (H. E. LeGrand, g, W) Sewage lagoon study (W. J. Powell, g, Tuscaloosa, Ala.) See also Detergents, Radioactive-waste disposal. Copper: Massive sufide deposits (A. R. Kinkel, Jr., W) Sandstone copper deposits, Southwest United States (C. B. Read, Albuquerque, N. Mex.) Alaska, southern Brooks Range (W. P. Brosgfi, M) Arizona: Benson and Mammoth quadrangles (S. C. Creasey, M) Globe-Miami area (D. W. Peterson, M) Klondyke quadrangle (F. G. Simons, D) Little Dragoons area (J. R. Cooper, D) Lochiel and Nogales quadrangles (F. S. Simons, D) Twin Buttes area (J. R. Cooper, D) Colorado, Lisbon Valley area (G. W. Weir, Berea, Ky.) Michigan, Michigan copper district (W. S. White, W) Nevada, Ely district (A. L. Brokaw, D) New Mexico, Silver City region (W. R. Jones, D) Tennessee, Ducktown district and adjacent areas (R. M. Hernon, D) Utah: Bingham Canyon district (R. J. Roberts, M) Lisbon Valley area (G. W. Weir, Berea, Ky.) White Canyon area (R. E. Thaden, Columbia, Ky.) Crustal studies. See Geophysics, regional. Crystallography. See Mineralogy and crystallography. Detergents: Behavior of detergents and other pollutants in soil-water environments (C. H. Wayman, h, D) Detergent contamination in three public-supply well fields, Suffolk County, N.Y. (N. M. Perlmutter, g, Albany) Engineering geologic studies. See Construction and terrain problems; Urban geology. Evaporation: Evaporation from Lake Helene, Fla. (R. B. Stone, s, Ocala) Pond-evaporation study (F. N. Lee, s, Baton Rouge, La.) Reservoir evaporation, San Diego County, Calif. (W. Hofmann, s, M) Evaporation suppression (G. E. Koberg, h, D) Evapotranspiration: Effect of removing riprian vegetation, Cottonwood Wash, Ariz. (J. E. Bowie, w, Tucson) Evapotranspiration measurements, Deep Creek, Tex. (F. W. Kennon, s, Austin) Evapotranspiration theory and measurement (O. E. Lep-panen, h, Phoenix, Ariz.) Hydrologic effects of vegetation modification (R. M. Myrick, h, Tucson, Ariz.) Phreatophyte study, Gila River, Ariz. (R. C. Culler, h, Tucson) Use of water by saltcedar in evapotranspirometers compared with energy-budget and mass-transfer computations (T. E. A. Van Hylckama, h, Tucson, Ariz.) Extraterrestrial studies: Astronauts, geologic-training program (R. E. Eggleton, Flagstaff, Ariz.) Extraterrestrial studies—Continued Cratering, impact, and thermal investigations : Experimental hypervelocity impact studies (H. J. Moore, M) Impact metamorphism (E. C. T. Chao, W) Shock-phase studies (D. J. Milton, M) Tension fractures and thermal investigations (A. H. Lachenbruch, M) Terrestrial impact structures (E. M. Shoemaker, Flagstaff, Ariz.) Thermoluminescence and mass physical properties (C. H. Roach, D) Lunar experiments: Lunar physical properties, measuring techniques (E. M. Shoemaker, Flagstaff, Ariz.) X-ray fluorescence equipment for lunar studies (I. Adler, W) Lunar mapping: Lunar stratigraphy and structure (R. J. Hackman, W; H. Masursky, M) Lunar photometry (W. A. Fischer, W) Lunar-terrain studies (C. R. Warren, W) Tektite and meteorite investigations: Magnetic properties of tektites (A. N. Thorpe, W) Chemistry of tektites (F. Cuttita, W) Mineralogy and petrology of meteorites and tektites (E. C. T. Chao, W) Ferro-alloy metals: Molybdenum-rhenium resource studies (R. U. King, D) Manganese, geology and geochemistry (D. F. Hewett, M) Ultramafic rocks of the Southeastern United States (D. M. Larrabee, W) California: Chromite deposits, northern California (F. G. Wells, W) Nickel deposits, Klamath Mountains (P. E. Hotz, M) Tungsten, Bishop district (P. C. Bateman, M) Idaho, Blackbird Mountain area (J. S. Vhay, Spokane, Wash.) Montana: Chromite resources and petrology, Stillwater complex (E. D. Jackson, Houston, Tex.) Manganese deposits, Philipsburg area (W. C. Prinz, W) Oregon: John Day area (T. P. Thayer, W) Nickel deposits, Klamath Mountains (P. E. Hotz, M) Utah, San Francisco Mountains (D. M. Lemmon, M) Flood characteristics of streams at selected sites: Alabama (C. O. Ming, s, Tuscaloosa) Florida (W. C. Bridges, s, Ocala) Georgia (C. M. Bunch, s, Atlanta) Illinois (W. D. Mitchell, s, Champaign) Kentucky (C. H. Hannum, s, Louisville) Mississippi (K. V. Wilson, and C. Humphreys, Jr., s, Jack-son) Nebraska (E. W. Beckman, s, Lincoln) Puerto Rico (I. J. Hickenlooper, w, San Juan) Tennessee (W. J. Randolph, w, Chattanooga) Wyoming (J. R. Carter, s, Cheyenne)FLOOD DISCHARGE—FOREIGN NATIONS A237 Flood discharge from small drainage areas: Arizona (B. N. Aldridge, w, Tucson) California (H. A. Ray, s, M) Georgia (C. M. Bunch, s, Atlanta) Illinois (W. D. Mitchell, s, Champaign) Iowa (H. H. Schwob, s, Iowa City) Kansas (L. W. Furness, s, Topeka) Maine (R. A. Morrill, s, Augusta) Maryland (E. H. Mohler, Jr., s, College Park) Massachusetts (C. G. Johnson, Jr., s, Boston) Mississippi (K. V. Wilson, s, Jackson) Missouri (M. S. Petersen, s, Rolla) Montana (F. C. Boner, s, Helena) Nebraska (E. W. Beckman, s, Lincoln) Nevada (E. E. Harris, w, Carson City) North Dakota (O. A. Crosby, s, Bismarck) Oklahoma (C. W. Sullivan, s, Oklahoma City) South Dakota (R. E. West, s, Pierre) Tennessee, Nashville-Davidson County metropolitan area (L. G. Conn, w, Chattanooga) Vermont (C. G. Johnson, Jr., s, Boston, Mass.) Flood frequency: Comparison of flood-frequency studies for coastal basins in California (R. W. Cruff, S. E. Rantz, s, M) Flood frequency, nationwide (A. R. Green, s, W) Flood magnitude and frequency, North Atlantic Slope basins (R. H. Tice, s, St. Louis, Mo.) Flood volume, duration, frequency (G. A. Kirkpatrick, s, W) Synthesis of flood frequency on small drainage areas from rainfall data (S. E. Rantz, s, M) Alabama (L. E. Carroon, s, Tuscaloosa) California (L. E. Young, s, M) Iowa (H. H. Schwob, s, Iowa City) Kansas (L. W. Furness, s, Topeka) North Carolina (H. G. Hinson, s, Raleigh) Ohio (W. P. Cross, s, Columbus) South Carolina (F. W. Wagener, J. S. Stallings, s, Columbia) Tennessee (W. J. Randolph, w, Chattanooga) Washington (B. N. Aldridge, J. C. Blodgett, s, Tacoma) Wisconsin (D. W. Ericson, s, Madison) Flood-inundation mapping: Flood-inundation maps (A. R. Green, Jr., s, W) Illinois, northeastern (W. D. Mitchell, s, Champaign) New Jersey (J. A. Bettendorf, s, Trenton) New York (D. F. Dougherty, s, Albany) North Carolina (G. C. Goddard, s, Raleigh) Puerto Rico: Arecibo area (M. A. Lopez, w, San Juan) Caguas area (M. A. Lopez, w, San Juan) Humacao area (M. A. L6pez, w, San Juan) Manati area (M. A. Ldpez, w, San Juan) Mayaguez area (M. A. Lopez, w, San Juan) Ponce area (M. A. Ldpez, w, San Juan) Tennessee, Nashville-Davidson County metropolitan area (L. G. Conn, w, Chattanooga) Texas: Dallas, Bachman Branch and Joes Creek (F. H. Ruggles, s, Austin) White Rock Creek (C. R. Gilbert, F. H. Ruggles, s, Austin) Flood investigations, areal: Flood reports (J. O. Rostvedt, s, W) Floods of 1963 (J. O. Rostvedt, s, W) Alabama: Flood gaging (L. E. Carroon, s, Tuscaloosa) Local floods (L. B. Peirce, s, Tuscaloosa) Arizona, Maricopa County, flood investigations (B. N. Aldridge, w, Tucson) Arkansas, flood investigations (R. C. Christensen, s, Little Rock) Georgia: Areal flood studies (C. M. Bunch, s, Atlanta) Flood gaging (C. M. Bunch, s, Atlanta) Hawaii, flood gaging, Oahu (S. H. Hoffard, s, Honolulu) Kansas (L. W. Furness, s, Topeka) Kentucky, floods of March 1964 along the Ohio River (H. C. Beaber, s, Louisville) Louisiana : Flood profile, Sabine River near Logansport (E. M. Miller, s, Baton Rouge) Floods in southwestern Louisiana—rainfall-runoff relations (A. J. Calandro, s, Baton Rouge) New Jersey, flood warning (J. E. McCall, s, Trenton) New York, peak discharge of ungaged streams (S. H. Hladio, s, Albany) North Carolina, flood gaging (H. G. Hinson, s, Raleigh) Ohio, flood of March 1964 (W. P. Cross, s, Columbus) South Carolina, Santee River basin flood study (A. E. Johnson, s, Columbia) Tennessee: Chattanooga Creek, flood profiles (A. M. F. Johnson, w, Chattanooga) Nashville-Davidson County metropolitan area, (L. G. Conn, w, Chattanooga) Texas, hydrologic effects of flood-retarding structures (F. W. Kennon, s, Austin) Utah, flood gaging (Elmer Butler, s, Salt Lake City) Virginia : Fairfax County and Alexandria city, flood hydrology (D. G. Anderson, s, Charlottesville) Flood investigations (C. W. Lingham, s, Charlottesville) Fluorspar: Colorado, Poncha Springs and Bonanza quadrangles (R. E. Van Alstine, W) Utah, Thomas and Dugway Ranges (M. H. Staatz, D) Foreign nations, geologic investigations: Bolivia, mineral resources and geologic mapping (advising and training) (C. M. Tschanz, La Paz) Brazil: Base-metal resources (A. J. Bodenlos, Rio de Janeiro) Geologic education (A. J. Bodenlos, Rio de Janeiro) Iron and manganese resources, Minas Gerais (J. V. N. Dorr II, W) Chile, mineral resources and national geologic mapping (W. Danilchik, Santiago) Colombia, minerals exploration and appraisal (E. Irving, BogotA) Costa Rica, volcanic studies (K. J. Murata, San Jose) Dahomey, minerals reconnaissance (J. A. MacKallor, Cotonou)A238 INVESTIGATIONS IN PROGRESS IN THE GEOLOGIC, WATER RESOURCES, AND CONSERVATION DIVISIONS Foreign nations, geologic investigations—Continued Greenland, eastern, surficial geology, construction-site planning (W. E. Davies, W) Indonesia (R. F. Johnson, Bandung) Japan, calderas, aeromagnetie-gravity studies (H. R. Blank, Jr., M) Liberia (D. L. Rossman, Monrovia) Libya, industrial minerals and national geologic map (G. H. Goudarzi, W) Pakistan, mineral-resources development—advisory and training (M. G. White, Quetta) Philippine Islands, iron, chromite, and nonmetallic mineral resources (J. F. Harrington, Manila) Saudi Arabia, crystalline shield, geologic and minerals reconnaissance (G. F. Brown, Jidda) Thailand, economic geology and mineral industry expansion—advisory (L. S. Gardner, Bangkok) Foreign nations, hydrologic investigations. See Water resources, other countries. Fuels, organic. See Coal, Oil shale, Petroleum and natural gas. Gas, natural. Sec Petroleum and natural gas. Geochemical distribution of the elements: Botanical exploration and research (H. L. Cannon, D) Coding and retrieval of geologic data (T. G. Lovering, D) “Data of Geochemistry” (M. Fleischer, W) Data of rock analyses (M. Hooker, W) Distribution of radioactivity (S. Rosenblum, W) Geochemical sampling and statistical analysis of data (A. T. Miesch, D) Geochemistry of minor elements (G. Phair, W) Mineral fractionation and trace element content of finegrained sedimentary rocks (T. D. Botinelly, D) Minor-element distribution in black shale (J. D. Vine, M) Minor elements in coal (P. Zubovic, W) Minor elements in volcanic rocks (R. R. Coats, M) Organometallic complexes, geochemistry (P. Zubovic, W) Sedimentary rocks, chemical composition (H. A. Tour-telot, D) Synthesis of ore-mineral data (D. F. Davidson, D) California, Sierra Nevada batholith, geochemical study (F. Dodge, M) Colorado, Mount Princeton area (P. Toulmin III, W) Georgia, biogeochemical reconnaissance (H. T. Shack-lette, D) Montana, Boulder batholith, petrochemistry (R. I. Tilling, W) Nevada, Mt. Wheeler mine area, beryllium distribution (D. E. Lee, M) Wisconsin, Driftless area, geochemical survey (H. T. Shacklette, D) Geochemical prospecting methods: Botanical exploration and research (H. L. Cannon, D) Dispersion pattern of minor elements related to igneous intrusions (W. R. Griflitts, D) Geochemical exploration abstracts (E. L. Markward, D) Instrument-development laboratory (W. W. Vaughn, D) Mineral exploration methods (G. B. Gott, D) Mobile spectrographic laboratory (F. N. Ward, D) Plant analysis laboratory (F. N. Ward, D) Geochemical prospecting methods—Continued Areal studies: Alaska, geochemical prospecting techniques (R. M. Chapman, College) Arizona, geochemical halos of mineral deposits (L. C. Huff, Manila, P.I.) Maine: Geochemical mapping (E. V. Post, D) The Forks quadrangle (F. C. Canney, E. V. Post, D) Nevada, geochemical halos of mineral deposits (R. L. Erickson, D) New Mexico, geochemical halos of mineral depostis (L. C. Huff, Manila, P.I.) Utah, geochemical halos of mineral deposits (R. L. Erickson, D) Geochemistry, experimental: Alkali and alkaline-earth salt systems (E. Zen, W) Environment of ore deposition (P. Toulmin III, W) Evaporite-mineral equilibria (E. Zen, W) Fluid inclusions in minerals (E. W. Roedder, W) Geologic thermometry (E. H. Roseboom, Jr., W) Hydrothermal silicate systems (P. Toulmin III, W) Hydrothermal solubility (G. W. Morey, W) Late-stage magmatic processes (G. T. Faust, W) Metallic sulfides and sulfosalt systems (P. Toulmin III, W) Mineral fractionation and trace element content of finegrained sedimentary rocks (T. D. Botinelly, D) Organic geochemistry (J. G. Palacas, D) Organic geochemistry and infrared analysis (I. A. Breger, W) Organometallic complexes, geochemistry (P. Zubovic, W) Rock weathering and alteration (J. J. Hemley, M) Solubility of minerals in aqueous fluid (R. O. Fournier, P. Toulmin III, W) Solution-mineral equilibria (O. L. Christ, W) Thermodynamic properties of minerals (E. H. Roseboom, Jr., W) Geochemistry, water: Age dating of water (W. D. Haney, h, W) Chemistry of atmospheric precipitation (A. W. Gambell, Jr., q, W) Fluoride in ground water, northwest Florida (L. Toler, q, Ocala) Fluoride in ground water, southern New Jersey (A. Sin-nott, g, Trenton) Geochemical controls of water quality (I. Barnes, h, M) Hydrology and geochemistry of the Atlantic coast Continental Shelf and Slope (R. H. Meade, Jr., F. T. Manheim, h, Woods Hole, Mass.) Hydrosolic metals in natural water (J. D. Hem, q, M) Mineral constituents in ground water, and their origin (J. H. Feth, g, M) Mineralogic controls of the chemistry of ground water (B. B. Hanshaw, h, W) Minor constituents in the Belle Fourche River, S. Dak. (L. R. Petri, q, Lincoln, Nebr.) Minor elements in fresh and saline waters of California, occurrence and distribution (W. D. Silvey, q, Sacramento) Minor elements in the Patuxent River basin, Maryland (S. G. Heidel, q, Rockville)GEOCHEMISTRY—GEOLOGIC MAPPING A239 Geochemistry, water—Continued Radioelements in water, occurrence and distribution (R. C. Scott, q, D) Rare halogens, occurrence and distribution (I. Barnes, h, M) Solute composition and minor-element distribution in lacustrine closed basin (B. F. Jones, q, W) Solute-solid relations in lacustrine closed basins of the alkali-carbonate type (B. F. Jones, q, W) Spatial distribution of chemical constituents in ground water (W. Back, h, W) Sulfur-water system under aerobic and anaerobic conditions (C. H. Wayman, h, D) Geochemistry and petrology, field studies : Cave deposits, stratigraphy and mineralogy (W. B. Davies, W) Geochemical sampling and statistical analysis of data (A. T. Miesch, D) Geochemistry of minor elements (G. Phair, W) Green River Formation, mineralogy and geochemistry (C. Milton, W) Humates, geology and geochemistry (V. E. Swanson, D) Igneous rocks of Southeastern United States (C. Milton, W) Jasperoids (T. G. Lovering, D) Manganese, geology and geochemistry (D. F. Hewett, M) Metamorphic rocks and ore deposits (R. G. Coleman, M) Ore lead, geochemistry and origins (R. S. Cannon, D) Pacific coast basalts, geochemistry (K. J. Murata, M) Pierre Shale, chemical and physical properties, Montana, North Dakota, South Dakota, Wyoming, and Nebraska (H. A. Tourtelot, D) Rare-earth elements, resources and geochemistry (J. W. Adams, D) Sedimentary petrology laboratory (H. A. Tourtelot, D) Selenium, resources and geochemistry (D. F. Davidson, D) Taconic sequence, Massachusetts, New York, and Connecticut (E. Zen, W) Thermal waters, origin and characteristics (D. E. White, M) Alaska, petrology and volcanism, Katmai National Monument (C. H. Curtis, M) California: Burney area (G. A. MacDonald, Honolulu, Hawaii) Franciscan Formation, glaucophane schist (R. G. Coleman, M) Sierra Nevada batholith, geochemical study (F. Dodge, M) Colorado: Colorado Front Range, Boulder Creek batholith (G. Phair, W) Colorado Front Range, Laramide intrusives (G. Phair, W) Minturn quadrangle (T. S. Lovering, D) Mount Princeton area, distribution of elements (P. Toulmin III, W) Wet Mountains, wallrock alteration (G. Phair, W) Hawaii, Hawaiian volcanology (H. A. Powers, Hawaii National Park, Hawaii) Idaho, central Snake River plain, volcanic petrology (H. A. Powers, Hawaii) Montana: Bearpaw Mountains, petrology (W. T. Pecora, W) Geochemistry and petrology, field studies—Continued Montana—Continued Boulder batholith, petrochemistry (R. I. Tilling, W) Stillwater complex, petrology and chromite resources (E. D. Jackson, Houston, Tex.) Wolf Creek area, petrology (R. G. Schmidt, W) New Mexico: Grants area, mineralology of uranium-bearing rocks (A. D. Weeks, W) Valles Mountains (R. L. Smith, W) New York, Gouverneur area, metamorphism and origin of mineral deposits (A. E. J. Engel, La Jolla, Calif.) South Carolina, igneous and metamorphic rocks of the piedmont (W. C. Overstreet, Jidda, Saudi Arabia) Texas, Karnes and Duval Counties, mineralogy of uraniumbearing rocks (A. D. Weeks, W) Wisconsin, geochemical survey of the Driftless area (H. T. Shacklette, D) Wyoming: Green River Formation, geology and paleolimnology (W. H. Bradley, W) Yellowstone Park, thermal waters and deposits (G. W. Morey, R. O. Fournier, W) Geochronology: Carbon-14 method (M. Rubin, W) Geologic time scale (R. E. Zartman, W) K/A and Rb/Sr methods (H. H. Thomas and C. E. Hedge, W, and R. Kistler, M) Lead-alpha method (T. W. Stern, W) Lead-uranium method (P. Banks, W) Radioactive-disequilibrium studies (J. N. Rosholt, D) Southeastern Alaska (G. D. Eberlein, M. A. Lanphere, M) See also Isotope and nuclear studies. Geologic mapping: Map scale smaller than 1 inch to 1 mile: Colorado Plateau, geologic maps (2-minute sheets) (D. G. Wyant, D) Colorado Plateau, photogeologic mapping (A. B. Olson, W) Sino-Soviet Terrain Atlas (M. M. Elias, W) Alaska: Bristol Bay area, surficial geology (E. H. Muller, Ithaca, N.Y.) Buckland and Huslia Rivers area, west-central Alaska (W. W. Patton, Jr., M) Central and northern Alaska Cenozoic (D. M. Hopkins, M) Charley River quadrangle (E. E. Brabb, M) Compilation of geologic maps, 1:250,000 quadrangles (W. H. Condon, M) Delong Mountains and Point Hope quadrangles (I. L. Tailleur, M) Fairbanks quadrangle (F. R. Weber, College) Geologic map of State (G. O. Gates, M) Hughes-Shungnak area (W. W. Patton, Jr., M) Iliamna quadrangle (R. L. Detterman, M) Kenai lowland, surficial geology (T. N. V. Karl-strom, W) Klukwan iron district (E. C. Robertson, W) Kobuk River valley (A. T. Femald, W) Livengood quadrangle (B. Taber, M)A240 INVESTIGATIONS IN PROGRESS IN THE GEOLOGIC, WATER RESOURCES, AND CONSERVATION DIVISIONS Geologic mapping—Continued Map scale smaller than 1 Inch to 1 mile—Continued Alaska—Continued Lower Yukon-Koyukuk area (W. W. Patton, Jr., M) Lower Yukon-Norton Sound region (J. M. Hoare, M) Nelchina area (A. Grantz, M) Northern Alaska, petroleum investigations (G. Gryc, M) Southeastern Alaska, regional geology and mineral resources (R. A. Loney, M) Southern Brooks Range (W. P. Brosgd, M) Yukon-Koyukuk lowland, engineering geology (F. R. Weber, College) Antarctica: Eights and Walgreen coasts, reconnaissance geology (A. A. Drake, Jr., W) Western Antarctica, reconnaissance geology (E. L. Boudette, W) Colorado: Grand Junction 2-degree quadrangle (W. B. Cashion, D) Oil-shale investigations (D. C. Duncan, W) Idaho: Central Snake River plain, volcanic petrology (H. A. Powers, D) Mackay quadrangle (C. P. Ross, D) Spokane-Wallace region (A. B. Griggs, M) Montana, Spokane-Wallace region (A. B. Griggs, M) Nevada: Clark County (C. R. Longwell, M) Esmeralda County (.1. P. Albers, M) Eureka County (R. J. Roberts, M) Humboldt County (C. R. Willden, D) Lincoln County (C. M. Tschanz, La Paz, Bolivia) Lyon, Douglas, and Ormsby Counties (J. G. Moore, Hilo, Hawaii) Nevada Test Site, reconnaissance (F. N. Houser, D) Nye County, northern part (F. J. Kleinhampl, M) Nye County, southern part (H. R. Cornwall, M) Pershing County (D. B. Tatlock, M) Ruby Mountains (C. R. Willden, D) White Pine County (R. K. Hose, M) New Mexico, geologic map (C. H. Dane, W) Oregon, geologic map (G. W. Walker, M) Utah, Grand Junction 2-degree quadrangle (W. B. Cashion, D) Washington: Grays Harbor basin, regional compilation (H. M. Beikman, M) Spokane-Wallace region (A. B. Griggs, M) Map scale 1 inch to 1 mile, and larger: Alabama, Warrior quadrangle (W. C. Culbertson, D) Alaska: Aleutian Islands, eastern (R. E. Wilcox, D) Aleutian Islands, western (R. E. Wilcox, D) Aleutian Trench-Trinity Island (G. W. Moore, M) Geologic mapping—Continued Map scale 1 inch to 1 mile, and larger—Continued Alaska—Continued Anchorage-Matanuska Glacier area, surficial geology (T. N. V. Karlstrom, W) Beluga-Yentna area (F. F. Barnes, M) Bering River coal field (A. A. Wanek, c, Anchorage) Copper River Basin, northeastern, surficial geology (O. J. Ferrians, Jr., W) Copper River Basin, southeastern, surficial geology (D. R. Nichols, W) Copper River Basin, southwestern, surficial geology (J. R. Williams, W) Eastern Denali Highway, surficial geology (D. R. Nichols, W) Gulf of Alaska Tertiary province (G. Plafker, M) Heceta-Tuxekan area (G. D. Eberlein, M) Iniskin-Tuxedni region (R. L. Detterman, M) Johnson River district, surficial geology (H. L. Foster, W) Katmai National Monument, petrology and vol-canism (G. H. Curtis, M) Lost River mining district (C. L. Sainsbury, D) Lower Chitina Valley, surficial geology (L. A. Yehle, W) Mt. Chamberlain area, surficial geology (C. R. Lewis, W) Mt. Hayes D-3 and D—4 quadrangles (T. L. P6w£, College) Mount Michelson area (E. G. Sable, Elizabethtown, Ky.) Nenana coal investigations (C. Wahrhaftig, M) Nome C—1 and D-l quadrangles (C. L. Hummel, Bangkok, Thailand) Northeastern Alaska coastal plain and foothills (C. R. Lewis, W) Project chabiot (harbor construction) (C. D. Eberlein, M) Seward-Portage Railroad, surficial geology (T. N. V. Karlstrom, W) Slana-Tok area, surficial geology (H. R. Schmoll, W) Steese Highway area, surficial geology (W. E. Davies, W) Taylor Highway area, surficial geology (H. L. Foster, W) Tofty placer district (D. M. Hopkins, M) Upper Tanana River, surficial geology (A. T. Femald, W) Valdez-Tiekel belt, surficial geology (H. W. Coulter, W) Windy-Curry area (R. Kachadoorian, M) Antarctica: Horlick Mountains (A. B. Ford, W) Pensacola Mountains (A. B. Ford, W) Wrangell Mountains, southern (E. M. MacKevett, Jr., M) Arizona : Bradshaw Mountains (C. A. Anderson, W)GEOLOGIC MAPPING, ARIZONA-COLORADO A241 Geologic mapping—Continued Map scale 1 inch to 1 mile, and larger—Continued Arizona—Continued Carrizo Mountains area (J. D. Strobell, D) Christmas quadrangle (C. R. Willden, D) Cibecue-Grasshopper area (T. L. Finnell, D) Cochise County, southern part (P. T. Hayes, D) Elgin quadrangle (R. B. Raup, D) Gila River basin, upper part (R. B. Morrison, D) Globe-Miami area (D. W. Peterson, M) Heber quadrangle (E. J. McKay, D) Holy Joe Peak quadrangle (M. H. Krieger, M) Klondyke quadrangle (F. S. Simons, D) Little Dragoons area (J. R. Cooper, D) Lochiel and Nogales quadrangles (F. S. Simons, D) McFadden Peak and Blue House Mountain quadrangles (A. F. Shride, D) Mammoth and Benson quadrangles (S. C. Creasey, M) Mount Wrightson quadrangle (H. Drewes, D) Navajo Reservation, fuels potential (R. B. O’Sullivan, D) Prescott-Paulden area (M. H. Krieger, M) Show Low quadrangle (E. J. McKay, D) Twin Buttes area (J. R. Cooper, D) Winkelman quadrangle (M. H. Krieger, M) Arkansas: Arkansas Basin, coal investigations (B. R. Haley, D) Ft. Smith district (T. A. Hendricks, D) Malvern quadrangle (W. Danilchik, Santiago, Chile) Northern Arkansas, oil and gas investigations (E. E. Glick, D) California: Ash Meadows quadrangle (C. S. Denny, W) Beatty area (H. R. Cornwall, M) Big Maria, Little Maria, and Riverside Mountains (W. B. Hamilton, D) Bishop tungsten district (P. C. Bateman, M) Blanco Mountain quadrangle (C. A. Nelson, Los Angeles) Burney area (G. A. Macdonald, Honolulu, Hawaii) Coast Range ultramafic rocks (E. H. Bailey, M) Condrey Mountain quadrangle (P. E. Hotz, M) Cuyama Valley area (J. G. Vedder, M) Death Valley (C. B. Hunt, Baltimore, Md.) Furnace Creek area (J. F. McAllister, M) Independence quadrangle (D. C. Ross, M) Klamath Mountains, southern part (W. P. Irwin, M) Los Angeles area (J. T. McGill, Los Angeles) Los Angeles basin, eastern part (J. E. Schoell-hamer, W) Malibu Beach quadrangle (R. F. Yerkes, M) Merced Peak quadrangle (D. L. Peck, Hawaii) Mojave Desert, south-central (T. W. Dibblee, Jr., M) Mojave Desert, western (T. W. Dibblee, Jr., M) Geologic mapping—Continued Map scale 1 inch to 1 mile, and larger—Continued California—Continued Mt. Diablo area (E. H. Pampeyan, M) New York Butte quadrangle (W. C. Smith, M) Oakland East quadrangle (D. H. Radbruch, M) Palo Alto quadrangle (E. H. Pampeyan, M) Panamint Butte quadrangle (W. E. Hall, W) Point Dume quadrangle (R. H. Campbell, M) Priest Valley SW quadrangle (E. E. Richardson, c, Taft) Sacramento Valley, northwest part (R. D. Brown, Jr., M) Salinas Valley (D. L. Durham, M) San Andreas fault (L. F. Noble, Valyermo) San Francisco North quadrangle (J. Schlocker, M) San Francisco South quadrangle (M. G. Bonilla, M) San Mateo quadrangle (G. O. Gates, M) Searles Lake area (G. I. Smith, M) Shuteye Peak area (N. K. Huber, M) Sierra foothills mineral belt (L. D. Clark, M) Sierra Nevada batholith (P. C. Bateman, M) Sierra tungsten belt, eastern (N. K. Huber, M) Colorado: Air Force Academy (D. J. Vames, D) Animas River area (H. Barnes, D) Anthracite NE and NW, and Snowmass SW quadrangles (D. L. Gaskill, c, D) Aspen quadrangle (B. Bryant, D) Baggs area (G. E. Prichard, D) Berthoud Pass quadrangle (P. K. Theobald, D) Black Canyon of the Gunnison River (W. R. Hansen, D) Bottle Pass and Black Hawk quadrangles (R. B. Taylor, D) Boulder quadrangle (C. T. Wrucke, D) Bull Canyon district (C. H. Roach, D) Cameron Mountain quadrangle (M. G. Dings, D) Carbondale coal field (J. R. Donnell, D) Cheyenne Mountain, electrical properties (J. H. Scott, D) Creede district (T. A. Steven, D) Denver metropolitan area (R. M. Lindvall, D) Eldorado Springs quadrangle (J. D. Wells, D) Elk Springs quadrangle (J. R. Dyni, c, D) Empire quadrangle (W. A. Braddock, D) Fort Lupton, Hudson, Platteville, Hanover NW and Carrol Bluffs quadrangles (P. E. Soister, c, D) Fraser and East Portal quadrangles (O. L. Tweto, D) Front Range, Fort Collins area (W. A. Braddock, D) Golden quadrangle (R. Van Horn, D) Grand-Battlement Mesa (J. R. Donnell, D) Green River Valley, upper part (W. R. Hansen, D) Holy Cross quadrangle (O. Tweto, D)A242 INVESTIGATIONS IN PROGRESS IN THE GEOLOGIC, WATER RESOURCES, AND CONSERVATION DIVISIONS Geologic mapping—Continued Map scale 1 inch to 1 mile, and larger—Continued Colorado—Continued Hot Sulphur Springs and Kremmling quadrangles (G. A. Izett, c, D) La Sal area (W. D. Carter, W) Lafayette quadrangle (K. B. Ketner, D) Lake George district (C. C. Hawley, D) Lisbon Valley area (G. W. Weir, Berea, Ky.) Maybell-Lay area (M. J. Bergin, W) Morrison quadrangle (J. H. Smith, D) Montrose 1 SW, 1 SE, 4 NE and Cerro Summit quadrangles (R. G. Dickinson, c, D) Mt. Antero (W. N. Sharp, D) Mt. Harvard quadrangle (M. R. Brock, D) Mountain front area, east-central Front Range (D. M. Sheridan, D) Nederland and Tungsten quadrangles (D. J. Gable, D) North Park, eastern (D. M. Kinney, W) North Park, western (W. J. Hail, D) Placita, SE quadrangle (L. D. Godwin, c, D) Poncha Springs and Bonanza quadrangles (R. E. Alstine, W) Powderhom area (J. C. Olson, D) Pueblo and vicinity (G. R. Scott, D) Ralston Buttes (D. M. Sheridan, D) Rico-Animas area (W. P. Pratt, D) Rico district (E. T. McKnight, W) San Juan mining area (R. G. Luedke, W) San Juan Mountains, western (A. L. Bush, D) Slick Rock district (D. R. Shawe, D) South Platte River, upper part (G. R. Scott, D) Squaw Pass, Evergreen, and Indian Hills quadrangles (D. M. Sheridan, D) Straight Creek tunnel (C. S. Robinson, D) Tenmile Range and Kokomo mining district (M. H. Bergendahl, D) Thornburg area (J. R. Dyni, c, D) Trinidad coal field (R. B. Johnson, D) Ute Mountains (E. B. Ekren, D) Wet Mountains (M. R. Brock, D) Connecticut: Ansonia and Milford quadrangles—bedrock (C. E. Fritts, D) Ashaway and Voluntown quadrangles—bedrock (T. G. Feininger, Boston, Mass.) Ashaway and Watch Hill quadrangles—surficial (J. P. Schafer, Boston, Mass.) Ashley Falls and Tolland Center quadrangles— materials mapping (G. W. Holmes, M) Bristol and New Britain quadrangles—bedrock (H. E. Simpson, D) Broad Brook and Manchester quadrangles (R. B. Colton, W) Columbia, Fitchville, and Marlborough quadrangles—bedrock (G. L. Suyder, D) Danielson, Hampton, Plainfield, and Scotland quadrangles—bedrock (H. R. Dixon, Boston, Mass.) Geologic mapping—Continued Map scale 1 inch to 1 mile, and larger—Continued Connecticut—Continued Durham quadrangle (H. E. Simpson, D) Meriden quadrangle—bedrock (P. M. Hanshaw, Boston, Mass.) Montville, Mystic, and Uncasville quadrangles— bedrock (R. Goldsmith, Boston, Mass.) New Hartford quadrangle (R. W. Schnabel, D) New London, Niantic, and Old Mystic quadrangles (R. Goldsmith, D) Southwick quadrangle (R. W. Schnabel, D) Springfield South quadrangle (J. H. Hartshorn, C. Koteff, Boston, Mass.) Taconic sequence (E. Zen, W) Tarriffville quadrangle—surficial (A. D. Randall, g, Middletown) Tarriffville and Windsor Locks quadrangles—bedrock (R. W. Schnabel, D) Thompson quadrangle (P. M. Hanshaw, H. R. Dixon, Boston, Mass.) Watch Hill quadrangle—bedrock (G. E. Moore, Jr., Columbus, Ohio) West Springfield quadrangle (R. B. Colton, J. H. Hartshorn, Boston, Mass.) District of Columbia, Washington metropolitan area (H. W. Coulter and C. F. Withington, W) Florida: Attapulgus-Thomasville fuller’s earth deposits (S. H. Patterson, W) Land-pebble phosphate deposits (J. B. Cathcart, D) Georgia, Attapulgus-Thomasville fuller’s earth deposits (S. H. Patterson, W) Greenland, Schuchert Dal, East Greenland, glacial geology (J. S. Hartshorn, Boston, Mass.) Idaho: American Falls region (D. E. Trimble, D) Aspen Range-Dry Ridge area (V. E. McKelvey, W) Bancroft quadrangle (S. S. Oriel, D) Bayhorse area (S. W. Hobbs, D) Big Creek quadrangle (B. F. Leonard, D) Blackbird Mountain area (J. S. Vhay, Spokane, Wash.) Central Idaho, radioactive placer deposits (D. L. Schmidt, W) Clarks Fork and Packsaddle Mountain quadrangles (J. E. Harrison, W) Coeur d’ Alene mining district (S. W. Hobbs, D) Doublesprings quadrangle (W. J. Mapel, D) Driggs quadrangle (E. H. Pampeyan, c, D) Gams Mountain quadrangle (M. H. Staatz, c, D) Greenacres quadrangle (P. L. Weis, Spokane, Wash.) Hawley Mountain quadrangle (W. J. Mapel, D) Irwin 1, 2, 4NE, and 4 NW quadrangles (D. A. Jobin, c, D) Leadore and Patterson quadrangles (E. T. Rup-pel, D)GEOLOGIC MAPPING, IDAHO-MONTANA A243 Geologic mapping—Continued Map scale 1 inch to 1 mile, and larger—Continued Idaho—Continued Morrison Lake quadrangle (E. R. Cressman, Lexington, Ky.) Mt. Spokane quadrangle (A. E. Weissenbom, Spokane, Wash.) Orofino area (A. Hietanen-Makela, M) Owyhee and Mountain City quadrangles (R. R. Coats, M) Pocatello quadrangle (D. E. Trimble, D) Riggins quadrangle (W. B. Hamilton, D) Soda Springs quadrangle (F. C. Armstrong, D) Upper Valley quadrangle (R. L. Rioux, c, D) Yellow Pine quadrangle (B. F. Leonard, D) Illinois, Wisconsin zinc-lead mining district (J. W. Whitlow, W) Indiana, Owensboro quadrangle, Quaternary geology (L. L. Ray, W) Iowa, Omaha-Council Bluffs and vicinity (R. D. Miller, D) Kansas: Shawnee County (W. D. Johnson, Jr., Lawrence) Wilson County (H. C. Wagner, M) Kentucky: Note: The entire State of Kentucky is being mapped geologically by 7%-minute quadrangles under a cooperative program with the Kentucky Geological Survey; 91 quadrangles have been published and 227 more are currently in progress. Project is under the supervision of P. W. Richards, Lexington, Ky. The following investigations are separate from the cooperative mapping program: Eastern Kentucky coal investigations (K. J. Eng-lund, W) Jellico West and Ketchen quadrangles, Tennessee and Kentucky (K. J. Englund, W) Owensboro quadrangle, Quaternary geology (L. L. Ray, W) Southern Appalachian folded belt (L. D. Harris, W) Maine: Aroostook County, southern (L. Pavlides, W) Attean quadrangle (A. L. Albee, Pasadena, Calif.) Big Lake area (D. M. Larrabee, W) Greenville quadrangle (G. H. Espenshade, W) Kennebago Lake quadrangle (E. L. Boudette, W) Moosehead gabbro (G. H. Espenshade, W) Paleozoic stratigraphy, regional (R. B. Neuman, W) Stratton quadrangle, geophysical and geologic mapping (A. Griscom, W) The Forks quadrangle (F. C. Canney, E. V. Post, D) Maryland: Allegany County (W. de Witt, Jr., W) Harford County (D. South wick, W) Washington, D.C., metropolitan area (H. W. Coulter, C. F. Withington, W) Massachusetts: Assawompsett Pond quadrangle (C. Kotefif, Boston) Geologic mapping—Continued Map scale 1 inch to 1 mile, and larger—Continued Massachusetts—Continued Athol quadrangle (D. F. Eschman, Ann Arbor, Mich.) Billerica, Lowell, Tyngsboro, and Westford quadrangles (R. H. Jahns, University Park, Pa.) Blue Hills quadrangle (N. E. Chute, Syracuse, N.Y.) Boston and vicinity (C. A. Kaye, Boston, Mass.) Clinton and Shrewsbury quadrangles, bedrock (R. F. Novotny, Boston) Concord quadrangle (N. P. Cuppels, C. Koteff, Boston) Duxbury and Scituate quadrangles (N. E. Chute, Syracuse, N.Y.) Georgetown quadrangle (N. P. Cuppels, Boston) Lawrence, Reading, South Groveland, and Wilmington quadrangles—bedrock (R. O. Castle, Los Angeles, Calif.) Norwood quadrangle (N. E. Chute, Syracuse, N.Y.) Plainfield quadrangle—bedrock (P. H. Osberg, Orono, Maine) Reading and Salem quadrangles—surficial geology (R. N. Oldale, Boston) Rowe and Heath quadrangles (A. H. Ohidester, D; J. H. Hartshorn, Boston) Salem quadrangle—bedrock (P. Toulmin III, W) Southwick quadrangle (R. W. Schnabel, D) Springfield South quadrangle (J. H. Hartshorn, C. Koteff, Boston) Taconic sequence (E. Zen, W) Taunton quadrangle (J. H. Hartshorn, Boston) West Springfield quadrangle (R. B. Colton, D; J. H. Hartshorn, Boston) Michigan : Dickinson County, southern (R. W. Bay ley, M) Cogebic Range, eastern (W. C. Prinz, W) Iron County, eastern (K. L. Wier, D) Iron River-Crystal Falls district (H. L. James, Minneapolis, Minn.) Lake Algonquin drainage (J. T. Hack, W) Marquette district, eastern (J. E. Gair, D) Michigan copper district (W. S. White, W) Negaunee and Palmer quadrangles (J. E. Gair, D) Mississippi, Tatum salt dome (W. S. Twenhofel, D) Missouri, southeastern lead deposits (T. H. Kiilsgaard, W) Montana: Alberton quadrangle (J. D. Wells, W) Anaconda 3 NW quadrangle (A. A. Wanek, c, D) Bearpaw Mountains, petrology (W. T. Pecora, W) Black Butte and Hedstrom quadrangles (A. W. Bateman, c, Great Falls) Boulder batholith area (M. R. Klepper, W) Browning area, Quaternary geology (G. M. Richmond, D) Clarks Fork and Packsaddle Mountain quadrangles (J. E. Harrison, W) Crazy Mountains Basin (B. A. Skipp, D)A244 INVESTIGATIONS IN PROGRESS IN THE GEOLOGIC, WATER RESOURCES, AND CONSERVATION DIVISIONS Geologic mapping—Continued Map scale 1 inch to 1 mile, and larger—Continued Montana—Continued Divide 2 SW quadrangle (G. D. Fraser, c, D) Gardiner SW quadrangle (G. D. Fraser, c, D) Girard coal field (G. E. Prichard, D) Great Falls area (R. W. Lemke, D) Holter Lake quadrangle (G. D. Robinson, D) Hughesville quadrangle (I. J. Witkind, D) Jordan quadrangle (G. D. Mowat, c, Great Falls) Livingston-Trail Creek area (A. E. Roberts, D) Maudlow quadrangle (B. A. Skipp, D) Montaqua quadrangle (E. D. Patterson, c, W) Morrison Lake quadrangle (E. R. Cressman, Lexington, Ky.) Neihart 1 quadrangle (W. R. Keefer, D) Philipsburg area, manganese deposits (W. C. Prinz, W) Powder River coal fields (N. W. Bass, D) Rocky Reef and Hardy quadrangles (K. S. Soward, c, Great Falls) Southwestern part, ore deposits (K. L. Wier, D) Sun River Canyon area (M. R. Mudge, D) Tepee Creek quadrangle (I. J. Witkind, D) Toston quadrangle (G. D. Robinson, D) Varney and Cameron quadrangles (J. B. Hadley, W) Willis quadrangle (W. B. Myers, D) Wolf Creek area, petrology (R. G. Schmidt, W) Wolf Point area (R. B. Colton, D) Nebraska: Franklin, Webster, and Nuckolls Counties (R. D. Miller, D) Omaha-Council Bluffs and vicinity (R. D. Miller, D) Valley County (R. D. Miller, D) Nevada: Antler Peak quadrangle (R. J. Roberts, M) Ash Meadows quadrangle (C. S. Denny, W) Beatty area (H. R. Cornwall, M) Cortez quadrangle (J. Gilluly, D) Ely district (A. L. Brokaw, D) Eureka, Pinto Summit, and Bellevue Peak quadrangles (T. B. Nolan, W) Frenchie Creek quadrangle (L. J. P. Muffler, M) Horse Creek Valley quadrangle (H. Masursky, M) Humboldt Range, Unionville and Buffalo Mountain quadrangles (R. E. Wallace, M) Jiggs quadrangle (C. R. Willden, D) Kobeh Valley (T. B. Nolan, W; C. W. Merriam, M) Las Vegas-Lake Mead area (C. R. Longwell, M) Montello area (R. G. Wayland, c, Los Angeles, Calif.) Mt. Lewis and Crescent Valley quadrangles (J. Gilluly, D) Nevada Test Site, geologic studies (F. A. Mc-Keown, D) Nevada Test Site, Pahute Mesa (F. N. Houser, D) Nevada Test Site, site studies (R. E. Davis, D) Geologic mapping—Continued Map scale 1 inch to 1 mile, and larger—Continued Nevada—Continued Nevada Test Site, underground air storage (R. B. Johnson, D) Owyhee and Mountain City quadrangles (R. R. Coats, M) Pioche district (C. M. Tschanz, La Paz, Bolivia) Railroad district (J. F. Smith, Jr., D) Schell Creek Range (H. D. Drewes, D) Snake Range, Wheeler Peak and Garrison quadrangles (D. H. Whitebread, M) Sonoma Range, northern, orogenic processes (J. Gilluly, D) New Jersey: Delaware River basin, lower (J. P. Owens, W) Delaware River basin, middle (A. A. Drake, Jr., W) Selected iron deposits (A. F. Buddington, Princeton, N.J.) New Mexico: Animas River area (H. Barnes, D) Carrizo Mountains area (J. D. Strobell, D) Franklin Mountains (R. L. Harbour, D) Gila River basin, upper part (R. B. Morrison, D) Grants area (R. E. Thaden, Columbia, Ky.) Johnson Trading Post quadrangle (J. S. Hinds, c, Farmington) Laguna district (R. H. Moench, D) Las Vegas quadrangle, western half (E. H. Baltz, g, Albuquerque) Manzano Mountains (D. A. Myers, D) Mesa Portales quadrangle (J. E. Fassett, c, Farmington) Nash Draw quadrangle (L. M. Gard, D) Oscura Mountains, southern part, and northern San Andres Mountains (G. O. Bachman, D) Raton coal basin, eastern (G. H. Dixon, D) Raton coal basin, western (C. L. Pillmore, D) San Juan Basin, east side (C. H. Dane, W) Silver City area (W. R. Jones, D) Valles Mountains, petrology (R. L. Smith, W) New York: Dannemora and Plattsburgh quadrangles—surfi-cial geology (C. S. Denny, W) Gouverneur area, metamorphism and origin of mineral deposits (A. E. J. Engel, La Jolla, Calif.) Mooers and Ohio quadrangles (D. R. Wiesnet, W) Richville quadrangle (H. M. Bannerman, W) Selected iron deposits (A. F. Buddington, Princeton, N.J.) Taconic sequence (E. Zen, W) North Carolina: Central Piedmont (H. Bell, W) Franklin quadrangle (F. G. Lesure, W) Grandfather Mountain (B. H. Bryant, D) Great Smoky Mountains (J. B. Hadley, W) Morganton area, geomorphic studies (J. T. Hack, W) Mount Rogers area (D. W. Rankin, W) Volcanic Slate series (A. A. Stromquist, D)GEOLOGIC MAPPING, NORTH DAKOTA-UTAH A245 Geologic mapping—Continued Map scale 1 inch to 1 mile, and larger—Continued North Dakota: Dengate and Heart Butte NW quadrangles (E. V. Stephens, c, D) Glen Ullin quadrangle (C. S. V. Barclay, c, D) New Salem 2 SW and North Altmont quadrangles (H. L. Smith, c, D) Oklahoma, Ft. Smith district (T. A. Hendricks, D) Oregon: Bandon SE and Coquille SW quadrangles (E. M. Baldwin, c, Los Angeles, Calif.) Columbia River Gorge, Quaternary history (C. B. Hunt, Baltimore, Md.) John Day area (T. P. Thayer, W) Monument quadrangle (R. E. Wilcox, D) Newport Embayment (P. D. Snavely, Jr., M) Ochoco Reservation, Lookout Mountain, Eagle Rock, and Post quadrangles (A. C. Waters, Baltimore, Md.) Pacific Islands: Bikini and nearby atolls (H. S. Ladd, W) Guam (J. I. Tracey, Jr., W) Ishigaki, Ryukyu Islands (H. L. Foster, W) Okinawa (G. Corwin, W) Pagan Island (G. Corwin, W) Palau Islands (G. Corwin, W) Yap and Caroline Islands (C. G. Johnson, Honolulu, Hawaii) Pennsylvania: Allentown northeast quadrangle (J. M. Aaron, W) Anthracite mine-drainage projects, geology in the vicinity of (J. F. Robertson, Mt. Carmel) Anthracite region, flood control (M. J. Bergin, Mt. Carmel) Bituminous coal resources (E. D. Pattersen, W) Delaware River basin, lower (J. P. Owens, W) Delaware River basin, middle (A. A. Drake, Jr., W) Devonian stratigraphy of State (G. W. Colton, W) Philadelphia district, Lower Cambrian (J. H. Wallace, W) Southern anthracite field (G. H. Wood, Jr., W) Washington County (H. Berryhill, Jr., D) Western Middle anthracite field (H. Arndt, W) Wind Gap and adjacent quadrangles (J. B. Epstein, W) Puerto Rico (W. H. Monroe, San Juan, P.R.) Rhode Island: Ashaway and Voluntown quadrangles (T. G. Fein-inger, Boston, Mass.) Ashaway and Watch Hills quadrangles—surficial (J. P. Schafer, Boston, Mass.) Carolina and Quonochontaug quadrangles—surficial (J. P. Schafer, Boston, Mass.) Chepachet, Crompton, and Tiverton quadrangles— bedrock (A. W. Quinn, Providence) Clayville, Coventry Center, Kingston, Newport, and Prudence Island quadrangles—bedrock (G. E. Moore, Jr., Columbus, Ohio) Geologic mapping—Continued Map scale 1 inch to 1 mile, and larger—Continued Rhode Island—Continued Thompson quadrangle (P. M. Hanshaw, and H. R. Dixon, Boston, Mass.) Watch Hill quadrangle (G. E. Moore, Jr., Columbus, Ohio) Wickford quadrangle—bedrock (R. B. Williams, Lawrence, Kans.) South Dakota: Four Comers quadrangle (J. A. Van Lieu, Laramie, Wyo.) Black Hills, southern (G. B. Gott, D) Fort Randall Reservoir area (H. D. Vames, D) Harding County and adjacent areas (G. N. Pipi-ringos, D) Hill City pegmatite area (J. C. Ratt6, D) Keystone pegmatite area (J. J. Norton, W) Rapid City area (E. Dobrovolny, D) Tennessee: Ducktown district and adjacent areas (R. M. Hemon, D) East Tennessee zinc studies (A. L. Brokaw, D) Great Smoky Mountains (J. B. Hadley, W) Ivydell and Pioneer quadrangles, Tennessee, and Jellico West and Ketchen quadrangles, Tennessee and Kentucky (K. J. Englund, W) Knoxville and vicinity (J. M. Cattermole, Columbia, Ky.) Mount Rogers area (D. W. Rankin, W) Southern Appalachian folded belt, Kentucky, Tennessee, and Virginia (L. D. Harris, W) Texas: Coastal plain, geophysical and geological studies (D. H. Eargle, Austin) Del Rio area (V. L. Freeman, D) Franklin Mountains (R. L. Harbour, D) North-central, Pennsylvanian Fusulinidae (D. A. Myers, D) San Antonio and vicinity (R. D. Miller, D) Sierra Blanca area (J. F. Smith, Jr., D) Sierra Diablo region (P. B. King, M) Utah: Abajo Mountains (I. J. Witkind, D) Alta quadrangle (M. D. Crittenden, Jr., M) Bingham Canyon district (R. J. Roberts, M) Circle Cliffs area (E. S. Davidson, Tucson, Ariz.) Coal-mine bumps (F. W. Osterwald, D) Confusion Range (R. K. Hose, M) Crawford Mountains (W. C. Gere, c, Salt Lake City) Elk Ridge area (R. Q. Lewis, Columbia, Ky.) Green River valley, upper part (W. R. Hansen, D) Gunsight Butte quadrangle (F. Peterson, c, D) Hurricane fault, southwestern Utah (P. Averitt, D) Kaiparowits Peak 4 quadrangle (H. D. Zeller, c. D) Kolob Terrace coal field, southern part (W. B. Cashion, D) La Sal area (W. D. Carter, W)A246 INVESTIGATIONS IN PROGRESS IN THE GEOLOGIC, WATER RESOURCES, AND CONSERVATION DIVISIONS Geologic mapping—Continued Map scale 1 inch to 1 mile, and larger—Continued U tah—Continued Lehi quadrangle (M. D. Crittenden, Jr., M) Lisbon Valley area (G. W. Weir, Berea, Ky.) Little Cottonwood area (G. M. Richmond, D) Moab-Interriver area (E. N. Hinrichs, D) Navajo Reservation, fuels potential (R. B. O’Sullivan, D) Nipple Butte quadrangle (H. A. Waldrop, c, D) Oak City area (D. J. Varnes, D) Ogden 1 SE and 4 quadrangles (T. A. Mullens, c, D) Orange Cliffs area (F. A. McKeown, D) Park City area (M. D. Crittenden, Jr., M) Park City district (C. S. Bromfield, D) Promontory Point (R. B. Morrison, D) Sage Plain area (L. C. Huff, Manila, P.I.) Salt Lake City and vicinity (R. Van Horn, D) San Francisco Mountains (D. M. Lemmon, M) San Rafael Swell (C. C. Hawley, D) Sheeprock Mountains, West Tintic district (H. T Morris, M) Snake Range, Wheeler Peak and Garrison quadrangles (D. H. Whitebread, M) Strawberry Valley and Wasatch Mountains (A. A. Baker, W) Thomas and Dugway Ranges (M. H. Staatz, D) Tintic lead-zine district, eastern (H. T. Morris, M) Uinta Basin oil shale (W. B. Cashion, D) White Canyon area (R. E. Thaden, Columbia, Ky.) Vermont: North-central (W. M. Cady, D) Rowe and Heath quadrangles (A. H. Chidester, D; J. H. Hartshorn, Boston, Mass.) Virginia: Big Stone Gap district (R. L. Miller, W) Herndon quadrangle (R. E. Eggleton, M) Mount Rogers area (D. W. Rankin, W) Potomac Basin studies (J. T. Hack, W) Southern Appalachian folded belt (L. D. Harris, W) Washington, D.C., metropolitan area (H. W. Coulter, C. F. Withington, W) Washington: Bald Knob quadrangle (M. H. Staatz, D) Bodie Mountain quadrangle (R. C. Pearson, D) Chewelah 1 quadrangle (L. D. Clark, M) Columbia River Gorge, (Quaternary history (C. B. Hunt, Baltimore, Md.) Glacier Peak quadrangle (D. F. Crowder, M) Grays Harbor basin, western part (H. C. Wagner, M) Grays River quadrangle (E. W. Wolfe, M) Holden and Lucerne quadrangles (F. W. Cater, D) Hunters quadrangle (A. B. Campbell, D) Inchelium quadrangle (A. B. Campbell, D) Loomis quadrangle (C. D. Rinehart, M) Maple Valley, Hobart and Cumberland quadrangles (J. D. Vine, M) Geologic mapping—Continued Map scale 1 inch to 1 mile, and larger—Continued Washington—Continued Metaline lead-zinc district (M. G. Dings, D) Mt. Spokane quadrangle (A. E. Weissenborn, Spokane) Olympic Peninsula, eastern (W. M. Cady, D) Olympic Peninsula, northern (R. D. Brown, Jr., M) Puget Sound Basin (D. R. Crandell, D) Republic-Curlew area (R. L. Parker, D) Seattle and vicinity (D. R. Mullineaux, D) Stevens County (R. G. Yates, M) Wilmont Creek quadrangle (G. E. Becraft, D) West Virginia, Potomac Basin studies (J. T. Hack, W) Wisconsin: Florence County (C. E. Dutton, Madison) Zinc-lead mining district (J. W. Whitlow, W) Wyoming: Adam Weiss Peak quadrangle (W. L. Rohrer, c, D) Atlantic City district (R. W. Bayley, M) Baggs area (G. E. Prichard, D) Beaver Divide area (F. B. Van Houten, Princeton, N.J.) Black Hills, Inyan Kara Group (W. J. Mapel, D) Bradley Peak quadrangle (R. W. Bayley, M) Carbon and Northern Laramie basins (H. J. Hyden, c, D) Clark, Deep Lake, and Beartooth Butte quadrangles (W. G. Pierce, M) Cokeville quadrangle (W. W. Rubey, Los Angeles, Calif.) Crawford Mountains (W. C. Gere, Salt Lake City, Utah) Crooks Gap area (J. G. Stephens, D) Crowheart Butte area (J. F. Murphy, D) Ferris quadrangle (R. L. Rioux, c, D) Fish Lake and Kissinger Lakes quadrangles (W. L. Rohrer, c, D) Fossil basin (J. I. Tracey, Jr., W) Four Corners quadrangle (J. A. Van Lieu, Laramie, Wyo.) Gas Hills district (H. D. Zeller, D) Grand Teton National Park (J. D. Love, Laramie) Jackson 30-minute quadrangle (D. A. Jobin, c. D) LaBarge 1 SW and SE quadrangles (R. L. Rioux, c, D) Lamont-Baroil area (M. W. Reynolds, D) Oregon Buttes area (H. D. Zeller, c, D) Powder River Basin, Pumpkin Buttes area (W. N. Sharp, D) Sheep Mountain quadrangle (W. L. Rohrer, c, D) Shirley Basin area (E. N. Harshman, D) Spence-Kane area (R. L. Rioux, c, D) Sweetwater County, Green River Formation (W. C. Culbertson, D) Tepee Creek quadrangle (I. J. Witkind, D) Wedding of Waters-Devil Slide quadrangles (E. K. Maughan, D) Whalen-Wheatland area (L. W. McGrew, Laramie)GEOLOGIC MAPPING, WYOMING---GEOPHYSICS A247 Geologic mapping—Continued Map scale 1 inch to 1 mile, and larger—Continued W yoming—Continued Wind River Basin, regional stratigraphy (W. R. Keefer, Laramie ) Wind River Mountains, Quaternary geology (G. M. Richmond, D) Subsurface: Alabama, subsurface geologic study (W. J. Powell, g, Tuscaloosa) Geomorphology: Basic processes of erosion and resultant landforms in dryland regions (G. G. Parker, h, D) Effects of exposure on slope morphology (R. F. Hadley, h, D) Effects of sediment characteristics on fluvial morphology and hydraulics (S. A. Schumm, h, D) Erosion characteristics of clays (A. V. Jopling, s, Boston, Mass.) Geomorphology of glacier streams (R. K. Fahnestock, h, D) Mass movement and surface runoff in an upland wooded hillslope (L. B. Leopold, w, W) Mechanics of hillslope erosion (S. A. Schumm, h, D) Mudflow studies CD. R. Crandell, D) Alabama, Russell Cave (J. T. Hack, W) Alaska, physiographic divisions (C. Wahrhaftig, M) Arizona, Tusayan Washes, study of channel flood-plain aggradation, (R. F. Hadley, h, D) California, Death Valley, morphologic changes on alluvial fans (L. K. Lustig, q, Sacramento) Indiana, Owensboro quadrangle, Quaternary geology (L. L. Ray, W) Iowa, channel-geometry studies (H. H. Schwob, s, Iowa City) Kentucky, Owensboro quadrangle, Quaternary geology (L. L. Ray, W) Massachusetts, sea-cliff erosion studies (C. A. Kaye, Boston) Michigan, Lake Algonquin drainage (J. T. Hack. W) Montana, Browning area, Quaternary geology (G. M. Richmond, D) New Mexico, Santa Fe, particle movement and channel scour and fill of an ephermal arroyo (L. B. Leopold, w, W) New York, northeast Adirondacks (C. S. Denny, W) North Carolina: Morganton area (J. T. Hack, W) Stream-channel characteristics (L. A. Martens, s, Raleigh) North Dakota, hydrology of prairie potholes (W. S. Eisen-lohr, Jr., h, D) Ohio River valley, geologic development (L. L. Ray, W) Washington-Oregon, Columbia River Gorge, Quaternary history (C. B. Hunt, Baltimore, Md.) Virginia and West Virginia, Potomac Basin studies (J. T, Hack, W) Wyoming, Wind River Mountain, Quaternary geology (G. M. Richmond, D) See also Sedimentation. Geophysics, regional: Aeroradioactivity surveys: California, San Francisco (J. A. Pitkin, W) Colorado, Rocky Flats (J. A. MacKallor, W) Idaho, National Reactor Testing Station (R. G. Bates, W) Illinois, Chicago (G. M. Flint, Jr., W) Maryland, Bel voir area (S. K. Neuschel, W) Minnesota, Elk River (J. A. Pitkin, W) Northeastern United States (P. Popenoe, W) Ohio, Columbus (R. G. Bates, W) Pennsylvania, Pittsburgh (R. W. Johnson, Knoxville, Tenn.) Puerto Rico (J. A. Pitkin, W) Texas, Fort Worth (J. A. Pitkin, W) Virginia, Belvoir area (S. K. Neuschel, W) Arctic, geophysical studies (I. Zietz, W) Central United States, aeromagnetic surveys (J. W. Henderson, W) Colorado Plateau, regional geophysical studies (H. R. Joe-sting, W) Colorado Plateau and southern Rocky Mountains, aeromagnetic surveys (H. R. Joesting, W) Costa Rica, volcanic studies (K. J. Murata, San Jose, Costa Rica) Cross-country aeromagnetic profiles (E. R. King, W) Crust and upper mantle : Analysis of traveltime data (J. H. Healy, D) Geophysical studies (L. C. Pakiser, D) Gravity surveying (D. P. Hill, D) Rocky Mountain seismic network (J. P. Eaton, D) Seismic-refraction profiling (W. H. Jackson, D) Eastern Central United States, tectonic patterns (I. Zietz, W) Eastern United States, aeromagnetic surveys (R. W. Bromery, W) Folded Appalachians, geophysical studies (J. S. Watkins, W) Gravity map of the United States (H. R. Joesting, W) Japan, calderas, aeromagnetic-gravity studies (H. R. Blank, Jr., M) Lake Superior region, geophysical studies (G. D. Bath, M) New England, geophysical studies (M. F. Kane, W) Northeastern United States, gravity study (G. Simmons, Dallas, Tex.) Pacific Northwest, aeromagnetic surveys (W. E. Davis, M) Pacific Northwest, geophysical studies (W. E. Davis, M) Pacific Ocean, geophysical studies (D. F. Barnes, M) Pacific Southwest, aeromagnetic surveys (D. R. Mabey, M) Pacific Southwest, geophysical studies (D. R. Mabey, M) Tri-State eruptive-tectonic complex, Wyoming-Montana-Idaho, geophysical study (H. R. Blank, M) Ultramafic intrusions, geophysical studies (G. A. Thompson, M) Alaska: Aeromagnetic surveys (G. E. Andreasen, W) Regional gravity surveys (D. F. Barnes, M) Arizona: Central Arizona, geophysical study (D. R. Mabey, M) Safford Valley, geophysical studies (G. E. Andreasen, W) 746-002 0 - 64 - 17A248 INVESTIGATIONS IN PROGRESS IN THE GEOLOGIC, WATER RESOURCES, AND CONSERVATION DIVISIONS Geophysics, regional—Continued Arkansas, Wichita Mountains system, aeroinagnetic interpretation (A. Griscom, W) California: Los Angeles basin, gravity study (T. H. McCulloh, Riverside) Sacramento Valley and Coast Range, geophysical studies (G. D. Bath, M) San Francisco Bay area, geophysical studies (G. D. Bath, M) Sierra Nevada, geophysical studies (H. W. Oliver, M) Colorado: Arkansas Valley geophysical study (J. E. Case, D) Cheyenne Mountain, electrical properties (J. H. Scott, D) District of Columbia, and vicinity, correlation of aeroradio-activity with geology (S. K. Neuschel, W) Iowa, central, aeromagnetic survey (J. R. Henderson, W) Maine: Island Falls quadrangle, electromagnetic mapping (F. C. Frischknecht, W) Stratton quadrangle, geophysical and geologic mapping (A. Griscom, W) Maryland: Montgomery County, geophysical studies (A. Griscom, W) Washington, D.C., and vicinity, correlation of aero-radioactivity with geology (S. K. Neuschel, W) Massachusetts: Application of geology and seismology to public-works planning (C. R. Tuttle and R.' N. Oldale, Boston) Geophysical studies (R. W. Bromery, W) Michigan: Gogebic district, aeromagnetic study (J. E. Case, D) Marquette district, aeromagnetic study (J. E. Case, D) Mississippi, Tatum salt dome (W. S. Twenhofel, D) Missouri, southeast, aeromagnetic study (J. W. Allingham, W) Montana: Bearpaw Mountains, aeromagnetic study (K. G. Books, W) Boulder batholith, aeromagnetic and gravity studies (W. E. Davis, M) Nevada: Central Nevada, geophysical studies (D. R. Mabey, M) Clark County, gravity investigations (M. F. Kane, W) Nevada Test Site, aeromagnetic surveys (J. W. Allingham, W) Nevada Test Site, soil conductivity measurements (J. H. Scott, D) New Jersey: Gettysburg-Newark Basin, geophysical investigations (M. E. Beck, W) New York-New Jersey Highlands, aeromagnetic studies (A. Jespersen, W) New Mexico, Valles caldera, geophysical study (H. R. Joest-ing, W) Geophysics, regional—Continued New York: Adirondacks area, aeromagnetic studies (J. R. Balsley, W) • New York-New Jersey Highlands, aeromagnetic studies (A. Jespersen, W) North Carolina, Concord quadrangle, geophysical studies (R.G. Bates, W) Ohio, seismic survey for buried valleys (J. S. Watkins, W) Oregon: Oregon Cascades, geophysical study (H. R. Blank, M) West-central, aeromagnetic and gravity studies (R. W. Bromery, W) Pennsylvania: Gettysburg-Newark Basin, geophysical investigations (M. E. Beck, W) Gravity survey (R. W. Bromery, W) Triassic area, aeromagnetic study (R. W. Bromery, W) Puerto Rico, geophysical studies (A. Griscom, W) South Dakota, Hills area, regional gravity studies (R. M. Hazlewood, D) Tennessee, central eastern, geophysical studies (J. S. Watkins, W) Texas, coastal plain, geophysical and geological studies (D. H. Eargle, Austin) Utah: Iron Springs areomagnetic survey (H. R. Blank, M) Sheeprock Mountains, West Tintic district (D. R. Mabey, M) Virginia, Washington, D.C., and vicinity, correlation of aeroradioactivity with geology (S. K. Neuschel, W) Washington: Northeastern, geophysical studies (W. T. Kinoshita, M) Western, gravity survey (D. J. Stuart, D) West Virginia, Washington, D.C., and vicinity, correlation of aeroradioactivity with geology (S. K. Neuschel, W) Wisconsin: Florence County, aeromagnetic study (E. R. King, W) Wausau area, aeromagnetic studies (J. W. Allingham, W) Wyoming, Black Hills area, regional gravity studies (R. M. Hazlewood, D) Geophysics, theoretical and experimental: Borehole geophysics as applied to geohydrology (W. S. Keys, h, D) Elastic and inelastic properties of earth materials (L. Peselnick, W) Electric and magnetic properties of minerals (A. N. Thorpe, W) Electrical effects of nuclear explosions (G. V. Keller, D) Electrical methods, development (C. J. Zablocki, D) Electrical properties of rocks (G. V. Keller, D) Electromagnetic exploration methods (F. C. Frischknecht, D) Electromagnetic radiation studies (W. A. Fischer, W) Geophysical abstracts (J. W. Clarke, W) Geophysical data, interpretation using electronic computers (R. G. Henderson, W)GEOPHYSICS—HYDRAULICS A249 Geophysics, theoretical and experimental—Continued Geothermal studies (A. H. Lachenbruch, M) Gravity and magnetic anomalies, analysis (W. H. Diment, W) Heat flow in the Appalachian Mountains (W. H. Diment, W) Heat transfer in salt (E. C. Robertson, W) Infrared and ultraviolet radiation studies (R. M. Moxham, W) Magnetic and luminescent properties (F. E. Senftle, W) Magnetic model studies (I. Zietz, W) Magnetic properties of crystals (A. N. Thorpe, W) Magnetic properties of rocks (A. Griscom, W) Nevada Test Site, soil conductivity measurements (J. H. Scott, D) Propagation of seismic waves in porous media (J. A. da-Costa h, Phoenix, Ariz.) Radon, geologic behavior (A. B Tanner, W) Remanent magnetization of rocks (R. R. Doell, M) Remote sensing of hydrologic phenomena (C. J. Robinove, w, St. Louis, Mo.) Rock behavior at high temperature and pressure (E. C. Robertson, W) Tension fractures and thermal investigation (A. H. Lachenbruch, M) Thermodynamic properties of rocks (R. A. Robie, W) Tiltmeter investigations (G. W. Greene, M) Ultramafic intrusions, geophysical studies (G. A. Thompson, M) Glacial geology: Alaska, glacial map (H. W. Coulter, W) Antarctica, Pensacola Mountains (A. B. Ford, W) California, west-central Sierra Nevada (F. M. Fryxell, Rock Island, 111.) Greenland, Schuchert Dal (J. S. Hartshorn, Boston, Mass.) Washington-Oregon, Columbia River Gorge, Quaternary history (C. B. Hunt, Baltimore, Md.) Glaciology: Glaciological research (M. F. Meier, h, Tacoma, Wash.) Alaska, Barrier Glacier (Mount Spurr) (G. C. Giles, c, Tacoma, Wash.) Montana: Grinnell Glacier, hydrology (F. Stermitz, s, Helena) Grinnell and Sperry Glaciers (Glacier National Park) (A. Johnson, c, W) Washington, Nisqually Glacier (Mount Rainier National Park) (G. C. Giles, c, Tacoma) Gold: Gold deposits, United States (M. H. Bergendahl, D) Alaska: Nome C-l and D-l quadrangles (C. L. Hummel, Bangkok, Thailand) Tofty placer district (D. M. Hopkins, M) CoJorado, Tenmile Range and Kokomo mining district (M. H. Bergendahl, D) Wyoming, Atlantic City district (R. W. Bayley, M) Ground water-surface water relations: Bank-seepage studies (E. C. Pogge, s, Iowa City, Iowa) Flow losses in ephemeral stream channels (R. F. Hadley, h, D) Ground water-surface water relations—Continued Ground water-surface water interrelations (M. W. Busby, s, Topeka, Kans.) Streamflow in relation to aquifer characteristics (G. R. Kunkle, s, W) California, water-loss and water-gain studies (E. G. Pearson, s, M) Florida, Lake Okeechobee, levee underseepage (F. W. Meyer, g, Tallahassee) Montana, Hungry Horse Reservoir, bank storage (A. F. Bateman, Jr., c, Great Falls) New Jersey, Ramapo River basin (J. Vecchioli, g, Trenton) New Mexico, White Sands Missile Range, research on paving a small watershed (H. O. Reeder, g, Albuquerque) Tennessee, Upper Buffalo River (W. J. Perry, w, Chattanooga) Washington: Cedar River loss study, surface and ground water (F. T. Hidaka, s, Tacoma) Columbia River basin, relation of ground-water storage and streamflow (M. I. Rorabaugh, h, Tacoma) Wisconsin, Little Plover River basin, hydrology (E. P. Weeks, g, D. W. Ericson, s, Miadison) Health, relation to distribution of elements: Distribution of radioactivity (S. Rosenblum, W) Hydraulics, ground-water: Aquifer-test reevaluation, California (E. J. McClelland, g, Sacramento) Directional permeability and nonhomogeneity, mathematical relations (J. A. daCosta, h, Phoenix, Ariz.) Effects of heterogeneity (H. E. Skibitzke, h, Phoenix, Ariz.) Geohydrologic environmental studies (.1. Norman Payne, h, Baton Rouge, La.) Mechanics of aquifers—principles of compaction and deformation (J. F. Poland, g, Sacramento, Calif.) Mechanics of fluid flow in porous media (A. Ogata, h, Honolulu, Hawaii) Permeability distribution study—Atlantic Coastal Plain (P. M. Brown, h, Raleigh, N.C.) Permeability research, California (A. I. Johnson, g, D) Regional hydrologic system analysis—hydrodynamics (R. R. Bennett, h, W) Regional hydrologic system analysis—permeability distribution (J. D. Bredehoeft, h, W) Research on laboratory and field methods (A. I. Johnson, g, D) Theory of multiphase flow—applications (R. W. Stallman, h, D) Theory of unsaturated flow (H. E. Skibitzke, h, Phoenix, Ariz.) Transient flow in saturated porous media (W. O. Smith, h, W) Treatise on ground-water mechanics (J. G. Ferris, g, Tucson, Ariz.) Unsaturated flow in porous media (W. O. Smith, h, W) Unsaturated-flow theory related to drainage and infiltration (Jacob Rubin, h, M) Unsteady flow to multiaquifer wells (I. S. Papadopulos, g, W)A250 INVESTIGATIONS IN PROGRESS IN THE GEOLOGIC, WATER RESOURCES, AND CONSERVATION DIVISIONS Hydraulics, surface flow: Channel characteristics: Changes below dams—river channels (M. G. Wol-man, h, Baltimore, Md.) Controls for sand channel streams (F. A. Kilpatrick, s,W) Large-scale roughness (J. Davidian, s, W) Manning coefficient, determination from measured bed roughness in natural channels (L. E. Young, s, M) Channel constrictions: Field measurement of hydraulic factors—performance of channel changes (P. O. Jefferson, s, Tuscaloosa, Ala.) Overall efficiency of bridges (Braxtel L. Neely, Jr., s, Jackson, Miss.) Verification of hydraulic computation methods for bridge openings (C. O. Ming, s, Tuscaloosa, Ala.) Verification of hydraulic techniques (W. J. Randolph, w, Chattanooga, Tenn.) Flow characteristics: Dispersion by turbulent flow in open channels (R. W. Carter, s, W) Flow through bends (C. H. Hannum, s, Louisville, Ky.) Gaging streamflow through turbines (B. J. Frederick, w, Chattanooga, Tenn.) Unsteady flow in natural channels (R. A. Boltzer, s, W) Variation in velocity-head coefficient (H. Hulsing, s, M) Vertical-velocity characteristics of Columbia River gaging stations, Washington (G. L. Bodhaine, J. Savini, s, Tacoma) Laboratory studies: Analysis of bedform data from laboratory flumes (J. F. Kennedy, q, Albuquerque, N. Mex.) Effect of grain heterogeneity in flume transport (L. B. Leopold, G. Williams, w, W) Flow through wide constructions—channel constrictions with spur dikes (F. Chang, s, Atlanta, Ga.) Laboratory studies of open channel flow (H. J. Tracy, s, W) Time of travel, Rockaway River, N.J. (E. L. Meyer, s, W) Time of travel of solutes (J. F. Wilson, Jr., s, W) Time-of-travel studies (A. A. Vickers, s, Trenton, N.J.) Time-of-travel studies (B. Dunn, s, Albany, N.Y.) Hydrologic-data collection and processing: Automation systems and equipment for water (W. L. Isher-wood, s, W) Con-elation of monthly streamflow (R. O. R. Martin, s, W) Data-collection program, new criteria (M. A. Benson, s, W) Data on water quality, automation and processing techniques for (G. A. Billingsley, q, Raleigh, N.C.) Data-proeessing methods, evaluation (A. I. Johnson, g, D) Digital recorders and computer techniques (W. L. Isher-wood, s, W) Drainage-area determinations: Arkansas (R. C. Christensen, s, Little Rock) Kentucky (H. C. Beaber, s, Louisville) Hydrologic-data collection and processing—Continued Drainage-area determinations—Continued New Jersey, for gazetteer of streams (A. A. Vickers, s, Trenton) South Carolina (W. M. Bloxham, s, Columbia) Texas (P. H. Holland, s, Austin) Flood and base-flow gaging, New Jersey (E. G. Miller, s, Trenton) River-systems gaging (H. C. Riggs, s, W) Sediment loads in streams—methods used in measurement and analysis (B. C. Colby, q, Minneapolis, Minn.) Sediment manual (R. B. Vice, q, W) Statistical inferences (N. C. Matalas, s, W) Vigil Network Survey—observations of channel and slope processes (W. W. Emmett, L. B. Leopold, w, W) Hydrologic instrumentation : Acoustic velocity-measuring equipment—water (W. Hofmann, s, M) Controls and Instrumentation for gaging alluvial streams (F. A. Kilpatrick, s, Fort Collins, Colo.) Electronic-equipment development—water (J. E. Eddy, h, W) Evaluation equipment for brine disposal, Eddy County, N. Mex. (E. R. Cox, g, Albuquerque) Instrumentation research—water (E. G. Barron, s, Columbus, Ohio) Instrumentation to study unstable flow in steep channels (W. Smith, s, M) Instruments for energy-budget evaporation studies (C. R. Daum, h, D) Instruments for laboratory research—water (G. F. Smoot, s, W) Hydrology, ground-water: Geohydrologic environmental study (J. N. Payne, h, Baton Rouge, La.) Hydrology of Alabama oil fields (W. J. Powell, g, Tuscaloosa) Mechanics of aquifers, San Joaquin-Santa Clara Valleys, Calif. (J. F. Poland, g, Sacramento) Piketon aquifer test, Ohio (S. E. Norris, and R. E. Fidler, g, Columbus) Problems in quantitative hydrology (M. I. Rorabaugh, h, Tacoma, Wash.) Specific-yield studies, California (A. I. Johnson, g, D) Hydrology, surface-water: Diurnal fluctuations of streams, New York (F. L. Robison, s, Albany) Flow probability of New Jersey streams (E. G. Miller, s, Trenton) Hydrologic and hydraulic studies, Virginia (C. W. Ling-ham, s, Charlottesville) Hydrologic effects of small reservoirs, Sandstone Creek, Okla. (F. W. Kennon, s, Austin, Tex.) Hydrology of small streams, New Hampshire (C. E. Hale, s, Boston, Mass.) Lake mapping and stabilization, Indiana (D. C. Perkins, s, Indianapolis) Long-term chronologies of hydrologic events (W. D. Simons, h, Tacoma, Wash.)H YDROLOG Y—LI M NOLOG Y A251 Hydrology, surface-water—Continued Natural diurnal fluctuation in streams (R. E. Oltman, s, W) Peak inflow and outflow through ponds (J. E. McCall, s, Trenton, N. J.) Rates of runoff from small rural watersheds in Alabama (L. B. Peirce, s, Tuscaloosa) Small streams, Alabama (L. B. Peirce, s, Tuscaloosa) Unit graphs and infiltration rates, Alabama (L. B. Peirce, s, Tuscaloosa) Variations in streamflow, Utah (G. L. Whitaker, s, Salt Lake City) Variations in streamflow due to earthquakes, Utah (W. N. Jibson, s, Salt Lake City) Verification of hydraulic and hydrologic design factors, Montlemar Creek (AVragg Swamp canal), Alabama (L. H. Terry, s, Tuscaloosa) Water quality and streamflow characteristics of the Passaic River basin, New Jersey (P. W. Anderson, q, Philadelphia, Pa.) Industrial minerals: Ultramafic rocks of the Southeast (D. M. Larrabee, W) See also specific minerals. Iron: Clinton iron ores of the southern Appalachians (R. P. Sheldon, D) Alaska, Klukwan iron district (E. C. Robertson, AV) Michigan: Dickinson County, Southern (R. W. Bayley, M) East Marquette district (J. E. Gair, D) Gogebic Range, eastern (W. C. Prinz, W) Iron County, eastern (K. L. Wier, D) Iron River-Crystal Falls district (H. L. James, Minneapolis, Minn.) Negaunee and Palmer quadrangles (J. E. Gair, D) Minnesota, North Cuyuna range (R. G. Schmidt, AV) Montana, southwestern (K. L. AVier, D) New Jersey and New York, selected iron deposits (A. F. Buddington, Princeton, N.J.) Tennessee, Ducktown district and adjacent areas (R. M. Hernon, D) AVisconsin, Florence County (C. E. Dutton, Madison) Wyoming: Atlantic City district (R. AV. Bayley, M) Bradley Peak quadrangle (R. AV. Bayley, M) Isotope and nuclear studies : Isotope geology of lead (A. P. Pierce, D) Isotope ratios in rocks and minerals (I. Friedman, AV) Isotopic hydrology (G. L. Stewart, q, AAr) Isotopic studies of crustal processes (B. Doe, AA7) Light stable isotopes (I. Friedman, W) Magnetic-acoustic studies (F. E. Senftle, AA7) Nuclear irradiation (C. M. Bunker, D) Ore lead, geochemistry and origins (R. S. Cannon, D) Oxygen—isotope geothermometry (H. L. James, Minneapolis, Minn.) Radiation-damage studies (F. E. Senftle, AV) Radioactive nuclides in minerals (F. E. Senftle, W) Tritium concentrations in precipitation, surface waters, and ground waters of the coastal plain of New Jersey (E. C. Rhodehamel, g, Trenton) Isotope and nuclear studies—Continued See also Geochronology. Lake levels: Elevations of Great Salt Lake (H. AV. Chase, s, Salt Lake City, Utah) Land subsidence: Land-subsidence studies, San Joaquin Valley, Calif (J. F. Poland, g. Sacramento) Lead and zinc: Mississippi Valley type ore deposits, origin (A. V. Heyl, W) Ore lead, geochemistry and origins (R. S. Cannon, D) AVestern oxidized-zinc deposits (A. V. Heyl, AV) Zinc resources of the world (T. H. Kiilsgaard, AV) Arizona, Lochiel and Nogales quadrangles (F. S. Simons, D) California, Panamint Butte quadrangle (AV. E. Hall, W) Colorado, Rico district (E. T. McKnight, AA7) Idaho, Coeur d’Alene mining district (S. AA7. Hobbs, D) Illinois, AA7isconsin zinc-lead mining district (J. W. Whitlow, W) Kansas, Richer lead-zinc district (E. T. McKnight, W) Missouri: Picher lead-zinc district (E. T. McKnight, W) Southeastern part (T. H. Kiilsgaard, W) Nevada: Ely district (A. L. Brokaw, D) Pioche district (C. M. Tschanz, La Paz, Bolivia) New Mexico, Silver City area (W. R. Jones, D) Oklahoma, Picher lead-zinc district (E. T. McKnight, W) Tennessee: Eastern zinc studies (A. L. Brokaw, D) Origin and depositional control of some Tennessee and A7irginia zinc deposits (H. Wedow, Jr., Knoxville) Utah: East Tintic lead-zinc district (H. T. Morris, M) Park City district (C. S. Bromfield, D) Sheeprock Mountains, West Tintic district (H. T. Morris, M) A7irginia, origin and depositional control of some Tennessee and A7irginia zinc deposits (H. Wedow, Jr., Knoxville, Tenn.) Washington, Metaline lead-zinc district (M. G. Dings, D) Wisconsin, Wisconsin zinc-lead mining district (J. W. AVhitlow, W) Limestone-terrane hydrology: Artesian water in Tertiary limestones in the southeastern United States (V. T. Stringfield, w, W) Limestone-terrane hydrology (F. A. Swenson, g, D) Limnology: Chemical hydrology of Great Salt Lake (D. C. Hahl, q, Salt Lake City, Utah) Hydrology and geochemistry of topographically closed lakes in south-central Oregon (K. N. Phillips, s, Portland) Organisms, effect on water quality of streams (K. V. Slack, q, AV) Temperature and chemical quality of Bull Shoals and Norfork Reservoirs, Ark. (J. H. Hubble, q, Little Rock, Ark.)A252 INVESTIGATIONS IN PROGRESS IN THE GEOLOGIC, WATER RESOURCES, AND CONSERVATION DIVISIONS Limnology—Continued Thermal and biological characteristics of lakes, Indiana (J. F. Ficke, h, Fort Wayne) Low flow and flow duration: Arkansas, low-flow frequency studies (M. S. Hines, s, Little Rock) Georgia: Low-flow studies (R. F. Carter, s, Atlanta) Relation of geology to low flow (O. J. Cosner, s, Atlanta) Source of base flow to streams (F. A. Kilpatrick, s, Atlanta) Illinois: Low-flow frequency analyses (W. D. Mitchell, s, Champaign) Low-flow partial-record investigation (W. D. Mitchell, s, Champaign) Iowa: Low-flow frequency studies (H. H. Schwob, s, Iowa City) Origin of base flow for small drainage basins (G. R. Kunkle, E. C. Pogge, s, Iowa City) Kansas: Low-flow data collection (T. J. Irza, s, Topeka) Seepage flow of Kansas streams (M. W. Busby, s, Topeka) Massachusetts, low-flow characteristics (G. K. Wood, s, Boston) Mississippi, low-flow characteristics (H. G. Golden, s, Jackson) Missouri, low-flow characteristics (M. S. Petersen, s, Rolla) New York: Low-flow analysis for stream classification (O. P. Hunt, s, Albany) Low-flow frequency (O. P. Hunt, s, Albany) Ohio, low-flow and storage requirements (W. P. Cross, s, Columbus) Pennsylvania, low-flow frequency analysis (W. F. Busch, s, Harrisburg) South Carolina, low-flow gaging (F. W. Wagener, W. W. Evett, s, Columbia) Tennessee, low-flow studies (J. S. Cragwall, Jr., w, Chattanooga ) Texas: Base flow, quantity and quality—San Gabriel River (D. K. Leifeste, q, J. T. Smith, s, Austin) Base flow, quantity and quality—Little Cypress Creek (J. H. Montgomery, s, Austin) Base flow studies (W. B. Mills, s, Austin) Wisconsin, low-flow analyses (D. W. Ericson, s, Madison) Lunar geology. See Extraterrestrial studies. Manganese. See Ferro-alloy metals. Marine geology: Atlantic coastal plain, regional synthesis (J. C. Maher, M) East coast continental shelf and margin (R. H. Meade, Woods Hole, Mass.) Marine hydrology: Effects of heated-water outfall into brackish tidal water, Patuxent River, Md. (R. L. Cory, h, W) Marine hydrology—Continued Minimum tides of Delaware Estuary (A. C. Lendo, s, Trenton, N.J.) Recognition of late glacial substages in New England and New York (J. E. Upson, h, W) Tidal discharge and velocity studies (A. C. Lendo, s, Trenton, N.J.) Washington: Influence of industrial and municipal wastes on estuarine and offshore water quality (J. F. Santos, q, Portland, Oreg.) Willapa Bay project (A. O. Waananen, s, M) See also Sea-water intrusion. Meteorites. See Extraterrestrial studies. Mineral and fuel resources—compilations and topical studies: Alaska: Metallogenic provinces (C. L. Sainsbury, D) Southeastern Alaska, regional geology and mineral resources (R. A. Loney, M) Drilling data, statistical techniques in the analysis of (H. Wedow, Knoxville, Tenn.) Energy resources of the United States (T. A. Hendricks, D) Massive sulfide deposits (A. R. Kinkel, Jr., W) Metallogenic maps, United States (T. H. Kiilsgaard, W) Mineral exploration, Northwestern United States (D. R. MacLaren (Spokane, Wash.) Mineral fuel resources, United States (L. C. Conant, W) Mineral-resource information and research (H. Kirkemo, W) Mississippi Valley type ore deposits, origin (A. V. Heyl, W) Oxygen isotope geothermometry (H. L. James, Minneapolis, Minn.) Resource data storage and retrieval (R. A. Weeks, W) Resource study techniques (R. A. Weeks, W) Tennessee and Virginia zinc deposits, origin and deposi-tional control (H. Wedow, Jr., Knoxville, Tenn.) Uranium-bearing veins (G. W. Walker, D) Uranium deposits, formation and redistribution (K. G. Bell, D) Utah, mineral-resource map (L. S. Hilpert, Salt Lake City, Utah) Western oxidized-zinc deposits (A. V. Heyl, W) Wisconsin, northern, mineral-resources appraisal (C. E. Dutton, Madison) Zoning of mineral deposits (D. A. Gallagher, M) See also specific minerals or fuels. Mineralogy and crystallography, experimental: Crystal chemistry (H. T. Evans, Jr., W) Crystal chemistry—borate minerals (J. R. Clark, C. L. Christ, W) Crystal chemistry—phosphate minerals (M. E. Mrose, W) Crystal chemistry—rock-forming silicate minerals (D. E. Appleman, W) Crystal chemistry—uranium minerals (H. T. Evans, W) Mineralogic services and research (A. D. Weeks, W; T. Botinelly, D) New minerals (D. E. Appleman, W)MINERALOGY AND CRYSTALLOGRAPHY—PALEONTOLOGY A253 Mineralogy and crystallography, experimental—Continued New minerals—micas and chlorites (M. D. Foster, W) Petrological services and research (C. Milton, W) Sedimentary mineralogy (P. D. Blackmon, D) See also Geochemistry, experimental. Mining hydrology: Mining hydrology (W. T. Stuart, g, W) Study of the hydrologic and related effects of strip mining in Beaver Creek watershed, Kentucky (J. J. Mus-ser, q, Columbus, Ohio) Minor elements: Black shale (J. D. Vine, M) Coal (P. Zubovic, W) Dispersion pattern of minor elements related to igneous intrusions (W. R. Griffitts, D) Geochemistry (G. Phair, W) Niobium: Colorado, Wet Mountains (R. L. Parker, D) Phosphoria Formation, stratigraphy and resources (R. A. Gulbrandsen, M) Rare-earth elements, resources and geochemistry (J. W. Adams, D) Sedimentary rocks, mineral fractionation and fine-grained trace element content (T. D. Botinelly, D) Selenium resources and geochemistry (D. F. Davidson, D) Tantalum-niobium resources of the United States (R. L. Parker, D) Trace-analysis methods, development (H. W. Lakin, D) Trace-analysis methods, research (F. N. Ward, D) Volcanic rocks (R. R. Coats, M) Model studies, hydrologic: Analog analysis of the hydrology of the Blue River basin, Nebraska (P. A. Emery, g, Lincoln) Analog model—unsaturated flow (H. E. Skibitzke, h, Phoenix, Ariz.) Analog model—unsteady-state flow (H. E. Skibitzke, h, Phoenix, Ariz.) Analytical model of the land phase of the hydrological cycle (D. R. Dawdy, s, W) Houston Ship Channel model study (R. E. Smith, s, Austin, Tex.) Snake River Plain, aquifer electric analog (E. H. Walker, g, Boise, Idaho) Molybdenum. See Ferro-alloy metals. Monazite: Geology of monazite (W. C. Overstreet, Jidda, Saudi Arabia) Southeastern United States (W. C. Overstreet, Jidda, Saudi Arabia) Nickel. See Ferro-alloy metals. Nuclear explosions, hydrology: Geologic and hydrologic evaluations of the Tatum salt dome area, Mississippi (R. E. Taylor, g, Jackson) Hydrologic studies of the Nevada Test Site (I. J. Wino-grad, w, Carson City) Potential applications of nuclear explosives in development and management of water resources (A. M. Piper, F. W. Stead, w, M) Project chariot, hydrology (A. M. Piper, w, M) Oil shale: Colorado: Grand-Battlement Mesa (J. R. Donnell, D) State resources (D. C. Duncan, W) Utah, Uinta Basin (W. B. Cashion, D) Wyoming, Green River Formation, Sweetwater County (W. C. Culbertson, D) Paleobotany, systematic: Diatom studies (K. E. Lohman, W) Floras: Cenozoic, Western United States (J. A. Wolfe, W) Devonian (J. M. Schopf, Columbus, Ohio) Pennsylvania, Illinois and adjacent States (C. B. Read, Albuquerque, N. Mex.) Permian (S. H. Mamay, W) Fossil wood and general paleobotany (R. A. Scott, D) Plant microfossils: Cenozoic (E. B. Leopold, D) Mesozoic (R. H. Tschudy, D) Paleozoic (R. M. Kosanke, D) Paleoecology: Coal-ball studies, Pennsylvanian (S. H. Mamay, W) Diatoms (K. E. Lohman, W) Faunas, Late Pleistocene, Pacific Northwest (W. O. Addi-eott, M) Foraminifera: Ecology (M. R. Todd, W) Larger, deformity in (K. N. Sachs, Jr., W) Recent, Central America (P. J. Smith, M) Green River Formation, Wyoming, geology and paleolim-nology (W. H. Bradley, W) Mollusks, Tertiary nonmarine, biogeography, Snake River Plain and adjacent areas (D. W. Taylor, W) Paleoenvironment studies, Miocene, Atlantic Coastal Plain (T. G. Gibson, W) Pollen, Recent, distribution studies (E. B. Leopold, D) Tempskya, Southwestern United States (C. B. Read, Albuquerque, N. Mex.) Vertebrate faunas, biogeography, Ryukyu Islands (F. C. Whitmore, Jr., W) Paleontology, invertebrate, systematic: Brachiopods: Carboniferous (M. Gordon, Jr., W) Ordovician (R. B. Neuman, W; R. J. Ross, Jr., D) Permian (R. E. Grant, W) Upper Paleozoic (J. T. Dutro, Jr., W) Bryozoans: Ordovician (O. L. Karklins, W) Upper Paleozoic (H. M. Duncan, W) Cephalopods: Jurassic (R. M. Imlay, W) Triassic (N. J. Silberling, W) Upper Cretaceous (W. A. Cobban, D) Upper Paleozoic (M. Gordon, Jr., W) Chitinozoans, Lower Paleozoic (J. M. Schopf, Columbus, Ohio) Conodonts, Paleozoic (J. W. Huddle, W)A254 INVESTIGATIONS IN PROGRESS IN THE GEOLOGIC, WATER RESOURCES, AND CONSERVATION DIVISIONS Paleontology, invertebrate, systematic—Continued Corals, rugose: Mississippian (W. J. Sando, W) Silurian-Devonian (W. A. Oliver, Jr., W) Foraminifera: Cenozoic (R. Todd, W) Cenozoic, California and Alaska (P. J. Smith, M) Cretaceous (J. F. Mello, W) Fusuline and orbitoline (R. C. Douglass, W) Mississippian (B. A. L. Skipp, D) Pennsylvanian-Permian, fusuline (L. G. Henbest, W) Tertiary, larger (K. N. Sachs, Jr., W) Gastropods: Mesozoic (N. F. Sohl, W) Miocene-Pliocene, Atlantic Coast (T. G. Gibson, W) Oligocene, Mississippi (F. S. MacNeil, M) Paleozoic (E. L. Yochelson, W) Graptolites, Ordovician-Silurian (R. J. Ross, Jr., D) Mollusks: Cenozoic (F. S. MacNeil, M) Late Cenozoic, nonmarine (D. W. Taylor, W) Ostracodes: Cenozoic (J. E. Hazel, W) Lower Paleozoic (J. M. Berdan, W) Upper Paleozoic (I. G. Sohn, W) Pelecypods: Inoceramid (D. L. Jones, M) Jurassic (R. W. Imlay, W) Oligocene, Mississippi (F. S. MacNeil, M) Paleozoic (J. Pojeta, Jr., W) Triassic (N. J. Silberling, W) Radiolaria (K. N. Sachs, Jr., W) Trilobites: Cambrian (A. R. Palmer, W) Ordovician (R. J. Ross, Jr., D) Paleontology, stratigraphic: Cenozoic: Coastal Plains (D. Wilson, W) Diatoms: California and Nevada (K. E. Lohman, W) Nonmarine, Great Plains (G. W. Andrews, W) Foraminifera: Lodo Formation, California (M. C. Israelsky, M) New Jersey coastal plain (H. E Gill, g, Trenton) Smaller, Pacific Ocean and islands (M. R. Todd, W) Trent Marl and related units (P. M. Brown, g, Raleigh, N.C.) Miocene, Pacific Coast (W. O. Addicott, M) Mollusks: Alaska (F. S. MacNeil, M) Oregon (E. J. Moore, M) Western Pacific islands (H. S. Ladd, W) Pollen and spores, Kentucky (R. H. Tschudy, D) Vertebrates: Atlantic coast (F. C. Whitmore, Jr., W) Pacific coast (C. E. Repenning, M) Panama Canal Zone( F. C. Whitmore, Jr., W) Pleistocene (G. E. Lewis, D) Paleontology, stratigraphic—Continued Mesozoic: Cretaceous: Foraminifera, Nelchina area, Alaska (H. R. Berg-quist, W) Gulf coast and Caribbean (N. F. Sohl, W) Western interior United States (W. A. Cobban, D) Jurassic, North American (R. W. Imlay, W) Pacific coast (D. L. Jones, M) Pierre Shale, Front Range area (W. A. Cobban and G. R. Scott, D) Triassic marine faunas and stratigraphy (N. J. Silberling, M) Paleozoic: Cambrian (A. R. Palmer, W) Corals, Redwall Limestone, Arizona (W. J. Sando, W) Fusuline Foraminifera, Nevada (R. C. Douglass, W) Mississippian: Corals, northern Alaska (H. M. Duncan, W) Stratigraphy and brachiopods, northern Rocky Mountains and Alaska (J. T. Dutro, Jr., W) Stratigraphy and corals, northern Rocky Mountains (W. J. Sando, W) Ordovician: Stratigraphy and brachiopods, Eastern United States (R. B. Neuman, W) Western United States (R. J. Ross, Jr., D) Paleobotany and coal studies, Antarctica (J. M. Schopf, Columbus, Ohio) Pennsylvanian: Fusulinidae, north-central Texas (D. A. Myers, D) Spores and pollen, Kentucky (R. M. Kosanke, D) Permian: Floras, Southwest United States (S. H. Mamay, W) Stratigraphy and brachiopods, Southwest United States (R. E. Grant, W) Silurian-Devonian: Corals, Northeastern United States (W. A. Oliver, Jr., W) Great Basin and Pacific coast (C. W. Merriam, M) Upper Silurian-Lower Devonian, Eastern United States (J. M. Berdan, W) Subsurface rocks, Florida (J. M. Berdan, W) Type Morrow Series, Washington County, Ark. (L. G. Henbest, W) Upper Paleozoic, Great Basin (M. Gordon, Jr., W) Paleontology, vertebrate, systematic: Artidactyls, primitive (F. C. Whitmore, Jr., W) Pleistocene fauna, Big Bone Lick, Ky. (F. C. Whitmore, Jr., W) Tritylodonts, American (G. E. Lewis, D) Paleotectonic maps. See Regional studies and compilations. Pegmatites: North Carolina: Franklin quadrangle (F. G. Lesure, W) Southern Blue Ridge Mountains, mica deposits (F. G. Lesure, W)PEGMATITES—PHOSPHATE A255 Pegmatites—Continued South Dakota: Hill City pegmatite area (J. C. Rattd, D) Keystone pegmatite area (J. J. Norton, W) Permafrost studies: Distribution and general characteristics (W. E. Davies, W) Ground ice in central Alaska (T. L. Pdwd, College) Alaska, ground water and permafrost (J. R. Williams, g, Anchorage) Petroleum and natural gas: Continental shelves of the world (G. M. Everhart, New Philadelphia, Ohio) Mesozoic rocks of Florida and the eastern Gulf coast (E. R. Applin, Jackson, Miss.) Organic geochemistry (J. G. Palacas, D) Pre-Selma Cretaceous rocks of Alabama and adjacent States (L. C. Conant, W) Tuffs of the Green River Formation (R. L. Griggs, D) Upper Jurassic stratigraphy, northeast Texas, southwest Arkansas, northwest Louisiana (K. A. Dickinson, D) Williston Basin, Wyoming, Montana, North Dakota, South Dakota (C. A. Sandberg, D) Alaska: Gulf of Alaska Tertiary province (G. Plafker, M) Iniskin-Tuxedni region (R. L. Detterman, M) Lower Yukon-Koyukuk area (W. W. Patton, Jr., M) Nelchina area (A. Grantz, M) Northern, petroleum (G. Gryc, W) Arizona: Central and northwestern, Devonian rocks and paleo-geography (C. Teichert, Pakistan) Navajo Reservation, fuels potential (R. B. O’Sullivan, D) Arkansas: Ft. Smith district (T. A. Hendricks, D) Malvern quadrangle (W. Danilchik, Santiago, Chile) Northern, oil and gas investigations (E. E. Glick, D) California i Eastern Los Angeles basin (J. E. Schoellhamer, W) Salinas Valley (D. L. Durham, M) Vedder sand, structure-contour map (E. E. Richardson, c, Taft) Colorado: Animas River area (H. Barnes, D) Elk Springs quadrangle (J. R. Dyni, c, D) Grand Junction 2-degree quadrangle (W. B. Cashion, D) Northwestern, Upper Cretaceous stratigraphy (T. A. Hendricks, D) Thornburg area (J. R. Dyni, c, D) Kansas: Sedgwick Basin (W. L. Adkison, Lawrence) Shawnee County (W. D. Johnson, Jr., Lawrence) Wilson County (H. O. Wagner, M) Mississippi, Homochitto National Forest (E. L. Johnson, c, Tulsa, Okla.) Petroleum and natural gas—Continued Montana: Structure-contour map of the Montana Plains, revision (C. E. Erdmann, c, Great Falls) Nebraska, central Nebraska basin (G. E. Prichard, D) New Mexico: Animas River area (H. Barnes, D) Guadalupe Mountains (P. T. Hayes, D) San Juan Basin, east side (C. H. Dane, W) North Dakota: Dengate and Heart Butte NW quadrangles (E. V. Stephens, c, D) Glen Ullin quadrangle (C. S. V. Barclay, c, D) New Salem 2 SW and North Altmont quadrangles (H. L. Smith, c, D) Oklahoma: Ft. Smith district (T. A. Hendricks, D) McAlester Basin (S. E. Frezon, D) Utah: Grand Junction 2-degree quadrangle (W. B. Cashion, D) Navajo Reservation, fuels potential (R. B. O’Sullivan, D) Northeastern, Upper Cretaceous stratigraphy (T. A. Hendricks, D) Virginia, Big Stone Gap district (R. L. Miller, W) Washington: Grays Harbor basin, regional compilation (H. M. Beik-man, M) Grays Harbor basin, western part (H. C. Wagner, M) Wyoming: Crowheart Butte area (J. F. Murphy, D) LaBarge 1 SW and 2 SE quadrangles (R. L. Rioux, c, D) Lamont-Baroil area (M. W. Reynolds, D) Spence-Kane area (R. L. Rioux, c, D) Upper Cretaceous regional stratigraphy (T. A. Hendricks, D) Petrology. See Geochemistry and petrology. Phosphate: Phosphoria Formation, stratigraphy and resources (R. A. Gulbrandsen, M) Southeastern United States, phosphate resources (J. B. Cathcart, D) California, Monterey Formation phosphate (H. D. Gower, M) Florida, land-pebble phosphate deposits (J. B. Cathcart, D) Idaho: Aspen Range-Dry Ridge area (V. E. McKelvey, W) Divide 2 SW quadrangle (G. D. Fraser, c, D) Drigs quadrangle (E. R. Cressman, c, D) Garns Mountain quadrangle (M. H. Staatz, c, D) Irwin 1, 2, 4 NE, and 4 NW quadrangles (D. A. Jobin, c, D) Soda Springs quadrangle (F. C. Armstrong, D) Upper Valley quadrangle (R. L. Rioux, c, D) Montana, south central (R. W. Swanson, Spokane) Nevada, Montello area (R. G. Wayland, c, Los Angeles, Calif.)A256 INVESTIGATIONS IN PROGRESS IN THE GEOLOGIC, WATER RESOURCES, AND CONSERVATION DIVISIONS Phosphate—Continued North Carolina, phosphorite deposits in Beaufort County, geohydrology (J. O. Kimrey, g, Raleigh) Oriskany Formation (W. D. Carter, W) Ogden 1 SE and 4 quadrangles (T. A. Mullens, c, D) Utah and Wyoming, Crawford Mountains (W. C. Gere, c, Salt Lake City) Wyoming, Jackson 30-minute quadrangle (D. A. Jobin, c, D) Plant ecology: Basic research in vegetation and hydrology (R. S. Sigafoos, h, W) Ecologic criteria for conversion of juniper-piny on woodlands to grasslands (R. S. Aro, w, D) Vegetation changes in southwestern North America (R. M. Turner, h, Tucson, Ariz.) See also Vegetation. Potash: Colorado and Utah, Paradox basin (O. B. Raup, D) Colorado and Utah, Paradox basin, subsurface study of Paradox member (R. J. Hite, c, Salt Lake City) New Mexico, Carlsbad, potash and other saline deposits (C. L. Jones, M) Precipitation: Precipitation measurements in forested areas, New Jersey (E. C. Rhodehamel, g, Trenton) Precipitation records, Alabama (L. B. Peirce, s, Tuscaloosa) Storm patterns, using radar techniques (A. Wilson, h, Tucson, Ariz.) Public and industrial water supplies : Chemical characteristics of larger public water supplies in the United States (C. N. Durfor, q, W) Chemical and physical quality characteristics of public water supplies in North Carolina (J. C. Chemerys, q, Raleigh) Use of water by municipalities in New Mexico (G. A. Din-widdie, g, Albuquerque) Water requirements of the iron and steel industry (F. B. Walling, w, W) Water utilization studies—statewide, Kentucky (R. A. Krieger, q, Columbus, Ohio) Quality of water: Delaware River, chemical characteristics (D. McCartney, q, Philadelphia, Pa.) Delaware River, summary of data between Bristol, Pa., and Marcus Hook. Pa. (W. B. Keighton, q, Philadelphia) Housatonic River basin (F. H. Pauszek, q, Albany, N.Y.) Lower Columbia River, Washington-Oregon (L. B. Laird, q, Portland, Oreg.) Saline ground-water of the United States (J. H. Feth, g, M) Alabama, compilation of chemical quality of water (J. R. Avrett, q, Tuscaloosa) California, effect of diversion works on the Trinity River (G. Porterfield, q, Sacramento) Delaware, chemical quality, statewide (E. F. McCarren, q, Philadelphia, Pa.) Indiana, saline-water resources (R. A. Krieger, q, Columbus, Ohio) Kansas: South Fork Ninnescah River basin (A. M. Diaz, q, Lincoln, Nebr.) Quality of water—Continued Kansas—Continued Walnut River basin (R. F. Leonard, q, Lincoln, Nebr.) Kentucky, saline-water investigations (H. T. Hopkins, g, Louisville) Maryland, chemical-quality reconnaissance of streams (J. D. Thomas, q, Rockville) Missouri: Meramec Basin (J. H. Hubble, q, Little Rock, Ark.) Missouri surface waters (C. T. Taylor, q, Little Rock, Ark.) Nebraska: Niobrara River basin (H. D. Stephens, q, Lincoln) Petrography and water-mineral relationships of two Quaternary fills in eastern Nebraska (E. C. Schu-ett, q, Lincoln) New Jersey, basic water-quality network (P. W. Anderson, q, Philadelphia, Pa.) New Mexico, maps showing quality of water by counties (E. C. John, g, Albuquerque) New York, Glowegee Creek at AEC reservation near West Milton (F. H. Pauszek, q, Albany) North Dakota: Devils Lake area (H. T. Mitten, q, Lincoln, Nebr.) Heart River drainage basin, chemical quality of surface waters and sedimentation (M. L. Maderak, q, Lincoln, Nebr.) Ohio: Maumee River basin (M. Deutsch, J. W. Wallace, w, Columbus) Miami River basin (G. W. Whetstone, q, Columbus) Quality of surface and ground waters—statewide inventory (G. W. Whetstone, q, Columbus) Oklahoma, Washita River basin (J. J. Murphy, q, Oklahoma City) Oregon, appraisal of water quality and water-quality problems of certain streams (R. J. Madison, q, Portland) Pennsylvania, quality of water, statewide (D. McCartney, q, Philadelphia) Texas: Hubbard Creek basin (C. H. Hembree, q, Austin) Quality of base flow of streams (C. H. Hembree, q, Austin) Statewide reconnaissance of streams (L. S. Hughes, q, Austin) Surface waters (L. S. Hughes, q, Austin) Surface waters of the Brazos River basin (H. B. Mendieta, q, Austin) Utah, ground water (C. A. Horr, q, Salt Lake City) Washington: Chemical quality of ground water (A. S. Van Denburgh, q, Portland, Oreg.) Influence of natural gas on ground-water quality (L. B. Laird, q, Portland, Oreg.) Quality of surface water (J. F. Santos, q, Portland, Oreg.) Water quality of Grays Harbor (L. B. Laird, q, Portland, Oreg.) See also Sedimentation.QUICKSILVER—SEDIMENTATION A257 Quicksilver: Alaska, southwestern (E. W. MacKevett, Jr., M) California, Coast Range ultramaflc rocks (E. H. Bailey, M) Mercury deposits and mercury resources (E. H. Bailey, M) Oregon, Ochoco Reservation, Lookout Mountain, Eagle Rock, and Post quadrangles (A. C. Waters, Baltimore, Md.) Radioactive materials, transport in water: Clinch River, Tenn. (P. H. Carrigan, w, Chattanooga) Distribution and concentration of radioactive waste in streams by fluvial sediments (W. W. Sayre, q, Fort Collins, Colo.) Exchange phenomena and chemical reactions of radioactive substances (E. A. Jenne, q, D) Mineralogy and exchange capacity of fluvial sediments (V. C. Kennedy, q, D) Movement of radionuclides in the Columbia River estuary, Oregon-Washington (D. W. Hubbell, q, Portland, Oreg.) Removal of radionuclides from water by earth materials of the Nevada Test Site (W. A. Beetem, q, D) Savannah River study (A. E. Johnson, s, Columbia, S.C.) Sediment transport in the Columbia River as related to the movement of radionuclides (W. L. Haushild, q, Portland, Oreg.) Radioactive-waste disposal: Geology and hydrology of the Western States as related to the management of radioactive materials (R. W. Maclay, g, St. Paul, Minn.) Hydrogeologic studies at the National Reactor Testing Station, Idaho (D. A. Morris, g, Boise) Hydrogeologic studies of the Savannah River Plant, S.C. (I. W. Marine, g, Columbia) Hydrology pertaining to deep-well disposal of wastes (W. Drescher, g, Madison, Wis.) Laboratory investigations (C. R. Naeser, W) Nuclear-irradiation studies (C. M. Bunker, D) Oak Ridge Reservation hydrologic studies (R. M. Richardson, w, Chattanooga, Tenn.) Waste-contamination studies at Los Alamos, N. Mex.— ground water (W. D. Purtyman, g, Albuquerque) Rare-earth metals. See Minor elements. Regional studies and compilations, large areas of the United States: Basement rock map of United States (R. W. Bayley, M) Continental shelves of the world (G. M. Everhart, New Philadelphia, Ohio) Geologic map of the United States (P. B. King, M) Geologic map of the United States between lats 35° N and 39° N, scale 1:1,000,000 (C. R. Willden, D) Gravity map of the United States (H. R. Joesting, W) Military intelligence studies (M. M. Elias, W) Paleotectonic-map folios: Mississippian System (L. C. Craig, D) Pennsylvanian System (E. D. McKee, D) Permian System (E. D. McKee, D) Sino-Soviet Terrain Atlas (M. M. Elias, W) Rhenium. See Minor elements and Ferro-alloy metals Saline minerals: Colorado and Utah, Paradox basin (O. B. Raup, D) New Mexico, Carlsbad potash and other saline deposits (C. L. Jones, M) Wyoming, Green River Formation, Sweetwater County (W. Culbertson, D) Sea-water intrusion: Salinity conditions of the lower Delaware River basin (D. McCartney, q, Philadelphia, Pa.) Salinity in the Miami River, Florida (S. D. Leach, s, Ocala) Salinity of estuaries in Everglades National Park, Fla. (K. A. MacKichan, q, Ocala) Salt-water encroachment in the Brunswick, Ga., area (R. L. Wait, g, Atlanta) Salt-water encroachment in the Savannah, Ga. area (H. B. Counts, g, Atlanta) Salt-water encroachment studies—Dade County and city of Miami, Fla. (H. Klein, g, Tallahassee) Salt-water intrusion in coastal streams (T. H. Woodard, q, Raleigh, N.C.) Sedimentation: Effect of sedimentation on the propagation of trout in small streams, Montana (A. R. Gustafson, q, Worland, Wyo.) Fall velocity of fluvial sediment particles as affected by size, shape, density, concentration and turbulence (H. P. Guy, q, Fort Collins, Colo.) Hyperconcentrations of suspended sediment (J. P. Beverage, J. K. Culbertson, q, Albuquerque, N. Mex.) Ripples, dunes, and antidunes, statistical analysis (C. F. Nordin, Jr., q, Fort Collins, Colo.) Roughness in alluvial channels, and sediment transportar tion (H. P. Guy, q, Fort Collins, Colo.) Sediment transport and channel roughness in natural and artificial channels (T. Maddock, Jr., h, Tucson, Ariz.) Some sediment-transport formulas, application to the Rio Grande near Bernalillo, New Mexico (C. F. Nordin, Jr., J. P. Beverage, q, Albuquerque) Some sedimentation characteristics of a sand-bed stream (D. M. Culbertson, q, Lincoln, Nebr.) Sources, movement, and distribution of sediment in a small watershed (M. G. Wolman, h, Baltimore, Md.) Arkansas River basin, fluvial sediment (J. O. Mundorff, q, Lincoln, Nebr.) California, Cache Creek, sediment transport (L. K. Lustig, q, Sacramento) Eel and Mad River basins, sediment transport (G. Porterfield, q, Sacramento) Colorado, Kiowa Creek, fluvial sedimentation and runoff (R. Brennan, q, D) Columbia River basin, fluvial sediment transport (R. C. Williams, q, Portland, Oreg.) Sediment-transport characteristics of certain streams (P. A. Glancy, q, Portland, Oreg.) Indiana, reconnaissance of sediment yields in streams (R. F. Flint, q, Columbus, Ohio) Kansas, Little Blue River basin, fluvial sediment and quality of water (J. C. Mundorff, q, Lincoln, Nebr.) Little Arkansas River basin, sedimentation (C. D. Albert, q, Lincoln, Nebr.)A258 INVESTIGATIONS IN PROGRESS IN THE GEOLOGIC, WATER RESOURCES, AND CONSERVATION DIVISIONS Sedimentation—Continued Missouri, St. Louis, special sediment investigations at Mississippi River (C. H. Scott, q, Lincoln, Nebr.) Nebraska, Little Blue River basin, fluvial sediment and quality of water (J. C. Mundorff, q, Lincoln, Nebr.) Medicine Creek basin, erosion and deposition (J. C. Brice, q, Lincoln) New Jersey, Stony Brook watershed, fluvial sedimentation (J. R. George, q, Philadelphia, Pa.) North Carolina, upper Yadkin River basin, sediment yield (H. E. Reeder, q, Raleigh) Oregon, Alsea River basin, sedimentation in forested drainage areas (R. C. Williams, q, Portland) Pennsylvania, Bixler Run watershed, hydrology and sedimentation (J. R. George, q, Philadelphia) Conestoga Creek watershed, sedimentation (J. R. George, q, Philadelphia) Corey Creek and Elk Run watershed (J. R. George, q, Philadelphia) Sedimentation Statewide (J. R. George, q. Harrisburg) Susquehanna River basin, fluvial sediment reconnaissance (J. R. George, q, Harrisburg, Pa.) Texas, reconnaissance sediment investigations (C. T. Wel-born, q, Austin) Upper Trinity River basin, sedimentation (C. H. Hembree, q, Austin) Washington, Chehalis River basin, sedimentation and chemical quality of surface waters (P. A. Glancy, q, Portland, Oreg.) Palouse River basin, sedimentation and chemical quality of surface waters (P. R. Boucher, q, Portland, Oreg.) Walla Walla River basin, sedimentation and chemical quality of surface waters (B. E. Mapes, q, Portland, Oreg.) Wisconsin, reconnaissance sediment investigations (C. R. Collier, q, Columbus, Ohio) Wyoming, Wind River basin, sedimentation and chemical quality of surface waters (D. C. Dial, q, Worland) See also Geomorphology and Quality of water. Sedimentation, reservoirs: California, Stony Gorge Reservoir (J. M. Knott, q, Sacramento) Colorado, Kiowa Creek basin, K-79 reservoir (R. Brennan, q, D) Georgia, North Fork Broad River, subwatershed 14 near Avalon (D. E. Shattles, q, Ocala, Fla.) Louisiana, Bayou Dupont watershed, reservoir (S. F. Ka-pustka, q, Baton Rouge) Nevada, Pea vine Creek (J. E. Parkes, w, Carson City) New Jersey, Baldwin Creek reservoir (J. R. George, q, Philadelphia, Pa.) Texas, Escondido Creek (C. H. Hembree, q, Austin) Utah, Paria River basin, Sheep Creek near Tropic sediment barrier (G. C. Lusby, w, D) Selenium. See Minor elements. Silica: Oriskany Formation (W. D. Carter, W) Tintic Quartzite (K. B. Ketner, D) Soil moisture: Effect of mechanical treatment on arid lands in the Western United States (F. A. Branson, w, D) Effects of grazing exclusion, Badger Wash area, Colorado (G. 0. Lu^by, w, D) Iron distribution, water movement in soils, and vegetation (R. F. Miller, w, D) Plant and soil-water response to thermal gradient, Ogal-lala Formation (F. A. Branson, w, D) Plants as indicators of soil-moisture availability (F. A. Branson, w, D) Spectroscopy: Mobile spectographic laboratory (F. N. Ward, D) Spectrographic analytical services and research (A. W. Helz. W; A. T. Myers, D; H. Bastrom, M) X-ray spectroscopy (H. J. Rose, Jr., W; W. W. Brannock, M) Springs: Discharge of Rattlesnake Springs and nearby irrigation wells, Eddy County, N. Mex. (E. R. Cox, g., Albuquerque) Springs of California (C. F. Berkstresser, Jr., q, Sacramento) Springs of Colorado (J. A. McConaghy, g, D) Stratigraphy and sedimentation: Atlantic Coastal Plain: Regional synthesis (J. C. Maher. M) Southern part (J. E. Johnston, W) Basement rock map of United States (R. W. Bayley, M) Cave deposits, stratigraphy and mineralogy (W. E. Davies, W) Colorado Plateau: Lithologic studies (R. A. Cadigan, D) San Rafael Group, stratigraphy (J. C. Wright, W) Stratigraphic studies (L. C. Craig, D) Triassic stratigraphy and lithology (J. H. Stewart, M) East coast continental shelf and margin (J. S. Schlee, Woods Hole, Mass.) Front Range. Pennsylvanian and Permian stratigraphy (E. K. Maughn, D) Green River Formation, tuffs (R. L. Griggs, D) Northern Rocky Mountains and Great Plains, Middle and Late Tertiary history (N. M. Denson, D) Phosphoria Formation, stratigraphy and resources (R. A. Gulbrandsen, M) Pierre Shale: Paleontology and stratigraphy, Front Range area (W. A. Cobban, G. R. Scott, D) Montana, North Dakota, South Dakota, Wyoming, and Nebraska, chemical and physical properties (H. A. Tourtelot, D) Sedimentary environments, classification (E. J. Crosby, D) Sedimentary mineralogy (P. D. Blackmon, D) Sedimentary-petrology laboratory (H. A. Tourtelot, D) Sedimentary structures, model studies (E. D. McKee, D) Subsurface-data center (L. C. Craig, D) Upper Jurassic stratigraphy, northeast Texas, southwest Arkansas, northwest Louisiana (K. A. Dickinson, D)STRATIGRAPHY AND SEDIMENTATION—URANIUM A259 Stratigraphy and sedimentation—Continued Williston Basin, Wyoming, Montana, North Dakota and South Dakota (C. A. Sandberg, D) Alaska: Matanuska stratigraphic studies (A. Grantz, M) Mesozoic stratigraphy (W. W. Patton, A. Grantz, M) Arizona : Dripping Spring quartzite (H. C. Granger, D) Redwall limestone (E. D. McKee, D) Supai and Hermit Formations (E. D. McKee, D) California, Lower Cambrian strata of southern Great Basin (J. H. Stewart, M) Colorado: Northwestern Jurassic stratigraphy (G. N. Pipiringos, D) Northwestern, upper Cretaceous stratigraphy (T. A. Hendricks, D) Pennsylvanian evaporite, northwest Colorado (W. W. Mallory, D) Kansas, Sedgwick Basin (W. L. Adkison, Lawrence) Maine, regional Paleozoic stratigraphy (R. B. Neuman, W) Maryland, Allegany County (W. deWitt, Jr., W) Massachusetts, central Cape Cod, subsurface studies (R. N. Oldale, C. R. Tuttle, and C. Koteff, Boston) Nebraska, central Nebraska basin (G. E. Prichard, D) Nevada, Lowrer Cambrian strata of southern Great Basin (J. H. Stewart, M) New Mexico, Guadalupe Mountains (P. T. Hayes, D) New York, Dunkirk and related beds (W. deWitt, Jr., W) Oklahoma : McAlester Basin (S. E. Frezon, D) Southern, Permian stratigraphy (D. H. Eargle, Austin, Tex.) Pennsylvania, Devonian stratigraphy (G. W. Colton, W) Texas, northern, Permian stratigraphy (D. H. Eafgle, Austin, Tex.) Utah: Northeastern, Upper Cretaceous stratigraphy (T. A. Hendricks, D) Old River Bed (R. B. Morrison, D) Washington, Grays Harbor basin, regional compilation (H. M. Beikman, M) Wyoming: Black Hills, Inyan Kara Group (W. J. Mapel, D) Green River Formation, geology and paleolimnology (W. H. Bradley, W) Lamont-Baroil area (M. W. Reynolds, D) South-central, Jurassic stratigraphy (G. N. Pipiringos, D) Upper Cretaceous, regional stratigraphy (T. A. Hendricks, D) Wedding of Waters-Devil Slide quadrangle (E. K. Maughan, D) Wind River Basin, regional stratigraphy (W. R. Keefer, Laramie) See also Paleontology, stratigraphic, and specific areas under Geologic mapping. Structural geology and tectonics : Deformation research (D. J. Vames, D) Ground-movement inventory (A. S. Allen, W) Structural geology and tectonics—Continued Isotopic studies of crustal processes (B. Doe, W) Rock behavior at high temperature and pressure (E. C. Robertson, W) Alaska, tectonic map (G. Gryc, M) California: San Andreas fault (L. F. Noble, Valyermo) Sierra foothills mineral belt (L. D. Clark, M) Montana, Hebgen Lake, earthquake investigations (J. B. Hadley, W, and I. J. Witkind, D) Nevada, orogenic processes northern Sonoma Range (J. Gilluly, D) See also specific areas under Geologic mapping. Talc: Southeast United States, ultramafic rocks (D. M. Larra-bee, W) Vermont, north-central (W. M. Cady, D) Tantalum. See Minor elements. Temperature studies, water: Streamflow and temperatures of Glowegee Creek, N.Y. (D. F. Dougherty, s, Albany) Temperature distribution in natural streams (E. J. Jones, s, M) Temperature of Alabama streams (L. E. Carroon, s, Tuscaloosa) Temperature of Oregon streams—compilation, correlation, and analysis of data (A. M. Moore, s, Portland) Temperature studies, White River, Ark. (L. D. Hauth, s, Little Rock) Thermal characteristics of aquifer systems (R. Schneider, h, W) Thorium : Alaska, uranium-thorium reconnaissance (E. M. Mac-Kevett, Jr., M) Colorado: Gunnison County, Powderhorn area (J. C. Olson, D) Wet Mountains (M. R. Brock, D) Idaho, central, radioactive placer deposits (D. L. Schmidt, W) Western States, thorium investigations (M. H. Staatz, D) Tin: Alaska: Lost River Mining district (C. L. Sainsbury, D) Seward Peninsula (P. L. Killeen, W) Tofty placer district (D. M. Hopkins, M) Tungsten. See Ferro-alloy metals. Uranium: Colorado Plateau, uranium-vanadium deposits in sandstone (R. P. Fischer, D) Formation and redistribution of uranium deposits (K. G. Bell, D) Uranium-bearing pipes, Colorado Plateau and Black Hills (C. G. Bowles, D) Uranium-bearing veins (G. W. Walker, D) Uranium in black shales, mid-continent area (D. H. Eargle, Austin, Tex.) Arizona, Dripping Spring quartzite (H. C. Granger, D) Colorado : Baggs area (G. E. Prichard, D)A260 INVESTIGATIONS IN PROGRESS IN THE GEOLOGIC, WATER RESOURCES, AND CONSERVATION DIVISIONS U ranium—Continued Colorado—Continued Bull Canyon district (C. H. Roach, D) Gypsum Valley district (C. F. Withington, W) La Sal area (W. D. Carter, W) Lisbon Valley area (G. W. Weir, Berea, Ky.) Maybell-Lay area (M. J. Bergin, W) Slick Rock district (D. R. Shawe, D) Uravan district (R. L. Boardman, W) Idaho, Mt. Spokane quadrangle (A. E. Weissenborn, Spokane) New Mexico: Ambrosia Lake district (H. C. Granger, D) Grants area (R. E. Thaden, Columbia, Ky.) Laguna district (R. H. Moench, D) Northwestern part (L. S. Hilpert, Salt Lake City, Utah) South Dakota: Harding County and adjacent areas (G. N. Pipiringos, D) Southern Black Hills (G. B. Goot, D) Texas, coastal plain, geophysical and geological studies (D. H. Eargle, Austin) Utah: La Sal area (W. D. Carter, W) Lisbon Valley area (G. W. Weir, Berea, Ky.) Sage Plain area (L. C. Huff, Manila, P.I.) San Rafael Swell (C. C. Hawley, D) White Canyon area (R. E. Thaden, Columbia, Ky.) Washington, Mt. Spokane quadrangle (A. E. Weissenborn, Spokane) Wyoming: Baggs area (G. E. Prichard, D) Central, selected uranium deposits (F. C. Armstrong, D) Crooks Gap area (J. G. Stephens, D) Gas Hills district (H. D. Zeller, D) Powder River Basin, Pumpkin Buttes area (W. N. Sharp, D) Shirley Basin area (E. N. Harshman, D) Urban geology: California: Los Angeles area (J. T. McGill, Los Angeles) Malibu Beach quadrangle (R. F. Yerkes, F) Oakland East quadrangle (D. H. Radbruch, M) Palo Alto quadrangle (E. H. Pampeyan, M) Point Dume quadrangle (R. H. Campbell, M) San Francisco North quadrangle (J. Schlocker, M) San Francisco South quadrangle (M. G. Bonilla, M) San Mateo quadrangle (G. O. Gates, M) Colorado: Denver metropolitan area (R. M. Lind vail, D) Golden quadrangle (R. Van Horn, D) Morrison quadrangle (J. H. Smith, D) Pueblo and vicinity (G. R. Scott, D) District of Columbia, Washington metropolitan area (H. W. Coulter and C. F. Withington, W) Iowa, Omaha-Council Bluffs and vicinity (R. D. Miller, D) Maryland, Washington, D.C., metropolitan area (H. W. Coulter and C. F. Withington, W) Urban geology—Continued Massachusetts, Boston and vicinity (C. A. Kaye, Boston, Mass.) Montana, Great Falls area (R. W. Lemke, D) Nebraska, Omaha-Council Bluffs and vicinity (R. D. Miller, D) South Dakota, Rapid City area (E. Dobrovolny, D) Texas, San Antonio and vicinity (R. D. Miller, D) Utah, Salt Lake City and vicinity (R. Van Horn, D) Virginia, Washington, D.C., metropolitan area (H. W. Coulter and C. F. Withington, W) Washington: Puget Sound Basin (D. R. Crandell, D) Seattle and vicinity (D. R. Mullineaux, D) Urbanization, hydrologic effects: Effects of urbanization in the Northwest Branch, Anacostia River basin, Maryland (F. L. Keller, q. Rockville) Effect of urbanization on flood runoff in the Wichita area, Kansas (M. W. Busby, s, Topeka) Effects of urbanization on hydrology (J. D. Thomas, q, Rockville, Md.) Hydrologic effects of urbanization (J. R. Crippen, s, M) Influence of urbanization on flood flows, Nashville-David-son County metropolitan area, Tennessee (L. G. . Conn, w, Chattanooga) Urban runoff, Turtle Creek, Tex. (F. H. Ruggles, s. Austin) Urban runoff, Waller Creek, Tex. (W. H. Espey, Jr., s, Austin) Vanadium: Colorado Plateau, uranium-vanadium deposits in sandstone (R. P. Fischer, D) Commodity studies (R. P. Fischer, D) Geology and resources, bibliography (J. P. Ohl, D) Colorado: Bull Canyon district (C. H. Roach, D) La Sal area (W. D. Carter, W) Lisbon Valley area (G. W. Weir, Berea, Ky.) Slick Rock district (D. R. Shawe, D) Uravan district (R. L. Boardman, W) Utah: La Sal area (W. D. Carter, W) Lisbon Valley area (G. W. Weir, Berea, Ky.) Sage Plain area (L. C. Huff, Manila, P.I.) Vegetation: Alaska, vegetation map (L. A. Spetzman, W) Pacific islands, vegetation (F. R. Fosberg, W) Plant-analysis laboratory (F. N. Ward, D) See also Plant ecology. Volcanic-terrane hydrology: Columbia River Basalt hydrology (R. C. Newcomb, g, Portland, Oreg.) Volcanology: Alaska, Ratmai National Monument, petrology and volean-ism (G. H. Curtis, M) Costa Rica volcanic studies (K. J. Murata, San Jose, Costa Rica) Hawaii, volcanology (J. G. Moore, Hawaii) Idaho, central Snake River Plain, volcanic petrology (H. A. Powers, D)VOLCANOLOGY—WATER RESOURCES, COLORADO A261 Volcanology—Continued Montana: Bearpaw Mountains, petrology (W. T. Peeora, W) Wolf Creek area, petrology (R. G. Schmidt, W) New Mexico, Valles Mountains, petrology (R. L. Smith, W) Pacific coast basalts, geochemistry (K. J. Murata, M) Silicic ash beds, correlation (H. A. Powers, D) Water management: Water-land relationships in the Patuxent River basin, Maryland (D. O’Bryan, w, W) Water resources: Areal hydrology, public domain, Western States (G. C. Lusby, w, D) Connecticut River basin—Vermont, New Hampshire, Massachusetts, Connecticut (D. J. Cederstrom, g, Boston, Mass.) Lower Colorado basin, hydrology (C. C. McDonald, g, Yuma, Ariz.) Mississippi Embayment, hydrology (E. M. Cushing, g, Memphis, Tenn.) Ohio River basin (M. Deutsch, w, Cahanna, Ohio) Upper Brazos River, basin project, Permian Basin program (P. R. Stevens, h, Austin, Tex.) Upper Mississippi River basin (P. G. Olcott, g, Madison, Wis.) Water-supply exploration on the public domain—Pacific coast area (C. T. Snyder, w, M) Water-supply exploration on the public domain—Rocky Mountain area (N. J. King, w, D) Alabama (Tuscaloosa) : Geologic and hydrologic profile along U.S. Highway 31 in Butler County (J. G. Newton, g) Hydrologic atlas of the State (C. F. Hains, s) Hydrology of Choctawhatchee-Escambia River basins (J. C. Scott, g) Hydrology of southwest Alabama (L. B. Pierce, s) Hydrology of the Tennessee Valley in Alabama (J. R. Harkins, s) Ground water: Barbour County (R. V. Chafin, g) Cullman County (R. J. Faust, g) Dallas County (J. C. Scott, g) Greene County (K. D. Wahl, g) Hale County (T. H. Sanford, g) Marion County (L. V. Causey, g) Marshall County (T. H. Sanford, g) Pickens County (K. D. Wahl, g) Sumter County (J. G. Newton, g) Sylacauga area (G. W. Swindel, g) Talladega County (L. V. Causey, g) Surface-water resources, Calhoun County (J. R. Harkins, s) Alaska (Anchorage) : Hydrologic conditions in the Anchorage area (M. V. Marcher, g) Water-supply investigations for the U.S. Air Force (A. J. Feulner, g) American Samoa (Honolulu, Hawaii) : Ground water (K. J. Takasaki, g) Water resources—Continued Arizona (Tucson) : Sycamore Creek basin, water resources (B. Thomsen, w) Ground water: Beardsley area (W. Kam, w) Big Sandy Valley (W. Kam, w) Dateland-Hyder area (P. W. Johnson, w) Fort Huachuca (S. G. Brown, w) Navajo Indian Reservation (M. E. Cooley, w) Papago Indian Reservation (L. A. Heindl, w, W) Pinal County, northwestern part (W. F. Hardt, w) Safford area (E. S. Davidson, w) San Simon basin (N. D. White, w) Tucson basin (E. F. Pashley, Jr., w) Willcox basin (S. G. Brown, w) Arkansas (Little Rock) : Grant-Hot Spring Counties, water resources (H. N. Halberg, g) Jackson-Independence Counties, water resources (D. R. Albin, g) Ground water: Arkansas River valley (M. S. Bedinger, g) Pulaski-Saline Counties (R. O. Plebuch, g) California (Sacramento) : Lompoc Plain, hydrologic study (R. E. Evenson, g) Point Reyes National Seashore, hydrologic study (R. H. Dale, g) Ground water: Antelope Valley-East Kern Water Agency (J. E. Weir, Jr., g) Camp Pendleton Marine Corps Base (J. J. French, g) Death Valley National Monument: Ashford Mill (M. G. Croft, g) Emigrant Junction (M. G. Croft, g) Edwards Air Force Base (W. R. Moyle, g) Elwood-Gaviota area (R. E. Evenson, g) Inyokern Naval Ordnance Test Station (J. E. Weir, Jr., g) Kaweah-Tule area (M. G. Croft, g) Kern River fan (R. H. Dale, g) Kings Canyon National Park, Grant Grove area (R. H. Dale, g) Kings River area (R. W. Page, g) Lassen County water-supply exploration on the public domain (F. Kunkel, g) Mission Indians (F. W. Giessner, g) Pala-Rineon area (J. J. French, g) Point Arguello area (K. S. Muir, g) Santa Maria Valley (R. E. Evenson, g) Santa Ynez Uplands (G. F. LaFreniere, g) Summerland area (K. S. Muir, g) Twenty-nine Palms Marine Corps Training Center (J. E. Weir, Jr., g) Yosemite National Park, Forrest area (R. H. Dale, g) Colorado (Denver) : Hydrology of Arkansas River basin-Canon City to State line (J. E. Moore, g)A262 INVESTIGATIONS IN PROGRESS IN THE GEOLOGIC, WATER RESOURCES, AND CONSERVATION DIVISIONS Water resources—Continued Colorado (Denver)—Continued Ground water: Occurrence and development in State (J. A. Mc-Conaghy, g) Summary of pumping tests in State (W. W. Wilson, g) Bent County (J. H. Irwin, g) Big Sandy Valley below Limon (D. L. Coffin, g) Colorado High Plains, trends in ground-water development (A. J. Boettcher, g) Denver Basin (G. H. Chase, g) Denver Basin, ground-water trends (C. A. J. Boettcher, g) East-central, Quaternary deposits (H. E. McGovern, g) Parts of Larimer, Logan, Morgan, Sedgwick, and Weld Counties (W. G. Weist, g) Pueblo and Fremont Counties (H. E. McGovern, g) Southeastern, bedrock aquifers (J. H. Irwin, g) Ute Mountain-Ute Indian Reservation (J. H. Irwin, g) Connecticut (q, s, Hartford; g, Middletown): Ground water, Hamden-Wallingford area (A. M. La-Sala, Jr, g) Water resources of Connecticut: Part 1, Quinebaug River basin (A. D. Randall, g) Part 2, Shetucket River basin (M. P. Thomas, s) Part 3, Thames River basin (C. E. Thomas, Jr., q) Florida (g, Tallahassee; s, q, Ocala) : Statewide, special studies (C. S. Conover, g; K. A. Mac-Kichan, q; A. O. Patterson, s) Water atlas (W. E. Kenner, s) Ground water: Cape Canaveral area, Brevard County, geohydrology (D. W. Brown, g) Dade County, special studies (H. Klein, g) Dade County, Area B, special studies (F. A. Kohout, g) Duval, Nassau, and Baker Counties (G. W. Leve, g) Fort Lauderdale area, special studies (H. Klein, g) Marion County (F. N Visher, g) Polk County (H. G. Stewart, g) Venice well field, Sarasota County, geohydrology (W. E. Clark, g) Water resources: Broward County (C. B. Sherwood, g) Econfina Creek basin area (R. H. Musgrove, s) Escambia and Santa Rosa Counties (R. H Musgrove, s) Everglades National Park (J. H. Hartwell, s) Green Swamp area (R. W. Pride, s) Lower Hillsboro Canal area (R. G. Grantham, q) Middle Gulf basins (R. N. Cherry, q) Myakka River basin (B. F. Joyner, q) Orange County (W. F. Liehtler, g) Georgia (Atlanta) : River-systems studies (A. N. Cameron, s) Water resources—Continued Georgia (Atlanta) —Continued Ground water: Floyd and Polk Counties (C. W. Cressler, g) Seminole, Decatur, and Grady (C. W. Sever, g) Water resources: Cook County (C. W. Sever, g) Pulaski County (R. C. Vorhis, g) Rockdale County (M. J. McCollum, g) Thomas County, Cairo area (C. W. Sever, g) Thomas, Brooks, and Colquitt Counties (C. W. Sever, g) Guam, (Honolulu, Hawaii) : Ground water (D. A. Davis, g) Surface water (S. H. Hoffard, s) Hawaii (Honolulu) : Hydrologic studies (G. T. Hirashima, s) Water production from the Waiaha catchment area, Hawaii (S. S. Chinn, s) Water resources: Hilo-Puna area, Hawaii, reconnaissance (G. Yaina-naga, s) Kahuku area, Oahu (K. J. Takasaki, g) Kau area, Hawaii, reconnaissance (D. A. Davis, g) Mokuleia-Waialua area, Oahu (J. C. Rosenau, g) Waianae district, Oahu (C. P. Zones, g) Windward Oahu (K. .T. Takasaki. g) Idaho (Boise) : Little Lost River basin, water resources (H. A. Waite, g) Ground water: Aberdeen-Springfield area (II. G. Sisco, g) American Falls (M. J. Mundorff, g) Artesian City-Oakley area (E. G. Crosthwaite, g) Lower Teton Basin (E. G. Crosthwaite, g) Mud Lake Basin (P. R. Stevens, g) Salmon Falls Creek area (E.G. Crosthwaite, g) Indiana (Indianapolis) : Ground water: Delaware County (R. E. Hoggatt, g) Northwestern (J. D. Hunn. g) West-central (L. W. Cable, g) Iowa (Iowa City) : Availability and utilization of water in central Iowa (F. W. Twenter, R. W. Cole, g) Ground water: Cerro Gordo County (W. L. Steinhilber, g) Linn County (R. E. Hansen, g) The Mississippian aquifer of Iowa (P. J. Horiek. W. L. Steinhilber, g) Water availability from glacial deposits of south-central Iowa (J. W. Cagle, g) Kansas (Lawrence) : Ground water: Brown County (C. K. Bayne, g) Butler County (J. M. McNellis, g) Cherokee County (W. J. Seevers, g) Decatur County (W. G. Hodson, g) Ellsworth County (C. K. Bayne, g)WATER RESOURCES, KANSAS-MISSISSIPPI A263 Water resources—Continued Kansas (Lawrence)—Continued Ground water—Continued Finney, Kearny, and Hamilton Counties (W. R. Meyer, g) Johnson County (H. G. O’Connor, g) Labette County (W. L. Jungmann, g) Linn County (W. J. See vers, g) Miami County (D. E. Miller, g) Montgomery County (H. G. O’Connor, g) Morton County (L. C. Burton, g) Neocho County (W. L. Jungmann, g) Northwestern (S. W. Fader, g) Pratt County (D. W. Layton, g) Republican River valley (S. W. Fader, g) Rush County (J. McNellis, g) Southwestern Kansas (W. R. Meyer, g) Walnut River basin (J. M. McNellis, g) Kentucky (Louisville) : Mammoth Cave area, water resources (R. V. Cushman, g) Quality of surface and ground water—Statewide inventory (R. A. Krieger, q, Columbus, Ohio) Ground water: Alluvial terraces of the Ohio River (W. E. Price, g) Jackson Purchase area (R. W. Davis, g) Louisville area (E. A. Bell, g) Louisiana (Baton Rouge) : Ground water: Geismar-Burnside area (R. A. Long, g) Greater New Orleans area (J. R. Rollo, g) Water resources: Lake Pontchartrain study (G. T. Cardwell, g) Ouachita Parish (J. E. Rogers, g) Plaquemine-White Castle area (R. A. Long, g) Pointe Coupee Parish (M. D. Winner, Jr., g) Rapides Parish (R. Newcome, Jr., g, Raymond Sloss, s) Southwestern (A. H. Harder, g, S. M. Rogers, q) Vernon Parish (A. J. Calandro, s, J. E. Rogers, g) Maine (Augusta) : Ground water: Coastal area of southwestern Maine (G. C. Prescott, g) Lower Penobscot basin (G. C. Presseott, g) Maryland (Baltimore) : Systems planning studies of the Gunpowder Falls basin (D. O’Bryan, w, W) Water resources of the Salisbury area (D. H. Boggess, g) Ground water: Baltimore County, use of ground water (C. P. Laughlin, g) C&O Canal (E. G. Otton, g) Prince Georges County (F. K. Mack, g) Massachusetts (Boston) : Water resources of the Housatonic River basin (R. F. Norviteh, g) Water resources—Continued Massachusetts (Boston) —Continued Ground water: Assabet River basin (S. J. Pollock, g) Brockton-Pembroke area (R. G. Petersen, g) Cape Cod National Seashore (R. G. Petersen, g) Central Boston area (W. N. Palmquist, g) Ipswich River drainage basin (E. A. Sammell, g) Lower Merrimack valley (J. E. Cotton, g) Parker and Rowley River drainage basins (E. A. Sammel, g) Southern Plymouth County (J. M. Weigle, g) Ten Mile-North Taunton River basin (R. G. Petersen, g) Westfield River basin (R. G. Petersen, g) Michigan (Lansing) : Ground water: Battle Creek area (K. E. Vanlier, g) Dickinson County (T. G. Newport, g) Menominee County (K. E. Vanlier, g) Surface water, North Branch Clinton River basin (S. W. Wiitala. s) Water resources: Grand River Basin (K. E. Vanlier, g) Marquette Iron Range (S. W. Wiitala, s) Upper Au Sable River (G. E. Hendrickson, g) Van Buren County (G. E. Hendrickson, g) Minnesota (St. Paul) : Hydrologic investigation of the Tamarac River basin, Marshall County (R. W. Maclay, g) Water resources reconnaissance of watershed units: Big Stone Lake unit, Big Stone, Swift, and Lac qui Parle Counties (R. D. Cotter, g) Middle River unit, Red River of the North, Kittson and Marshall Counties (R. W. Maclay, g) Pomme de Terre River unit, Big Stone, Chippewa, Douglas, Grant, Otter Tail, Stevens, and Swift Counties (R. D. Cotter, g) Ground water: Grand Rapids area (E. L. Oakes, g) Kittson, Marshall, and Roseau Counties (G. R. Schiner, g) Minneapolis-St. Paul area, chemical quality of ground water (M. A. Maderak, q, Lincoln Nebr.) Mississippi (Jackson) : Ground water: Hancock County, National Aeronautics and Space Administration Test Facility (Roy Newcome, Jr. g) Lauderdale County, geology and ground-water resources (J. W. Lang, E. H. Boswell, g) Northwestern (B. E. Wasson, g) Water resources: Aberdeen, Columbus, West Point areas (B. E. Wasson, g) Jones, Wayne, Forrest, Perry, and Green Counties (W. L. Broussard, q, Baton Rouge) Middle Pascagoula River basin (H. G. Golden, s) Monroe, Clay, Oktibbeha, and Lowndes Counties (M. W. Gaydos, q, Baton Rouge, La.) 746-002 0 - 64 - 18A264 INVESTIGATIONS IN PROGRESS IN THE GEOLOGIC, WATER RESOURCES, AND CONSERVATION DIVISIONS Water resources—Continued Missouri (Rolla) : Water resources of the Joplin area (E. J. Harvey, g) Montana (Billings) : Ground water: Bitterroot Valley, Ravalli County (R. G. McMurt-rey, g) Cedar Creek anticline, west flank (O. J. Taylor, g) Deer Lodge Valley (R. L. Konizeski, g) Fort Belknap Indian Reservation (D. C. A1 verson, g) Frazier-Wolf Point irrigation project (W. B. Hopkins, g) Judith Basin, western part (E. A. Zimmerman, g) Lower Bighorn River valley Hardin Unit (L. J. Hamilton, g) Missoula Valley (R. G. McMurtrey, g) Nebraska (Lincoln) : Geology and hydrology of Saline County (P. A. Emery, g) Ground water: Adams County, availability of ground water (C. F. Keech, g) Fillmore County (C. F. Keech, g) York County (C. F. Keech, g) Nevada (Carson City) : Hydrology of a portion of the Humboldt River valley (P. Cohen, W) Ground water: Coyote Spring, Kane Spring, and Muddy River Springs area (T. E. Eakin, w) Dixie and Fairview Valleys (P. Cohen, D. E. Everett, w) Eagle Valley (G. F. Worts, Jr., w) Edwards Creek Valley (D. E. Everett, w) Kings River valley (G. T. Malmberg, w) Lake Valley (F. E. Rush, w) Monitor, Antelope, and Kobeh Valleys (F. E. Rush, w) Pahrump Valley (G. T. Malmberg, w) Quinn River valley (C. J. Huxel, Jr., w) Smith Creek valley (D. E. Everett, w) Spring Valley (F. E. Rush, w) Upper Reese River valley (F. E. Rush, w) Washoe Valley (G. F. Worts, Jr., w) White River valley system (T. E. Eakin, w) New Hampshire (Boston, Mass.) : Ground water, lower Merrimack River basin (J. M. Weigle, g) New Jersey (Trenton) : Drought in the Delaware River basin, (J. E. McCall, s) Water budget of Great Swamp (E. G. Miller, s) Ground water: Camden County (E. Donsky, g) Cumberland County (J. G. Rooney, g) Essex County (J. Vecchioli, g) Morris County (H. E. Gill, g) Ocean County (H. R. Anderson, g) Pine Barrens (E. C. Rhodehamel, g) Rahway area (H. R. Anderson, g) Water resources—Continued New Jersey (Trenton)—Continued Ground water—Continued Water-level fluctuations in New Jersey, 1958-62 (C. R. Austin, g) Wharton Tract (E. C. Rhodehamel, g) New Mexico (Albuquerque) : Evaluation of pumping effects in the Malaga Bend area, Eddy County (E. R. Cox, g) Evaluation of well-field data at Los Alamos (R. L. Cushman, g) Hydrologic almanac of State (W. E. Hale, g) Hydrology of damsites on the Mescalero Apache Indian Reservation (J. S. Havens, g) Miscellaneous activities under the New Mexico State Engineer program (L. V. Davis, g) Water supply for Los Alamos (R. L. Cushman, g) Ground water: Fort Bayard Hospital, Grant County, geology and ground-water resources (F. D. Trauger, g) Gila Cliff Dwellings National Monument, Catron County (F. D. Trauger, g) Grant County (F. D. Trauger, g) Guadalupe County (A. Clebsch, Jr., g) Lake McMillan and Carlsbad Springs, ground-water conditions between (E. R. Cox, g) Luna County, southern (G. C. Doty, g) MAR Facility water supply (G. C. Doty, g) McKinley County, southeastern (J. B. Cooper, g) McMillan delta area (E. R. Cox, g,) Mesita, Laguna Indian Reservation, ground-water exploration (G. A. Dinwiddie, g) Pojoaque Pueblo Grant, Santa Fe County, availability of ground water for irrigation (G. A. Dinwiddie, g) Quay County (W. A. Mourant, g) Roswell basin, Chaves and Eddy Counties, quantitive analysis of the ground-water system (G. E. Maddox, g) San Juan County, northern (F. D. Trauger, g) Sandia and Manzano Mountains area (F. B. Titus, g) Torreon and Ojo Encino School wells (G. A. Dinwiddie, g) White Sands Integrated Range, northern (J. E. Weir, g) White Sands Missile Range, reconnaissance, ground-water resources at selected sites (G. C. Doty, g) Zuni Reservation water supply (S.W. West, g) New York (Albany) : Ground water: Jamestown area (L. J. Crain, g) Nassau County (N. M. Perlmutter, g) Nassau County, northeast (J. Isbister, g) Orange and Ulster Counties (M. H. Frimpter, g) Queens County (J. Soren, g) Rensselaer County, Schodack terrace (J. Joyce, g) Schenectady County, eastern (J. D. Winslow, g) Suffolk County, mid-island area (J. Soren, g) Syracuse area (I. H. Kantrowitz, g)WATER RESOURCES, NEW YORK-SOUTH DAKOTA A265 Water resources—Continued New York (Albany)—Continued Surface water: Gazetteer of streams (F. L. Robison, s) Surface-water resources of New York (J. C. Kram-merer, g) Water resources: Genesee River basin (B. K. Gilbert, s) Lake Erie-Niagara area (A. L. LaSala, g) North Carolina (Raleigh) : Stream sanitation and water supply of State (G. C. Goddard, s) Ground water: Cape Hatteras National Park, quality of ground water (H. B. Wilder, q) Chowan County (O. B. Lloyd, Jr., g) Craven County (E. O. Floyd, g) New Hanover County (G. Bain, g) Pitt County (C. T. Sumsion, g) Surface water: Interpretation of surface-water data (G. C. Goddard, s) Neuse River headwaters, surface-water resources (G. C. Goddard, s) North Dakota (Grand Forks) : Ground water: Barnes County (T. E. Kelly, g) Burleigh County (P. G. Randich, g) Cass County (R. L. Klausing, g) Devils Lake area (Q. F. Paulson, g) Divide County (C. A. Armstrong, g) Foster and Eddy Counties (Henry Trapp, g) Renville and Ward Counties (W. A. Pettyjohn, g) Richland County (Q. F. Paulson, g) Stutsman County (C. J. Huxeljg) Traill County (H. M. Jensen, g) Williams County (E. A. Ackroyd, g) Ohio (Columbus) : Ground water: Fairfield County (G. D. Dove, g) Geauga County (J. Baker, g) Miami River basin (A. M. Spieker, g) Northeastern Ohio (J. L. Rau, g) Oklahoma (Oklahoma City) : Quality of water in the upper Arkansas River Basin (R. P. Orth, q) Special investigations and reports (A. R. Leonard, g) Thickness of the fresh ground-water zone (D. L. Hart, Jr., g) Ground water: Arkansas and Verdigris River valleys (H. H. Tanaka, g) Oklahoma and Cleveland Counties, ground water in the Garber Sandstone and Wellington Formation (P. R. Wood, g) Woodward County (P. R. Wood, g) Surface water: Kiamichi River Basin (L. L. Laine, s, T. R. Cummings, q) Little River basin (A. O. Westfall, s, R. I’. Orth, q) Water resources—Continued Oklahoma (Oklahoma City)—Continued Surface water—Continued Muddy Boggy River Basin (A. O. Westfall, s, T. R. Cummings, q) Oregon (Portland) : Ground water, northern Williamette Valley: Eola-Amity Hills area (D. Price, g) French Prairie area (D. Price, g) Molalla-Salem slope area, (E. R. Hampton, g) Pennsylvania (g, Harrisburg; q, Philadelphia) Chemical quality, Lehigh River Basin (S. D. Faust, q) Water resources of the Schuylkill River Basin (J. R. George, q) Ground water: Brunswick Formation (S. M. Longwill, g) Chester County, metamorphic and igneous rocks (C. W. Poth, g) Lancaster County, carbonate rocks (H. Meisler, g) Martinsburg Shale (L. D. Carswell, g) New Oxford Formation (H. E. Johnston, g) Puerto Rico (San Juan) : Water resources: Gudnica area (N. E. McClymonds, w) Guayanilla area (J. W. Crooks, w) Jobos area (N. E. McClymonds, w) Lower Tallaboa Valley (I. G. Grossman, w) Ponce area (N. E. McClymonds, w) Rhode Island (Providence) : Ground water: Block Island (A. J. Hansen. Jr., g) Potowomut-Wickford area (G. R. Schiner, g) South Branch Pawtuxet area (W. B. Allen, g) Southeastern Rhode Island (G. R. Schiner, g) Upper I’awcatuck Basin, availability (W. B. Allen, g) South Carolina (Columbia) : Ground water: Coastal plain, northeastern, geology and ground-water resources (G. E. Siple, g) Coastal plain, subsurface geology and hydrology (G. E. Siple, g) Greenville County, geology and ground-water resources (N. C. Koch, g)i Leesville area, potential sand aquifers (G. E. Siple, W. D. Paradeses, g) Piedmont, alluvial aquifers (G. E. Siple, g) Savannah River Plant, hydrologic effect of pump-age (G. Siple, N. C. Koch, g) Surface water: Analyses of streamflow characteristics (A. E. Johnson, s) Compilation, streamflow records (A. E. Johnson, s) South Dakota (Huron) : Ground water: Beadle County (L. W. Howells, g) Clay County (J. C. Stephens, g) Dakota Sandstone (C. F. Dyer, g) Hydrology of glacial drift in selected drainage basins: Big Sioux Basin from Sioux Falls to Brookings County line (M. J. Ellis, g)A266 INVESTIGATIONS IN PROGRESS IN THE GEOLOGIC, WATER RESOURCES, AND CONSERVATION DIVISIONS Water resources—Continued South Dakota (Huron)—Continued Ground water—Continued Lake Madison-Skunk Creek drainage basin (M. J. Ellis, g) Pine Ridge Indian Reservation (M. J. Ellis, g) Sanborn County (L. W. Howells, g) Studies of artesian wells and selected shallow aquifers (C. F. Dyer, g) Tennessee (Chattanooga) : Ground water: Germantown-Collierville area (D. J. Nyman, w) Highland Rim Plateau (D. T. Marsh, W) Memphis area (E. A. Bell, w) Water resources: Lawrence County (R. H. Bingham, w) Lewis County (R. H. Bingham, w) Montgomery County (G. K. Moore, w) Trace Creek (J. H. Criner, Jr., w) Texas (Austin) : Annotated bibliography of ground-water literature (R. C. Baker, g) Permian Basin program—eastern problem area (P. R. Stevens, h) Hydrologic investigations: Deep Creek (W. B. Mills, s) Escondido Creek (F. W. Kennon, s) Little Elm Creek (E. E. Schroeder, s) Mukewater Creek (S. P. Sauer, s) Trinity, Brazos, Colorado, and San Antonio River basins (C. R. Gilbert, s) Ground water: Atascosa and Frio Counties (Roger C. Baker, g) Bee County (B. N. Myers, g) Brazos River alluvium, occurrence and availability of ground water (J. G. Cronin, g) Caldwell County (C. R. Follett, g) Camp, Franklin, Morris, and Titus Counties (M. E. Broom, g) Carson and part of Gray County (G. McAdoo, g) Conzales County (G. H. Shafer, g) DeWitt County (C. R. Follett, g) El Paso area, continuing quantitative studies (M. E. Davis, g) Gaines County (P. L. Rettman, g) Galveston County (R. K. Gabrysch, g) Guadalupe County (G. H. Shafer, g) Hardin County (E. T. Baker, Jr., g) Harrison County (M. E. Broom, g) Houston County, occurrence and availability of ground water (G. H. Tarver, g) Houston district, continuing quantitative studies (R. K. Gabrysch, g) Jackson County (E. T. Baker, Jr„ g) Jasper and Newton Counties (J. B. Wesselman, g) LaSalle and McMullen Counties (H. B. Harris, g) Lee County (G. L. Thompson, g) Menard County (R. C. Baker, g) Orange County (J. B. Wesselman, g) Water resources—Continued Texas (Austin)—Continued Ground water—Continued Padre Island National Seashore (B. N. Myers, g) Refugio County (C. C. Mason, g) San Antonio area (S. Garza, g) San Augustine and Sabine Counties (R. B. Anders, g) Upper and lower Rio Grande basins, Brazos, Guadalupe, San Antonio, Nueces, Red, and Gulf Coast basins, reconnaissance ground-water investigations (L. A. Wood, g) Utah (Salt Lake City) Chemical characteristics of water resources of Western Utah (O. Hattori, q) Water resources of Salt Lake County (W. V. Iorns, g) Ground water: Ground-water conditions in Utah (T. Arnow, g) Northern Utah Valley (R. M. Cordova, S. Su-bitzky, g) Selected basins in southwestern Utah (G. W. Sandberg, g) Sevier Desert (R. W. Mower, R. D. Feltis, g) Sevier River basin between Yuba Dam and Leamington Canyon (L. J. Bjorkiund, g) Tooele Valley (J. S. Gates, g) Upper Sevier Valley (C. H. Carpenter, L. J. Bjorkiund, G. B. Robinson, g) Weber Basin (J. H. Feth, g) Virginia : Ground waters, Northern Neck peninsula (A. Sinnott. g, Trenton, N.J.) Virgin Islands (San Juan, P.R.) : Water resources (D. G. Jordan, O. J. Cosner, w) Washington (Tdfcoma) : King County, water resources (D. Richardson, s) Ground water: Grant, Adams, and Franklin Counties (J. W. Bingham, g) Island County (H. W. Anderson, Jr., g) King County, southwest (J. E. Luzier, g) Mason County (J. B. Noble, g) Spokane County, northern part (D. R. Cline, g) Whitman County (K. L. Walters, g) Surface water: Cedar River basin (F. T. Hidaka, s) Chehalis River basin (D. Richardson, s) West Virginia (Morgantown) : Grotand water. Mason and Putnam Counties (B. M. Wilmoth, g) Water resources of the Monongahela River basin (G. Meyer, g) Wisconsin (Madison) : Ground water: Milwaukee area (J. H. Green, g) Racine-Kenosha Counties (R. D. Hutchinson, g) Water resources: Little Plover River Basin (E. P. Weeks, g. D. W. Ericson, s) Lower Wisconsin River Valley (L. .T. Hamilton, g) Upper Wisconsin River Valley (R. W. Devaul, g)WATER RESOURCES, WISCONSIN-ZINC A267 Water resources—Continued Wisconsin (Madison)—Continued Water resources—Continued Water resources and geology of Portage County (C. L. R. Holt, Jr., g) Water resources and geology of Winnebago County (P. G. Olcott, g) Wyoming (g, Cheyenne; q, Worland) : Ground water; Cheyenne area (L. J. McGreevy, g) Devils Tower National Monument (E. D. Gordon, g) Grand Teton National Park (E. D. Gordon, g) Great Divide and Washakie structural basins and Rock Springs uplift (G. E. Welder, g) Johnson County, northern and central (H. A. Whitcomb, g) Laramie County (M. E. Lowry, g) Sheridan County (M. E. Lowry, g) Yellowstone National Park, selected areas (E. D. Gordon, g) Other countries : Afghanistan, surface-water resources of Helmand River basin (A. O. Westfall, w, Lashkar Gah) Brazil: Hydrogeologic investigations in northeastern Brazil (S. L. Schoff, w, Recife) Surface-water investigations in northeastern Brazil (L. J. Snell w, Recife) Libya, nationwide ground-water investigation and pilot development (J. R. Jones, w, Tripoli) Nepal, nationwide surface-water investigations (D. E. Havelka, w, Katmandu) Nigeria: Hydrogeologic investigation of artesian water in Chad Basin (R. E. Miller, w, Maiduguri) Hydrogeologic investigations in the Sokoto Basin (Wm. Ogilbee, w, Sokoto) National ground-water program (D. A. Phoenix, w, Kaduna) Okinawa, southern, ground water (D. A. Davis, g, Honolulu) Pakistan, hydrologic investigations related to waterlogging and salinity control in the Punjab Region (M. J. Mundorff, w, Lahore) Sudan, ground-water investigations, Kordofan and Darfur Provinces (H. G. Rodis, w, Khartoum) Tunisia, ground-water investigations and hydrogeologic mapping (V. C. Pishel, w, Tunis) Turkey, nationwide ground-water investigations advisory work (C. R. Murray, w, Ankara) United Arab Republic (Egypt), ground-water investigation and pilot development in the New Valley project (R. W. Sundstorm, w, Cairo) Waterpower classification: Alaska : Crescent Lake (west of Cook Inlet) (L. F. Pease, c, W; G. C. Giles, c, Tacoma, Wash.) Waterpower classification—Continued Alaska—Continued Grace Lake (near Ketchikan) (J. B. Dugwyler, c, Tacoma, Wash.) Taiya River, West Creek powersite (J. B. Dugwyler, c, Tacoma, Wash.) Tyee Lake (near Wrangell) (J. B. Dugwyler, c, Tacoma, Wash.) Waterpower resources (compiled for Senate report on mineral and water resources of Alaska) (G. C. Giles, c, Tacoma, Wash.) Arizona, inventory of waterpower resources (W. C. Senk-piel, c, D) California : Inventory of waterpower resources (R. N. Doolittle, c, Sacramento) Kern River basin (R. N. Doolittle, c, Sacramento) Mono Creek basin (K. W. Sax, c, Sacramento) Owens Lake basin (R. N. Doolittle, c, Sacramento) San Joaquin River basin (R. N. Doolittle, c, Sacramento) Smith River (K. W. Sax, c, Sacramento) Colorado: Inventory of waterpower resources (W. C. Senkpiel, c, D) Red Park Creek and Little Red Park Creek (H. D. Tefft, c, D) Idaho: Salmon River basin (L. L. Young, c, Portland, Oreg.) Waterpower resources (compiled for Senate report on mineral and water resources of Idaho) (L. L. Young, c, Portland, Oreg.) Weiser River basin (J. L. Colbert, c. Portland, Oreg.) Montana, inventory of waterpower resources (J. B. Dugwyler, c, Tacoma, Wash.) Nevada, waterpower resources (compiled for Senate report on mineral and water resources of Nevada) (R. N. Doolittle, c, Sacramento, Calif.) New Mexico, inventory of waterpower resources (W. C. Senkpiel, c, D) Oklahoma, inventory of waterpower resources (W. C. Senkpiel, c, D) Oregon: Alsea River (L. L. Young, c, Portland) Nehalen River (L. L. Young, c, Portland) Siuslaw River (J. L. Colbert, c. Portland) Utah : Colorado River basin (Glen Canyon Dam to Moab, Utah) (H. D. Tefft, c, D) Waterpower resources of Utah (mineral and waterpower resources of Utah—Senate report) (W. C. Senkpiel, c, D; A. Johnson, c. W) Washington, inventory of waterpower resources (J. B. Dugwyler, c, Tacoma) Waterpower resources—United States and other countries of the world (L. L. Young, c, Portland, Oreg.) Zeolites, in southeastern California (R. A. Sheppard, D) Zinc. See Lead and zinc.HOW TO ORDER U.S. GEOLOGICAL SURVEY PUBLICATIONS All book publications, maps, and charts published by the Survey are listed in “Publications of the Geological Survey 1879-1961”, and in supplements, which keep the list up to date. New releases are announced each month in “New Publications of the Geological Survey”. All of these lists of publications are free upon request to the geological survey, Washington, d.c., 2024 2. They may be consulted at many public and educational-institution libraries, and at the Geological Survey offices named below. Books, maps, charts, and folios that are out of print can no longer be purchased from any official source. They may be consulted at many libraries, and some can be purchased from dealers in second-hand books. 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The release of revised indexes is announced in the monthly list of new publications of the Geological Survey. Each State index shows the areas mapped and gives lists of Geological Surveys offices from which maps may be purchased and of local agents who sell the maps. Advance material available from current topographic mapping is indicated on quarterly releases of State index maps. This material, including such items as aerial photography, geodetic-control data, and preliminary maps in various stages of preparation and editing, is available for purchase. Information concerning the ordering of these items is given on each State index. Requests for indexes or inquiries concerning availability of advance materials should be directed to the map information OFFICE, U.S. GEOLOGICAL SURVEY, WASHINGTON, D.C., 20242. State water-resources investigations folders A series of 8- by 10y2-inch folders entitled “Water Resources Investigations in [State]” is a new project of the Water Resources Division to inform the public about its current program in the 50 States and Puerto Rico. As the State programs change, the folders will be revised. Folders for all 50 States and Puerto Rico are available free on request to the U.S. Geological Survey. Open-file reports Open-file reports include unpublished manuscript reports, maps, and other material made available for public consultation and use. Arrangements can generally be made to reproduce them at private expense. The date and places of availability for consultation by the public are given in press releases or other forms of public announcement. In general, open-file reports are A269A270 HOW TO ORDER U.S. GEOLOGICAL SURVEY PUBLICATIONS placed in one or more of the three Geological Survey libraries: room 1033, general services bldg., Washington, D.C.; BLDG. 23, FEDERAL CENTER, DENVER, COLO.; and 345 MIDDLEFIELD ROAD, MENLO PARK, CALIF. Other de- positories may include one or more of the Geological Survey offices listed on pages A227 to A232, or interested State agencies. Many open-file reports are replaced later by formally printed publications.CONTENTS OF GEOLOGICAL SURVEY RESEARCH 1964, CHAPTERS B, C, AND D Listed below are the contents of Professional Papers 501-B, -C, and -D, comprising 135 articles, many of which are cited in the preceding pages. References to chapters B and C are given in the text in the following form: King (p. B1-B8); the chapter is identified by the letter preceding the page number. References to chapter D are given as: Hinds (chapter D); the chapter is still in press and page numbers are not available. PROFESSIONAL PAPER 501-B Structural geology Page Interpretation of the Garden Springs area, Texas, by the “down-structure” method of tectonic analysis, by P. B. King_ B1 Cryptoexplosive structure near Versailles, Ky., by D. F. B. Black_________________________________________________ 9 A late Tertiary low-angle fault in western Juab County, Utah, by D. R. Shawe------------------------------------ 13 Structure of part of the Timber Mountain dome and caldera, Nye County, Nev., by W. .1. Carr------------------- 16 Diverse recurrent movement along segments of a major thrust fault in the Schell Creek Range near Ely, Nev., by Harald Drewes__________________________________________________________________________________________________ 20 Stratigraphy and paleontology Facies relations of exposed Rome Formation and Conasauga Group of northeastern Tennessee with equivalent rock in the subsurface of Kentucky and Virginia, by L. D. Harris____________________________________________________ 25 Stratigraphy of the Lee Formation in the Cumberland Mountains of southeastern Kentucky, by K. J. Englund------ 30 The Little Stone Gap Member of the Hinton Formation (Mississippian) in southwest Virginia, by R. L. Miller____ 39 The Chattanooga Shale (Devonian and Mississippian) in the vicinity of Big Stone Gap, Va., by J. B. Roen, R. L. Miller, and J. W. Huddle___________________________________________________________________________________ 43 The Wildcat Valley Standstone (Devonian) of southwest Virginia, by R. L. Miller, L. D. Harris, and J. B. Roen- 79 The Goose Egg Formation in the Laramie Range and adjacent parts of southeastern Wyoming, by E. K. Maughan— 53 Foraminifera from the Exogyra ponderosa zone of the Marshalltown Formation at Auburn, N.J., by J. F. Mello, J. P. Minard, and J. P. Owens_____________________________________________________________________________________ 61 Mineralogy and petrology Rare-earth silicatian apatite from the Adirondack Mountains, N.Y., by M. L. Lindberg and Blanche Ingram__________ 64 Ferroan northupite in the Green River Formation of Wyoming, by Charles Milton and Robert Meyrowitz--------------- 66 Walsen composite dike near Walsenburg, Colo., by R. B. Johnson--------------------------------------------------- 69 Zonal features of an ash-flow sheet in the Piapi Canyon Formation, southern Nevada, by P. W. Lipman and R. L. Christiansen_____________________________________________________________________________________________ 74 A welded-tuff dike in southern Nevada, by P. W. Lipman________________________________________________________ 79 A new uranyl tricarbonate, K2Ca3(U02)2(C03)o-9-10H20, by Robert Meyrowitz, D. R. Ross, and Malcolm Ross_______ 82 Geochemistry Fraction of uranium isotopes and daughter products in weathered granite and uranium-bearing sandstone, Wind River basin region, Wyoming, by J. N. Rosholt, E. L. Garner, and W. R. Shields______________________________ 84 Hafnium content and Hf/Zr ratio in zircon from the southern California batholith, by David Gottfried and C. L. Waring________________________________________________________________________________________________ 88 Geochemical anomalies in the lower plate of the Roberts thrust near Cortez, Nev., by R. L. Erickson, Harold Masursky, A. P. Marranzino, Uteana Oda, and W. W. Janes___________________________________________________ 92 Cesium and strontium sorption studies on glauconite, by M. M. Schnepfe, Irving May, and C. R. Naeser__________ 95 Distribution of beryllium in igneous rocks, by D. R. Shawe and Stanley Bernold________________________________ 100 Geophysics T-phase of May 11, 1962, recorded in Hawaii, by H. L. Krivoy and R. A. Eppley_________________________________ 105 Effects of the gnome nuclear explosion upon rock salt as measured by acoustical methods, by D. D. Dickey________ 108 Economic geology Habit of the Rocky Valley thrust fault in the West New Market area, Mascot-Jefferson City zinc district, Tennessee, by J. G. Bumgarner, P. K. Houston, J. E. Ricketts, and Helmuth Wedow, Jr____________________________________ 112 Relation of economic deposits of attapulgite and fuller’s earth to geologic structure in southwestern Georgia, by C. W. Sever_________________________________________________________________________________________________ 116 Geomorphology and glacial geology Profiles of rivers of uniform discharge, by W. B. Langbein____________________________________________________ 119 Large retrogressive landslides in north-central Puerto Rico, by W. H. Monroe__________________________________ 123 The zanjon, a solution feature of karst topography in Puerto Rico, by W. H. Monroe____________________________ 126 A271A272 CONTENTS OF GEOLOGICAL SURVEY RESEARCH 1964, CHAPTERS B, C, AND D Geomorphology and glacial geology—Continued Page The Charleston, Mo., alluvial fan, by L. L. Ray_________________________________________________________________ B130 Pleistocene glaciations of the southwestern Olympic Peninsula, Wash., by D. R. Crandell_________________________ 135 Sedimentation Preliminary report on bed forms and flow phenomena in the Rio Grande near El Paso, Tex., by R. K. Fahnestock and Thomas Maddock, Jr________________________________________________________________________________________ 140 Rapid method of estimating lithology of glacial drift of the Adirondack Mountains, New York, by O. S. Denny and A. W. Postel____________________________________________________________________________________________________ 143 Analytical techniques Determination of hafnium content and Hf/Zr ratios in zircon with the direct-reading emission spectrometer, by C. L. Waring---------------------------------------------------------------------------------------------------- 146 A spectrographic method for the determination of cesium, rubidium, and lithium in tektites, by Charles Annell___ 148 Staining of plagioclase feldspar and other minerals with F.D. and C. Red No. 2, by R. V. Laniz, R. E. Stevens, and M. B. Norman____________________________________________________________________________________________________ 152 Successful separation of silt-size minerals in heavy liquids, by Robert Schoen and D. E. Lee____________________ 154 Surface water Effect of seiches and setup on the elevation of Elephant Butte Reservoir, N. Mex., by G. L. Haynes, Jr__________ 158 Flood inundation mapping, San Diego County, Calif., by L. E. Young and H. A. Ray________________________________ 163 The relation of discharge to drainage area in the Rappahannock River basin, Virginia, by H. C. Riggs____________ 165 Ground water The artesian aquifer of the Tierra del Fuego area, Chile, by W. W. Doyel and Octavio Castillo U_________________ 169 Quality of water A method for evaluating oil-field-brine pollution of the Walnut River in Kansas, by R. B. Leonard_______________ 173 Theoretical hydrology Computing stream-induced ground-water fluctuation, by M. S. Bedinger and J. E. Reed_____________________________ 177 Use of water-level recession curves to determine the hydraulic properties of glacial outwash in Portage County, Wis., by E. P. Weeks__________________________________________________________________________________________ 181 Tree growth proves nonsensitive indicator of precipitation in central New York, by W. J. Schneider and W. J. Conover______________________________________________________________________________________________________ 185 PROFESSIONAL PAPER 501-C Structural geology page Late Mesozoic orogenies in the ultramafic belts of northwestern California and southwestern Oregon, by W. P. Irwin____________________________________________________________________________________________________________ Cl Westward tectonic overriding during Mesozoic time in north-central Nevada, by R. E. Wallace and N. J. Silbeling— 10 Strike-slip faulting and broken basin-ranges in east-central Idaho and adjacent Montana, by E. T. Ruppel-------- 14 Evidence for a concealed tear fault with large displacement in the central East Tintic Mountains, Utah, by H. T. Morris and W. M. Shepard_____________________________________________________________________________________ 19 Shape and structure of a gabbro body near Lebanon, Conn., by M. F. Kane and G. L. Snyder------------------------ 22 Outline of the stratigraphic and tectonic features of northeastern Maine, by Louis Pavlides, Ely Mencher, R. S. Naylor, and A. J. Boueot------------------------------------------------------------------------------------- 28 Stratigraphy and paleontology Stratigraphic importance of corals in the Redwall Limestone, northern Arizona, by W. J. Sando------------------- 39 Younger Precambrian formations and the Bolsa(?) Quartzite of Cambrian age, Papago Indian Reservation, Ariz., by L A. Heindl and N. E. McClymonds__________________________________________________________________________ 43 Occurrence and paleogeographic significance of the Maywood Formation of Late Devonian age in the Gallatin Range, southwestern Montana, by C. A. Sandberg and W. J. McMannis_____________________________________________ 50 Petrography of the basement gneiss beneath the Coastal Plain sequence, Island Beach State Park, N.J., by D. L. Southwick________________________________________________________________________________________________________ 55 Offshore extension of the upper Eocene to Recent stratigraphic sequence in southeastern Georgia, by M. J. McCollum and S. M. Herrick_______________________________________________________________________________________ 61 Upper Eocene smaller Foraminifera from Shell Bluff and Griffin Landings, Burke County, Ga., by S. M. Herrick— 64 Mineralogy and petrology Post-Paleocene West Elk laccolithic cluster, west-central Colorado, by L. H. Godwin and D. L. Gaskill----------- 66 Chemistry of greenstone of the Catoctin Formation in the Blue Ridge of central Virginia, by J. C. Reed, Jr------ 69 Occurrence and origin of laumontite in Cretaceous sedimentary rocks in western Alaska, by J. M. Hoare, W. H. Condon, and W. W. Patton, Jr_________________________________________________________________________________ 74 Clay minerals from an area of land subsidence in the Houston-Galveston Bay area, Texas, by J. B. Corliss and R. H. Meade______________________________________________________________________________________________________ 79 Attapulgite from Carlsbad Caverns, N. Mex., by W. E. Davies_____________________________________________________ 82 Diagram for determining mineral composition in the system MnCOs-CaCOs-MgCOa, by W. C. Prinz--------------------- 84CONTENTS OF GEOLOGICAL SURVEY RESEARCH 1964, CHAPTERS B, C, AND D A273 Geochemistry Lithium associated with beryllium in rhyolitic tuff at Spor Mountain, western Juab County, Utah, by D. R. Page Shawe, Wayne Mountjoy, and Walter Duke------------------------------------------------------------------------ C86 A geochemical investigation of the High Rock quadrangle, North Carolina, by A. A. Stromquist, A. M. White, and J. B. McHugh______________________________________________________________________________________________ 88 Evaluation of weathering in the Chattanooga Shale by Fischer assay, by Andrew Brown and I. A. Breger------------ 92 Measurement of relative cationic diffusion and exchange rates of montmorillonite, by T. E. Brown---------------- 96 Geophysics Preliminary structural analysis of explosion-produced fractures, hardhat event, Area 15, Nevada Test Site, by F. N. Houser and W. L. Emerick________________________________________________________________________________ 100 Seismicity of the lower east rift zone of Kilauea Volcano, Hawaii, January 1962-March 1963, by R. Y. Koyanagi— 103 Economic geology Paleolatitudinal and paleogeographic distribution of phosphorite, by R. P. Sheldon------------------------------ 106 Reconnaissance of zeolite deposits in tuffaceous rocks of the western Mojave Desert and vicinity, California, by R. A. Sheppard and A. J. Gude, 3d_____________________________________________________________________________ 114 Ore controls at the Kathleen-Margaret (MacLaren River) copper deposit, Alaska, by E. M. MacKevett, Jr----------- 117 Geomorphology and Pleistocene geology Cavities, or “tafoni”, in rock faces of the Atacama Desert, Chile, by Kenneth Segerstrom and Hugo Henriquez----- 121 Negaunee moraine and the capture of the Yellow Dog River, Marquette County, Mich., by Kenneth Segerstrom-------- 126 Ancient lake in western Kentucky and southern Illinois, by W. I. Finch, W. W. Olive, and E. W. Wolfe------------ 130 Outline of Pleistocene geology of Martha’s Vineyard, Mass., by C. A. Kaye----------------------------------- 134 Illinoian and Early Wisconsin moraines of Martha’s Vineyard, Mass., by C. A. Kaye------------------------------- 140 Glacial geology of the Mountain Iron-Virginia-Eveleth area, Mesabi iron range, Minnesota, by R. D. Cotter, and J. E. Rogers__________________________________________________________________________________________________ 144 Glaciology Recent retreat of the Teton Glacier, Grand Teton National Park, Wyo., by J. C. Reed, Jr------------------------- 147 Analytical techniques A simple oxygen sheath for flame photometry, by Irving May, J. I. Dinnin, and Fred Rosenbaum-------------------- 152 Determination of iodine in vegetation, by Margaret Cuthbert and F. N. Ward---------------------------------------- 154 Judging the analytical ability of rock analysts by chi-squared, by F. J. Flanagan---------------------------- 157 Ultrasonic dispersion of samples of sedimentary deposits, by R. P. Moston and A. I. Johnson--------------------- 159 Ground water Tritium content as an indicator of age and movement of ground water in the Roswell basin, New Mexico, by H. O. Reeder____________________________________________________________________________________________________ 161 Relation of surface-water hydrology to the principal artesian aquifer in Florida and southeastern Georgia, by V. T. Stringfield_______________________________________________________________________________________________ 164 Quality of water Contamination of ground water by detergents in a suburban environment—South Farmingdale area, Long Island, N.Y, by N. M. Perlmutter, Maxim Lieber, and H. L. Frauenthal-------------------------------------------------- 170 Relation of chemical quality of water to recharge to the J ordan Sandstone in the Minneapolis-St. Paul area, Minnesota, by M. L. Maderak---------------------------------------------------------------------------------------- 176 Engineering hydrology Geohydrology of storage of radioactive waste in crystalline rocks at the AEC Savannah River Plant, S.C., by G. E. Siple_____________________________________________________________________________________________________ 180 Theoretical hydrology Stream discharge regressions using precipitation, by H. C. Riggs------------------------------------------------ 185 Relation of annual runoff to meteorological factors, by M. W. Busby--------------------------------------------- 188 Photogrammetry Photogrammetric countouring of areas covered by evergreen forests, by James Halliday---------------------------- 190 PROFESSIONAL PAPER 501-D Page Mineralogy and petrology Temperatures in the crust and melt of Alae lava lake, Hawaii, after the August 1963 eruption of Kilauea Volcano—a preliminary report, by D. L. Peck, J. G. Moore, and George Kojima_____________________________________________ D1 Variation in modes and norms of an “homogeneous” pluton of the Boulder batholith, Montana, by R. I. Tilling----- Mafic lavas of Dome Mountain, Timber Mountain caldera, southern Nevada, by S. J. Luft___________________________ Structural geology Preliminary report on the structure of the southeast Gros Ventre Mountains, Wyoming, by W. R. Keefer------------ Pre-Fall River folding in the southern part of the Black Hills, South Dakota, by G. B. Gott_____________________A274 CONTENTS OF GEOLOGICAL SURVEY RESEARCH 1964, CHAPTERS B, C, AND D Stratigraphy and paleontology Chinle Formation and Glen Canyon Sandstone in northeastern Utah and northwestern Colorado, by F. G. Poole and J. H. Stewart_________________________________________________________________;_________________________________ Significance of Triassic ostracodes from Alaska and Nevada, by I. G. Sohn_________________________________________ Middle Devonian plant fossils from northern Maine, by J. M. Schopf________________________________________________ Geochronology Radiometric ages of zircon and biotite in quartz diorite, Eights Coast, Antarctica, by A. A. Drake, Jr., T. W. Stern, and H. H. Thomas____________________________________________________________________________________________________ Geochemistry Qualitative X-ray emission analysis studies of enrichment of common elements in wallrock alteration in the Upper Mississippi Valley zinc-lead district, by J. W. Hosterman, A. V. Heyl, and J. L. Jolly__________________________ Suggested exploration target in west-central Maine, by F. C. Canney and E. V. Post________________________________ Geophysics Radioactivity- and density- measuring devices for oceanographic studies, by C. M. Bunker__________________________ Aeromagnetic interpretation of the Globe-Miami copper district, Gila and Pinal Counties, Arizona, by Anna Jesrpesen, Economic geology Epigenetic uranium deposits in sandstone, by W. I. Finch__________________________________________________________ The occurrence of phosphate rock in California, by H. D. Gower and B. M. Madsen___________________________________ The distribution and quality of oil shale in the Green River Formation of the Uinta Basin, Utah-Colorado, by W. B. Cashion.________________________________________________________________________________________________________ Btu values of Fruitland Formation coal deposits in Colorado and New Mexico, as determined from rotary-drill cuttings, by J. S. Hinds__________________________________________________________________________________________________ Marine geology Giant submarine landslides on the Hawaiian Ridge, by J. G. Moore__________________________________________________ Engineering geology A zone of montmorillonitic weathered clay in Pleistocene deposits at Seattle, Washington, by D. R. Mullineaux, T. C. Nichols, and R. A. Speirer_____________________?._______________________________________________________________ Quaternary geology and glaciology Three pre-Bull Lake tills in the Wind River Mountains, Wyoming—a reinterpretation, by G. M. Richmond______________ Post-hypsithermal glacier advances at Mount Rainier, Washington, by D. R. Crandell and R. D. Miller_______________ Sedimentation Occurrence of dissolved solids in surface waters in the United States, by W. B. Langbein and D. R. Dawdy__________ Statistical parameters of Cape Cod beach and eolian sands, by John Schlee, Elazar Uchupi, and J. V. A. Trumbull___ Analytical techniques An instrumental technique for the determination of submicrogram concentrations of mercury in soils, rocks, and gas, by W. W. Vaughn and J. H. McCarthy, Jr_____________________________________________________________________________ Determination of mercury in vegetation with dithizone —a single extraction procedure, by F. N. Ward and J. B. McHugh, Ion-exchange separation of tin from silicate rocks, by Claude Huffman and A. J. Bartel____________________________ Determination of carbonate, bicarbonate, and total C02 in carbonate brines, by S. L. Rettig and B. F. Jones_______ Cartography Mapmaking applications of orthophotography, by M. B. Scher________________________________________________________ Ground water Ground-water conduits in the Ashland Mica Schist, northern Georgia, by C. W. Sever________________________________ Temperature and chemical quality of water from a well drilled through permafrost near Bethel, Alaska, by A. J. Feulner and R. G. Schupp________________________________________________________________________________________________ Hydrogeologic reconnaissance of the Republic of Korea, by W. W. Doyel and R. J. Dingman___________________________ Source of heat in a deep artesian aquifer, Bahia Blanca, Argentina, by S. L. Schoff, J. H. Salso, and Jose Garcia_ The Carrizo Sand, a potential aquifer in south-central Arkansas, by R. L. Hosman__________________________________ Geohydrology of the Spiritwood aquifer, Stutsman and Barnes Counties, North Dakota, by T. E. Kelly________________ Variation of permeability in the Tensleep Sandstone in the Bighorn Basin, Wyoming, as interpreted from core analyses and geophysical logs, by J. D. Bredehoeft_______________________________________________________________________ Ground-water-surface-water relations Uniformity of discharge of Muddy River Springs, southeastern Nevada, and relation to interbasin movement of ground water, by T. E. Eakin and D. O. Moore___________________________________________________________________________ Geologic factors affecting discharge of the Sheyenne River in southeastern North Dakota, by Q. F. Paulson_________ Surface water Magnitude and frequency of storm runoff in southeastern Louisiana and southwestern Mississippi, by V. B. Sauer____ Correlation and analysis of water-temperature data for Oregon streams, by A. M. Moore_____________________________ Engineering hydrology Elimination of thermal stratification by an air-bubbling technique in Lake Wohlford, Calif., by G. E. Koberg______ PageCONTENTS OP GEOLOGICAL SURVEY RESEARCH 19 64, CHAPTERS B, C, AND D A275 Theoretical hydrology Field methods for determining vertical permeability and aquifer anisotropy, by E. P. Weeks________________________ Two-variable linear correlation analyses of water-level fluctuations in artesian wells in Florida, by H. G. Healy- Hydrologic instrumentation A periscope for the study of borehole walls, and its use in ground-water studies in Niagara County, N.Y., by F. W. Trainer and J. E. Eddy___________________________________________________________________________________________ Page *PUBLICATIONS IN FISCAL YEAR 1964 A complete list of abstracts, papers, reports, and maps (exclusive of topographic maps) by U.S. Geological Survey authors published or otherwise released to the public during fiscal year 1964 (July 1,1963-June 30,1964) is given below. Publications are listed alphabetically by senior author. Each citation is identified by a number: for example, 1-64, which indicates the first entry for that author for the calendar year 1964. The number is followed by the names of coauthors and the citation itself. References to this list are identified in the preceding text by author and serial number; for example, Schmidt (1-63). LIST OF PUBLICATIONS AARON, J. M. 1-64. (and FORD, A. B.) Isotope age determinations in the Thiel Mountains, Antarctica [abs.]: Geol. Soc. America Spec. Paper 76, p. 1, 1964. ADAMS, J. K. 1- 63. (and BOGGESS, D. H.) Water-table, surface-drainage, and engineering soils map of the St. Georges area, Delaware: U.S. Geol. Survey Hydrol. Inv. Atlas HA-60, 1963. 2- 63. (and BOGGESS, D. H.) Water-table, surface-drainage, and engineering soils map of the Dover area, Delaware: U.S. Geol. Survey open-file report, 1963. 3- 63. (and BOGGESS, D. H.) Water-table, surface-drainage, and engineering soils map of the Frankford area, Delaware: U.S. Geol. Survey open-file report, 1963. 4- 63. (and BOGGESS, D. H.) Water-table, surface-drainage, and engineering soils map of the Sharptown area, Delaware: U.S. Geol. Survey open-file report, 1963. 5- 63. (and BOGGESS, D. H.) Water-table, surface drainage, and engineering soils map of the Trap Pond area, Delaware: U.S. Geol. Survey open-file report, 1963. 1- 64. (and BOGGESS, D. H.) Water-table surface-drainage, and engineering soils map of the Wilmington area, Delaware: U.S. Geol. Survey Hydrol. Inv. Atlas HA-79, 1964. 2- 64. (and BOGGESS, D. H.) Water-table, surface-drainage, and engineering soils map of the Taylors Bridge area, Delaware: U.S. Geol. Survey Hydrol. Inv. Atlas HA-80, 1964. ADDICOTT, W. O. 1-63. (and VEDDER, J. G.) Paleotemperature inferences from late Miocene mollusks in the San Luis Obispo-Bakersfield area, California: U.S. Geol. Survey Prof. Paper 475-C, p. C63-C68, 1963. ADK1SON, W. L. 1-63. (and SHELDON, M. G.) Sample descriptions and correlations for wells on a cross section from Barber County, Kansas, to Caddo County, Oklahoma: Oklahoma Geol. Survey, Guidebook 13, 139 p., 1963. 1-64. (and JOHNSTON, J. E.) Geology of the Salyersville North quadrangle, Kentucky: U.S. Geol. Survey Geol. Quad. Map GQ-276, 1964. ADLER, Isidore 1-63. (and BARTON, P. B., Jr.) Application of the electron probe to the analysis of (Zn,Fe)S solid solutions [abs.]: Econ. Geology, v. 58, no. 7, p. 1191, 1963. 1-64. (and BARTON, P. B., Jr.) Application of the electron probe to the analysis of (Zn, Fe)S solid solutions [abs.]: Geol. Soc. America Spec. Paper 76, p. 3, 1964. ADOLPHSON, D. G. 1-64. (and ELLIS, M. J.) Basic hydrogeologic data, Skunk Creek-Lake Madison drainage basin. South Dakota: U.S. Geol. Survey open-file report, 1964. AGNEW, A. F. 1-63. Geology of the Platteville quadrangle, Wisconsin: U.S. Geol. Survey Prof. Paper 1123-E, p. 245-277, 1963. AKERS, J. P. 1-63. (COOLEY, M. E„ and DENNIS, P. E.) Synopsis of ground-water conditions of the San Francisco Plateau near Flagstaff, Coconino County, Arizona: U.S. Geol. Survey open-file report, 30 p., 1963. ALBEE, H. F. 1-64. Preliminary geologic map of the Garns Mountain NE quadrangle, Teton County, Idaho: U.S. Geol. Survey Mineral Inv. Field Studies Map MF-274, 1964. ALBERS, J. P. 1- 64. Geology of the French Gulch quadrangle, Shasta and Trinity Counties, Calif.: U.S. Geol. Survey Bull. 1141-J, p. J1-J70, 1964. 2- 64. Jurassic "oroclipal" folding and related strike-slip faulting in the Western United States Cordillera [abs.]: Geol. Soc. America Spec. Paper 76, p. 4, 1964. 3- 64. (KINKEL, A. R., Jr., DRAKE, A. A., and IRWIN, W. P.) Geology of the French Gulch quadrangle, California: U.S. Geol. Survey Geol. Quad. Map GQ-336, 1964. ALBIN, D. R. 1- 64. Geology and ground-water resources of Bradley, Calhoun, and Ouachita Counties, Ark.: U.S. Geol. Survey Water-Supply Paper 1779-G, p. G1-G32, 1964. 2- 64. Water-resources reconnaissance of the Ouachita Mountains, Ark.: U.S. Geol. Survey open-file report, 32 p., 1964. ALDRIDGE, B. N. 1-63. Floods of August 1963 in Prescott, Arizona: U.S. Geol. Survey open-file report, 15 p., 1963. ALEXANDER, G. N. li64. A graphical solution to the joint distribution of flood magnitudes and flood occurrence using a finite record [abs.]: Am. Geophys. Union Trans., v. 45, no. 2, p. 346, 1964. ALEXANDER, W. H., Jr. 1-63. (MYERS, B. N., and DALE, O. C.) A reconnaissance of the ground-water resources of the Guadalupe, San Antonio, and Nueces River basins, Texas: U.S. Geol. Survey open-file report, 182 p., 1963. ALLEN, H. E. 1-63. (and MAY, V. J.) Floods in Harvey quadrangle, Illinois: U.S. Geol. Survey open-file report, 10 p., 1963. A277A278 PUBLICATIONS IN FISCAL YEAR 1964 ALLEN, H. E.--Continued 2- 63. (and MAY, V. J.) Floods in Lombard quadrangle, Illinois: U.S. Geol. Survey open-file report, 11 p., 1963. 3- 63. (and WYERMAN, T. A.) Floods in Joliet quadrangle, Illinois: U.S. Geol. Survey open-file report, lip., 1963. 1- 64. (ELLIS, D. W., and LONG, D. E.) Floods in Palatine quadrangle, Illinois: U.S. Geol. Survey Hydrol. Inv. Atlas HA-87, 1964. 2- 64. (and MAY, V. J.) Floods in Naperville quadrangle, Illinois: U.S. Geol. Survey open-file report, 11 p., 1964. ALLEN, W. B. 1-63. (HAHN, G. W., and TUTTLE, C. R.) Geohydrological data for the Upper Pawcatuck River Basin: Rhode Island Water Resources Coordinating Board Geol. Bull. 13, 68 p., 1963. ALLINGHAM, J. W. 1-63. Geology of the Dodgeville and Mineral Point quadrangles, Wisconsin: U.S. Geol. Survey Bull. 1123-D, p. 169-244, 1963. ALTSCHULER, Z. S. 1-63. (DWORNIK, E. J., and KRAMER, Henry) Transformation of montmorillonite to kaolinite during weathering: Science, v. 141, no. 3576, p. 148-152, 1963. ANDERS, R. B. 1-63. (and NAFTEL, W. L.) Pumpage of ground water and changes in water levels in Galveston County, Texas, 1958-1962: Texas Water Comm. Bull. 6303, 32 p., 1963. ANDERSEN, B. G. 1-63. Preliminary report on glaciology and glacial geology of the Thiel Mountains, Antarctica: U.S. Geol. Survey Prof. Paper 475-B, p. B140-B143, 1963. ANDERSON, C. A. 1-63. Simplicity in structural geology, in C. C. Albritton, Jr., ed.. The fabric of geology: Addison-Wesley Pub. Co., Reading, Mass., p. 175-183, 1963. ANDERSON, L. A. 1-64. (HAWKINS, Daniel, and others) Aeromagnetic map of parts of Wilkin, Otter Tail, Grant, and Traverse Counties, Minn.: U.S. Geol. SurveyGeophys. Inv. MapGP-358, 1964. ANDERSON, P. W. 1- 63. Variations in the chemical character of the Susquehanna River at Harrisburg, Pennsylvania: U.S. Geol.Survey Water-Supply Paper 1779-B, p. B1-B17, 1963. 2- 63. (and MCCARTHY, L. T., Jr.) Chemical character of streams in the Delaware River basin: U.S. Geol. Survey open-file report, 11 p., 1963. ANDREASEN, G. E. 1- 63. (and BROOKHART, J. W.) Reverse water-level fluctuations, in Methods of collecting and interpreting ground-water data, compiled by Ray Bentall: U.S. Geol. Survey Water-Supply Paper 1544-H, p. H30-H35, 1963. 2- 63. (and PETRAFESO, F. A.) Aeromagnetic map of the east-central part of the Death Valley National Monument, Inyo County, Calif.: U.S. Geol. Survey Geophys. Inv. Map GP-428, 1963. 3- 63. (and PETRAFESO, F. A.) Aeromagnetic map of Georgetown and vicinity, east-central Texas: U.S. Geol. Survey Geophys. Inv. Map GP-416, 1963. 4- 63. (and PETRAFESO, F.A.) Aeromagnetic map of the Llano Uplift, Mason-Burnet area, central Texas: U.S. Geol. Survey Geophys. Inv. Map GP-417, 1963. 5- 63. (and PITKIN, J. A.) Aeromagnetic map of the Twin Buttes area, Pima and Santa Cruz Counties, Ariz.: U.S. Geol. Survey Geophys. Inv. Map GP-426, 1963. 6- 63. (and ZANDLE, G. L.) Aeromagnetic map oftheBer-nardston quadrangle, Franklin County, Massachusetts, and Windham County, Vermont: U.S. Geol. Survey Geophys. Inv. Map GP-430, 1963. 7- 63. (and ZANDLE, G. L.) Aeromagnetic map of the Col-rain quadrangle, Franklin County, Massachusetts, and Windham County, Vermont: U.S. Geol. Survey Geophys. Inv. Map GP-431, 1963. ANDREASEN, G. E.--Continued 8-63. (and ZANDLE, G. L.) Aeromagnetic map of the North-field quadrangle, Franklin County, Massachusetts, Windham County, Vermont, and Cheshire County, New Hampshire: U.S. Geol. Survey Geophys. Inv. MapGP-435, 1963. 1- 64. (and BROMERY, R. W.) Total intensity aeromagnetic profiles over northeastern Oklahoma: U.S. Geol. Survey open-file report, map, 1964. 2- 64. (PITKIN, J. A., and PETRAFESO, F. A.) Aeromagnetic map of eastern Los Angeles and vicinity, California: U.S. Geol. Survey Geophys. Inv. Map GP-465, 1964. 3- 64. (PITKIN, J. A., and PETRAFESO, F. A.) Aeromagnetic map of Oxnard and vicinity, Ventura County, Calif.: U.S. Geol. Survey Geophys. Inv. Map GP-463, 1964. 4- 64. (WAHRHAFTIG, Clyde, and ZIETZ, Isidore) Aeromagnetic reconnaissance of the east-central Tanana Lowland, Alaska: U.S. Geol. Survey Geophys. Inv. Map GP-447, 2 sheets, 1964. ANDREWS, D. A. 1-63. (SCHOECHLE, G. L., and BROWN, G. W.) The Geological Survey's training program for geologists from less developed countries: Jour. Geol. Education, v. 11, no. 4, p. 113-118, 1963. ANNELL, Charles 1-64. A spectrographic method for the determination of cesium, rubidium, and lithium in tektites, in Geol. Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B148-B151, 1964. ANTWEILER, J. C. 1-63. Chemical preparation of samples for lead isotope analysis: U.S. Geol. Survey Prof. Paper 475-C, p. C166-C170, 1963. APPLIN, E. R. 1-64. Some middle Eocene, lower Eocene, and Paleocene microfaunas from west Florida: Cushman Found. Foram. Research Contr., v. 15, pt. 2, p. 45-72, 1964. ARMSTRONG, C. A. 1-63. Ground-water resources near Max, McLean and Ward Counties, North Dakota: North Dakota State Water Conserv. Comm. Ground-Water Studies 45, 24 p., 1963. ARMSTRONG, F. C. 1-64. The Bannock thrust zone, southeastern Idaho: U.S. Geol. Survey open-file report, 95 p., 1964. ARNOW, Lois 1-63. (St. CLAIR, Fiona, and ARNOW, Ted) The mollusca of a logoonal area at Playa de Vega Baja, Puerto Rico: Caribbean Jour. Sci., v. 3, p. 163-172, 1963. ARNOW, Ted 1-63. Ground-water geology of Bexar County, Tex.: U.S. Geol. Survey Water-Supply Paper 1588, 36 p., 1963. 1-64. Statement to the local press with water-level-change maps 18-32 for 11 areas in Utah: U.S. Geol. Survey open-file report, 1 p., 1964. ARONOW, Saul 1-63. Late Pleistocene glacial drainage in the Devils Lake region, North Dakota: Geol. Soc. America Bull., v. 74, no. 7, p. 859-874, 1963. ASH,S. R. 1- 63. Ground-water conditions in northern Lea County, N. Mex.: U.S. Geol. Survey Hydrol. Inv. Atlas HA-62,1963. 2- 63. Bibliography and index of conodonts, 1959-1961: Brigham YoungUniv. Geology Studies, v. 10, p.3-50, 1963. AVERITT, Paul 1-63. Upper Tertiary surficial deposits near Cedar City, Iron County, Utah: Geol. Soc. America Bull., v. 75, no. 1, p. 37-44, 1963. 1-64. Recent trends in coal production in the U.S.S.R. and Communist China: Econ. Geology, v. 59, no. 2, p. 323-324, 1964. AVRETT, J. R. 1-63. (and CARROON, L. E.) Temperature of Alabama streams: U.S. Geol. Survey open-file report, 165 p., 1963.LIST OF PUBLICATIONS A279 AYER, G. R. 1-63. (and PAUSZEK, F. H.) Creeks, brooks and rivers in Rockland County, New York and their relation to planning for the future: New York State Dept. Commerce Bull. 6, 140 p., 1963. BACK, William 1-63. Preliminary results of a study of calcium carbonate saturation of ground water in central Flordia: Internat. Assoc. Sci. Hydrology Bull., v. 8, no. 3, p. 43-51, 1963. BADER, J. S. 1-64. A reconnaissance of saline ground water in California: U.S. Geol. Survey open-file report, 14 p., 1964. BAILEY, E. H. 1-63. (IRWIN, W. P., and JONES, D. L.) Franciscan and related rocks and their significance in the geology of western California: Geol. Soc. Sacramento Guidebook, Ann. Field Trip, Sacramento, Calif., p. 39-47, 1963. 1- 64. Mesozoic sphenochasmic rifting along the San Andreas fault north of the Transverse Ranges [abs.]: Geol. Soc. America Spec. Paper 76, p. 186-187, 1964. 2- 64. (and EVERHART, D. L.) Geology and quicksilver deposits of the New Almaden district, Santa Clara County, Calif.: U.S. Geol. Survey Prof. Paper 360, 206 p., 1964. BAILEY, R. A. 1-63. Paleovolcanism: Am. Geophys. Union Trans., v. 44, no. 2, p. 512-518, 1963. BAKER, A. A. 1- 64. Geology of the Aspen Grove quadrangle, Utah: U.S. Geol. Survey Geol. Quad. Map GQ-239, 1964. 2- 64. Geology of the Orem quadrangle, Utah: U.S. Geol. Survey Geol. Quad. Map GQ-241, 1964. BAKER, E. T., Jr. 1-63. (LONG, A. T„ REEVES, R. D„ and WOOD, L. A.) Reconnaissance investigation of the ground-water resources of the Red River, Sulphur River, and Cypress Creek Basins, Texas: Texas Water Comm. Bull. 6306, 1963. 1-64. Geology and ground-water resources of Hardin County, Texas: Texas Water Comm. Bull. 6406, 179 p., 1964. BAKER, J. A. 1-63. (LANG, S. M., and THOMAS, M. P.) Geology and hydrology of the Hartford Research Center, Canel site, Middletown, Connecticut: U.S. Geol. Survey open-file report, 72 p., 1963. 1-64. Ground-water resources of the Lowell area, Massachusetts: U.S. Geol. Survey Water-Supply Paper 1669-Y, p. Y1-Y37, 1964. BAKER, J. H. 1-64. (BEETEM, W. A., and WAHLBERG, J.S.) Absorption equilibria between earth materials and radionuclides, Cape Thompson, Alaska: U.S. Geol. Survey open-file report, 41 p., 1964. BAKER, L. N. 1-63. Geology of the New Madrid S. E., and Hubbard Lake quadrangles in Kentucky: U.S. Geol. Survey Geol. Quad. Map GQ-292, 1963. BAKER, R. C. 1-64. (DALE, O. C., and BAUM, G. H.) Ground-water conditions in Menard County, Texas: U.S. Geol. Survey open-file report, 38 p., 1964. BALDWIN, H. L. 1-63. (and McGUINNESS, C. L.) "A primer on ground water,": U.S. Geol. Survey Misc. Rept., 26 p., 1963. BALLANCE, W. C. 1-63. Ground-water levels in New Mexico, 1962: New Mexico State Engineer Basic-Data Rept., 126 p., 1963. BALSLEY, J. R. 1-64. (and PETRAFESO, F. A.) Aeromagnetic mapof parts of Marquette, Dickinson, Baraga, Alger, and Schoolcraft Counties, Michigan: U.S. Geol. Survey open-file report, map, 1964. BALSLEY, J. R.--Continued 2-64. (and VARGO, J. L.) Aeromagnetic map of the Berg-land and part of the White Pine quadrangle, Ontonagon and Gogebic Counties, Michigan: U.S. Geol. Survey open-file report, map, 1964. BALTZ, E. H., Jr. 1-64. Analysis of Laramide geologic structure of the eastern side of the San Juan Basin and adjacent uplifts, New Mexico [abs.]: Geol. Soc. America Spec. Paper 76, p. 263-264, 1964. BARKER, F. B. 1-64. (and JOHNSON, J. O.) Determination of radium in water: U.S. Geol. Survey Water-Supply Paper 1696-B, p. B1-B29, 1964. BARKER, Fred 1- 64. Reaction between mafic magma and pelitic schist, Cortlandt, New York [abs.]: Geol. Soc. America Spec. Paper 76, p. 8, 1964. 2- 64. Reaction between mafic magma and pelitic schist, Cortlandt, New York: Am. Jour. Sci., v. 262, no. 5, p. 614-634, 1964. 3- 64. Sapphirine-bearing rock, Valle Codera, Italy: Am. Mineralogist, v. 49, no. 1-2, p. 146-152, 1964. BARNES, D. F. 1-64. (and MacCARTHY, G. R.) Preliminary report on tests of the application of geophysical methods to Arctic ground water problems: U.S. Geol. Survey open-file report, 37 p., 1964. BARNES, H. H., Jr. 1-63. Floods of March 1963, Alabama to West Virginia: U.S. Geol. Survey open-file report, 75 p., 1963. BARNES, Harley 1-63. (HOUSER, F. N., and POOLE, F. G.) Geologic map of the Oak Spring quadrangle, Nye County, Nev.: U.S. Geol. Survey Geol. Quad. Map GQ-214, 1963. BARNES, Ivan 1- 64. Field measurement of alkalinity and pH: U.S. Geol. Survey Water-Supply Paper 1535-H, p. H1-H17, 1964. 2- 64. (and BACK, William) Dolomite solubility in ground water: U.S. Geol. Survey Prof. Paper 475-D, p. D179-D180, 1964. 3- 64. (and CLARKE, F. E.) Geochemistry of groundwater in mine drainage problems: U.S. Geol. Survey Prof. Paper 473-A, p. A1-A6, 1964. 4- 64. (STUART, W. T., and FISHER, D. W.) Field investigation of mine waters in the northern anthracite field, Pennsylvania: U.S. Geol. Survey Prof. Paper 473-B, p. B1-B8, 1964. BARRON, E. G. 1-63. New instruments for surface-water investigations, in Selected techniques in water resources investigations, compiled by G. N. Mesnier and K. T. Iseri: U.S. Geol. Survey Water-Supply Paper 1669-Z, p. Z1-Z12, 1963. 1-64. Water-level sensing device: U.S. Geoi. Survey open-file report, 1 p., 1964. BARTEL, A. J. 1-63. (FENNELLY, E. J., HUFFMAN, Claude, Jr., and RADER, L. F., Jr.) Some new data on the arsenic content of basalt: U.S. Geol. Survey Prof. Paper 475-B, p. B20-B23, 1963. BARTON, P. B., Jr. 1- 63. (and TOULMIN, Priestley, 3d) Sphalerite phase equilibria in the system Fe-Zn-S between 580°C and 850°C [abs.]: Econ. Geology, v. 58, no. 7, p. 1191-1192, 1963. 2- 63. (BETHKE.P.M., and TOULMIN, Priestley, 3d) Equilibrium in ore deposits: Mineralog. Soc. America Spec. Paper 1, p. 171-185, 1963. 1- 64. (and TOULMIN, Priestley, 3d) Sphalerite phase equilibria in the system Fe-Zn-S between 580°C and 850°C [abs.]: Geol. Soc. America Spec. Paper 76, p. 8-9, 1964. 2- 64. (and TOULMIN, Priestley, 3d) The electrumtarnish method for the determination of the fugacity of sulfur in 746-002 0—64 19A280 PUBLICATIONS IN FISCAL YEAR 1964 BARTON, P. B., Jr.--Continued laboratory sulfide systems: Geochim. et Cosmochim. Acta, v. 28, no. 5, p. 619-640, 1964. BASS, N. W. 1-63. (and NORTHROP, S. A.) Geology of Glenwood Springs quadrangle and vicinity, northwestern Colorado: U.S. Ge-ol. Survey Prof. Paper 1142-J, p. J1-J74, 1963. 1-64. Composition of crude oils in Northwestern Colorado and Northeastern Utah suggests local sources: Am. Assoc. Petroleum Geologists Bull., v. 47, p. 2039-2064, 1964. BATEMAN, P. C. 1-63. (CLARK, L. D„ HUBER, N. K., MOORE, J. G„ and RINEHART, C. D.) The Sierra Nevada batholith—A synthesis of recent work across the central part: U.S. Geol. Survey Prof. Paper 414-D, p. D1-D46, 1963. BECRAFT, G. E. 1-63. (PINCKNEY, D. M., and ROSENBLUM, Sam) Geology and mineral deposits of the Jefferson City quadrangle, Jefferson and Lewis and Clark Counties, Mont.: U.S. Geol. Survey Prof. Paper 428, 101 p., 1963 [1964], 1-64. Preliminary geologic map of the Wilmont Creek quadrangle, Ferry and Stevens Counties, Wash.: U.S. Geol. Survey Mineral Inv. Field Studies Map MF-283, 1964. BEDINGER, M. S. 1- 63. (EMMETT, L. F., and JEFFERY, H. G.) Ground-water potential of the alluvium of the Arkansas River between Little Rock and Fort Smith, Arkansas: U.S. Geol. Survey Water-Supply Paper 1669-L, p. L1-L29, 1963. 2- 63. (and EMMETT, L. F.) Mapping transmissibility of alluvium in the lower Arkansas River valley, Arkansas: U.S. Geol. Survey Prof. Paper 475-C, p. C188-C190, 1963. 1- 64. (and JEFFERY, H. G.) Ground water in the lower Arkansas River valley, Arkansas: U.S. Geol. Survey^ Water-Supply Paper 1669-V, p. V1-V17, 1964. 2- 64. (and REED, J. E.) Computing stream-induced ground-water fluctuation, in Geol. Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B177-B180, 1964. BELL, E. A. 1-63. (KELLOGG, R. W., and KULP, W. K.) Progress report on the ground-water resources of the Louisville area, Kentucky, 1949-55: U.S. Geol. Survey Water-Supply Paper 1579, 47 p., 1963. BELL, Henry, III 1-63. Geochemical and heavy-mineral reconnaissance of the Kannapolis quadrangle. North Carolina: U.S. Geol. Survey Mineral Inv. Field Studies Map MF-268, 1963. 1-64. Geochemical and heavy-mineral reconnaissance of the Harrisburg quadrangle, North Carolina: U.S. Geol. Survey Mineral Inv. Field Studies Map MF-272, 1964. BELL, K. G. 1-63. Uranium in carbonate rocks: U.S. Geol.Survey Prof. Paper 474-A, p. A1-A29, 1963. BENSON, M. A. 1-63. Closure to discussion of "Plotting positions and economics of engineering planning": Am. Soc. Civil Engineers Proc., v. 89, Jour. Hydraulics Div., no. HY 6, pt. 1, p. 251-252, 1963. 1-64. Factors affecting the occurrence of floods in the Southwest: U.S. Geol. Survey Water-Supply Paper 1580-D, p. D1-D72, 1964. BENT ALL, Ray 1- 63. (compiler) Methods of collecting and interpreting ground-water data: U.S. Geol. Survey Water-Supply Paper 1544-H, p. H1-H97, 1963. 2- 63. (compiler) Methods of determining permeability, transmissibility, and drawdown: U.S. Geol. Survey Water-Supply Paper 1536-1, p. 243-341, 1963. 1-64. (compiler) Shortcuts and special problems in aquifer tests: U.S. Geol. Survey Water-Supply Paper 1545-C, p. C1-C117, 1964. BENTLEY, L. E. 1-64. (and SPEERT, J. L., and MOORE, R. H.) Discussion of paper "Control traverses and their adjustment," by Everett D. Morse: Am. Soc. Civil Engineers Proc., v. 90, Jour. Surveying and Mapping Div., no. SU1, p. 81-84, 1964. BERDAN, J. M. 1-64. The Helderberg Group and the position of the Silu-rian-Devonian boundary in North America: U.S. Geol. Survey Bull. 1180-B, p. B1-B19, 1964. BERG, H. C. 1-64. Reconnaissance geochemistry of stream sediments from three areas near Juneau, Alaska: U.S. Geol.Survey open-file report, 4 p., 1964. BERGENDAHL, M. H. 1-63. Geology of the northern part of the Tenmile Range, Summit County, Colo.: U.S. Geol. Survey Bull. 1162-D, p. D1-D19, 1963. BERGIN, M. J. 1-64. Bedrock geology of the Penn Yan and Keuka Park quadrangles, New York: U.S. Geol. Survey Bull. 1161-G, p. G1-G35, 1964. BERGMAN, D. L. 1-63. (and SULLIVAN, C. W.) Channel changes onSandstone Creek near Cheyenne, Okla.: U.S. Geol. Survey Prof. Paper 475-C, p. C145-C148, 1963. BERKSTRESSER, C. F., Jr. 1-64. Ground-water resources of Waupaca County, Wis.: U.S. Geol. Survey Water-Supply Paper 1669-U, p. U1-U38, 1964. BERNOLD, Stanley 1-64. (and SHAWE, D. R.) Beryllium in volcanic rocks [abs.]: Geol. Soc. AmericaSpec. Paper 76, p. 13-14, 1964. BERRYHILL, H. L., JR. 1-63. Geology and coal resources of Belmont County, Ohio: U.S. Geol. Survey Prof. Paper 380, 113 p., 1963. 1- 64. Geology of the Amity quadrangle, Pennsylvania: U.S. Geol. Survey Geol. Quad. Map GQ-296, 1964. 2- 64. (and SWANSON, V. E.) Geology of the Washington west quadrangle, Pennsylvania: U.S. Geol. Survey Geol. Quad. Map GQ-283, 1964. BERTAIOLA, Mario 1-64. Ground water in the Azzahra-Annasira-Al Amiria area, Tripolitania: U.S. Geol. Survey open-file report, 36 p., 1964. BINGHAM, R. H. 1- 63. Summary of ground-water levels in Tennessee, 1952-61: Tennessee Acad. Sci., Jour., v. 38, no. 4, p. 126-132, 1963. 2- 63. (and MOORE, G. K.) Well water for home supplies in Montgomery County: Tennessee Div. Water Resources Hydrol. Atlas 2, [10 p.], 1963. BLACK, D. F. B. 1- 64. Cryptoexplosive structure near Versailles, Ky., in Geol. Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B9-B12, 1964. 2- 64. (and CRESSMAN, E. R.) Gamma-ray logs from central Bluegrass region, Kentucky: U.S. Geol. Survey open-file report, 1 pi., 1964. BLACK, R. F. 1-64. Gubik Formation of Quaternary age in northern Alaska: U.S. Geol. Survey Prof. Paper 302-C, p.59-91, 1964. BLADE, L. V. 1-63. Geology of the Hazel quadrangle in Kentucky: U.S. Geol. Survey Geol. Quad. Map GQ-203, 1963. BODHAINE, G. L. 1- 64. (FOXWORTHY, B. L., SANTOS, J. F., and CUM-MANS, J. E.) The role of water in shaping the economy of the Pacific Northwest: U.S. Geol. Survey open-file report, 317 p., 1964. 2- 64. (and THOMAS, D. M.) Magnitude and frequency of floods in the United States, Part 12, Pacific Slope basinsLIST OF PUBLICATIONS A281 BODHAINE, G. L.—Continued in Washington and upper Columbia River basin: U.S. Geol. Survey Water-Supply Paper 1687, 337 p., 1964. BOGGESS, D. H. 1- 63. (and ADAMS, J. K.) Water-table, surface-drainage, and engineering soils map of the Newark area, Delaware: U.S. Geol. Survey Hydrol. Inv. Atlas HA-64, 1963. 2- 63. (and ADAMS, J. K.) Water-table, surface-drainage, and engineering soils map of the Bethany Beach area, Delaware: U.S. Geol. Survey open-file report, 1963. 3- 63. (and ADAMS, J. K.) Water-table, surface-drainage, and engineering soils map of the Kenton area, Delaware: U.S. Geol. Survey open-file report, 1963. 4- 63. (and ADAMS, J. K.) Water-table, surface-drainage, and engineering soils map of the Laurel area, Delaware: U.S. Geol. Survey open-file report, 1963. 5- 63. (and ADAMS, J. K.) Water-table, surface-drainage, and engineering soils map of the Little Creek area, Delaware: U.S. Geol. Survey open-file report, 1963. 6- 63. (and ADAMS, J. K.) Water-table, surface-drainage, and engineering soils map of the Millsboro area, Delaware: U.S. Geol. Survey open-file report, 1963. 7- 63. (DAVIS, C. F., and COSKERY, O. J.) Water-•table, surface-drainage, and engineering soils map of the Burrsville area, Delaware: U.S. Geol. Survey open-file report, 1963. 8- 63. (DAVIS, C. F„ and COSKERY, O. J.) Water-table, surface-drainage, and engineering soils map of the Milford area, Delaware: U.S. Geol. Survey open-file report, 1963. 9- 63. (DAVIS, C. F., and COSKERY, O. J.) Water-table, surface-drainage, and engineering soils map of the Wyoming area, Delaware: U.S. Geol. Survey open-file report, 1963. 1- 64. (and ADAMS, J. K.) Water-table, surface-drainage, and engineering soils map of the Middletown area, Delaware: U.S. Geol. Survey Hydrol. Inv. Atlas HA-82, 1964. 2- 64. (ADAMS, J. K., and DAVIS, C. F.) Water-table, surface-drainage, and engineering soils map of the Smyrna area, Delaware: U.S. Geol. Survey Hydrol. Inv. Atlas HA-81, 1964. BOGUE, R. G. 1-63. Manganese deposits at Sanjro near Bela, Kalat Division, West Pakistan: Pakistan Geol. Survey Mineral Inf. Circ. 9, 14 p., 1963. BONILLA, M. G. 1- 64. Bedrock-surface map of the San Francisco South quadrangle, California: U.S. Geol. Survey open-file report, map, 1964. 2- 64. (and BAILEY, E. H.) (Check list for geologic study of earthquake effects) AGI Data Sheet 44B: GeoTimes, v. 8, no. 5, pt. 1, p. 41-42, 1964. BOSWELL, E. H. 1- 63. Cretaceous aquifers of northeastern Mississippi: Mississippi Board Water Comm. Bull. 63-10, 202 p., 1963. 2- 63. (and others) Cretaceous aquifers in the Mississippi embayment, with discussions of quality of water, by H. C. Jeffery: U.S. Geol. Survey open-file report, 87 p., 1963. BOUCOT, A. J. 1-64. (FIELD, M. T., FLETCHER, Raymond, FORBES, W. H„ NAYLOR, R. S., and PAVLIDES, Louis) Reconnaissance bedrock geology of the Presque Isle quadrangle, Maine: Maine Geol. Survey Quad. Mapping Ser. no. 2, 123 p., 1964. BOWERS, W. E. 1-64. Outline of the geology of the U12i andU12i.01 tunnels and lithology of the U12i.01 drill hole, Nevada Test Site: U.S. Geol. Survey Rept. TEI-842 (open-file report), 23 p., 1964. BOWLES, C. G. 1-63. (and BRADDOCK, W. A.) Solution breccias of the Minnelusa Formation in the Black Hills, South Dakota and BOWLES, C. G.--Continued Wyoming: U.S. Geol. Survey Prof. Paper 475-C, p. C91-C95, 1963. BOYNTON, G. R. 1- 63. (MEUSCHKE, J. L„ and VARGO, J. L.) Aeromagnetic map of the Timber Mountain quadrangle and part of the Silent Canyon quadrangle, Nye County, Nev.: U.S. Geol. Survey Geophys. Inv. Map GP-443, 1963. 2- 63. (MEUSCHKE, J. L., and VARGO, J. L.) Aeromagnetic map of the Tippipah Spring quadrangle and parts of the Papoose Lake and Wheelbarrow Peak quadrangles, Nye County, Nev.: U.S. Geol. Survey Geophys. Inv. Map GP-441, 1963. 3- 63. (and VARGO, J. L.) Aeromagnetic map of the Cane Spring quadrangle and parts of the Frenchman Lake, Specter Range, and Mercury quadrangles, Nye County, Nev.: U.S. Geol. Survey Geophys. Inv. MapGP-442, 1963. 4- 63. (and VARGO, J. L.) Aeromagnetic map of the Topo-pah Spring quadrangle and part of the Bare Mountain quadrangle, Nye County, Nev.: U.S. Geol. Survey Geophys. Inv. Map GP-440, 1963. 1- 64. (and GILBERT, F. P.) Aeromagnetic map of the Cup-suptic quadrangle, Oxford and Franklin Counties, Maine: U.S. Geol. Survey open-file report, map, 1964. 2- 64. (and GILBERT, F. P.) Aeromagnetic map of the Oquossoc quadrangle, Oxford and Franklin Counties, Maine: U.S. Geol. Survey open-file report, map, 1964. 3- 64. (and GILBERT, F. P.) Aeromagnetic map of the Phil -lipps quadrangle, Franklin County, Maine: U.S. Geol. Survey open-file report, map, 1964. 4- 64. (and GILBERT, F. P.) Aeromagnetic map of the Rangeley quadrangle and part of the Kennebago Lake quadrangle, Franklin and Oxford Counties, Maine: U.S. Geol. Survey open-file report, map, 1964. BRADDOCK, W. A. 1- 63. Geology of the Jewel Cave SW quadrangle, Custer County, S. Dak.: U.S. Geol. Survey Bull. 1063-G, p. 217-268, 1963 [1964], 2- 63. (and BOWLES, C. G.) Calcitization of dolomite by calcium sulfate solutions in the Minnelusa Formation, Black Hills, South Dakota and Wyoming: U.S. Geol. Survey Prof. Paper 475-C, p. C96-C99, 1963. BRADLEY, Edward 1-63. (PETRI, L. R., and ADOLPHSON, D. G.) Geology and ground-water resources of Kidder County, North Dakota, Part III, Ground water and chemical quality of water: North Dakota Geol. Survey Bull. 36; and North Dakota State Water Conserv. Comm. County Ground Water Studies 1, 38 p., 1963. BRADLEY, W. H. 1- 63. Unmineralized fossil bacteria: Science, v. 141, no. 3584, p. 919-921, 1963. 2- 63. Continental Divide — Split: GeoTimes, v. 8, no. 3, p. 26, 1963. 3- 63. Geologic laws, in C. C. Albritton, Jr., ed., The fabric of geology: Addison-Wesley Pub. Co., Reading, Mass.,p. 12-23, 1963. 1-64. Aquatic fungi from the Green River Formation of Wyoming: Am. Jour. Sci., v. 262, no.3,p. 413-416, 1964. BRAMKAMP, R. A. 1- 63. (BROWN, G. F., HOLM, D. A., and LAYNE, N. M., Jr.) Geologic map of the Wadi As Sirhan quadrangle. Kingdom of Saudi Arabia: U.S. Geol. Survey Misc. Geol. Inv. Map I-200A, 1963. 2- 63. (GIERHART, R. D., OWENS, L. D., and RAMIREZ, L. F. Geologic map of the Western Rub A1 Khali quadrangle, Kingdom of Saudi Arabia: U.S. Geol. Survey Misc. Geol. Inv. Map I-218A, 1963 [1964]. 3- 63. (and RAMIREZ, L. F.) Geologic map of the Darb Zubaydah quadrangle, Kingdomof Saudi Arabia: U.S. Geol. Survey Misc. GeoK Inv. Map 1-202 A, 1963. 4- 63. (RAMIREZ, L. F., STEINEKE, Max, and REISS, W.H.) Geologic map of the Jawf-Sakakah quadrangle. KingdomA282 PUBLICATIONS IN FISCAL YEAR 1964 BRAMKAMP, R. A.--Continued of Saudi Arabia: U.S. Geol. Survey Misc. Geol. Inv. Map 1-201 A, 1963. BREDEHOEFT, J. D. 1- 63. Hydrogeology of the lower Humboldt River basin, Nevada: Nevada Dept. Conserv. and Nat. Resources, Water Resources Bull. 21, 50 p., 1963. 2- 63. (BLYTH, C. R., WHITE, W. A., and MAXEY, G. B.) Possible mechanisms for the concentration of brines in subsurface formations: Am. Assoc. Petroleum Geologists Bull., v. 47, no. 2, p. 257-269, 1963. BREGER, I. A. 1-63. (and BROWN, Andrew) Distribution and types of organic matter in a barred marine basin: New York Acad. Sci. Trans., Ser. 2, v. 25, p. 741-755, 1963. 1-64. (and DANIELS, Grafton) Criteria for evaluating the degree of weathering of coals [abs.] Geol. Soc. America Spec. Paper 76, p. 20, 1964. BREW, D. A. 1-63. (LONEY, R. A., POMEROY, J. S., and MUFFLER, L. J. P.) Structural influence on development of linear topographic features, southern Baranof Island, southeastern Alaska: U.S. Geol. Survey Prof. Paper 475-B, p. B110-B113, 1963. 1-64. Synorogenic sedimentation of Mississippian age. Eureka quadrangle, Nevada: U.S. Geol. Survey open-file report, 296 p., 1964. BRICE, H. D. 1-63. Tipping-bucket rain-gage attachment for a water-stage recorder, in Selected techniques in water resources investigations, compiled by G. N. Mesnier and K. T. Iseri: U.S. Geol. Survey Water-Supply Paper 1669-Z, p. Z53-Z57, 1963. BRICE, J. C. 1-64. Channel patterns and terraces of the Loup Rivers in Nebraska: U.S. Geol. Survey Prof. Paper 422-D, p. Dl-D41, 1964. BRIETKRIETZ, Alex 1-64. Basic water data report No. 1, Missoula Valley, Montana: Montana Bur. Mines and Geology Bull. 37, 43 p., 1964. BRIGGS, R. P. 1-64. Provisional geologic map of Puerto Rico and adjacent islands: U.S. Geol. Survey Misc. Geol. Inv. Map I-392, 1964. BROBST, D. A. 1-63. (and EPSTEIN, J. B.) Geology of the Fanny Peak quadrangle, Wyoming-South Dakota: U.S. Geol. Survey Bull. 1063-1, p. 323-377, 1963 [1964]. BROEKER, M. E. 1-63. (and WINSLOW, J. D.) Ground-water levels in observation wells in Kansas, 1962: Kansas Geol. Survey Bull 167, 89 p., 1963. BROMERY, R. W. 1- 64. (and GRISCOM, Andrew) Gravity studies of serpen-tinite anticlines near the AMSOC Test Hole, southwest Puerto Rico [abs.]: Geol. Soc. America Spec. Paper 76, p. 22-23, 1964. 2- 64. (and TYSON, N. S.) Aeromagnetic map of the Garlock area, Kern and Los Angeles Counties, California: U.S. Geol. Survey open-file report, map, 1964. BROMFIELD, C. S. 1-63. (and CONROY, A. R.) Preliminary geologic mapof the Mount Wilson quadrangle, San Miguel County [and Dolores County], Colo.: U.S. Geol. Survey Mineral Inv. FieldStud-ies Map MF-273, 1963 [1964], BROSGl5, W. P. 1-64. (and REISER, H. N.) Geologic map and section of the Chandalar quadrangle, Alaska: U.S. Geol. Survey Misc. Geol. Inv. Map 1-375, 1964. BROUGHTON, J. G. 1-64. (and STEWART, H. G.) Geology and hydrology of western New York Nuclear Service Center [abs.]: Geol. Soc. America Spec. Paper 76, p. 23, 1964. BROWN, Andrew 1-63. Geology and the Tullahoma campaign of 1863: Geo-Times, v. VIII, no. 1, p. 20-22, 53, 1963. BROWN, C. E. 1-63. (and THAYER, T. P.) Low-grade mineral facies in Upper Triassic and Lower Jurassic rocks of the Aldrich Mountains, Oregon: Jour. Sed. Petrology, v. 33, no. 2, p. 411-425, 1963. BROWN, G. F. 1- 63. (JACKSON, R. O., BOGUE, R. G., and ELBERG, E. L., Jr.) Geologic map of the northwestern Hijaz quadrangle, Kingdom of Saudi Arabia: U.S. Geol. Survey Misc. Geol. Inv. Map 1-204 A, 1963. 2- 63. (JACKSON, R. O., BOGUE, R. G., and MacLEAN, M. H.) Geologic map of the Southern Hijaz quadrangle. Kingdom of Saudi Arabia: U.S. Geol. Survey Misc. Geol. Inv. Map 1-210 A, 1963. 3- 63. (LAYNE, Newton, GOUDARZI, G. H., and MACLEAN, W. H.) Geologic map of the Northeastern Hijaz quadrangle, Kingdom of Saudi Arabia: U.S. Geol. Survey Misc. Geol. Inv. Map 1-205 A, 1963. BROWN, P. M. 1-63. The geology of northeastern North Carolina: Atlantic Coastal Plain Geol. Assoc., 4th Ann. FieldConf., Oct. 18-19, 1963, Guidebook, 44 p., 1963. BROWN, R. D., Jr. 1-64. Thrust-fault relations in the northern Coast Ranges, Calif.: U.S. Geol. Survey Prof. Paper 475-D, p. D7-D13, 1964. BROWN, R. H. 1-63. Drawdowns resulting from cyclic intervals of discharge, in Methods of determining permeability, trans-missibility, and drawdown, compiled by Ray Bentall: U.S. Geol. Survey Water-Supply Paper 1536-1, p. 324-330, 1963. 2-63. Ground water movement in a rectangular aquifer bounded by four canals, in Shortcuts and special problems in aquifer tests, compiled by Ray Bentall: U.S. Geol. Survey Water-Supply Paper 1545-C, p. C86-C100, 1963. 3-63. The cone of depression and the area of diversion around a discharging well in an infinite strip aquifer subject to uniform recharge, in Shortcuts and special problems in aquifer tests, compiled by Ray Bentall: U.S. Geol. Survey Water-Supply Paper 1545-C, p. C69-C85, 1963. 1-64. Hydrologic factors pertinent to ground-water contamination: Ground Water, v. 2, no. 1, p. 5-12, 1964. BROWN, S. G. 1-63. (SCHUMANN, H. H., KISTER, L. R., and JOHNSON, P. W.) Basic ground-water data of the Willcox Basin, Graham and Cochise Counties, Arizona: Arizona State Land Dept., Water Resources Rept. 14, 93 p., 1963. BROWNE, Ruth 1-63. (and HERRICK, S. M.) Smaller Paleocene Foramini-fera from Riedland, Kentucky: Bulls. Am. Paleontology, v. 46, no. 210, p. 247-284, 1963. BRYANT, Bruce 1-63. Geology of the Blowing Rock quadrangle. North Carolina: U.S. Geol. Survey Geol. Quad. Map GQ-243, 1963. BUCKNER, H. D. 1-64. (and THOMPSON, G. L.) Base flow study—Blanco River, Texas, February-March 1963: U.S. Geol. Survey open-file report, 22 p., 1964. BULL, W. B. 1- 64. Geomorphology of segmented alluvial fans in western Fresno County, Calif.: U.S. Geol. Survey Prof. Paper 352-E, p. 89-129, 1964. 2- 64. History and causes of channel trenching in western Fresno County, California: Am. Jour. Sci., v. 262, no. 2, p. 249-258, 1964. BUMGARNER, J. G. 1-64. (HOUSTON, P. K., RICKETTS, J. E., and WEDOW, Helmuth, Jr.) Habit of the Rocky Valley thrust fault in theLIST OF PUBLICATIONS A283 BUMGARNER, J. G.--Continued West New Market area, Mascot-Jefferson City zinc district, Tennessee, in Geol. Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B112-B115, 1964. BUNKER, Carl M. 1- 63. Preliminary radioisotope measurements, U12e.05 reentry tunnel, Nevada Test Site, Nye County, Nevada: U.S. Geol. Survey Tech. Letter, Area 12-13, 5 p., 1963. 2- 63. Gamma-ray spectral analyses of rock samples from the vicinity of the Marshmallow nuclear test: U.S. Geol. Survey Tech. Letter, Marshmallow-7, 7 p., 1963. 3- 63. (and BRADLEY, W. A.) Measurements of subsurface natural gamma-radioactivity. Project Dribble, Lamar County, Mississippi: U.S. Geol. Survey Tech. Letter, Dribble-37, 14 p., 1963. 4- 63. (and BUSH, C. A.) Gamma-ray spectral analyses of rock samples from 3B and 3E crosscuts, U16a reentry drift, Marshmallow site, Nevada Test Site: U.S. Geol. Survey Tech. Letter, Marshmallow-8, 6 p., 1963. 5- 63. (and BUSH, C. A.) Gamma-ray spectral analyses of rock samples from the 3A crosscut, Ul6a reentry tunnel. Marshmallow site, Nevada Test Site: U.S. Geol. Survey Tech. Letter, Marshmallow-9, 5 p., 1963. 6- 63. (and BUSH, C. A.) Gamma-ray spectral analyses of rock samples from 2A crosscut, U16a reentry drift, Marshmallow site, Nevada Test Site: U.S. Geol. Survey Tech. Letter, Marshmallow-10, 5 p., 1963. 7- 63. (and BUSH, C. A.) Gamma-ray spectral analyses of rock samples from the Number 3 drift, U16a reentry tunnel. Marshmallow site, Nevada Test Site: U.S. Geol. Survey Tech. Letter, Marshmallow-11, 6 p., 1963. BUSBY, M. W. 1-63. Yearly variations in runoff for the conterminous United States, 1931-60: U.S. Geol. Survey Water-Supply Paper 1669-S, p. S1-S49, 1963. BUTLER, R. G. 1-63. Semiannual report of water levels in selected observation wells in Utah--October 1963: U.S. Geol. Survey open-file report, 2 p., 1963. BYERS, F. M., Jr. 1- 64. (BARNES, Harley) Geologic map of the Paiute Ridge quadrangle, Nye and Lincoln Counties, Nevada: U.S. Geol. Survey Rept. TEI-826 (open-file report), map, 1964. 2- 64. (ORKILD, P. P., CARR, W. J., and CHRISTIANSEN, R. L.) Timber Mountain caldera, Nevada Test Site and vicinity--a preliminary report [abs.]: Geol. Soc. America Spec. Paper 76, p. 267, 1964. CADIGAN, R. A. 1-63. Tuffaceous sandstones in the Triassic Chinle Formation, Colorado Plateau: U.S. Geol. Survey Prof. Paper 475-B, p. B48-B51, 1963. CADY, W. M. 1-63. (ALBEE, A. L., and CHIDESTER, A. H.) Bedrock geology and asbestos deposits of the upper Missisquoi Valley and vicinity, Vermont: U.S. Geol. Survey Prof. Paper 1122-B, p. B1-B78, 1963. CALLAHAN, J. A. 1-64. (SKELTON, J., EVERETT, D. E., and HARVEY, E. J.) Available water for industry in Adams, Claiborne, Jefferson, and Warren Counties, Mississippi: Mississippi Indus, and Technol. Research Comm. Bull. 64-1, 45 p., 1964. CALLAHAN, J. T. 1- 63. (and BLANCHARD, H. E., Jr.) The quality of ground water, and its problems, in the crystalline rocks of Georgia: Georgia Mineral Newsletter, v. 16, nos. 3-4, p. 66-68, 1963. 2- 63. (WAIT, R. L., and McCOLLUM, M. J.) Television -A new tool for the ground-water geologist: Ground Water, v. 1, no. 4, p. 4-6, 1963. 1-64. The yield of sedimentary aquifers of the Coastal Plain, Southeast River basins: U.S. Geol. Survey Water-Supply Paper 1669-W, p. W1-W56, 1964. CALLAHAN, J.T.--Continued 2-64. (and WAIT, R. L.) Relations of fresh and salty ground water along the southeastern U. S. Atlantic Coast [abs.]: Geol. Soc. America Spec. Paper 76, p. 27, 1964. CALVERT, R. H. 1-64. Geology of the Philpot quadrangle, Kentucky: U.S. Geol. Survey Geol. Quad. Map GQ-297, 1964. CAMP, J. D. 1-63. Floods near Baton Rouge, Louisiana: U.S. Geol. Survey open-file report, 6 p., 1963. CAMPBELL, A. B. 1-64. (and RAUP, O. B.) Preliminary geologic map of the Hunters quadrangle, Stevens and Ferry Counties, Wash.: U.S. Geol. Survey Mineral Inv. FieldStudies MapMF-276, 1964. CANNEY, F. C. 1- 64. (and NOWLAN, G. A.) Determination of ammonium citrate-soluble cobalt in soils and sediments: U.S. Geol. Survey open-file report, 15 p., 1964. 2- 64. (and NOWLAN, G. A.) Solvent effect of hydroxylamine hydrochloride in the citrate-soluble heavy metals test: Econ. Geology, v, 59, no. 4, p. 721-722, 1964. 3- 64. (and POST, E. V.) Preliminary geochemical and geological map of part of Squaretown, Somerset County, Maine: U.S. Geol. Survey open-file report, map, 1964. CANNON, H. L. 1- 63. Biogeochemistry of vanadium: Soil Science, v. 98, no. 3, p. 196-204, 1963. 2- 63. Report on symposium on "Relation of geology and trace element distribution to nutritional problems": Science, v. 143, no. 3607, p. 704-706, 1963. CANNON, R. S. 1-63. (PIERCE, A. P„ Jr., and DELEVAUX, M. H.) Lead isotope variation with growth zoning in a galena crystal: Science, v. 142, no. 3592, p. 574-576, 1963. CARDWELL, G. T. 1-63. (ROLLO, J. R., and LONG, R. A.) Basic ground-water data for the Mississippi River Parishes South of Baton Rouge, Louisiana: Louisiana Dept. Public Works, 5 p., 1963. CARDWELL, W. D. E. 1-63. (and JENKINS, E. D.) Ground-water geology and pump irrigation in Frenchman Creek basin above Palisade, Nebr., with a section on The chemical quality of the water, by E. R. Jochens and R. A. Krieger: U.S. Geol. Survey Water-Supply Paper 1577, 472 p., 1963. CARLSTON, C. W. 1-63. Drainage density and streamflow: U.S. Geol. Survey Prof. Paper 422-C, p. C1-C8, 1963. 1- 64. Tritium-hydrologic research—Some results of the U.S. Geological Survey research program: Science, v. 143, no. 3608, p. 804-806, 1964. 2- 64. Free and incised meanders in the United States and their geomorphic and paleoclimatic implications [abs.]: Geol. Soc. America Spec. Paper 76, p. 28-29, 1964. CARPENTER, C. H. 1-64. (ROBINSON, G. E., Jr., and BJORKLUND, L. J.) Selected hydrologic data. Upper Sevier River drainage basin, parts of Garfield, Iron, Kane, Piute, and Sevier Counties, Utah: U.S. Geol. Survey open-file report, 1964. CARR, W. J. 1-64. Structure of part of the Timber Mountain dome and caldera, Nye County, Nev., in Geol. Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B16-B19, 1964. CARROLL, Dorothy 1-63. Petrography of some sandstones and shales of Paleozoic age from borings in Florida: U.S. Geol. Survey Prof. Paper 454-A, p. A1-A15, 1963.A284 PUBLICATIONS IN FISCAL YEAR 1964 CARROLL, Dorothy—Continued 2- 63. (and HATHAWAY, J. C.) Mineralogy of selected soils from Guam, with a section on Description of soil profiles, by C. H. Stensland: U.S. Geol. Survey Prof. Paper 403-F, p. F1-F53, 1963. 3- 63. Sediments from Bay St. George, Newfoundland: Sed-imentology, v. 2, no. 2, p. 149-155, 1963. 1-64. Chlorite in sediments off the Atlantic Coast of the United States [abs.]: Geol. Soc. America Spec. Paper 76, p. 239-240, 1964. CARSWELL, L. D. 1-63. (and BENNETT, G. D.) Geology and hydrology of the Neshannock quadrangle, Mercer and Lawrence Counties, Pennsylvania: Pennsylvania Geol. Survey, 4th ser., Bull. W 15, 90 p., 1963. CARTER, J. R. 1-63. (and GREEN, A. R.) Floods in Wyoming, magnitude and frequency: U.S. Geol. Survey Circ. 478, 27 p., 1963 [1964]. CARTER, R. W. 1- 63. (and ANDERSON, I. E.) Accuracy of current meter measurements: Am. Soc. Civil Engineers Proc., v. 89, Paper 3572, Jour. Hydraulics Div., no. HY 4, pt. 1, p., 105-115, 1963. 2- 63. (ANDERSON, W. L., BHERWOOD, W. L„ ROLFE, K. W., SHOWEN, C. R., and SMITH, Winchell) Automation of streamflow records: U.S. Geol. Survey Circ. 474, 18 p., 1963. CASE, J. E. 1- 64. Aeromagnetic survey of the Marquette iron range, Republic trough, and adjacent areas, Michigan [abs.], in A. T. Broderick, ed., Tenth Ann. Inst, on Lake Superior Geology, Ishpeming, Mich., p. 1-2, 1964. 2- 64. Upper Cretaceous stratigraphy, Berkeley and San Leandro Hills, California [abs.]: Geol.Soc. AmericaSpec. Paper 76, p. 194-195, 1964. CASEY, D. J. 1-63. Runoff compilation: Woods Hole Oceanog. Inst. Summ. Inv. Conducted 1962, Reference 63-18, Chemistry-Geology, p. 16, 1963. CASHION, W. B. 1-63. Geology of the Hazel Green quadrangle, Kentucky: U.S. Geol. Survey Geol. Quad. Map GQ-266, 1963. CATER, F. W. 1-64. Reinterpretation of the late growth of the Gypsum Valley salt anticline, San Miguel County, Colo.: U.S. Geol. Survey Prof. Paper 475-D, p. D33-D37, 1964. CATHCART, J. B. 1- 63. Economic geology of the Chicora quadrangle, Florida: U.S. Geol. Survey Bull. 1162-A, p. A1-A66, 1963. 2- 63. Economic geology of the Plant City quadrangle, Florida: U.S. Geol. Survey Bull. 1142-D, p. D1-D56, 1963. CATTERMOLE, J. M. 1-63. Geology of the Waterview quadrangle, Kentucky: U.S. Geol. Survey Geol. Quad. Map GQ-286, 1963 [1964]. CAUSEY, L. V. 1-63. Geology and ground-water resources of St. Clair County, Alabama: Alabama Geol. Survey Bull. 73, 84 p., 1963. CEDERSTROM, D. J. 1-64. (and BERTAIOLA, Mario) Ground-water resources of the Tripoli area, Libya: U.S. Geol. Survey open-file report, 361 p., 1964. CHAO, E. C. T. 1-63. The petrographic and chemical characteristics of tektites, jn John A. O'Keefe, ed., Tektites: Univ. Chicago Press, p. 51-94, 1963. CHAPMAN, R. M. 1-64. (DETTERMAN, R. L., and Mangus, M. D.) Geology of the Killik-Etivluk Rivers region, Alaska: U.S. Geol. Survey Prof. Paper 303-F, p. 325-407, 1964. CHIDESTER, A. H. 1-64. (ENGEL, A. E. J., and WRIGHT, L[auren] A.) Talc resources of the United States: U.S. Geol. Survey Bull. 1167, 61 p., 1964. CHRIST, C. L. 1-64. (and TRUESDELL, A. H.) Cation exchange in clays interpreted by regular solution theory [abs.]: Geol. Soc. America Spec. Paper 76, p. 32-33, 1964. CHRISTIANSEN, R. L. 1- 64. (and LIPMAN, P. W.) Geologic map of the Topopah Spring NW quadrangle, Nye County, Nevada: U.S. Geol. Survey Rept. TEI-847 (open-file report), map, 1964. 2- 64. (and LIPMAN, P. W.) Emplacement and thermal history of a rhyolite flow near Fortymile Canyon, southern Nevada [abs.]: Geol. Soc. America Spec. Paper 76, p. 268, 1964. CHURKIN, Michael, Jr. 1-64. Graptolite beds in thrust plates of central Idaho and their correlation with sequences in Nevada [abs.]: Geol. Soc. America Spec. Paper 76, p. 195-196, 1964. CLARK, J. R. 1- 63. Boron-oxygen polyanion in the crystal structure of tunellite: Science, v. 141, no. 3586, p. 1178-1179, 1963. 2- 63. (APPLEMAN, D. E., and CHRIST, C. L.) Crystal chemistry and structure refinement of five hydrated calcium borates: Jour. Inorganic and Nuclear Chemistry, v. 26, no. 1, p. 73-95, 1963. 1- 64. New boron-oxygen polyanion, (BgOg(OH>2)*^ [abs.]: Geol. Soc. America Spec. Paper 76, p. 33, 1964. 2- 64. (and ERD, R. C.) The probable chemical formula of aksaite, a new hydrated magnesium borate: Am. Mineralogist, v. 48, no. 7-8, p. 930-935, 1963. CLARK, L. D. 1-63. (STROMQUIST, A. A., and TATLOCK, D. B.) Geologic map of the San Andreas quadrangle, Calaveras County, Calif: U.S. Geol. Survey Geol. Quad. MapGQ-222, 1963. CLARK, W. E. 1-63. (and MUSGROVE, R. H., and MENKE, C. G., and CAGLE, J. W., Jr.) Hydrology of Brooklyn Lake near Keystone Heights, Florida: Florida: Geol. Survey Rept. Inv. 33, 43 p., 1963. 1- 64. Possibility of salt-water leakage from proposed intracoastal waterway near Venice, Florida well field: Florida Geol. Survey Rept. Inv. 38, 33 p., 1964. 2- 64. (MUSGROVE, R. H., MENKE, C. G., and CAGLE, J. W., Jr.) Water resources of Alachua, Bradford, Clay, and Union Counties, Florida: Florida Geol. Survey Rept. Inv. 35, 170 p., 1964. CLARKE, J. W. 1- 63. (VITALIANO, D. B., NEUSCHEL, V. S., and others) Geophysical Abstracts, July 1963: U.S. Geol. Survey Geo-phys. Abs. no. 198, p. 573-663, 1963. 2- 63. (VITALIANO, D. B., NEUSCHEL, V. S., and others) Geophysical Abstracts, August 1963: U.S. Geol. Survey Geophys. Abs., no. 199, p. 665-749, 1963. 3- 63. (VITALIANO, D. B., NEUSCHEL, V. S., and others) Geophysical Abstracts,September 1963: U.S.Geol.Survey Geophys. Abs., no. 200, p. 751-841, 1963. 4- 63. (VITALIANO, D. B., NEUSCHEL, V. S., and others) Geophysical Abstracts, October 1963: U.S. Geol. Survey Geophys. Abs., no. 201, p. 843-929, 1963. 5- 63. (VITALIANO, D. B., NEUSCHEL, V. S., and others) Geophysical Abstracts, November 1963: U.S. Geol. Survey Geophys. Abs., no. 202, p. 931-1017, 1963. 6- 63. (VITALIANO, D. B., NEUSCHEL, V. S., and others) Geophysical Abstracts, December, 1963: U.S. Geol. Survey Geophys. Abs. no. 203, p. 1019-1103, 1963. 1-64. (VITALIANO, D. B., and NEUSCHEL, V. S.,and others) Geophysical Abstracts, January 1964: U.S. Geol. Survey Geophys. Abs., no. 204, p. 1-87, 1964.LIST OF PUBLICATIONS A285 CLARKE, J. W.--Continued 2- 64. (VITALIANO, D. B., and NEUSCHEL, V. S.,andoth-ers) Geophysical Abstracts, February 1964: U.S. Geol. Survey Geophys Abs., no. 205, p. 89-169, 1964. 3- 64. (VITALIANO, D. B., NEUSCHEL, V. S., and others) Geophysical Abstracts, March 1964: U.S. Geol. Survey Geophys. Abs., no. 206, p. 171-253, 1964. 4- 64. (VITALIANO, D. B., NEUSCHEL, V. S., and others) Geophysical Abstracts, April 1964: U.S. Geol. Survey Geophys. Abs., no. 207, p. 255-343, 1964. 5- 64. (VITALIANO, D. B., NEUSCHEL, V. S., and others) Geophysical Abstracts, May 1964: U.S. Geol. Survey Geophys. Abs., no. 208, p. 345-427, 1964. 6- 64. (VITALIANO, D. B., NEUSCHEL, V. S., and others) Geophysical Abstracts, June 1964: U.S. Geol. SurveyGe-ophys. Abs., no. 209, p. 429-517, 1964. CLARKE, F. E. 1-63. Appraisal of corrosion characteristics of western desert well waters, Egypt: U.S. Geol. Survey open-file report, 65 p., 1963. CLINE, D. R. 1-63. Hydrology of upper Black Earth Creek basin, Wisconsin, with a section on Surface water, by M. W. Busby: U.S. Geol. Survey Water-Supply Paper 1669-C, p. Cl-C27, 1963. CLOSS, Darcy 1-64. (GORDON, MacKenzie, Jr., and YOCHELSON, E. L.) Permian aptychi from Utah [abs.]: Geol. Soc. America Spec. Paper 76, p. 35, 1964. COATS, R. R. 1-63. (GOSS, W. D., and RADER, L. F.) Distribution of fluorine in unaltered silicic volcanic rocks of the western conterminous United States: Econ. Geology, v. 58, p. 941-951, 1963. 1-64. Geology of the Jarbidge quadrangle, Nevada-Idaho: U.S. Geol. Survey Bull. 1141-M, p. M1-M24, 1964. COBB, E. D. 1-64. (and DALE, R. H.) Low flow investigation of the North Fork Feather River below Beldon Diversion dam: U.S. Geol. Survey open-file report, 19 p., 1964. COBB, E. H. (compiler) 1-64. Placer gold occurrences in Alaska: U.S. Geol. Survey Mineral Inv. Resource Map MR-38, 1964. COBBAN, W. A. 1-63. Occurrence of the Late Cretaceous ammonite Hop-litoplacenticeras in Wyoming: U.S. Geol. Survey Prof. Paper 475-C, p. C60-C62, 1963. 1-64. The Late Cretaceous cephalopod Haresiceras Rees-ide and its possible origin: U.S. Geol. Survey Prof. Paper 454-1, p. 11-119, 1964. COHEN, Philip 1- 63. An evaluation of the water resources of the Humboldt River Valley near Winnemucca, Nevada: Nevada Dept. Conserv. and Nat. Resources, Water Resources Bull. 24, 104 p., 1963. 2- 63. Specific-yield and particle-size relations of Quaternary alluvium, Humboldt River valley, Nev.: U.S. Geol. Survey Water-Supply Paper 1669-M, p. M1-M24, 1963. 3- 63. (and EVERETT, D. E.) A brief appraisal of the ground-water hydrology of the Dixie-Fairview Valley area, Nevada: Nevada Dept. Conserv. and Natural Resources Ground-water Resources—Reconn. Ser. Rept. 23, 40 p., 1963. 1- 64. (ROBINSON, T. W„ and WAANANEN, A. O.) Progress report of the activities of the U.S. Geological Survey in the Humboldt River Research Project in 1963, in Humboldt River Research Project 5th Prog. Rept.: Nevada State Dept. Conserv. and Nat. Resources, p. 13-18, 1964. 2- 64. Geochemical aspects of hydrologic systems analysis for two areas in Nevada [abs.]: Geol. Soc. America Spec. Paper 76, p. 35, 1964. COLBERT, J. L. 1-64. (and YOUNG, L. L.) Review of waterpower withdrawals in Weiser River basin, Idaho: U.S. Geol. Survey open-file report, 34 p., 1964. COLBY, B. R. 1- 63. Fluvial sediments--A summary of source, transportation, deposition, and measurement of sediment discharge: U.S. Geoi. Survey Bull. 1181-A, p. A1-A47, 1963. 2- 63. Working graph for computing unmeasured sediment discharge, in Selected techniques in water resources investigations, compiled by G. N. Mesnier and K. T. Iseri: U.S. Geol. Survey Water-Supply Paper 1669-Z, Z49-Z52, 1963. 3- 63. Nomograph for computing effective shear on stream-bed sediment: U.S. Geol. Survey Prof. Paper 475-C, p. C202-C205, 1963. 1- 64. Discussion of "Accuracy of current meter measurements" by Rolland Carter and Irving Anderson: Am. Soc. Civil Engineers Proc., v. 90, Jour. Hydraulics Div., no. HY 1, pt. 1, p. 349-352, 1964. 2- 64. Discussion of "Sediment-transport capability in erodible channels", by Shieh-Wen Mao and Leonard Rice: Am. Soc. Civil Engineers Proc., v. 90, Jour. Hydraulics Div., no. HY 1, pt. 1, p. 337-345, 1964. 3- 64. Practical computations of bed-material discharge: Am. Soc. Civil Engineers Proc. v. 90, Paper 3843, Jour. Hydraulics Div., no. HY 2, pt. 1, p. 217-246, 1964. 4- 64. Scour and fill in sand-bed streams: U.S. Geol. Survey Prof. Paper 462-D, p. D1-D32, 1964. COLE, W. S. 1-63. (and APPLIN, E. R.) Problems of the geographic and stratigraphic distribution of American middle Eocene larger Foraminifera: Bull. Am. Paleontology, v. 47, no. 212, p. 1-48, 1963. COLEMAN, R. G. 1-63. (and LEE, D. E.) Glaucophane-bearing metamorphic rock types of the Cazadero area, California: Jour. Petrology, v. 4, no. 3, p. 260-301, 1963. COLLIER, C. R. 1- 64. (and FLINT, R. F.) Fluvial sedimentation in Mammoth Cave, Ky.: U.S. Geol. Survey Prof. Paper 475-D, p. D141-D143, 1964. 2- 64. (and others) Influences of strip mining on the hydro-logic environment of parts of Beaver Creek basin, Kentucky, 1955-59: U.S. Geol. Survey Prof. Paper 427-B, p. B1-B85, 1964. COLTON, G. W. 1- 63. Devonian and Mississippian correlations in part of north-central Pennsylvania--a report of progress, in Symposium on Middle and Upper Devonian Stratigraphy in Pennsylvania and adjacent states: Pennsylvania Geol. Survey Bull. G-39, p. 115-125, 1963. 2- 63. Bedrock geology and surface structure of the Cedar Run quadrangle, Tioga and Lycoming Counties, Pennsylvania: Pennsylvania Geol. Survey Prog. Rept. no. 164, 1963. COLTON, R. B. 1- 63. Geologic map of the Brockton quadrangle, Roosevelt and Richland Counties, Mont.: U.S. Geol. Survey Misc. Geol. Inv. Map 1-362, 1963. 2- 63. Geologic map of the Chelsea quadrangle, Roosevelt and McCone Counties, Mont.: U.S. Geol. Survey Misc. Geol. Inv. Map 1-363, 1963. 3- 63. Geologic map of the Oswego quadrangle, Valley, Roosevelt, and McCone Counties, Mont.: U.S. Geol. Survey Misc. Geol. Inv. Map 1-366, 1963. 4- 63. Geologic map of the Poplar quadrangle, Roosevelt, Richland, and McCone Counties, Mont.: U.S. Geol. Survey Misc. Geol. Inv. Map 1-367, 1963. 5- 63. Geologic map of the Todd Lakes quadrangle. Valley and Roosevelt Counties, Mont.: U.S. Geol. Survey Misc. Geol. Inv. Map 1-370, 1963.A286 PUBLICATIONS IN FISCAL YEAR 1964 COLTON, R. B.—Continued 6- 63. (and CUSHMAN, R. V.) Contour map of the bedrock surface of the Manchester quadrangle, Connecticut: U.S. Geol. Survey Hydrol. Inv. Atlas 1-402, 1963. 7- 63. (LEMKE, R. W., and LINVALL, R. M.) Preliminary glacial map of North Dakota: U.S. Geol. Survey Misc. Geol. Inv. Map 1-331, 1963. 1- 64. Aggregate and riprap resources map of the Wolf Point area, Montana: U.S. Geol. Survey Misc. Geol. Inv. Map 1-429, 1964. 2- 64. Geologic map of the south half of the Baylor, Larslan West Fork, Police Creek, Kahle, and Lundville quadran-les. Valley, Roosevelt, and Daniels Counties, Mont.: U.S. Geol. Survey Misc. Geol. Inv. Map 1-361, 1964. CONANT, L. C. 1-64. (and GOUDARZI, G. H.) Geologic map of Kingdom of Libya: U.S. Geol. Survey Misc. Geol. Inv. Map 1-350 A, 1964. CONNOR, J. J. 1- 64. (and MIESCH, A. T.) Analysis of geochemical prospecting data from the Rocky Range, Beaver County, Utah: U.S. Geol. Survey Prof. Paper 475-D, p. D79-D83, 1964. 2- 64. (and MIESCH, A. T.) Application of trend analysis to geochemical prospecting data from Beaver County, Utah: Computers in the Mineral Industries, Part 1: Stanford Univ. Pub., Geol. Sci., v. 9, no. 1, p. 110-125, 1964. CONOVER, C. S. 1- 63. U.S. Geological Survey water resources studies in Florida: Florida Water News, v. 5, no. 12, 4 p., 1963. 2- 63. (and REEDER, H. O.) Special drawdown scales for predicting water-level changes throughout heavily pumped areas, in Shortcuts and special problems in aquifer tests, compiled by Ray Bentall: U.S. Geol. Survey Water-Supply Paper 1545-C, p. C38-C44, 1963. 3- 63. (THEIS, C. V., and GRIGGS, R. L.) Geology and hydrology of Valle Grande and Valle Toledo, Sandoval County, N. Mex.: U.S. Geol. Survey Water-Supply Paper 1619-Y, p. Y1-Y37, 1963. COOK, K. L. 1-64. (HOSKINSON, A. J., and SHELTON, G. R.) Principal facts for a gravity survey made in northeastern Oklahoma and southeastern Kansas during 1948: U.S. Geol. Survey open-file report, 24 p., 1964. COOLEY, M. E. 1-63. (and DAVIDSON, E. S.) The Mogollon Highlands— Their influence on Mesozoic and Cenozoic erosion and sedimentation: Arizona Geol. Soc. Digest, v. 6, p. 7-35, 1963. 1-64. (and DAVIDSON, E. S.) Synoptic Cenozoic geologic history of the Colorado Plateaus and Basin and Range Provinces of Arizona [abs.]: Geol. Soc. America Spec. Paper 76, p. 269, 1964. COOPER, G. A. 1-64. (and GRANT, R. E.) Permian brachiopods of the Glass Mountains, west Texas [abs.]: Geol. Soc. America Spec. Paper 76, p. 36-37, 1964. COOPER, H. H., Jr. 1- 63. The zone of diffusion and its consequences: Am. Assoc. Adv. Sci., Symposium on Water Improvement, p. 38-49, 1963. 2- 63. Type curves for nonsteady radial flow in an infinite leaky artesian aquifer, in Shortcuts and special problems in aquifer tests, compiled by Ray Bentall: U.S. Geol. Survey Water-Supply Paper 1545-C, p. C48-C55, 1963. 3- 63. (RORABAUGH, M. I.) Ground-water movements and bank storage due to flood stages in surface streams: U.S. Geol. Survey Water-Supply Paper 1536-J, p. 343-366, 1963. 4- 63. (and RORABAUGH, M. I.) Changes in ground-water movement and bank storage caused by flood waves in surface streams: U.S. Geol. Survey Prof. Paper 475-B, p. B192-B195, 1963. COOPER, H. H., Jr.—Continued 1-64. (KOHOUT, F. A., HENRY, H. R., andGLOVER, R. E.) Sea water in coastal aquifers: U.S. Geol. Survey Water-Supply Paper 1613-C, p. C1-C84, 1964. CORDOVA, R. M. 1-63. Reconnaissance of the ground-water resources of the Arkansas Valley region, Arkansas: U.S. Geol.Survey Water-Supply Paper 1669-BB, p. BB1-BB33, 1963. 1-64. Hydrologic reconnaissance of part of the headwaters area of the Price River, Utah: Utah Geol. and Mineralog. Survey Water Resources Bull. 4, 26 p., 1964. CORNWALL, H. R. 1-63. The Bullfrog Hills caldera and related ore deposits, Nye County, Nevada [abs.]: Mining Eng., v. 15, no. 8, p. 54, 1963. CORY, R. L. 1-64. Environmental factors affecting attached macroorganisms, Patuxent River estuary, Maryland: U.S. Geol. Survey Prof. Paper 475-D, p. D194-D197, 1964. COTTER, R. D. 1-63. (YOUNG, H. L., PETRI, L. R., and PRIOR, C. H.) Ground and surface water in the Mesabi and Vermilion Iron Range area, northeastern Minnesota: U.S. Geol. Survey open-file report, 63 p., 1963. COULTER, H. W. 1-64. (and CARROLL, G. V.) Selected geologic localities in the Washington area: Washington Acad. Sci. Jour., v. 54, no. 5, p. 153-159, 1964. COUNTS, H. B. 1-63. (and DONSKY, Ellis) Salt-water encroachment, geology, and ground-water resources of Savannah area, Georgia and South Carolina: U.S. Geol. Survey Water-Supply Paper 1611, 100 p., 1963 [1964]. COX, Allan 1- 63. (DOELL, R. R., and DALRYMPLE, G. B.) Radiometric dates of several recent reversals of the geomagnetic field [abs.]: Internat. Union Geodesy and Geophysics, General Assembly, 13th, Berkeley, Calif., Aug., Abstracts of Papers, v. 5, p. 42, 1963. 2- 63. (DOELL, R. R., and DALRYMPLE, G. B.) Geomagnetic polarity epochs: Sierra Nevada II: Science, v. 142, no. 3590, p. 382-385, 1963. 3- 63. (DOELL, R. R., and DALRYMPLE, G. B.) Geomagnetic polarity epochs: Science, v. 143, no. 3604, p. 351-352, 1963. 1- 64. Angular dispersion due to random vectors: Royal Astron. Soc. Geophys. Jour., v. 8, no.4,p. 343-355, 1964. 2- 64. (DOELL, R. R., and DALRYMPLE, G.B.) Reversals of the earth's magnetic field: Science, v. 144, no. 3626, p. 1537-1543, 1964. 3- 64. (DOELL, R. R., and DALRYMPLE, G. B.) Geomagnetic field behavior [abs.]: Am. Geophys. Union Trans., v. 45, no. 1, p. 105, 1964. CRAIG, F. C. 1-63. Variation in velocity distribution in a tide-affected stream, .in Selected techniques in water resources investigations, compiled by G. N. Mesnier and K. T. Iseri: U.S. Geol. Survey Water-Supply Paper 1669-Z, p. Z17-Z24, 1963. CRAIN, L. J. 1-63. Sources of large ground-water supplies in the vicinity of Jamestown, New York--A preliminary report: U.S. Geol. Survey open-file report, 15 p., 1963. CRANDELL, D. R. 1- 63. Surficial geology and geomorphology of the Lake Tapps quadrangle, Washington: U.S. Geol. Survey Prof. Paper 388-A, p. A1-A84, 1963. 2- 63. Paradise debris flow at Mount Rainier, Wash.: U.S. Geol. Survey Prof. Paper 475-B, p. B135-B139, 1963. 1-64. Pleistocene glaciations of the southwestern Olympic Peninsula, Wash., in Geol. Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B135-B139, 1964.LIST OF PUBLICATIONS A287 CRANDELL, H. C. 1-63. Geology and ground-water resources of the Town of Southold, Suffolk County, N. Y.: U.S. Geol. Survey Water-Supply Paper 1619-GG, p. GG1-GG36, 1963. CRESSLER, C. W. 1-63. Geology and ground-water resources of Catoosa County, Georgia: Georgia Geol. Survey Inf. Circ. 28, 19 p., 1963. 1- 64. Geology and ground-water resources of the Paleozoic rock area, Chattooga County, Georgia: Georgia Geol. Survey Inf. Circ. 27, 14 p., 1964. 2- 64. Geology and ground-water resources of Walker County, Georgia: Georgia Geol. Survey Inf. ,Circ. 29, 15 p., 1964. CRESSMAN, E. R. 1-64. Geology of the Georgetown Canyon-Snowdrift Mountain area, southeastern Idaho: U.S. Geol. Survey Bull. 1153, 105 p., 1964. CRIPPEN, J. R. 1-63. Natural water loss and recoverable water in mountain basins of southern California: U.S. Geol. Survey open-file report, 68 p., 1963; abs.. Am. Geophys. Union Trans., v. 44, no. 4, p. 871, 1963. CRITTENDEN, M. D., JR. 1- 63. New data on the isostatic deformation of Lake Bonneville: U.S. Geol. Survey Prof. Paper 454-E, p. E1-E31, 1963. 2- 63. Emendation of the Kelvin Formation and Morrison( ?) Formation near Salt Lake City, Utah: U.S. Geol. Survey Prof. Paper 475-B, p. B95-B98, 1963. 3- 63. Effective viscosity of the earth derived from isostatic loading of Pleistocene Lake Bonneville: Jour. Geophys. Research, v. 68, no. 19, p. 5517-5530, 1963. CROFT, M. G. 1-63. Geology and ground-water resources of Bartow County, Ga.: U.S. Geol. Survey Water-Supply Paper 1619-FF, p. FF1-FF32, 1963. 1-64. Geology and ground-water resources of Dade County, Georgia: Georgia Geol. Survey Inf. Circ. 26, 17 p., 1964. CRONIN, J. G. 1-63. (FOLLETT, C. R., SHAFER, G. H., and RETTMAN, P. L.) A reconnaissance of the ground-water resources of the Brazos River basin, Texas: Texas Water Comm. Bull. 6310, 152 p., 1963. 1-64. A summary of the occurrence and development of ground water in the Southern High Plains of Texas, with a section on Artificial recharge studies, by B.N. Myers: U.S. Geol. Survey Water-Supply Paper 1693, 88 p., 1964. CROSS, W. P. 1-63. Low-flow frequencies and storage requirements for selected Ohio streams: Ohio Dept. Nat. Resources, Div. Water Bull. 37, 66 p., 1963. 1-64. (and FEULNER, A. J.) Anomalous streamflow-ground-water regimen in the Mad River basin, near Springfield, Ohio: U.S. Geol. Survey Prof. Paper 475-D, p. D198-D201, 1964. CROSTHWAITE, E. G. 1-63. Ground-water appraisal of Antelope and Middle Reese River Valleys, Lander County, Nevada: Nevada Dept. Conserv. and Nat. Resources, Ground-Water Resources Reconn. Ser. Rept. 19, 33 p., 1963. CROWDER, D. F. 1-63. Geology of the Parrot quadrangle, Kentucky: U.S. Geol. Survey Geol. Quad. Map GQ-236, 1963. 1-64. (and TABOR, R. W.) The Suiattle Gateway—an excerpt from "Guide to the North Cascades, routes and rocks from Glacier Peak to Lake Chelan": The Mountaineer, v. 57, no. 4, p. 52-65, 1964. CULBERTSON, D. M. 1-63. Coordinated water-quality investigations in Kansas: Missouri Basin Inter-Agency Comm. Meeting, 130th, April 25, 1963, Minutes, App. D, p. 1-7, 1963. CULBERTSON, J. K. 1-64. (and DAWDY, D. R.) A study of fluvial characteristics and hydraulic variables, middle Rio Grande, New Mexico: U.S. Geol. Survey Water-Supply Paper 1498-F, p. F1-F74, 1964. CULBERTSON, W. C. 1- 64. Geology and coal resources of the coal-bearing rocks of Alabama: U.S. Geol. Survey Bull. 1182-B, p. B1-B79, 1964. 2- 64. Oil shale resources and stratigraphy of the Green River Formation in Wyoming [abs.]: Intermountain Assoc. Petroleum Geologists Newsletter, v. 5, no. 3, p. 2-3,1964. CUMMINGS, David 1-64. Eddies as indicators of local flow direction in rhyolite: U.S. Geol. Survey Prof. Paper 475-D, p. D70-D72, 1964. CUMMINGS, T. R. 1-63. Chemical character of surface waters of Oklahoma, 1957-1958: U.S. Geol. Survey open-file report, 164 p., 1963. 1-64. Chemical character of surface waters of Oklahoma, 1958-59: U.S. Geol. Survey open-file report, 117 p., 1964. CUPPELS, N. P. 1-63. Geology of the Clifton quadrangle, Wyoming and South Dakota: U.S. Geol. Survey Bull. 1063-H, p. 271-321, 1963. CURREY, D. R. 1-64. A preliminary study of valley asymmetry in the Ogotoruk Creek area, northwestern Alaska: Arctic, v. 17, no. 2, p. 85-98, 1964. CUSHING, E. M. 1-64. (BOSWELL, E. H., and HdSMAN, R. L.) General geology of the Mississippi embayment: U.S. Geol. Survey Prof. Paper 448-B, p. B1-B28, 1964. CUSHMAN, R. L. 1-63. (and HALPENNY, I. C.) Safford Valley, in Effects of drought in the Colorado River basin, by H. E. Thomas and others: U.S. Geol. Survey Prof. Paper 372-F, p. F29-F32, 1963. 1-64. An evaluation of the aquifer and well characteristics of the municipal well fields in the Los Alamos and Guaje Canyons near Los Alamos, New Mexico: U.S. Geol. Survey open-file report, 89 p., 1964. CUSHMAN, R. V. 1- 63. Geology of the Hartford North quadrangle, Connecticut: U.S. Geol. Survey Geol. Quad. Map GQ-223, 1963. 2- 63. (and COLTON, R. B.) Contour map of the bedrock surface of the Broad Brook quadrangle, Connecticut: U.S. Geol. Survey Misc. Geol. Inv. Map 1-401, 1963. 1- 64. Ground-water resources of north-central Connecticut: U.S. Geol. Survey Water-Supply Paper 1752, 96 p., 1964. 2- 64. (BAKER, J. A., and MEIKLE, R. L.) Records and logs of selected wells and test borings and chemical analyses of water in North-Central Connecticut: U.S. Geol. Survey open-file report, 7 p., 1964. 3- 64. (TANSKI, D., and THOMAS, M. P.) Water resources of the Hartford-New Britain area, Connecticut: U.S. Geol. Survey Water-Supply Paper 1499-H, p. H1-H96, map, 1964. da COSTA, J. A. 1-63. Review of Les Eaux Souterraines, by H. Schoeller: Am. Geophys. Union Trans., v. 44, no. 1, p. 151-152, 1963. DALQUEST, W. A. 1-63. (and MAMAY, S. H.) A remarkable concentration of Permian amphibian remains in Jones County, Texas: Jour. Geology, v. 71, no. 5, p. 641-643, 1963. DALRYMPLE, G. B. 1-63. Argon retention in a granitic xenolith from a Pleistocene basalt, Sierra Nevada, California: Nature, v. 201, no. 4916, p. 282, 1963.A288 PUBLICATIONS IN FISCAL YEAR 1964 DALRYMPLE, Tate 1-64. Discussion of "Shortcuts in hydrology", by Arthur I. McCutchan: Am. Soc. Civil Engineers Proc., v. 90, Jour. Hydraulics Div., no. HY 1, pt. 1, p. 300-302, 1964. DANILCHK, Walter 1-64. (and HALEY, B. R.) Geology of the Paleozoic area in the Malvern quadrangle, Garland and Hot Spring Counties, Arkansas: U.S. Geol. Survey Misc. Geol. Inv. Map 1-405, 1964. DAVIDIAN, Jacob 1- 63. (and CAHAL, D. I.) Direct measurement of shear in open-channel flow: U.S. Geol. Survey Prof. Paper 475-C, p. C228-C229, 1963. 2- 63. (and CAHAL, D. I.) Distribution of shear in rectangular channels: U.S. Geol. Survey Prof. Paper 475-C, p. C206-C208, 1963. DAVIDSON, E. S. 1-64. (and COOLEY, M. E.) Stratigraphy and structure of Tertiary and Quaternary rocks of southeastern Arizona [abs.j: Geol. Soc. America j3pec. Paper 76, p. 270, 1964. DAVIES, W. E. 1- 63. (KRINSLEY, D. B., and NICOL, A. H.) Geology of the North Star Bay area, northwest Greenland: Medd. om Gr^nland, v. 162, no. 12, 1963. 2- 63. Book review of "Katmai" by W. F. Erskine: Explorers Jour., v. 41, no. 2, p. 52-53, 1963. 1-64. Arctic biological work by theU.S. Geological Survey: Bioscience, v. 14, no. 5, p. 378-381, 1964. DAVIS, C. F. 1- 63. (BOGGESS, D. H., and COSKERY, O. J.) Water-table, surface-drainage, and engineering soils map of the Frederica area, Delaware: U.S. Geol. Survey open-file report, 1963. 2- 63. (and BOGGESS, D. H.) Water-table, surface-drainage, and engineering soils map of the Harrington area, Delaware: U.S. Geol. Survey open-file report, 1963. 3- 63. (and BOGGESS, D. H.) Water-table surface-drainage, and engineering soils map of the Marydel area, Delaware: U.S. Geol. Survey open-file report, 1963. 4- 63. (and BOGGESS, D. H.) Water-table, surface-drainage, and engineering soils map of the Mispillion River area, Delaware: U.S. Geol. Survey open-file report, 1963. DAVIS, D. A. 1- 63. Ground-water reconnaissance of American Samoa: U.S. Geol. Survey Water-Supply Paper 1608-C, p. Cl-C21, 1963. 2- 63. (and YAMANAGA, G.) Preliminary report on the water resources of Kohala Mountain and Mauna Kea, Hawaii: Hawaii Dept. Land and Nat. Resources, Div. Water and Land Devel. Circ. C14, 44 p., 1963. DAVIS, G. H. 1- 63. Southern San Joaquin Valley, in Effects of drought along Pacific Coast in California, by H. E. Thomas and others: U.S. Geol. Survey Prof. Paper 372-G, p. G20-G24, 1963. 2- 63. (SMALL, J. B., and COUNTS, H. B.) Land subsidence related to decline of artesian pressure in the Ocala limestone at Savannah, Georgia: Geol. Soc. America Eng. Geology Case Histories, no. 4, 8 p., 1963. 3- 63. Formation of ridges through differential subsidence of peatlands of the Sacramento-San Joaquin Delta, California: U.S. Geol. Survey Prof. Paper 475-C, p. C162-C165, 1963. 1-64. (LOFGREN, B. E., and MACK, Seymour) Use of ground-water reservoirs for storage of surface water in San Joaquin Valley, California: U.S. Geol. Survey Water-Supply Paper 1618, 125 p., 1964. DAVIS, L. C., Jr. 1-64. The Amazon's rate of flow—measurements shatter previous estimates: Nat. History, v. 73, no. 6, p. 15-19, 1964. DAVIS, M. E. 1-64. Development of ground water in the El Paso district, Texas, 1960-63, progress rept. no. 9: U.S. Geol. Survey open-file report, 69 p., 1964. DAVIS, R. E. 1-64. Geology of the 410 area, Nevada TestSite, Nye County, Nevada: U.S. Geol. Survey Rept. TEI-789 (open-file report), 24 p., 1964. DAVIS, W. E. 1-63. (KINOSHITA, W. T., and SMEDES, H. W.) Bouguer gravity, aeromagnetic, and generalized geologic map of East Helena and Canyon Ferry quadrangles and part of the Diamond City quadrangle, Lewis and Clark, Broadwater, and Jefferson Counties, Mont.: U.S. Geol. Survey Geophys. Inv. Map GP-444, 1963. DeBUCHANANNE, G. D. 1-63. Impact shock absorption characteristics of rocks and soil areas of parts of the Vandenberg Air Force Base, the Point Arguello Naval Missile facilities, and the Sudden Ranch, California: U.S. Geol. Survey open-file report, 13 p., 1963. de LAGUNA, Wallace 1-63. Geology of Brookhaven National Laboratory and vicinity, Suffolk County, N. Y.: U.S. Geol. Survey Bull. 1156-A, p. A1-A35, 1963. DELEVAUX, M. H. 1-63. Lead reference sample for isotopic abundance ratios: U.S. Geol. Survey Prof. Paper 475-B, p. B160-B161, 1963. DEMPSEY, W. J. 1- 63. (FACKLER, W. D., and others) Aeromagnetic map of the Bagdad area, Yavapai County, Ariz.: U.S. Geol. Survey Geophys. Inv. Map GP-411, 1963. 2- 63. (FACKLER, W. D., and others) Aeromagnetic map of the Cochise quadrangle, Cochise County, Ariz.: U.S. Geol. Survey Geophys. Inv. Map GP-413, 1963. 3- 63. (and GILBERT, F. P.) Aeromagnetic map of Melbourne and vicinity, Brevard County, Fla.: U.S. Geol. Survey Geophys. Inv. Map GP-425, 1963. 4- 63. (HILL, M. E., and others) Aeromagnetic map of central Yavapai County, Ariz., including the Jerome mining district: U.S. Geol. Survey Geophys. Inv. Map GP-402, 1963. 5- 63. (and HILL, M. E.) Aeromagnetic map of parts of the Phoenix, Mesa, Camelback andNew River SE quadrangles, Maricopa County, Ariz.: U.S. Geol. Survey Geophys. Inv. Map GP-420, 1963. 6- 63. (and HILL, M. E.) Aeromagnetic map of parts of the Wilcox and Luzena quadrangles, Cochise County, Ariz.: U.S. Geol. Survey Geophys. Inv. Map GP-418, 1963. 7- 63. (and HILL, M. E.) Aeromagnetic map of the Mammoth quadrangle, Pinal and Pima Counties, Ariz.: U.S. Geol. Survey Geophys. Inv. Map GP-419, 1963. DENNY, C. S. 1-63. (and LYFORD, W. H.) Surficial geology and soils of the Elmira-Williamsport region. New York and Pennsylvania, with a section on Forest regions and great soil groups by J. C. Goodlett and W. H. Lyford: U.S. Geol. Survey Prof. Paper 379, 60 p., 1963. 1-64. (and POSTEL, A. W.) Rapid method of estimating lithology of glacial drift of the Adirondack Mountains, New York, in Geol. Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B143-B145, 1964. DETTERMAN, R. L. 1- 63. (BICKEL, R. S., and GRYC, George) Geology of the Chandler River region, Alaska: U.S. Geol. Survey Prof. Paper 303-E, p. E223-E324, 1963. 2- 63. Revised stratigraphic nomenclature and age of the Tuxedni Group in the Cook Inlet region, Alaska: U.S. Geol. Survey Prof. Paper 475-C, p. C30-C34, 1963. 1-64. (and REED, B. L.) Preliminary map of the geology of the Iliamna quadrangle, Alaska: U.S. Geol. Survey Misc. Geol. Inv. Map 1-407, 1964.LIST OF PUBLICATIONS A289 DEUTSCH, Morris 1-63. Ground-water contamination and legal controls in Michigan: U.S. Geol. Survey Water-Supply Paper 1691, 79 p., 1963 [1964]. 1-64. Natural controls involved in shallow-aquifer contamination [abs.]: Geol. Soc. America Spec. Paper 76, p. 43, 1964. deWITT, Wallace, Jr. 1-64. Memorial to James Franklin Pepper, 1898-1963: Geol. Soc. America Bull., v. 75, no. 4, p. 61-66, 1964. DICKEY, D. D. 1- 64. Effects of the GNOME nuclear explosion upon rock salt as measured by acoustical methods, in Geol. Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B108-B111, 1964. 2- 64. (and MONK, E. F.) Determining density and porosity of tuff containing zeolites: U.S. Geol. Survey Prof. Paper 475-B, p. B169-B170, 1964. DIMENT, W. H. 1-63. (and ROBERTSON, E. C.) Temperature, thermal conductivity, and heat flow in a drill hole near Oak Ridge, Tennessee: Jour. Geophys. Research, v. 68, no. 17, p. 5035-5048, 1963. 1- 64. Gravity and magnetic anomalies in northeastern New York [abs.j: Geol. Soc. America Spec. Paper 76, p.45, 1964. 2- 64. (and WEAVER, J. D.) Heat flow near Mayaguez, Puerto Rico: Am. Geophys. Union Trans., v. 45, no. 1, p. 123, 1964. 3- 64. (and WERRE, R. W.) Terrestrial heat flow near Washington, D. C.: Jour. Geophys. Research, v. 69, no. 10, p. 2143-2150, 1964. DINGMAN, R. J. 1-63. (and LOHMAN, K. E.) Late Pleistocene diatoms from the Arica area, Chile: U.S. Geol. Survey Prof. Paper 475-C, p. C69-C72, 1963. DINWIDDIE, G. A. 1-63. Municipal water supplies and uses, southeastern New Mexico: New Mexico State Engineer Tech. Rept. 29A, 140 p., 1963. 1- 64. Availability of ground water for irrigation on the Pojoaque Pueblo Grant, Santa Fe County, New Mexico: U.S. Geol. Survey open-file report, 14 p., 1964. 2- 64. Municipal water supplies and uses in northeastern New Mexico: U.S. Geol. Survey open-file report, 1964. 3- 64. (and MOTTS, W. S.) Availability of ground water in parts of the Acoma and Laguna Indian Reservations, N. Mex.: U.S. Geol. Survey Water-Supply Paper 1576-E, p. E1-E65, 1964. DOBROVOLNY, E. 1-63. (SHARPS, J. A., and FERM, J. C.) Geology of the Ashland quadrangle, Kentucky-Ohio, and the Catlettsburg quadrangle in Kentucky: U.S. Geol. Survey Geol. Quad. Map GQ-196, 1963. DODSON, C. L. 1-63. (and HARRIS, W. F., Jr.) Geology and ground-water resources of Morgan County, Alabama, with a section on Chemical quality of the water, by James C. Warman: U.S. Geol. Survey open-file report, 152 p., 1963. DOE, B. R. 1-63. (HEDGE, C. E., and WHITE, D. E.) Preliminary isotopic data for brine and obsidian near Niland, California [abs.]: Mining Eng., v. 15, no. 11, p. 60, 1963. 1-64. Provincial aspects of lead isotopes in granitic rocks of the United States [abs.]: Am. Geophys. Union Trans., v. 45, no. 1, p. 108-109, 1964. DOELL, R. R. 1-63. (and COX, Allan) Secular variations in the eastern Pacific region [abs.]: Internat. Union Geodesy and Geophysics, General Assembly, 13th, Berkeley, Calif., Aug., Abstracts of Papers, v. 5, p. 41, 1963. DOELL, R. R.—Continued 1- 64. (and COX, Allan) Measurement of the remanent magnetization of igneous rocks: U.S. Geol. Survey open-file report, 51 p., 1964. 2- 64. (COX, Allan, and DALRYMPLE, G. B.) Radiometric ages of Pleistocene geomagnetic field reversals and their stratigraphic significance [abs.]: Geol. Soc. America Spec. Paper 76, p. 46-47, 1964. DOLL, W. L. 1-63. (MEYER, G., and ARCHER, R. J.) Water resources of West Virginia: West Virginia Dept, of Nat. Resources, Div. Water Resources, 134 p., 1963. DONNELL, J. R. 1-63. (and JOHNSTON, J. E.) Geology of the Quicksand quadrangle, Kentucky: U.S. Geol. Survey Geol. Quad. Map GQ-240, 1963. DONSKY, Ellis 1-63. Records of wells and ground-water quality in Camden County, New Jersey, with special reference to public water supplies, a preliminary report: New Jersey Div. Water Policy and Supply Water Resources Circ. 10, 70 p., 1963. DOOLITTLE, R. N. 1-64. (and SAX, K. W.) Gross theoretical waterpower, developed and undeveloped. State of California: U.S. Geol. Survey open-file report, 28 p., 1964. DORR, J. V. N., 2d T-63. (and MIRANDA BARBOSA, A. L. de) Geology and ore deposits of the Itabira District, Minas Gerais, Brazil: U.S. Geol. Survey Prof. Paper 341-C, p. C1-C110, 1963. 1-64. Origin of high-grade hematite ores of Minas Gerais, Brazil [abs.]: Geol. Soc. America Spec. Paper 76, p. 48-49, 1964. DOTY, G. C. 1-63. Water-supply development at the National Aeronautics and Space Agency - Apollo Propulsion system development facility. Dona Ana County, New Mexico: U.S. Geol. Survey open-file report, 40 p., 1963. DOUGLASS, R. C. 1-64. (LOEBLICH, A. R., Jr., and TAPPAN, Helen) Or-bitolinidae, in Treatise on invertebrate paleontology (R. C. Moore, ed.), pt. C, Protista 2 (Sarcodina, chiefly "The-camoebians" and Foraminiferida), v. 1: Geol.Soc. America, Univ. Kansas Press, p. 308-313, 1964. DOYEL, W. W. 1- 64. Ground water in the Arica area, Chile: U.S. Geol. Survey Prof. Paper 475-D, p. D213-D215, 1964. 2- 64. (and CASTILLO U., Octavio) The artesian aquifer of the Tierra del Fuego area, Chile, in Geol. Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B169-B172, 1964. 3- 64. (DINGMAN, R. J., and CASTILLO U., Octavio) Hydrogeology of the Santiago area, Chile: U.S. Geol. Survey Prof. Paper 475-D, p. D209-D212, 1964. 4- 64. (and MAGUIRE, F. J.) Ground-water resources of the Bengasi area, Cyrenaica, United Kingdon of Libya: U.S. Geol. Survey Water-Supply Paper 1757-B, p. Bl-B21, 1964. DRAKE, P. G. 1-63. Field filtering unit for water samples, in Selected techniques in water resources investigations, compiled by G. N. Mesnier and K. T. Iseri: U.S. Geol. Survey Water-Supply Paper 1669-Z, p. Z29-Z32, 1963. DRESCHER, W. J. 1- 63. Discussion of "Our fictitious water famine", by John E. Kinney: Am. City Mag., v. 78, no. 6, p. 33, 39, 1963. 2- 63. Hydrologic considerations in deep-well disposal of radioactive liquid wastes [abs.]: Am. Assoc. Petroleum Geologists Bull., v. 47, no. 12, p. 2073, 1963.A290 PUBLICATIONS IN FISCAL YEAR 1964 DREWES, Harald 1-64. Diverse recurrent movement along segments of a major thrust fault in the Schell Creek Range near Ely, Nev., in Geol. Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B20-B24, 1964. DUNNAM, C. A. 1-64. Sedimentation of Lake Pillsbury, Lake County, Calif.: U.S. Geol. Survey Water-Supply Paper 1619-EE, p. EE1-EE46, 1964. DURFOR, C. H. 1-64. (and BECKER, Edith) Selected data on public supplied of the 100 largest cities in the United States, 1962: Am. Water Works Assoc. Jour., v. 56, no. 3, p. 237-246, 1964. DURHAM, D. L. 1-63. Geology of the Reliz Canyon, Thompson Canyon, and San Lucas quadrangles, Monterey County, Calif.: U.S. Geol. Survey Bull. 1141-Q, p. Q1-Q41, 1963 [1964]. 1- 64. Geology of the Cosio Knob and Espinosa Canyon quadrangles, Monterey County, California: U.S. Geol. Survey Bull. 1161-H, p. H1-H29, 1964. 2- 64. (and YERKES, R. F.) Geology and oil resources of the eastern Puente Hills area, southern California: U.S. Geol. Survey Prof. Paper 420-B, p. B1-B62, 1964. DURUM, W. H. 1-63. (and HEM, J. D.) Geochemistry of water, in U.S. Natl. Rept., 1960-1963, Thirteenth General Assembly, Internat. Union Geodesy and Geophysics: Am. Geophys. Union Trans., v. 44, no. 2, p. 579-581, 1963. DUTCHER, L. C. 1- 63. (and GARRETT, A. A.) Geologic and hydrologic features of the San Bernardino area, California, with special reference to underflow across the San Jacinto fault: U.S. Geol. Survey Water-Supply Paper 1419, 114 p., 1963 [1964]. 2- 63. (and WORTS, G. F., Jr.) Geology, hydrology, and water supply on Edwards Air Force Base, Kern County, California: U.S. Geol. Survey open-file report, 251 p., 1963. DUTRO, J. T„ Jr. 1- 63. (and SANDO, W. J.) Age of certain post-Madison rocks in southwestern Montana and western Wyoming: U.S. Geol. Survey Prof. Paper 475-B, p. B93-B94, 1963. 2- 63. (and SANDO, W. J.) New Mississippian formations and faunal zones in the Chesterfield Range, Portneuf quadrangle, southeast Idaho: Am. Assoc. Petroleum Geologists Bull., v. 47, no. 11, p. 1963-1986, 1963. 3- 63. Review of "On the morphology and classification of the brachiopod suborder Chonetoidea" by Helen M. Muir-Wood: Quart. Rev. Biology, v. 38, no. 3, p. 259, 1963. 1-64. (and ROSS, R. J., Jr.) Probable late Ordovician (Ash-gill) brachiopods from east-central Alaska [abs.]: Geol. Soc. America Spec. Paper 76, p. 53, 1964. DUTTON, C. E. 1-64. Geology of the Florence area, Wisconsin-Michigan [abs.], in A. T. Broderick, ed., Tenth Ann. Inst, on Lake Superior geology, Ishpeming, Mich., p. 21-22, 1964. DYER, H. B. 1-63. (BADER, J. S„ GIESSNER, F. W„ and others) Wells and springs in the lower Mojave Valley area, San Bernardino County, California: California Dept. Water Resources Bull. 91-10, p. 1-19, A1-A88, B1-B33, C1-C37, D1-D17, 1963. EAKIN, T. E. 1- 63. Ground-water appraisal of Dry Lake and Delanaar Valleys, Lincoln County, Nevada: Nevada Dept. Conserv. and Nat. Resources Ground-water Resources - Reconn. Ser. Rept. 16, 26 p., 1963. 2- 63. Ground-water appraisal of Garden and Coal Valleys, Lincoln and Nye Counties, Nevada: Nevada Dept. Conserv. and Nat. Resources Ground-Water Resources - Reconn. Ser. Rept. 18, 29 p., 1963. EAKIN, T. E.—Continued 3- 63. Ground-water appraisal of Pahranagat and Pahroc Valleys, Lincoln and Nye Counties, Nevada; Nevada Dept. Conserv. and Nat. Resources Ground-Water Resources - Reconn. Ser. Rept. 21, 36 p., 1963. 4- 63. (SCHOFF, S. L., and COHEN, Philip) Regional hydrology of a part of southern Nevada--A reconnaissance: U.S. Geol. Survey open-file report, 40 p., 1963. 1-64. Ground-water appraisal of Coyote Spring and Kane Spring Valleys and Muddy River Springs area, Lincoln and Clark Counties, Nevada: Nevada Dept. Conserv. and Nat. Resources Ground-Water Resources - Reconn. Ser. Rept. 25, 40 p., 1964. EARGLE, D. H. 1- 64. Surface and subsurface stratigraphic sequence in southeastern Mississippi: U.S. Geol. Survey Prof. Paper 475-D, p. D43-D48, 1964. 2- 64. Descriptions of samples and cores from four wells in southeastern Mississippi: U.S. Geol. Survey open-file report, 31 p., 1964. EATON, J. P. 1-63. Crustal structure from San Francisco, California, to Eureka, Nevada, from seismic-refraction measurements: Jour. Geophys. Research, v. 68, no. 20, p. 5789-5806, 1963. 1- 64. Crustal structure from San Francisco, California, to Eureka, Nevada, from seismic-refraction measurements [abs.]: Geol. Soc. America Spec. Paper 76, p. 198-199, 1964. 2- 64. (HEALY, J. H., JACKSON, W. H., and PAKISER, L. C.) Upper mantle velocity and crustal structure in the eastern Basin and Range Province determined from SHOAL and chemical explosions near Delta, Utah [abs.]: Seismol. Soc. America, 60th Ann. Mtg., March 27-28, 1964, Program, p. 30-31, 1964. EDDY, J. E. 1-64. Television apparatus for borehole exploration: U.S. Geol. Survey Prof. Paper 475-D, p. D219-D220, 1964. EISENLOHR, W. S., Jr. 1-63. Current studies of the hydrology of prairie potholes [abs.]: Am. Geophys. Union Trans., v. 44, no. 4, p. 870, 1963. EKREN, E. B. 1-64. (and SARGENT, K. A.) Geologic map of the Skull Mountain quadrangle at the Nevada TestSite, Nye County, Nev.: U.S. Geol. Survey Rept. TEI-845, map, 1964. ELLIS, C. H. 1-64. (and Tschudy, R. H.) Morphology and distribution of the Cretaceous megaspore genus Arcellites Miner, 1935 (Pyrobolospora Hughes, 1955): Micropaleontology, v. 10, no. 1, p. 73-79, 1964. ELLIS, D. W. 1- 63. (ALLEN, H. E., and NOEHRE, A. W.) Floods in Aurora North quadrangle, Illinois: U.S. Geol. Survey Hy-drol. Inv. Atlas HA-70, 1963. 2- 63. (ALLEN, H. E„ and NOEHRE, A. W.) Floods in Elmhurst quadrangle, Illinois: U.S. Geol. Survey Hydrol. Inv. Atlas HA-68, 1963. 3- 63. (ALLEN, H, E., andNOEHRE, A. W.) Floods in Highland Park quadrangle, Illinois: U.S. Geol. Survey Hydrol. Inv. Atlas HA-69, 1963. 4- 63. (ALLEN, H. E., and NOEHRE, A. W.) Floods in Wheeling quadrangle, Illinois: U.S. Geol. Survey Hydrol. Inv. Atlas HA-71, 1963. 5- 63. (and others) Floods at Wichita, Kans.: U.S. Geol. Survey Hydrol. Inv. Atlas HA-63, 1963. 1- 64. (ALLEN, H. E., andNOEHRE, A. W.) Floods in Hinsdale quadrangle, Illinois: U.S. Geol. Survey Hydrol. Inv. Atlas HA-86, 1964. 2- 64. (ALLEN, H. E., and NOEHRE, A. W.) Floods in Park Ridge quadrangle, Illinois: U.S. Geol. Survey Hydrol. Inv. Atlas HA-85, 1964.LIST OF PUBLICATIONS A291 ELLISON, B. E., Jr. 1-63. (and BOSWELL, E. H.) Water levels and artesian pressures in observation wells in Mississippi: Mississippi Board Water Comm. Bull. 63-12, 36 p., 1963. EMERY, K. O. 1-63. (and SCHLEE, J. S.) The Atlantic Continental Shelf and Slope—A program for study: U.S.Geol. Survey Circ. 481, 11 p., 1963. EMERY, P. A. 1-63. Geology and ground-water resources of Richardson County, Nebraska: U.S. Geol. Survey open-file report, 44 p„ 1963. 1-64. (and MALHOIT, M. M.) Water levels in observation wells in Nebraska, 1963: Nebraska Univ. Conserv. and Survey Div., Nebraska Water Survey Paper 14, 163 p., 1964. EMMETT, W. W. 1-63. (and LEOPOLD, L. B.) Downstream pattern of river-bed scour and fill: U.S. Geol. Survey open-file report, 19 p., 1963. ENGEL, A. E. J. 1-64. (ENGEL, C. G., and HAVENS, R. G.) Mineralogy of amphibolite interlayers in the gneiss complex, northwest Adirondack Mountains, New York: Jour. Geology, v. 72, no. 2, p. 131-156, 1964. ENGLER, Kyle 1-63. (BAYLEY, F. H., 3d, andSNIEGOCKI, R. T.) Studies of artificial recharge in the Grand Prairie region, Arkansas; Environment and History: U.S. Geol. Survey Water-Supply Paper 1615-A, p. A1-A32, 1963. ENGLUND, K. J. 1- 64. Stratigraphy of the Lee Formation in the Cumberland Mountains of southeastern Kentucky, in Geol. Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B30-B38, 1964. 2- 64. (ROEN, J. B., and DeLANEY, A. O.) Geology of the Middlesboro north quadrangle, Kentucky: U.S. Geol.Survey Geol. Quad. Map GQ-300, 1964. ERDMANN, C. E. 1-63. Geology and mineral resources of Missouri River valley between head of Fort Peck Reservoir and Morony Dam, with a chapter on Engineering geology by Richard W. Lemke, App. 3, Geology, in Joint report on water resources development for Missouri River, Fort Peck Reservoir to vicinity of Fort Benton, Montana: Omaha, Nebr., U.S. Army Engineer District, and Billings, Mont., U.S. Bur. Reclamation, p. Ill— 1—III-122, 1963. ERICKSEN, G. E. 1-64. Geology of the salt deposits and the salt industry of northern Chile: U.S. Geol. Survey open-file report, 164 p., 1964. ERICKSON, R. L. 1-64. (MASURSKY, Harold, MARRANZINO, A. P., ODA, Uteana, and JANES, W. W.) Geochemical anomalies in the lower plate of the Roberts thrust near Cortez, Nev., in Geol. Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B92-B94, 1964. ESPENSHADE, G. H. 1-63. Geology of some copper deposits in North Carolina, Virginia, and Alabama: U.S. Geol. Survey Bull. 1142-1, p. 11-150, 1963. EVANS, H. B. 1-64. Factors influencing permeability and diffusion of radon in synthetic sandstones: U.S. Geol. Survey open-file report, 94 p., 1964. EVANS, H. T„ Jr. 1-63. (APPLEMAN, D. E., and HANDWERKER, D. S.) The least squares refinement of crystal unit cells with powder diffraction data by an automatic computer indexing method [abs.]: Am. Cryst. Assoc., Ann. Mtg., Cambridge, Mass., Mar. 1963, Program and Abs., Abs. E-10, p. 42-43, 1963. EVANS, H. T„ Jr.--Continued 1-64. (MILTON, Charles, CHAO, E.C.T., ADLER, Isidore, MEAD, Cynthia, INGRAM, Blanche, and BERNER, R. A.) Valleriite and the new iron sulfide, mackinawite: U.S. Geol. Survey Prof. Paper 475-D, p. D64-D69, 1964. EVENSON, R. E. 1-64. Results of test drilling, Naval Missile Facility, Point Arguello, Santa Barbara County, California, 1962-63: U.S. Geol. Survey open-file report, 18 p., 1964. EVERETT, D. E. 1-64. Ground-water appraisal of Edwards Creek Valley, Churchill County, Nevada: Nevada Dept. Conserv. and Nat. Resources Ground-Water Resources - Reconn. Ser. Rept. 26, 18 p., 1964. FADER, S. W. 1-64. (and GUTENTAG, E. D., LOBMEYER, D. H„ and MEYER, W. R.) Geohydrology of Grant and Stanton Counties, Kansas: U.S. Geol. Survey open-file report, 870 p., 1964. FAHNESTOCK, R. K. 1-63. Morphology and hydrology of a glacial stream—White River, Mount Rainier, Wash.: U.S. Geol. Survey Prof. Paper 422-A, p. A1-A70, 1963 [1964], 1- 64. (and MADDOCK, Thomas, Jr.) Preliminary report on bed forms and flow phenomena in the Rio Grande near El Paso, Tex., in Geol. Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B140-B142, 1964; abs., Geol. Soc. America Spec. Paper 76, p. 272-273, 1964. 2- 64. (and SAVINI, J.) Role of mudflows in the formation of glacial and fluvioglacial land forms [abs.]: Geol. Soc. America Spec. Paper 76, p. 56, 1964. FASSETT, J. E. 1-64. Subsurface geology of the Upper Cretaceous Kirtland and Fruitland Formations of the San Juan Basin, New Mexico and Colorado: U.S. Geol. Survey open-file report, 93 p„ 1964. FAUST, G. T. 1- 63. Physical properties and mineralogy of selected samples of the sediments from the vicinity of the Brookhaven National Laboratory, Long Island, New York: U.S. Geol. Survey Bull. 1156-B, p. B1-B34, 1963. 2- 63. Minor elements in serpentine—additional data:Geo-chim. et Cosmochim. Acta, v. 27, no. 6, p. 665-668, 1963. FEININGER, T. G. 1- 63. Trip G, Westerly Granite and related rocks of the Westerly-Bradford area (Rhode Is.), in New England Intercollegiate Geol. Conf. Guidebook, 55th Ann. Mtg., Providence, R. I., Oct. 4-6, 1963; p. 48-51, 1963. 2- 63. Westerly granite bodies in the Westerly-Bradford area, Rhode Island-Connecticut, in New England Intercollegiate Geol. Conf. Guidebook, 55th Ann. Mtg., Providence, R. I., Oct. 4-6, 1963. 1-64. Petrology of the Ashaway and Voluntown quadrangles, Connecticut-Rhode Island: U.S. Geol. Survey open-file report, 219 p., 1964. FELTIS, R. D. 1-63. (and ROBINSON, G. B., Jr.) Test drilling in the upper Sevier River drainage basin, Utah, 1962: U.S. Geol. Survey open-file report, 32 p., 1963. FELTZ, H. R. 1-63. (and HANSHAW, B. B.) Preparation of water sample for carbon-14 dating: U.S. Geol. Survey Circ. 480, 3 p., 1963. FENNELL, E. J. 1-63. Surveys and maps for industrial growth: Am. Soc. Civil Engineers Proc., v. 89, Jour. Surveying and Mapping Div., no. SU3, p. 117-122, 1963. FERRIANS, O. J., Jr. 1-63. Glaciolacustrine diamicton deposits in the Copper River Basin, Alaska: U.S. Geol. Survey Prof. Paper 475-C, p. C121-C125, 1963.A292 PUBLICATIONS IN FISCAL YEAR 1964 FERRIS, J. G. 1- 63. Cyclic water-level fluctuations as a basis for determining aquifer transmissibility, in Methods of determining permeability, transmissibility, and drawdown, compiled by Ray Bentall: U.S. Geol. Survey Water-Supply Paper 1536-1, p. 305-318, 1963. 2- 63. (and KNOWLES, D. B.) The slug-injection test for estimating the coefficient of transmissibility of an aquifer, in Methods of determining permeability, transmissibility, and drawdown, compiled by Ray Bentall: U.S. Geol. Survey Water-Supply Paper 1536-1, p. 299-304, 1963. FETH, J. H. 1-64. (ROBERSON, C. E„ and POLZER, W. L.) Sources of mineral constituents in water from granitic rocks. Sierra Nevada, California and Nevada: U.S. Geol. Survey Water-Supply Paper 1535-1, p. 11-170, 1964. FEULNER, A. J. 1- 63. Data on wells in the King Salmon area, Alaska: Alaska Dept, of Health and Welfare Water-Hydrol. Data, no. 24, 18 p., 1963. 2- 63. Water-supply potential in the Ohlson Mountain Area, Kenai Peninsula, Alaska: Alaska Dept. Health and Welfare, Water-Hydrol. Data, no. 22, 16 p., 1963. 3- 63. (and SCHUPP, R. G.) Seasonal changes in the chemical quality of shallow ground water in northwestern Alaska: U.S. Geol. Survey Prof. Paper 475-B, p. B189-B191, 1963. FINCH, W. I. 1-63. Geology of the Water Valley quadrangle in Kentucky: U.S. Geol. Survey Geol. Quad. Map GQ-269, 1963. FISCHER, R. P. 1-63. (and KING, R. U.) Trends in the consumption and supply of molybdenum and vanadium [abs.]: Mining Eng., v. 15, no. 11, p. 57, 1963. FISCHER, W. A. 1-63. Depiction of soil-covered structures by infrared aerial photography: U.S. Geol. Survey Prof. Paper 475-B, p. B67-B70, 1963. 1-64. (and HACKMAN, R. J.) Geologic map and sections of the Torrance Station 4 NE quadrangle, Lincoln County, N. Mex.: U.S. Geol. Survey Misc. Geol. Inv. Map 1-400, 1964. FISKE, R. S. 1-63. (HOPSON, C. A. and WATERS, A. C.) Geology of Mount Rainier National Park, Washington: U.S. Geol. Survey Prof. Paper 444, 93 p., 1963. 1-64. (HOPSON, C. A., and WATERS, A. C.) Geologic map and section of Mount Rainier National Park, Washington: U.S. Geol. Survey Misc. Geol. Inv. Map 1-432, 1964. FLEISCHER, Michael 1-62. Review of "The trace-element content of fertilizers" by D. J. Swaine: Econ. Geology, v. 57, no. 6, p. 986, 1962. 1-63. (and FAUST, G. T.) Studies on Manganese Oxide Minerals--[Pt.] 7, Lithiophorite: Schweizer. Mineralog. Petrog. Mitt., v. 43, no. 1, p. 197-216, 1963. 1- 64. Fluoride content of ground water in the conterminous United States [abs.]: Geol. Soc. America Spec. Paper 76, p. 59, 1964. 2- 64. Review of "Entstehung und Stoffbestand der Salz-lagerstatten" (Origin and material balance of salt deposits), by Otto Braitsch: GeoTimes, v. 8, no. 6, p. 48, 1964. FOLLETT, C. R. 1-64. (and GABRYSCH, R. K.) Ground-water resources of De Witt County, Texas: U.S. Geol. Survey open-file report, 163 p., 1964. FORD, A. B. 1-63. Cordierite-bearing hypersthene-quartz monzonite porphyry in the Thiel Mountains, Antarctica [abs.]: Polar Record, v. 11, no. 75, p. 771, 1963. FOSBERG, F. R. 1-63. The physical background of the humid tropics—substratum, in Admin, of Territory of Papua, New Guinea, FOSBERG, F. R.--Continued and UNESCO, Symposium on the impact of man on humid tropics vegetation, p. 35-37, 1963. 2- 63. Grazing animals and the vegetation of oceanic isla-lands, in Admin, of Territory of Papua, New Guinea, and UNESCO, Symposium on the impact of man on humid tropics vegetation, p. 168-169, 1963. 3- 63. Nature and detection of plant communities resulting from activities of early man, in Admin, of Territory of Papua, New Guinea, and UNESCO, Symposium on the impact of man on humid tropics vegetation, p. 251-262,1963. 4- 63. A theory on the origin of the coconut, in Admin, of Territory of Papua and New Guinea, and UNESCO, Symposium on the impact of man on humid tropics vegetation, p. 73-75, 1963. 5- 63. Introduction, in J. Linsley Gressitt, ed.. Pacific Basin Biogeography, a Symposium: Bishop Mus. Press, Honolulu, p. 187-188, 1963. 6- 63. Plant dispersal in the Pacific: Bishop Mus. Press, Honolulu, p. 273-281, 1963. 7- 63. Disturbance in island ecosystems: Bishop Mus. Press, Honolulu, p. 557-561, 1963. 8- 63. The island ecosystem, in F. R. Fosberg, ed., Man's place in the island ecosystem, a symposium: Bishop Mus. Press, Honolulu, p. 1-6, 1963. 9- 63. A buttressed elm from Ontario: Rhodora (New England Botanical Club), v. 65, p. 366, 1963. 1- 64. Studies in Pacific Rubiacae-[Pt.] 5: Brittonia, v. 16, p. 255-271, 1964. 2- 64. Conversations on ecology IX: TheGarden Jour. (New York Botanical Garden), v. 14, no. 2, p. 63-64, 1964. FOSTER, M, D. 1-64. Water content of micas and chlorites: U.S. Geol. Survey Prof. Paper 474-F, p. F1-F15, 1964. FOURNIER, R. O. 1-64. (ROWE, J. J., and MOREY, G.W.) Solubility of amorphous silica at 25°C [abs.]: Am. Geophys. Union Trans., v. 45, no. 1, p. 122-123, 1964. FOX, K. F., Jr. 1-63. (and SEELAND, D. A.) Geology of the Canton quadrangle, Kentucky: U.S. Geol. Survey Geol. Quad. Map GQ-279, 1963 [1964], FRANTZ, S. E. 1-63. Snowmelt hydrology of the North Yuba River basin, California: U.S. Geol. Survey Prof. Paper 475-C, p. C191-C193, 1963. FREEMAN, V. L. 1-64. Geologic map of the Indian Wells quadrangle, Terrell and Brewster Counties, Tex.: U.S. Geol. Survey Misc. Geol. Inv. Map 1-395, 1964. FRIEDMAN, Irving 1- 63. Physical properties and gas content of tektites, in O'Keefe, J. A., ed., Tektites: Chicago, Univ. Chicago Press, p. 130-136, 1963. 2- 63. (LONG, W. D., and SMITH, R. L.) Viscosity and water content of rhyolite glass as a function of temperature and water pressure: Jour. Geophys. Research, v. 68, no. 24, p. 6523-6535, 1963. 3- 63. (SIGURGEIRSSON, Thorbjorn, and GARDARSSON, Orn) Deuterium in Iceland waters: Geochim. et Cosmo-chim. Acta, v. 27, no. 6, p. 553-561, 1963. 4- 63. (SMITH, R. L., and CLARK, D.) Obsidian dating, in Science in archeology: London, Thames and Hudson, Ltd., p. 47-58, 1963. 1- 64. (SMITH, R. L., LEVIN, Betsy, and MOORE, Arthur) The water and deuterium content of phenocrysts from rhyolitic lavas, in_ N. Craig, R. Miller, andG. I. Wasser-burg, eds.. Isotopic and cosmic chemistry: Amsterdam, North Holland Publishing Company, p. 200-204, 1964. 2- 64. (and SMITH, R. L.) The hydration and devitrification of natural glasses [abs.]: Am. Geophys. Union Trans., v. 45, no. 1, p. 122, 1964.LIST OF PUBLICATIONS A293 FRIEDMAN, Irving--Continued 3-64. (REDFIELD, A. C., SCHOEN, Beatrice, and HARRIS, Joseph) The variation of the deuterium content of natural waters in the hydrologic cycle: Rev. Geophysics, v. 2, no. 1, p. 177-224, 1964. FRISCHKNECHT, F. C. 1- 63. (PETRAFESO, F. A., and others) Aeromagnetic map of part of the Los Gigantes Buttes quadrangle, Apache County, Ariz.: U.S. Geol. Survey Geophys. Inv. Map GP-404, 1963. 2- 63. (PETRAFESO, F. A., and others) Aeromagnetic map of the Yellowstone Canyon quadrangle, Apache County, Ariz.: U.S. Geol. Survey Geophys. Inv. MapGP-405, 1963. 1- 64. (and EKREN, E. B.) Evaluation of magnetic anomalies by electromagnetic measurements: U.S. Geol. Survey Prof. Paper 475-C, p. C117-C120, 1964. 2- 64. (and PETRAFESO, F. A.) Aeromagnetic map of the Kramer area, Kern, San Bernardino, and Los Angeles Counties, California: U.S. Geol. Survey open-file report, map, 1964. FRITTS, C. E. 1- 63. Bedrock geology of the Mount Carmel quadrangle, Connecticut: U.S. Geol. Survey Geol. Quad. Map GQ-199, 1963. 2- 63. Bedrock geology of the Southington quadrangle, Connecticut: U.S. Geol. Survey Geol. Quad. Map GQ-200, 1963. 1-64. Stratigraphy of Animikie (formerly Huronian) rocks east of Teal Lake, Negaunee, Michigan [abs.J, ic A. T. Broderick, ed., Tenth Ann. Inst, on Lake Superior geology, Ishpeming, Mich., p. 5-8, 1964. FRYE, P. M. 1-63. Establishment of crest-stage gages at discontinued gaging stations, in Selected techniques in water resources investigations, compiled by G. N. Mesnier and K. T. Iseri: U.S. Geol. Survey Water-Supply Paper 1669-Z, p. Z25-Z26, 1963. FRYKLUND, V. C., Jr. 1-63. (and FLEISCHER, Michael) The abundance of scandium in volcanic rocks, a preliminary estimate: Geochim. et Cosmochim. Acta, v. 27, no. 6, p. 643-664, 1963. GAIR, J. E. 1- 64. Structures in the eastern part of the Marquette syn-clinorium [abs.], in A. T. Broderick, ed.. Tenth Ann. Inst, on Lake Superior geology, Ishpeming, Mich.,p. 3-4, 1964. 2- 64. (and WIER, K. L.) Geologic and magnetic survey of a part of the Palmer 7 l/2-minute quadrangle, Michigan: U.S. Geol. Survey open-file report, map, 1964. 3- 64. Field Trip, May9, 1964, Marquette iron-mining district and Republic Trough: Ishpeming,Mich., Inst. Lake Superior Geology, 10th Ann. Field Trip, 12 p., 1964. GALLAHER, J. T. 1- 63. Geology and hydrology of alluvial deposits along the Ohio River in the Hawesville and Cloverport areas, Kentucky: U.S. Geol. Survey Hydrol. Inv. Atlas HA-72, 1963. 2- 63. Geology and hydrology of alluvial deposits along the Ohio River in the Lewisport and Owensboro areas, Kentucky: U.S. Geol. Survey Hydrol. Inv. Atlas HA-74, 1963 11964]. 3- 63. Geology and hydrology of alluvial deposits along the Ohio River in the Spottsville and Reed areas, Kentucky: U.S. Geol. Survey Hydrol. Inv. Atlas HA-96, 1963. 1-64. Geology and hydrology of alluvial deposits along the Ohio River between the Wolf Creek and West Point areas, Kentucky: U.S. Geol. Survey Hydrol. Inv. Atlas HA-95, 1964. GAMBELL, A. W. 1-63. Sulfate and nitrate content of precipitation over parts of North Carolina and Virginia: U.S. Geol. Survey Prof. Paper 475-C, p. C209-C211, 1963. GARZA, Sergio 1-63. Ground-water discharge from the Edwards and associated limestones, 1955-62,San Antonio Area, Texas: Edwards Underground Water Dist. Bull. 2, 4 p., 1963. GARZA, Sergio—Continued 2-63. Records of precipitation, aquifer head, and ground-water recharge to the Edwards associated limestones, 1960-62, San Antonio area, Texas: Edwards Underground Water Dist. Bull. 3, 7 p., 1963. 1-64. Chemical analyses of water from observation wells in the Edwards and associated limestones, San Antonio, Texas, 1963: U.S. Geol. Survey open-file report, 15 p., 1964. GASKILL, D. L. 1-63. (and GODWIN, L. H.) Redefinition and correlation of the Ohio Creek Formation (Paleocene) in west-central Colorado: U.S. Geol. Survey Prof. Paper 475-C, p. CSS-CSS, 1963. GATES, J. S. 1- 63. Ground water in the Navajo Sandstone at the east entrance, Zion National Park, Utah: U.S. Geol. Survey open-file report, 23 p., 1963. 2- 63. Hydrogeology of Middle Canyon, Oquirrh Mountains, Tooele County, Utah: U.S. Geol. Survey Water-Supply Paper 1619-K, p. K1-K40, 1963. 3- 63. Selected hydrologic data, Tooele Valley, Tooele County, Utah: Utah State Engineer Basic-Data Rept. 7, 23 p., 1963. GATEWOOD, J. S. 1-63. (and WILSON, Alfonso) Upper Salinas River Basin, in Effects of drought along Pacific Coast in California, by H. E. Thomas and others: U.S. Geol. Survey Prof. Paper 372-G, p. G19, 1963. 1-64. (WILSON, Alfonso, THOMAS, H. E., and KISTER, L. R.) General effects of drought on water resources of the Southwest: U.S. Geol. Survey Prof. Paper 372-B, p. B1-B55, 1964. GEORGE, J. R. 1-63. (and ANDERSON, P. W.) Water-quality studies of New Jersey streams: New Jersey Dept. Health, Public Health News, v. 44, no. 6, p. 154-159, 1963. GERLACH, A. C. 1-64. Technical problems in creating special subject maps: Surveying and Mapping, v. 24, no. 1, p.37-39, 1964. GIBBONS, A. B. 1-63. (HINRICHS, E. N., HANSEN, W. R., and LEMKE, R. W.) Geology of the Rainier Mesa quadrangle, Nye County, Nev.: U.S. Geol. Survey Geol. Quad. MapGQ-215, 1963. GIESSNER, F. W. 1- 63. Data on water wells and springs in the Chuckwalla Valley area. Riverside County, California: California Dept. Water Resources Bull. 91-7, 77 p., 1963. 2- 63. Data on water wells and springs in the Rice and Vidal Valley areas. Riverside and San Bernardino Counties, California: California Dept. Water Resources Bull. 91-8, 35 p., 1963. 1-64. A reconnaissance of the geology and water resources of the Mission Creek Indian Reservation, Riverside County, California: U.S. Geol. Survey open-file report, 31 p., 1964. GILBERT, C. R. 1-63. Floods on White Rock Creek above White Rock Lake at Dallas, Texas: U.S. Geol. Survey and City of Dallas open-file report, 66, 14 p., 1963. GILL, J. R. 1-63. Memorial to Alfred Dexter Zapp, 1916-1962: Am. Assoc. Petroleum Geologists Bull., v. 48, no. 1, p. 127-129, 1963. GILLULY, James 1- 63. Tectonic evolution of the western United States: Geol. Soc. London, Quarterly Jour., v. 119, no. 2, p. 133-174, 1963. 2- 63. The scientific philosophy of G. K. Gilbert, in C. C. Albritton, Jr., ed., The fabric of geology: Addison-Wesley Pub. Co., Reading, Mass., p. 218-224, 1963. 1-64. Atlantic sediments, erosion rates, and the evolution of the Continental Shelf—Some speculations: Geol. Soc. America Bull., v. 75, no. 6, p. 483-492, 1964.A294 PUBLICATIONS IN FISCAL YEAR 1964 GILSTRAP, R. C. 1-64. (and CHRISTIANSEN, R. C.) Floods of July 16-17, 1963, in vicinity of Hot Springs, Arkansas: U.S. Geol. Survey open-file report, 6 p., 1964. GIROUX, P. R. 1-63. (and HUFFMAN, G. C.) Summary of ground-water conditions in Michigan, 1962: Michigan Dept. Conserv., Geol. Survey Div. Water Supply Rept. 7, 80 p., 1963. GIUSTI, E. V. 1-63. Distribution of river basin areas in the conterminous United States: Internat. Assoc. Sci. Hydrology Bull., v. 8, no. 3, p. 20-29, 1963. GLICK, E. E. 1- 63. Geology of the Clarkson quadrangle, Kentucky: U.S. Geol. Survey Geol. Quad. Map GQ-278, 1963 [1964], 2- 63. Geologic maps versus other geologic theories — northern Arkansas [abs.]: Shale Shaker, v. 14, no. 2, p. 6-7, 1963. GLOVER, R. E. 1-64. Dispersion of dissolved or suspended materials in flowing streams: U.S. Geol. Survey Prof. Paper 433-B, p. B1-B32, 1964. GODDARD, G. C., Jr. 1-63. Water-supply characteristics of North Carolina streams: U.S. Geol. Survey Water-Supply Paper 1761, 223 p., 1963. GOERLITZ, D. F. 1-64. (and LAMAR, W. L.) Effluent collector for gas chromatography: U.S. Geol. Survey Prof. Paper 475-D, p. D164-D166, 1964. GOLDSMITH, Richard 1- 64. Geologic map of New England: 1) General geology, 2) Metamorphic zones, and 3) Radiometric ages: U.S. Geol. Survey open-file report, 3 maps, 1964. 2- 64. Geologic sketch map of eastern Connecticut: U.S. Geol. Survey open-file report, map, 1964. GORDON, Mackenzie, Jr. 1-63. Biostratigraphic correlation of Chester and Morrow rocks of northern Arkansas [abs.]: Shale Shaker, v. 14, no. 2, p. 7, 1963. 1-64. Mississippian productoid brachiopods from west-central Utah [abs.]: Geol. Soc. America Spec. Paper 76, p. 67-68, 1964. GOTTFRIED, David 1-64. (and WARING, C. L.) Hafnium content and Hf/Zr ratio in zircon from the southern California batholith, in Geol. Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B88-B91, 1964. GOWER, H. D. 1-63. (and WANEK, A. A.) Preliminary geologic map of the Cumberland quadrangle. King County, Washington: Washington Div. Mines and Geology, Geol. Map GM-2, 1963. GRANGER, H. C. 1- 63. Radium migration and its effect on the apparent age of uranium deposits at Ambrosia Lake, N. Mex.: U.S. Geol. Survey Prof. Paper 475-B, p. B60-B63, 1963. 2- 63. (and SANTOS, E. S.) An ore-bearing cylindrical collapse structure in the Ambrosia Lake uranium district, New Mexico: U.S. Geol. Survey Prof. Paper 475-C, p. C156-C161, 1963. 1-64. (and RAUP, R. B.) Stratigraphy of the Dripping Spring Quartzite, southeastern Arizona: U.S. Geol. Survey Bull. 1168, 119 p., 1964. GRANT, R. E. 1-64. Morphology, evolution, and life habits of the Camero-phoriacea (Brachiopoda) [abs.]: Geol.Soc. AmericaSpec. Paper 76, p. 68, 1964. GRANTZ, Arthur 1-63. Aerial reconnaissance of the outer Shumagin Islands, Alaska: U.S. Geol. Survey Prof. Paper 475-B, p. B106-B109, 1963. GRANTZ, Arthur—Continued 2-63. (THOMAS, Herman, STERN, T. W., and SHEFFEY, N. B.) Potassium-argon and lead-alpha ages for strati-graphically bracketed plutonic rocks in the Talkeetna Mountains, Alaska: U.S. Geol. Survey Prof. Paper 475-B, p. B56-B59, 1963. 1- 64. Stratigraphic reconnaissance of the Matanuska Formation in the Matanuska Valley, Alaska: U.S. Geol. Survey Bull. 1181-1, p. 11-133, 1964. 2- 64. (PLAFKER, George, and KACHADOORIAN, Reuben) Alaska's Good Friday earthquake, March 27, 1964, apre-liminary geologic evaluation: U.S. Geol. Survey Circ. 491, 35 p., 1964. GREEN, J. H. 1- 64. The effect of artesian-pressure decline on confined aquifer systems and its relation to land subsidence: U.S. Geol. Survey Water-Supply Paper 1779-T, p. Tl-Tll, 1964. 2- 64. (and HUTCHINSON, R. D.) Ground-water pumpage and water-level changes in the Milwaukee-Waukesha area, Wisconsin, 1950-1961: U.S. Geol. Survey open-file report, 41 p., 1964. GRIFFITTS, W. R. 1- 63. (and POWERS, H. A.) Beryllium and fluorine content of some silicic volcanic glasses from Western United States: U.S. Geol. Survey Prof. Paper 475-B, p. B18-B19, 1963. 2- 63. (and RADER, L. F., Jr.) Beryllium and fluorine in mineralized tuff, Spor Mountain, Juab County, Utah: U.S. Geol. Survey Prof. Paper 475-B, p. B16-B17, 1963. GRIMALDI, F. S. 1-63. (and SIMON, F. O.) Determination of traces of boron in halite and anhydritic halite rocks: U.S. Geol. Survey Prof. Paper 475-B, p. B166-B168, 1963. GRINNEL, R. S., Jr. 1-64. (and ANDREWS, G. W.) Morphologic studies of the brachiopod genus Composita: Jour. Paleontology, v. 38, no. 2, p. 227-248, 1964. GRBCOM, Andrew 1-63. (and LARRABEE, D. M.) Aeromagnetic interpretation and preliminary geology of the Danforth area, Maine: U.S. Geol. Survey Geophys. Inv. Map GP-423, 1963. 1-64. (and ZIETZ, Isidore) Differences between aeromagnetic and geologic depths to basement in the Appalachian Basin [abs.]: Geol. Soc. America Spec. Paper 76, p. 68-69, 1964. GROSSMAN, I. G. 1-63. Geology of the Gu=mica-Guayanilla Bay area, southwestern Puerto Rico: U.S. Geol. Survey Prof. Paper 475-B, p. B114-B116, 1963. GUILD, P. W. 1-63. Geology, in Review of developments in 1963: Mining Eng., v. 16, no. 2, p. 69-74, 1963. GULBRANDSEN, R. A. 1-63. (JONES, D. L„ TAGG, K. M., and REESER, D. W.) Apatitized wood and leucophosphite in nodules in the Moreno Formation, California: U.S. Geol. Survey Prof. Paper 475-C, p. C100-C104, 1963. GUTENTAG, E. D. 1-64. Studies of Pleistocene and Pliocene deposits in southwestern Kansas: Kansas Acad. Sci. Trans., v. 66, no. 4, p. 606-621, 1964. GUY, H. P. 1- 63. Residential construction and sedimentation at Kensington, Maryland: U.S. Geol. Survey open-file report, 16 p., 1963. 1 - 64. An analysis of some storm-period variables affecting stream sediment transport: U.S. Geol. Survey Prof. Paper 462-E, p. E1-E46, 1964. 2- 64. (and SIMONS, D. B.) Dissimilarity between spatial and velocity-weighted sediment concentrations: U.S. Geol. Survey Prof. Paper 475-D, p. D134-D137, 1964.LIST OF PUBLICATIONS A295 HACKETT, O. M. 1- 63. Ground-water levels in the United States, 1956-60, Northwestern States: U.S. Geol. Survey Water-Supply Paper 1760, 222 p., 1963. 2- 63. Ground-water levels in the United States, 1956-60, Southwestern States: U.S. Geol. Survey Water-Supply Paper 1770, 160 p., 1963. 1-64. The father of modern ground water hydrology: Ground Water, v. 2, no. 2, p. 2-5, 1964. HADLEY, J. B. 1-63. (and GOLDSMITH, Richard) Geology of the eastern Great Smoky Mountains, North Carolina and Tennessee: U.S. Geol. Survey Prof. Paper 349-B, p. B1-B118, 1963. 1- 64. Correlation between isotopic ages, crustal heating, and sedimentation in the Appalachian region [ abs.]: Geol. Soc. America Spec. Paper 76, p. 236, 1964. 2- 64. Correlation of isotopic ages, crustal heating, and sedimentation in the Appalachian region, in W. D. Lowry, ed., Tectonics of the Southern Appalachians: Virginia Polytechnic Inst., Dept. Geol.Sci. Mem. l,p. 33-45, 1964. HADLEY, R. F. 1-63. Hydrology of stock-water development in southeastern Idaho: U.S. Geol. Survey Water-Supply Paper 1475-P, p. 563-599, 1963. HAHL, D. C. 1- 63. (and MITCHELL, C. G.) Dissolved-mineral inflow to Great Salt Lake and chemical characteristics of the Salt Lake brine—Pt. 1, Selected hydrologic data: Utah Geol. and Mineralog. Survey, Water-Resources Bull. 3, pt. 1, 40 p., 1963. 2- 63. (and LANGFORD, R. H.) Dissolved-mineral inflow to Great Salt Lake, Utah, and chemical characteristics of the Lake brine—Pt. 2, Technical report: U.S. Geol. Survey open-file report, 39 p., 1963. HALBERG, H. N. 1-63. (and REED, J. E.) Ground-water resources of eastern Arkansas in the vicinity of U. S. Highway 70: U.S. Geol. Survey open-file report, 43 p., 1963. 1-64. (HUNT, O. P.,andPAUSZEK,F.H.) Water resources of the Albany-Schenectady-Troy area. New York: U.S. Geol. Survey Water-Supply Paper 1499-D, p. D1-D64, 1964. HALEY, B. R. 1-64. Geology of Paris quadrangle, Logan County, Arkansas: Arkansas Geol. and Conserv. Comm. Inf. Circ. 20-B, 40 p., 1964. HALL, W. E. 1- 63. (and FRIEDMAN, Irving) Composition of fluid in- clusions, Cave-in-Rock fluorite district, Illinois, and upper Mississippi Valley zinc-lead district: Econ. Geology, v. 58, no. 6, p. 886-911, 1963. 2- 63. (and STEPHENS, H. G.) Economic geology of the Pan-amint Butte quadrangle and Modoc district, Inyo County, California: Calif. Div. Mines Spec. Rept. 73, 39 p., 1963. HALLIDAY, James 1-63. The vital communications link--photoidentification of horizontal control: Photogramm. Eng., v. 29, no. 5, p. 804-808, 1963. HAMILTON, Warren 1- 63. Geology of the Fountain Run quadrangle, Kentucky-Tennessee: U.S. Geol. Survey Geol. Quad. Map GQ-254, 1963. 2- 63. Metamorphism in the Riggins region, western Idaho: U.S. Geol. Survey Prof. Paper 436, 95 p., 1963. 3- 63. (and HAYES, P. T.) Type section of the Beacon Sandstone of Antarctica: U.S. Geol. Survey Prof. Paper 456-A, A1-A18, 1963. 4- 63. Petrology of rhyolite and basalt, northwestern Yellowstone Plateau: U.S. Geol. Survey Prof. Paper 475-C, p. C78-C81, 1963. 5- 63. Antarctic tectonics and continental drift, in A. C. Munyan, ed., Polar wandering and continental drift: Soc. HAMILTON, Warren--Continued Econ. Paleontologists and Mineralogists Spec. Pub. no. 10, p. 74-93, 1963. 6-63. Diabase sheets differentiated by liquid fractionation, Taylor Glacier region. South Victoria Land [abs.]: Sci. Comm. Antarctic Research Bull. 15, p. 771-772, also in Polar Record, v. 75, no. 11, p. 49-50, 1963. 1- 64. Nappes in southeastern California [abs.]: Geol.Soc. America Spec. Paper 76, p. 274, 1964. 2- 64. Discussion of paper by D. I. Axelrod, "Fossil floras suggest stable, not drifting, continents": Jour. Geophys. Research, v. 69, no. 8, p. 1666-1668, 1964. HAMPTON, E. R. 1-63. Records of wells, water levels and chemical quality of ground water irf the Molalla-Salem slope area, northern Willamette Valley, Oregon: Oregon State Engineer, Ground Water Rept. 2, 174 p., 1963. HAMPTON, E. R. 1-64. (and BROWN, S. G.) Geology and ground-water resources of the upper Grande Ronde River basin. Union County, Oregon: U.S. Geol. Survey Water-Supply Paper 1597, 99 p., 1964. HANSEN, A. J., Jr. 1- 63. Preliminary map of Block Island, Rhode Island, showing availability of ground water: U.S. Geol. Survey open-file report, 1963. 2- 63. (and SCHINER, G. R.) Ground-water levels in Rhode Island, 1960-1962: Rhode Island Water Resources Coordinating Board Hydrol. Bull., no. 5, 49 p., 1963. HANSEN, W. R. 1-63. (LEMKE, R. W. CATTERMOLE, J. M., and GIBBONS, A. B.) Stratigraphy and structure of the Rainier and USGS Tunnel areas, Nevada Test Site: U.S. Geol. Survey Prof. Paper 382-A, p. A1-A49, 1963. 1- 64. Absolute age of the Red Creek quartzite (Precam-brian) exceeds 2 billion years [abs.]: Geol. Soc. America Spec. Paper 76, p. 274-275, 1964. 2- 64. Curecanti pluton, an unusual intrusive body in the Black Canyon of the Gunnison, Colorado: U.S. Geol. Survey Bull. 1181-D, p. D1-D15, 1964. 3- 64. Repeated movements on conjugate faults in the Black Canyon of the Gunnison National Monument, Colorado [abs.]: Geol. Soc. America Spec. Paper 76, p. 275, 1964. 4- 64. Rock formations of the Black Canyon area, Colorado: Gunnison, Colo., Colorado-Black Canyon of the Gunnison Natural History Assoc., 1964. HANSHAW, B. B. 1-63. Preliminary relations in the system Na2B4C>7-Ca2BgOn-H20: U.S. Geol. Survey Prof. Paper 475-B, p. B24-B27, 1963. 1-64. (BACK, William, and RUBIN, Meyer) Relation of carbon-14 concentrations to saline-water contamination of coastal aquifers [abs.]: Geol. Soc. America Spec. Paper 76, p. 74, 1964. HARBAUGH, T. E. 1-63. Discussion of "Analysis of synthetic unit-graph methods", by Paul E. Morgan and Stanley M. Johnson: Am. Soc. Civil Engineers Proc., v. 89, Jour. Hydraulics Div., no. HY3, pt. 1, p. 354-359, 1963. HARDISON, C. H. 1- 63. (and MARTIN, R. O. R.) Low-flow frequency curves for selected long-term stream-gaging stations in Eastern United States: U.S. Geol. Survey Water-Supply Paper 1669-G, p. G1-G30, 1963. 2- 63. (and MARTIN, R. O. R.) Water-supply characteristics of streams in the Delaware River basin and in southern New Jersey: U.S. Geol. Survey Water-Supply Paper 1669-N, p. N1-N45, 1963. 1-64. Reservoir storage on streams having log-normal distributions of annual discharge: U.S. Geol. Survey Prof. Paper 475-D, p. D192-D193, 1964. 746-002 0-64- 20A296 PUBLICATIONS IN FISCAL YEAR 1964 HARRIS, E. E. 1-63. (and RANTZ, S. E.) Effect of urban growth on streamflow regimen of Permanente Creek, Santa Clara County, California: U.S. Geol. Survey open-file report, 35 p., 1963. HARRIS, H. B. 1- 63. (MOORE, G. K„ and WEST, L. R.) Geology and ground-water resources of Colbert County, Alabama Alabama Geol. Survey County Rept. 10, 71 p., 1963. 2- 63. (PEACE, R. R., Jr., and HARRIS, W. F„ Jr.) Geology and ground-water resources of Lauderdale County, Alabama: Alabama Geol. Survey County Rept. 8, 178 p., 1963. 1-64. Ground-water resources of La Salle and McMullen Counties, Texas: U.S. Geol.Survey open-file report, 160 p., 1964. HARRIS, L. D. 1-63. (and MILLER, R. L.) Geology of the Stickleyville quadrangle, Virginia: U.S. Geol. Survey Geol. Quad. Map GQ-238, 1963. 1-64. Facies relations of exposed Rome Formation and Conasauga Group of northeastern Tennessee with equivalent rocks in the subsurface of Kentucky and Virginia, in Geol. Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B25-B29, 1964; [abs.], Tennessee Acad. Sci. Jour., v. 39, no. 2, p. 66, 1964. HARRIS, W. H. 1-64. (and WILDER, H. B.) Ground-water supply of Cape Hatteras National Seashore Recreational area, North Carolina—Pt. 3: U.S. Geol. Survey open-file report,35p., 1964. HARRISON, J. E. 1- 63. (and JOBIN, D. A.) Geology of the Clark Fork quadrangle, Idaho-Montana: U.S. Geol. Survey Prof. Paper 1141-K, p. K1-K38, 1963. 2- 63. (and CAMPBELL, A. B.) Correlations andproblems in Belt Series stratigraphy, northern Idaho and western Montana: Geol. Soc. America Bull., v. 74, no. 12, p. 1413-1428, 1963. HARSHMANN, E. N. 1-63. Uranium deposits and related alteration, Shirley Basin, Carbon County, Wyoming: Mining Eng., v. 15, no. 8, p. 53, 1963. 1- 64. Geologic map of the Bates Creek quadrangle, Carbon and Natrona Counties, Wyoming: U.S. Geol. Survey open-file report, map, 1964. 2- 64. Geologic map of the Chalk Hills quadrangle, Albany and Carbon Counties, Wyoming: U.S. Geol. Survey open-file report, map, 1964. 3- 64. Geologic map of the Horse Peak quadrangle. Carbon and Natrona Counties, Wyoming: U.S. Geol. Surveyopen-file report, map, 1964. 4- 64. Geologic map of the Measel Spring Reservoir quadrangle, Carbon County, Wyoming: U.S. Geol. Survey open-file report, map, 1964. 5- 64. Geologic map of the Moss Agate Reservoir quadrangle, Carbon County, Wyoming: U.S. Geol. Survey open-file report, map, 1964. 6- 64. Geologic map of the Mud Springs quadrangle. Carbon and Natrona Counties, Wyoming: U.S. Geol. Survey open-file report, map, 1964. 7- 64. Geologic mapof the Squaw Spring quadrangle, Albany, Carbon, Converse, and Natrona Counties, Wyoming: U.S. Geol. Survey open-file report, map, 1964. 8- 64. Geologic map of the Wild Irish Reservoir quadrangle, Carbon County, Wyoming: U.S. Geol. Survey open-file report, map, 1964. HART, D. L., Jr. 1-63. Ground water in the alluvial deposits of the Washita River between Clinton and Anadarko, Oklahoma: U.S. Geol. Survey open-file report, 49 p., 1963. HARTSHORN, J. H. 1-64. (and ATHERTON, J. S.) Preliminary surficial geology of the Bashbish Falls quadrangle, Massachusetts-Connecticut-New York: U.S. Geol. Survey open-file report, 12 p., map, 1964. HARVEY, E. J. 1-63. (and GRANTHAM, P. E.) Interim report on the hydrology of the Cockfield formation in the vicinity of Jackson, Mississippi: Mississippi Board Water Comm. Bull. 63-6, 19 p„ 1963. 1-64. (CALLAHAN, J. A., and WASSON, B. E.) Ground-water resources of Hinds, Madison, and Rankin Counties, Mississippi: Mississippi Board Water Comm. Bull. 64-1, 38 p., 1964. HATCH, N. L., Jr. 1-63. Geology of the London quadrangle, Kentucky: U.S. Geol. Survey Geol. Quad. Map GQ-245, 1963. 1-64. Geology of the Shopville quadrangle, Kentucky: U.S. Geol. Survey Geol. Quad. Map GQ-282, 1964. HATHAWAY, J. C. 1-63. Mineralogy: Woods Hole Oceanog. Inst. Summ. Inv. Conducted 1962, Reference no. 63-18, Chemistry-Geology, p. 23, 1963. HAWLEY, C. C. 1-63. Formation of beryllium-bearing greisens, Lake George area. Park County, Colorado [abs.]: Mining Eng., v. 15, no. 11, p. 59, 1963. 1- 64. Genetic relation of Pikes Peak granite and beryllium-bearing greisens. Lake George area, Park County, Colorado [abs.]: Geol. Soc. America Spec. Paper 76, p. 276, 1964. 2- 64. Geology of the Pikes Peak granite and associated ore deposits, Lake George beryllium area. Park County, Colorado: U.S. Geol. Survey open-file report, 283 p., 1964. HAYNES, D. D. 1-63. Geology of the Lucas quadrangle, Kentucky: U.S. Geol. Survey Geol. Quad. Map GQ-251, 1963. HAYNES, G. L„ Jr. 1-64. Effect of seiches and setup on the elevation of Elephant Butte Reservoir, N. Mex., in Geol. Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B158-B162, 1964. HAZLEWOOD, R. M. 1-64. Simple Bouguer gravity map of the northern part of the Black Hills, South Dakota: U.S. Geol. Survey open-file report, map, 1964. HEALEY, D. L. 1-63. (and MILLER, C. H.) Gravity survey of the Gold Meadows stock, Nevada Test Site, Nye County, Nev.: U.S. Geol. Survey Prof. Paper 475-B, p. B64-B66, 1963. HEALY, J. H. 1-63. Crustal structure along the coast of California from seismic-refraction measurements: Jour. Geophys. Research, v. 68, no. 20, p. 5777-5787, 1963. 1- 64. (WARREN, D. H., and JACKSON, W. H.) Crustal structure in southern Mississippi from seismic-refraction measurements [abs.]: Soc. Explor. Geophysicists 1964 Year Book, p. 208, 1964. 2- 64. (and WARRICK, R. E.) Digital processing of refraction seismograms [abs.]: Am. Geophys. Union Trans., v. 45, no. 1, p. 92, 1964. HEATH, R. C. 1-63. Ground water in New York State: The Conservationist, v. 18, no. 1, p. 8-14, 1963. 1- 64. Ground water in New York: New York Water Resources Comm. Bull. GW-51, map, 1964. 2- 64. "Lazy" thermometers and their use in measurin; ground-water temperatures: U.S. Geol. Survey Prof Paper 475-D, p. D216-D218, 1964. 3- 64. Seasonal temperature fluctuations in surficial sand near Albany, N. Y.: U.S. Geol. Survey Prof. Paper 475-D, p. D204-D208, 1964.LIST OF PUBLICATIONS A297 HEDGE, Carl E. 1-63. The role of Sr87 in crustal evolution [abs.]: Internal Union Geodesy and Geophysics, General Assembly, 13th, Berkeley, Calif., Aug. 1963, Abs. Papers, v. 9, p. 41, 1963. 1 - 64. Significance of radiogenic strontium in volcanic lavas [abs.]: Am. Geophys. Union Trans., v. 45, no. 1, p. 114, 1964. HEIDEL, S. G. 1-63. (and OTTON, E. G.) Geochemistry of water in the Salisbury, Maryland well field: U.S. Geol. Survey open-file report, 44 p., 1963. HELY, A. G. 1- 63. Determination of areal variations of mean annual runoff [abs.]: Am. Geophys. Union Trans., v. 44, no. 4, p. 871, 1963. 2- 63. (and OLMSTED, F. H.) Some relations between streamflow characteristics and the environment in the Delaware River region: U.S. Geol. Survey Prof. Paper 417-B, p. B1-B25, 1963. HELZ, A. W. 1- 64. A gas jet for d-c arc spectroscopy: U.S. Geol. Survey Prof. Paper 475-D, p. D176-D178, 1964. 2- 64. Review of "Spektralanalyse von Mineralien und Gesteinen" by Horst Moenke: Anal. Chemistry, v. 36, no. 3, p. 73-A, 1964. HEM, J. D. 1- 63. Aqueous solutions, in U. S. National Report, 1960- 1963, 13th General Assembly, International Union of Geodesy and Geophysics: Am. Geophys. Union Trans, v. 44, no. 2, p. 518-520, 1963. 2- 63. Chemical equilibria affecting the behavior of manganese in natural water: Internat. Assoc. Sci. Hydrology Bull., v. 8, no. 3, p. 30-37, 1963. 3- 63. Some aspects of chemical equilibrium in ground water: Ground Water, v. 1, no. 3, p. 30-34, 1963. 4- 63. Increased oxidation rate of manganese ions in contact with feldspar grains: U.S. Geol. Survey Prof. Paper 475-C, p. C216-C217, 1963. 1-64. Deposition and solution of manganese oxides: U.S. Geol. Survey Water-Supply Paper 1667-B, p. B1-B42, 1964. HEMBREE, C. H. 1-64. (and BLAKEY, J. F.) Chemical quality of surface waters in the Hubbard Creek watershed, Texas, progress report, September, 1963: U.S. Geol. Survey open-file report, 86 p., 1964. HEMLEY, J. J. 1-63. (and HOSTETLER, P. B.) A discussion: Facies and types of hydrothermal alteration: Econ. Geology, v. 58, no. 5, p. 808-811, 1963. HENBEST, L. G. 1- 63. Biology, mineralogy, and diagenesis of some typical late Paleozoic sedentary Foraminifera and algal-forami -niferal colonies: Cushman Found. Foram. Research Spec. Pub. 6, p. 1-44, 1963. 2- 63. Type section of MorowSeries, Lower Pennsylvanian, Washington County, Arkansas [abs.]: Shale Shaker, v. 14, no. 2, p. 7-8, 1963. HENDERSON, J. R. 1-63. (ZEITZ, Isidore, and WHITE, W. S.) Preliminary interpretation of an aeromagnetic survey in central and southwestern Iowa: U.S. Geol. Survey open-file report, 30 p., 1963. HENDERSON, R. G. 1- 64. (and WILSON, Alphonso) Polar charts for calculating aeromagnetic anomalies of three-dimensional bodies: U.S. Geol. Survey open-file report, 13 p., 1964. 2- 64. (and ALLINGHAM, J. W.) The magnetization of an inhomogeneous laccolith calculated on a digital computer: Stanford Univ. Pub., Geol. Sci., v. 9, no. 2, p. 481-497, 1964. HENDRICKSON, G. E. 1-63. Ground water for public supply in St. Croix, Virgin Islands: U.S. Geol. Survey Water-Supply Paper 1663-D, p. D1-D27, 1963. HERRICK, S. M. 1-63. (and VORHIS, R. C.) Subsurface geology of the Georgia coastal plain: Georgia Geol. Survey Inf. Circ. 25, 79 p„ 1963. 1- 64. Foraminiferal fauna of Late Miocene age from Georgia and South Carolina [abs.]: Geol. Soc. America, Southeastern Sec., 1964 Ann. Mtg., Baton Rouge, April 1964, Program, p. 23-24, 1963. 2- 64. Subsurface study of Pleistocene deposits in coastal Georgia [abs.]: Geol. Soc. America Spec. Paper 76, p. 245, 1964. ■ 3- 64. (and LeGRAND, H. E.) Solution subsidence of a limestone terrane in southwest Georgia: Internat. Assoc. Sci. Hydrology Bull., v. 9, no. 2, p. 25-36, 1964. HERSHEY, L. A. 1-64. (and SCHNEIDER, P. A., Jr.) Ground-water investigations in the lower Cache la Poudre River basin, Colorado: U.S. Geol. Survey Water-Supply Paper 1669-X, p. X1-X22, 1964. HEYL, A. V. 1- 63. Oxidized zinc deposits of the United States. Part 2. Utah: U.S. Geol. Survey Bull. 1135-B, p. B1-B104, 1963. 2- 63. (HOSTERMAN, J. W„ and BROCK, M. R.) Clay alteration in the Upper Mississippi Valley zinc-lead district [abs.], in Program and Abstracts, 12th Natl. Clay Conf., p. 16, 1963. 1- 64. (and BOZION, C. N.) Oxidized zinc districts in California and Nevada:U.S. Geol. Survey Mineral Inv. Resource Map MR-39, 2 sheets, 1964. 2- 64. (HOSTERMAN, J. W., HALL, W. E., and BROCK, M. R.) Clay-mineral alterations and other coordinated geochemical studies in the Upper Mississippi Valley zinc-lead district--A progress report [abs.], in A. T. Broderick, ed., Tenth Ann. Inst, on Lake Superior geology, Ishpeming, Mich., p. 46-47, 1964. HIETANEN, Anna 1- 63. Anorthosite and associated rocks in the Boehls Butte quadrangle and vicinity, Idaho: U.S. Geol. Survey Prof. Paper 344-B, p. B1-B78, 1963. 2- 63. Idaho batholith near Pierce and Bungalow, Clearwater County, Idaho: U.S. Geol. Survey Prof. Paper 344-D, p. D1-D42, 1963 [1964]. 3- 63. Metamorphism of the Belt series in the Elk River-Clarkia area, Idaho: U.S. Geol. Survey Prof. Paper 344-C, p. C1-C49, 1963 [1964]. HILL, D. P. 1- 63. (and PAKISER, L. C.) Crustal structure from seis- mic refraction measurements between Eureka, Nevada, and Boise, Idaho -[abs.]: Am. Geophys. Union Trans., v. 44, no. 4, p. 890, 1963. 2- 63. Gravity and crustal structure in the western Snake River Plain, Idaho: Jour. Geophys. Research, v. 68, no. 20, p. 5807-5819, 1963. HIRASHIMA, G. T. 1-63. Influence of water-development tunnels on stream-flow-ground-water relations in Haiku-Kahaluu area, Oahu, Hawaii: Hawaii Dept. Land and Nat. Resources, Div. Water and Land Devel. Circ. C21, 11 p., 1963. HOBBS, H. H., Jr. 1-64. (and BEDINGER, M. S.) A new troglobitic crayfish of the genus Cambarus (Decapoda, Astacidae) from Arkansas with a note on the range of Cambarus cryptodvtes: Biol. Soc. Washington Proc., v. 77, p. 9-16, 1964. HODGES, A. L., Jr. 1-63. (and ROGERS, S. M., and HARDER, A. H.) Gas and brackish water in fresh-water aquifers. Lake Charles area, Louisiana: Louisiana Dept. Conserv. Geol. Survey and Louisiana Dept. Public Works Water Resources Pamph. 13, 35 p., 1963.A298 PUBLICATIONS IN FISCAL YEAR 1964 HODSON, W. G. 1-63. Geology and ground-water resources of Wallace County, Kansas: Kansas Geol. Survey Bull. 161, 108 p., 1963. HOFMANN, Walter 1-63. (and RANTZ, S. E.) Floods of December 1955-Janu-ary 1956 in the Far Western States— Pt. 1, Description: U.S. Geol. Survey Water-Supply Paper 1650-A, p. Al-A156, 1963. HOGENSON, G. M. 1-64. Geology andground water of the Umatilla River basin, Oregon: U.S. Geol. Survey Water-Supply Paper 1620, 162 p., 1964. HOLLAND, P. H. 1- 64. Base flow* of Guadalupe River, Comal County, Texas, March 1962: U.S. Geol. Survey open-file report, 13 p., 1964. 2- 64. (and HUGHES, L. S.) Base-flow studies, Pedernales River, Texas, quantity and quality, April-May 1962: Texas Water Comm. Bull. 6407, 11 p., 1964. 3- 64. (and MENDIETA, H. B.) Base flow studies-quantity and quality of base flow of Llano River Texas: U.S. Geol. Survey open-file report, 28 p., 1964. 4- 64. (and WELBORN, C. T.) Quantity and quality of the base flow of Cibolo Creek, Texas, March 5-7, 1963: U.S. Geol. Survey open-file report, 29 p., 1964. HOLMBERG, G. D. 1-63. Status of ground-water storage in the Columbia River basin in 1963: Columbia Basin Water Forecast Comm., 26th Ann. Mtg., Portland, Oregon, April 1963, Proc., p. 17-23, 1963. HOLMES, G. W. 1- 64. Preliminary materials map, Ashley Falls quadrangle, Massachusetts-Connecticut: U.S. Geol. Surveyopen-file report, map, 1964. 2- 64. Preliminary materials map, Massachusetts portion of the Egremont quadrangle, Massachusetts-New York: U.S. Geol. Survey open-file report, map, 11 data sheets, 1964. 3- 64. Preliminary materials map, Massachusetts portion of the State Line quadrangle, Massachusetts-New York: U.S. Geol. Survey open-file report, map, 11 data sheets, 1964. 4- 64. Preliminary materials map, Monterey quadrangle, Massachusetts: U.S. Geol. Survey open-file report, map, 1964. 5- 64. Preliminary materials map,Stockbridge quadrangle, Massachusetts: U.S. Geol. Survey open-file report, map, 7 data sheets, 1964. 6- 64. Preliminary materials map of the Great Barrington quadrangle, Massachusetts: U.S. Geol. Survey open-file report, map, 21 data sheets, 1964. 7- 64. Preliminary materials map of the South Sandisfield quadrangle, Massachusetts-Connecticut: U.S. Geol. Survey open-file report, map, 9 data sheets, 1964. 8- 64. (and ANDERSEN, B. G.) Glacial chronology of Ulls-fjord, northern Norway: U.S. Geol. Survey Prof. Paper 475-D, p. D159-D163, 1964. HOLT, C. L. R., Jr. 1-63. Ground-water resources of Portage County, Wisconsin: U.S. Geol. Survey open-file report, 147 p., 1963. HOLT, R. J. 1-63. (PETERSEN, R. G., and MURPHY, V. J.) Seismic studies of buried valleys in southern New England[abs.]: Geol. Soc. America Spec. Paper 76, p. 82 A, 1963. HOOD, J. W. 1-63. Tularosa and Hueco Bolsons, New Mexico and Texas, in Effects of drought in basins of interior drainage, by H. E. Thomas and others: U.S. Geol. Survey Prof.Pa-per 372-E, p. E3-E6, 1963. HOOKER, Marjorie 1-63. Ten-year supplement to the bibliographies of Clarence S. Ross andWaldemar T.Schaller: Am. Mineralogist, v. 48, no. 11-12, p. 1410-1412, 1963. HOOVER, D. B. 1-64. Unmanned ten-day seismic-recording system [abs.]: Am. Geophys. Union Trans., v. 45, no. 1, p. 93, 1964. HOOVER, D. L. 1-64. Flow structures in a welded tuff, Nye County, Nevada [abs.]: Geol. Soc. America Spec. Paper 76, p. 83, 1964. HOPKINS, D. M. 1-63. Geology of the Imuruk Lake area, Seward Peninsula, Alaska: U.S. Geol. Survey Bull. 1141-C, p. C1-C101, 1963 [1964], HORN, G. H. 1-63. Geology of the east Thermopolis area, Hot Springs and Washakie Counties, Wyo.: U.S. Geol. Survey Oil and Gas Inv. Map OM-213, 1963. HOSE, R. K. 1- 63. Geologic map and section of the Cowboy Pass NE quadrangle, Confusion Range, Millard County, Utah: U.S. Geol. Survey Misc. Geol. Inv. Map 1-377, 1963. 2- 63. Geologic map and sections of the Cowboy Pass SE quadrangle. Confusion Range, Millard County, Utah: U.S. Geol. Survey Misc. Geol. Inv. Map 1-391, 1963 [1964]. 3- 63. (and REPENNING, C. A.) Geologic map and sections of the Cowboy Pass NW quadrangle, Confusion Range, Millard County, Utah: U.S. Geol. Survey Misc. Geol. Inv. Map 1-378, 1963. 4- 63. (and ZIONY, J. I.) Geologic map and sections of the Gandy NE quadrangle. Confusion Range, Millard County, Utah: U.S. Geol. Survey Misc. Geol. Inv. Map 1-376, 1963 [1964]. 1- 64. (and REPENNING, C. A.) Geologic map and sections of the Cowboy Pass SW quadrangle, Confusion Range, Millard County, Utah: U.S. Geol. Survey Misc. Geol. Inv. Map 1-390, 1964. 2- 64. (and ZIONY, J. I.) Geologic map and sections of the Gandy SE quadrangle, Confusion Range, Millard County, Utah: U.S. Geol. Survey Misc. Geol. Inv. Map 1-393, 1964. HOSKINS, D. M. 1-63. (ARNDT, H. H., WOOD, G. H., Jr., CONLIN, R. R„ DYSON, J. L., and TREXLER, J. P.) Lithology, subdivision and correlation of the Catskill Formation in east-central Pennsylvania, in Symposium on Middle and Upper stratigraphy of Pennsylvania and adjacent states: Pennsylvania Geol. Survey Bull. G-39, p. 147-163, 1963. HOSTERMAN, J. W. 1-63. Structure-contour map of the Olive Hill Clay Bed in northeastern Kentucky: U.S. Geol. Survey Mineral Inv. Field Studies Map MF-261, 1963. 1-64. (OVERSTREET, W. C., and WARR, J. J., Jr.) Thorium and uranium in monazite from Spokane County, Wash.: U.S. Geol. Survey Prof. Paper 475-D, p. D128-D130, 1964. HOSTETLER, P. B. 1- 63. The degree of saturation of magnesium and calcium carbonate minerals in natural waters: Internat. Assoc. Sci. Hydrology Pub. 64, Subterranean Waters Comm., p. 34-49, 1963. 2- 63. Complexing of magnesium with bicarbonate: Jour. Physical Chemistry, v. 67, p. 720-721, 1963. 3- 63. The degree of saturation of Mg and Ca carbonate minerals in natural waters [abs.]: Internat. Union Geodesy and Geophysics, General Assembly, 13th, Berkeley, Calif., Aug. 1963, Abstracts of Papers, v. 8, p. 12, 1963. HOTZ, P. E. 1- 64. (and WILLDEN, Ronald) Geology and mineral deposits of the Osgood Mountains quadrangle, Humboldt County, Nev.: U.S. Geol. Survey Prof. Paper 431, 128 p., 1964. 2- 64. Nickeliferous laterites in southwestern Oregon and northwestern California: Econ. Geology, v. 59, no. 3, p. 355-396, 1964. HUBBELL, D. W. 1-64. (and SAYRE, W. W.) Sand transport studies with radioactive tracers: Am. Soc. Civil Engineers Proc., v. 90, Jour. Hydraulics Div., no. HY3, Pt. 1, p. 39-68, 1964.LIST OF PUBLICATIONS A299 HUDDLE, J. W. 1-63. Conodonts from the Flynn Creek cryptoexplosive structure, Tennessee: U.S. Geol. Survey Prof. Paper 475-C, p. C55-C57, 1963. 1-64. Cavusgnathus, Idiognathoides, and Polygnathodella: a conodont nomenclatural and biologic problem: Jour. Paleontology, v. 38, no. 2, p. 400-401, 1964. HUFF, L. C. 1-63. Comparison of geological, geophysical, and geochemical prospecting methods at the Malachite mine, Jefferson County, Colo: U.S. Geol. Survey Bull. 1098-C, p. 161-179, 1963. HUGHES, G. H. 1-64. (and MCDONALD, C. C.) Operation of evapotrans-piration tanks near Yuma, Arizona: U.S. Geol. Survey open-file report, 14 p., 1964. HUGHES, L. S. 1-63. (and SHELBY, Wanda) Chemical composition of Texas surface waters, 1961: Texas Water Comm. Bull. 6304, 123 p., 1963. 1- 64. (and BLAKEY, J. F.) Chemical composition of Texas surface waters, 1962: U.S. Geol. Survey open-file report, 1964. 2- 64. (and LEIFESTE, D. K.) Rfeconnaissance of the chemical quality of surface waters of the Sabine River basin, Texas and Louisiana: Texas Water Comm. Bull. 6405, 64 p., 1964. HULSING, Harry 1-64. (and KALLIO, N. A.) Magnitude and frequency of floods intheUnited States,—Pt. 14, Pacific slope basins in Oregon and lower Columbia River basin: U.S. Geol. Survey Water-Supply Paper 1689, 320 p., 1964. HUMPHREYS, C. P., Jr. 1-63. Floods of 1959 in Mississippi: Mississippi Board Water Comm. Bull. 63-8, 19 p., 1963. HUNT, O. P. 1-63. Use of low-flow measurements to estimate flow-duration curves: U.S. Geol. Survey Prof. Paper 475-C, p. C196-C197, 1963. HURLEY, P. M. 1-64. (BATEMAN, P. C., FAIRBAIRN, H. W., and PINSON, W. H.) Preliminary investigation of Sr87_Rb87 relationships in the Sierra Nevada plutonic rocks [abs.J: Geol. Soc. America Spec. Paper 76, p. 85, 1964. HUXEL, C. J., Jr. 1-63. (and PETRI, L. R.) Geology and ground-water resources of Stutsman County, North Dakota,—Pt. 2, Ground water basic data: North Dakota Geol. Survey Bull. 41; and North Dakota State Water Conserv. Comm. County Ground Water Studies 2, 339 p., 1963. IMLAY, R. W. 1-64. Middle and Upper Jurassic fossils from southern California: Jour. Paleontology, v. 38, no. 3, p. 505-509, 1964. INTER-AGENCY SEDIMENTATION PROJECT 1-63. A summary of the work of the Federal Inter-Agency Sedimentation Project: Inter-Agency Report S, 29 p., 1963. IRELAN, B. 1-64. Trends in quality of water on the lower Colorado River: U.S. Geol. Survey open-file report, 13 p., 1964. IRWIN, W. P. 1-63. Preliminary geologic map of the Weaverville quadrangle, California: U.S. Geol. Survey Mineral Inv. Field Studies Map MF-275, 1963 [1964]. ISBISTER, J. 1-64. Geology and hydrology of northeastern Nassau County, Long Island, New York: U.S. Geol. Survey open-file report, 194 p., 1964. ISHERWOOD, W. L. 1-63. Digital water-stage recorder, jjiSelectedtechniques in water resources investigations, compiled by G. N. Mesnier and K. T. Iseri: U.S. Geol. Survey Water-Supply Paper 1669-Z, p. Z13-Z16, 1963. ISTO, R. E. 1-63. (and KESAM, Philip) Discussion of paper "Measuring the precision of a level," by Sumner B. Irish: Am. Soc. Civil Engineers Proc., v. 89, Jour. Surveying and Mapping Div., no. SU3, p. 191-192, 1963. IZETT, G. A. 1- 63. (and HOOVER, D. L.) Preliminary geologic map of the Hot Sulphur Springs SE quadrangle, Grand County, Colo.: U.S. Geol. Survey Mineral Inv. Field Studies Map MF-271, 1963. 2- 63. (and LEWE, G. E.) Miocene vertebrates from Middle Park, Colo.: U.S. Geol. Survey Prof. Paper 475-B, p. B120-B122, 1963. JACKSON, E. D. 1-63. Stratigraphic and lateral variation of chromite compositions in the Stillwater complex in_ Internat. Mineral-log. Assoc., 3d Gen. Mtg., 1962, Papers and Proc.: Mineralog. Soc. America Spec. Paper 1, p. 46-54, 1963. JACKSON, W. H. 1-63. (STEWART, S. W., and PAKEER, L. C.) Crustal structure in eastern Colorado from seismic-refraction measurements: Jour. Geophys. Research, v. 68, no. 20, p. 5767-5776, 1963. 1-64. (and TIBBETTS, B. L.) Lake Superior seismic experiment: U.S. Geol. Survey open-file report, 4 p., 1964. JACOB, C. E. 1- 63. Correction of drawdowns caused by a pumped well tapping less than the full thickness of an aquifer, in Methods of determining permeability, transmissibility and drawdown, compiled by Ray Bentall: U.S. Geol. Survey Water-Supply Paper 1536-1, p. 272-282, 1963. 2- 63. Determining the permeability of water-table aquifers, in Methods of determining permeability, transmissibility, and drawdown, compiled by Ray Bentall: U.S. Geol. Survey Water-Supply Paper 1536-1, p. 245-271, 1963. 3- 63. The recovery method for determining the coefficient of transmissibility, in Methods of determining permeability, transmissibility, and drawdown, compiled by Ray Bentall: U.S. Geol. Survey Water-Supply Paper 1536-1, p. 283-292, 1963. JACOBSON, H. S. 1-63. Integrated mineral exploration at Phu Hin Lek Fai Loei--Chiengkarn area, Thailand, in Proceedings of the seminar on geochemical prospecting methods and techniques, Bangkok, 1963: New York, United Nations Econ. Comm. Asia and Far East (ECAFE), Mineral Resources Devel. Ser. no. 21, p. 175-177, 1963. JAHREN, C. E. 1-63. Magnetic susceptibility of bedded iron-formation: Geophysics, v. 28, no. 5 (pt. 1), p. 756-766, 1963. JENKINS, C. T. 1- 63. Floods on St. Vrain and Lefthand Creeks at Longmont, Colorado: U.S. Geol. Survey open-file report, 39 p., 1963. 2- 63. Field verification of computation of peak discharge through culverts: U.S. Geol. Survey Prof. Paper 475-C, p. C194-C195, 1963. 3- 63. Graphical multiple-regression analysis of aquifer tests: U.S. Geol. Survey Prof. Paper 475-C, p. C198-C201, 1963. JENKINS, E. D. 1-64. Ground water in Fountain and Jimmy Camp Valleys, El Paso County, Colorado, with a section on Computations of drawdowns caused by the pumping of wells in Fountain Valley, by R. E. Glover and E. D. Jenkins: U.S. Geol. Survey Water-Supply Paper 1583, 66 p., 1964. JENSEN, F. S. 1-64. (and VARNES, H. D.) Geology of the Fort Peck area, Garfield, McCone and Valley Counties, Montana: U.S. Geol. Survey Prof. Paper 414-F, p. F1-F49, 1964. JENSEN, H. M. 1-63. (and BRADLEY, E.) Ground water in the vicinity of Hillsboro, Traill County, North Dakota: North DakotaA300 PUBLICATIONS IN FISCAL YEAR 1964 JENSEN, H. M.—Continued State Water Conserv. Comm. Ground-Water Studies 55, 18 p., 1963. JESPERSEN, Anna 1-64. Aeromagnetic prospecting for bauxite deposits in the Mississippi embayment, Arkansas and Missouri: U.S. Geol. Survey Geophys. Inv. Map GP-370, 1964. JOBIN, D. A. 1-64. (and SOISTER, P. E.) Geologic map ofthe Thompson Peak quadrangle, Bonneville County, Idaho: U.S. Geol. Survey Mineral Inv. Field Studies Map MF-284, 1964. JOHNSON, A. I. 1- 63. An outline of equipment useful for hydrologic studies: U.S. Geol. Survey open-file report, 23 p., 1963. 2- 63. Application of laboratory permeability data: U.S. Geol. Survey open-file report, 4 p., 1963. 3- 63. Compilation of specific yield for various materials: U.S. Geol. Survey open-file report, 1 p., 1963. 4- 63. Geophysical logging of boreholes for hydrologic studies: U.S. Geol. Survey open-file report, 10 p., 1963. 5- 63. Training aids--Hydrologic laboratory; Symbols and definitions from soil mechanics and soil physics; Design of well screen and filter pack; Portable equipment for borehole exploration; Modified Parshall flume: U.S. Geol. Survey open-file report, 46 p., 1963. 6- 63. Typical coefficients of permeability: U.S. Geol. Survey open-file report, 1 p., 1963. 7- 63. (PRILL, R. C., and MORRIS, D. A.) Specific yield-Column drainage and centrifuge moisture content: U.S. Geol. Survey Water-Supply Paper 1662-A, p. A1-A60, 1963. 1-64. Selected bibliography on laboratory and field methods in ground-water hydrology: U.S. Geol. Survey Water-Supply Paper 1779-Z, p. Z1-Z21, 1964. JOHNSON, Arthur 1-63. Waterpower investigations of lakes in Alaska: U.S. Geol. Survey Prof. Paper 475-B, p. B176-B178, 1963. 1-64. Glacier observations. Glacier National Park, Montana 1964: U.S. Geol. Survey open-file report, 23 p., 1964. JOHNSON, C. G. 1-63. Status of geological and geophysical study of the islands of the western north Pacific, in Tenth Pacific Science Congress Ser., Geology and Solid Earth Geophysics of the Pacific Basin, Report of the Standing Committee: Univ. Hawaii Press, p. 155-160, 1963. JOHNSON, J. Harlan 1-64. Fossil and Recent calcareous algae from Guam: U.S. Geol. Survey Prof. Paper 403-G, p. G1-G40, 1964. JOHNSON, R. B. 1- 64. Walsen composite dike near Walsenburg, Colo., in Geol. Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B69-B73, 1964. 2- 64. (and EGE, J. R.) Geology of the Pluto Site, Area 401, Nevada Test Site, Nye County, Nevada: U.S. Geol.Survey Rept. TEI-841 (open-file report), 128 p., 1964. JOHNSON, W. D., Jr. 1-64. (and SMITH, H. R.) Geology of the Winnett-Mosby area, Petroleum, Garfield, Rosebud, and Fergus Counties, Montana: U.S. Geol. Survey Bull. 1149, 91 p., 1964. JOHNSTON, P. M. 1-63. (and OTTON, E. G.) Availability of ground water for urban and industrial development in upper Montgomery County, Maryland: Maryland-Natl. Capital Park and Plan. Comm, and Maryland Dept. Geology, Mines and Water Resources, 47 p., 1963. 1- 64. Geology and ground-water resources of Washington, D. C., and vicinity, with a section on Chemical quality of the water, by D. E. Weaver and Leonard Siu: U.S. Geol. Survey Water-Supply Paper 1776, 97 p., 1964. 2- 64. Ground-water conditions during 1963 at the Marine Corps Base, Twentynine Palms, California: U.S. Geol. Survey open-file report, 36 p., 1964. JOLLY, J. L. 1- 64. (and HEYL, A. V.) Mineral paragenesis and zoning in the central Kentucky mineral districts: Econ. Geology, v. 59, no. 4, p. 596-624, 1964. 2- 64. (and HEYL, A. V.) Zoning in the central Kentucky mineral district [abs.]: Geol. Soc. America Spec. Paper 76, p. 87-88, 1964. JONES, B. F. 1-64. Layer sequence of saline minerals at Deep Spring Lake, California [abs.]: Geol. Soc. America Spec. Paper 76, p. 88, 1964. JONES, B. L. 1-64. Sedimentation and land use in Corey Creek and Elk River basins, Pennsylvania, 1954-60, a progress report: U.S. Geol. Survey open-file report, 132 p., 1964. JONES, D. L. 1-63. Upper Cretaceous (Campanian and Maestrichtian) ammonites from southern Alaska: U.S. Geol. Survey Prof. Paper 432, 53 p., 1963 [1964]. JONES, J. R. 1-63. (AKIN, P. D., and SCHNEIDER, Robert) Geologyand ground-water conditions in the southern part of the Camp Ripley Military Reservation, Morrison County, Minn.: U.S. Geol. Survey Water-Supply Paper 1669-A, p. Al-A32, 1963 [1964], 1-64. Water for municipal use at Agedabia, Libya: U.S. Geol. Survey open-file report, 23 p., 1964. JONES, P. H. 1-63. Hydrology of waste disposal. National Reactor Testing Station, Idaho, with special reference to the Idaho Chemical Processing Plant area, and the Materials Testing reactor—Engineering test reactor area: U.S. Geol. Survey open-file report, 42 p., 1963. 1-64. The velocity of ground-water flow in basalt aquifers of the Snake River Plain, Idaho: Internat. Assoc. Sci. Hydrology Pub. 64, p. 225-234, 1964. JONES, W. R. 1-63. Hydrogen metasomatism in silicate rocks [abs.]: Mining Eng., v. 15, no. 11, p. 59, 1963. 1-64. (CASE, J. E., and PRATT, W. P.) Aeromagnetic and geologic map of part of the Silver City mining region. Grant County, N. Mex.: U.S. Geol. Survey Geophys. Inv. Map GP-424, 1964. JOPLING, A. V. 1- 63. Hydraulic studies on the origin of bedding: Sedi-mentology, v. 2, p. 115-121, 1963. 2- 63. Effect of base-level changes on bedding development in a laboratory flume: U.S. Geol. Survey Prof. Paper 475-B, p. B203-B204, 1963. 1-64. Interpreting the concept of the sedimentation unit: Jour. Sed. Petrology, v. 34, no. 1, p. 165-172, 1964. JORDAN, P. R. 1- 64. Fluvial sediment of the Mississippi River at St. Louis, Missouri: U.S. Geol. Survey open-file report, 149 p., 1964. 2- 64. (JONES, B. F., and PETRI, L. R.) Chemical quality of surface waters and sedimentation in the Saline River basin, Kansas: U.S. Geol. Survey Water-Supply Paper 1651, 90 p., 1964. JOYNER, B. F. 1-63. Iron in Georgia ground water: Georgia Mineral Newsletter, v. 16, nos. 3-4, p. 73-74, 1963. KAM, William 1-64. Geology and ground-water resources of McMullen Valley, Maricopa, Yavapai, and Yuma Counties, Ariz.: U.S. Geol. Survey Water-Supply Paper 1665, 64 p., 1964. KAMMERER, J. C. 1-63. (and BALDWIN, H. L.) Water problems in the Spring -field-Holyoke area. Mass.: U.S. Geol. Survey Water-Supply Paper 1670, 68 p., 1963.LIST OF PUBLICATIONS A301 KANE, M. F. 1-64. Gravity observations and Bouguer anomaly values for northern Maine: U.S. Geol. Survey open-file report, 110 p„ 1964. KAPUSTKA, S. F. 1-63. (HARVEY, E. J., and HUDSON, J. W.) Water resources investigations during fiscal year 1963, Jackson County, Misssisippi: Mississippi Board Water Com. Bull. 63-7, 1963. 1-64. Chemical composition of surface waters of Louisiana 1943-58: Louisiana Dept. Public Works, 187 p., 1964. KARLSTROM, T. N. V. 1-64. Quaternary geology of the Kenai Lowland and glacial history of the Cook Inlet region, Alaska: U.S. Geol. Survey Prof. Paper 443, 69 p., 1964. KAYE, C. A. 1-63. Review of "Principles of soil mechanics" by R. F. Scott: Am. Mineralogist, v. 48, no. 7-8, p. 956-957, 1963. 1- 64. Boulder train of silicified Paleozoic wood, southeastern Massachusetts: Geol. Soc. America Bull., v. 75, no. 3, p. 233-236, 1964. 2- 64. The Pleistocene geology of Martha's Vineyard, Massachusetts: Friends Pleistocene, 27th Ann. Reunion, Martha's Vineyard, Mass., May 23-24, 1964, Field Trip, 19 p., 1964. 3- 64. Upper Cretaceous to Recent stratigraphy of Martha's Vineyard, Massachusetts [abs.]: Geol. Soc. America Spec. Paper 76, p. 91, 1964. 4- 64. (and BARGHOORN, E. S.) Late Quaternary sea-level change and crustal rise at Boston, Massachusetts, with notes on the autocompaction of peat: Geol. Soc. America Bull., v. 75, no. 2, p. 63-80, 1964. 5- 64. Boulder train of silicified Paleozoic wood, southeastern Massachusetts: Geol. Soc. America Bull., v. 75, no. 3, p. 233-236, 1964. KEECH, C. F. 1-63. Ground-water resources of Mirage Flats, Nebraska: U.S. Geol. Survey open-file report, 65 p., 1963. KEEFER, W. R. 1-63. Karst topography in the Gros Ventre Mountains, northwestern Wyoming: U.S. Geol. Survey Prof. Paper 475-B, p. B129-B130, 1963. 1-64. (and TROYER, M. L.) Geology of the Shotgun Butte area, Fremont County, Wyoming: U.S. Geol. Survey Bull. 1157, 123 p., 1964. KEHN, T. M. 1-63. Geology of the Madisonville East quadrangle, Kentucky: U.S. Geol. Survey Geol. Quad. Map GQ-252, 1963. KELLER, Fred, Jr. 1-63. (and HENDERSON, J. R.) Aeromagnetic map of part of the tri-state mining district, Kansas, Missouri, and Oklahoma: U.S. Geol. Survey Geophys. Inv. Map GP-427, 1963. KELLER, G. V. 1- 63. Electrical properties in the deep crust: Antennas and propagation: Trans. Inst. Electrical and Electronics Engineers (IEEE), v. AP-11, no. 3, p. 344-357, 1963. 2- 63. "Industrial and exploratory geophysical prospecting" by K. F. Zhigach [book review): Am. Geophys. Union Trans., v. 44, no. 4, p. 1017, 1963. KENNEDY, Daniel 1-63. Discussion of paper "Photogrammetric engineering and reservoir planning," by Pliny Gale: Am. Soc. Civil Engineers Proc., v. 89, Jour. Surveying and Mapping Div., no. SU3, p. 215, 1963. 1- 64. Discussion of paper "Aerial traverse and maximum bridging distance," by Sandor A. Veres: Am. Soc. Civil Engineers Proc., v. 90, Jour. Surveying and Mapping Div., no. SU1, p. 89, 1964. 2- 64. Discussion of paper "Surveys and maps for industrial growth," by Earle J. Fennell: Am. Soc. Civil Engi- KENNEDY, Daniel--Continued neers Proc., v. 90, Jour. Surveying and Mapping Div., no. SU1, p. 87, 1964. KENNEDY, E. J. 1-63. Streamflow records by digital computer: Am. Soc. Civil Engineers Proc. v. 89, Paper 3625, Jour. Irrig. and Drainage Div., no. IR3, pt. 1, p. 29-36, 1963. KENNEDY, J. F. 1-64. The formation of sediment ripples in closed rectangular conduits and in the desert: Jour. Geophys. Research, v. 69, no. 8, p. 1517-1524, 1964. KENNEDY, V. C. 1-64. Sediment transported by Georgia streams: U.S. Geol. Survey Water-Supply Paper 1668, 101 p., 1964. KENNER, W. E. 1-63. (and CROOKS, J. W.) Surface-water resources of St. Johns, Flagler, and Putnam Counties, Florida: Florida Geol. Survey Inf. Circ. 39, 44 p., 1963. 1-64. Maps showing depths of selected lakes in Florida: Florida Geol. Survey Inf. Circ. 40, 82 p., 1964. KEPFERLE, R. C. 1- 63. Geology of the Cecilia quadrangle, Kentucky: U.S. Geol. Survey Geol. Quad. Map GQ-263, 1963. 2- 63. Geology of the Howe Valley quadrangle, Kentucky: U.S. Geol. Survey Geol. Quad. Map GQ-232, 1963. 1-64. (PETERSON, W. L„ and SABLE, E. G.) Road log, Field Trip No. 2, Saturday, May 2, 1964, in Geologic features of the Mississippian Plateau in the Mammoth Cave and Elizabethtown areas, Kentucky: Geol. Soc. Kentucky Ann. Spring Field Conf. Guidebook, p. 24-32, 1964. KETNER, K. B. 1- 63. (and SMITH, J. F., Jr.) Geology of the Railroad mining district, Elko County, Nev.: U.S. Geol. Survey Bull. 1162-B, p. B1-B27, 1963. 2- 63. Bedded barite deposits of the Shoshone Range, Nev.: U.S. Geol. Survey Prof. Paper 475-B, p. B38-B41, 1963. 3- 63. (and SMITH, J. F., Jr.) Composition and origin of siliceous mudstone in the Carlin and Pine Valley quadrangles, Nevada: U.S. Geol. Survey Prof. Paper 475-B, p. B45-B47, 1963. KILBURN, Chabot 1-63. Ground water in upper part of the Teton Valley, Teton Counties, Idaho and Wyoming: U.S. Geol. Survey open-file report, 125 p., 1963. KILPATRICK, F. A. 1-64. (and BARNES, H. H.) Channel geometry of Piedmont streams as related to frequency of floods: U.S. Geol. Survey Prof. Paper 422-E, p. E1-E10, 1964. KIMMEL, G. E. 1-63. Contamination of ground water by sea-water intrusion along Puget Sound, Wash., an area having abundant precipitation: U.S. Geol. Survey Prof. Paper 475-B, p. B182-B185, 1963. KIMREY, J. O. 1-63. Description of a phosphorite unit in Beaufort County, North Carolina: U.S. Geol. Survey open-file report, 226 p., 1963. KINDSVATER, C. E. 1-64. Discharge characteristics of embankment-shaped weirs: U.S. Geol. Survey Water-Supply Paper 1617-A, p. A1-A114, 1964. KING, E. R. 1-64. (ZIETZ, Isidore, and ALLDREDGE, L. R.) The genesis of the Arctic Ocean basin: Science, v. 144, no. 3626, p. 1551-1557, 1964. KING, P. B. 1- 64. Further thoughts on tectonic framework of southeastern United States [abs.]: Geol. Soc. America Spec. Paper 76, p. 235, 1964. 2- 64. Geology of the central Great Smoky Mountains, Tennessee: U.S. Geol. Survey Prof. Paper 349-C, p. 1-148, 1964.A302 PUBLICATIONS IN FISCAL YEAR 1964 KING, P. B.—Continued 3- 64. Interpretation of the Garden Springs area, Texas, by the "down-structure" method of tectonic analysis, in Geol. Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B1-B8, 1964. 4- 64. Tectonic map of North America [abs.]: Geol. Soc. America Spec. Paper 76, p. 208, 1964. 5- 64. Further thoughts on tectonic framework of southeastern United States: Virginia Polytechnic Inst., Dept. Geol. Sci., Mem. 1, p. 5-31, 1964. KINKEL, A. R. 1-63. Author's reply to "Discussion" by R. W. Hutchinson on "The Ore Knob massive sulfide copper deposit. North Carolina": Econ.. Geology, v. 58, no. 7, p. 1159-1160, 1963. KINNISON, H. B. 1-63. (and SCEVA, J. E.) Effects of hydraulic and geologic factors on streamflow of the Yakima River basin, Washington: U.S. Geol. Survey Water-Supply Paper 1595, 134 p., 1963 [1964], KINOSHITA, W. T. 1-63. (KRIVOY, H. L., MABEY, D. R„ and MacDONALD, R. R.) Gravity survey of the island of Hawaii: U.S. Geol. Survey Prof. Paper 475-C, p. C114-C116, 1963. 1-64. (DAVIS, W. E„ SMEDES, H. W., and NELSON, W. H.) Bouguer gravity, aeromagnetic, and generalized geologic map of Townsend and Duck Creek Pass quadrangles, Broadwater County, Montana: U.S. Geol. Survey Geophys. Inv. Map GP-439, 1964. KIRKEMO, Harold 1-63. Some factors affecting long-range supply of minerals for the United States: Industrial College of the Armed Forces, Washington, D. C., Thesis no. 84, 77 p., 1963. KISTER, L. R. 1-63. (and MUNDORFF, J. C.) Sedimentation and chemical quality of water in Salt Creek basin, Nebraska: U.S. Geol. Survey Water-Supply Paper 1669-H, p. H1-H47, 1963. KISTLER, R. W. 1-64. (BATEMAN, P. C., and BRANNOCK, W. W.) Isotopic ages of minerals from granitic rocks of the east-central Sierra Nevada and Inyo Mountains, California [abs.]: Geol. Soc. America Spec. Paper 76, p. 91-92, 1964. KLASNER, J. S. 1-64. A study of buried bedrock valleys near South Haven, Michigan, by the gravity method: U.S. Geol. Survey open-file report, 39 p., 1964. KLAUSING, R. L. 1-64. (and LOHMAN, K. E.) Upper Pliocene marine strata on the east side of the San Joaquin Valley, Calif.: U.S. Geol. Survey Prof. Paper 475-D, p. D14-D17, 1964. KLEIN, Howard 1-64. (SCHROEDER, M. C., and LITCHTLER, W. F.) Geology and ground-water resources of Glades and Hendry Counties, Florida: Florida Geol. Survey Rept. Inv. 37, 101 p., 1964. KLEMIC, Harry 1- 63. Geology of the South Union quadrangle, Kentucky: U.S. Geol. Survey Geol. Quad. Map GQ-275, 1963. 2- 63. (WARMAN, J. C., and TAYLOR, A. R.) Geology and uranium occurrences of the northern half of the Leighton quadrangle and adjoining areas: U.S. Geol. Survey Bull. 1138, 97 p„ 1963. KNECHTEL, M. M. 1-63. Bauxitization of terra rossa in the southern Appalachian region: U.S. Geol. Survey Prof. Paper 475-C, p. C151-C155, 1963. KNOPF, Adolph 1-63. Geology of the northern part of the Boulder bathylith and adjacent area, Montana: U.S. Geol. Survey Misc. Geol. Inv. Map 1-381, 1963. KNOWLES, D. B. 1-63. (DRESCHER, W. J., and LeROUX, E. F.) Ground-water conditions at Argonne National Laboratory, Illinois, KNOWLES, D. B.--Continued 1948-60: U.S. Geol. Survey Water-Supply Paper 1669-0, p. 01-040, 1963. 2-63. (READE, H. L., Jr., and SCOTT, J. C.) Geology and ground-water resources of Montgomery County, Ala.: U.S. Geol. Survey Water-Supply Paper 1606, 76 p., 1963 [1964], 1- 64. Ground-water conditions in the Green Bay area, Wisconsin, 1950-60: U.S. Geol. Survey Water-Supply Paper 1669-J, p. J1-J37, 1964. 2- 64. Hydrologic aspects of the disposal of oil field brines in Alabama [abs.]: Geol. Soc. America Spec. Paper 76, p. 93-94, 1964. 3- 64. (DREHER, F. C„ and WHETSTONE, G. W.) Water resources of the Green Bay area, Wisconsin: U.S. Geol. Survey Water-Supply Paper 1499-G, p. G1-G67, 1964. KNOX, C. E. 1-64. (and JOHNSON, C. G., Jr.) Flood frequency formulas for Massachusetts: U.S. Geol. Survey open-file report, map, 1964. KOBERG, G. E. 1-64. Methods to compute long-wave radiation from the atmosphere and reflected solar radiation from a water surface: U.S. Geol. Survey Prof. Paper 272-F, p. F107-F136, 1964. KOHOUT, F. A. 1-64. (and LEACH, S. D.) Salt-water movement caused by control-dam operation in the Snake Creek Canal, Miami, Florida: Florida Geol. Survey Rept. Inv. 24, pt. 4, 49 p., 1964. KOOPMAN, F. C. 1-63. An improved water-stage recorder for hydraulic drill holes, in 11th Symposium on exploration drilling: Colorado School Mines Quart., v. 58, no. 4, p. 105-112, 1963. KOTEFF, Carl 1-63. Glacial lakes near Concord, Mass.: U.S. Geol. Survey Prof. Paper 475-C, p. C142-C144, 1963. KOYANAGI, R. Y. 1-64. Hawaiian seismic events during 1962: U.S. Geol. Survey Prof. Paper 475-D, p. D112-D117, 1964. KRACEK, F. C. 1-63. Melting and transformation temperatures of mineral and allied substances: U.S. Geol. Survey Prof. Paper 1144-D, p. D1-D81, 1963. KRIEGER, R. A. 1- 63. The chemistry of saline waters: Ground Water, v. 1, no. 4, p. 7-12, 1963. 2- 63. Understanding chemical analyses of ground water [abs.]: Water Well Jour., v. 17, no. 9, p. 60, 1963. KRINSLEY, D. B. 1-63. Influence of snow cover on frost penetration: U.S. Geol. Survey Prof. Paper 475-B, p. B144-B147, 1963; abs., Geol. Soc. America Spec. Paper 76, p. 300, 1964. KRIVOY, H. L. 1-64. (and EPPLEY, R. A.) T-phase of May 11, 1962, recorded in Hawaii, in Geol. Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B105-B107, 1964. KUNKEL, F. 1-63. A brief summary of ground water in the Furnace Creek Wash area, Death Valley National Monument, California: U.S. Geol. Survey open-file report., 7 p., 1963. LACHENBRUCH, A. H. 1-64. (and MARSHALL, B. V.) Heat Flux from the Arctic Ocean Basin, preliminary results: Am. Geophys. Union Trans., v. 45, no. 1, p. 123, 1964. LADD, H. S. 1-64. Review of "The Paleoecological history of two Pennsylvanian black shales," by Ranier Zangerl and E. S. Richardson, Jr.: Jour. Geology, v. 72, no. 2, p. 250-252, 1964.LIST OF PUBLICATIONS A303 LAINE, L. L. 1-63. Surface water of Kiamchi River basin in southeastern Oklahoma, with a section on Quality of water, by T. R. Cummings: U.S. Geol. Survey open-file report, 1963. LAKIN, H. W. 1- 63. (HUNT, C. B„ DAVIDSON, D. F., and ODA, Uteana) Variation in minor-element content of desert varnish: U. S. Geol. Survey Prof. Paper 475-B, p. B28-B31, 1963. 2- 63. (and THOMPSON, C. E.) Tellurium—Anew sensitive test: Science, v. 141, no. 3575, p. 42-43, 1963. 3- 63. (THOMPSON, C. E., and DAVIDSON, D. F.) Tellu- rium content of marine manganese oxides and other manganese oxides: Science, v. 142, no. 3599, p. 1568- 1569, 1963. LaMARCHE, V. C., Jr. 1-63. Origin and geologic significance of buttress roots of Bristlecone pines, White Mountains, Calif.: U.S. Geol. Survey Prof. Paper 475-C, p. C149-C150, 1963. LAMBERT, T. W. 1-63. (and BROWN, R. F.) Availability of ground water in Adair, Casey, Clinton, Cumberland, Pulaski, Russell, Taylor and Wayne Counties, Ky.: U.S. Geol. Survey Hydrol. Inv. Atlas HA-35, 1963. LANG, J. W. 1-64. (and NEWCOME, Roy, Jr.) Status of salt-water encroachment in aquifers along the Mississippi Gulf Coast, 1964: U.S. Geol. Survey open-file report, 17 p., 1964. LANG, S. M. 1- 63. Drawdown patterns in aquifers having a straight-line boundary, in Shortcuts and special problems in aquifer tests, compiled by Ray Bentall: U.S. Geol. Survey Water-Supply Paper 1545-C, p. C56-C68, 1963. 2- 63. (and RHODEHAMEL, E. C.) Aquifer test at a site on the Mullica River in the Wharton Tract, southern New Jersey: Internat. Assoc. Sci. Hydrology Bull., v. 8, no. 2, p. 31-38, 1963. LANGBEIN, W. B. 1-63. The hydraulic geometry of a shallow estuary: Internat. Assoc. Sci. Hydrology Bull., v. 8, no. 3, p. 84-94, 1963. 1- 64. Geometry of river channels: Am. Soc. Civil Engineers Proc. v. 90, Paper 3846, Jour. Hydraulics Div., no. HY 2, p. 301-312, 1964. 2- 64. Profiles of rivers of uniform discharge, in Geol. Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B119-B122, 1964. 3- 64. (and LEOPOLD, L. B.) Quasi-equilibrium states in channel morphology: Am. Jour. Sci., v. 262, no. 6, p. 782-794, 1964. LANIZ, R. V. 1-64. (STEVENS, R. E., and NORMAN, M. B.) Staining of plagioclase feldspar and other minerals with F. D. and C. Red No. 2, in Geol. Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B152-B153, 1964. LANPHERE, Marvin A. 1-64. (BREW, D. A., EBERLEIN, G. D., LONEY, R. A., and MacKEVETT, Jr., E. M.) Ar40_K40 ages of Paleozoic intrusive rocks in southwestern Alaska [abs.]: Am. Geophys. Union Trans., v. 45, no. 1, p. 116-117, 1964. LaROCQUE, G. A., Jr. 1- 63. Graphic method for plotting aquifer-test data, in Shortcuts and special problems in aquifer tests, compiled by Ray Bentall: U.S. Geol. Survey Water-Supply Paper 1545-C, p. C4-C9, 1963 [1964]. 2- 63. (SWENSON, H. A., and GREENMAN, D. W.) Ground water in the Crosby-Mohall area. North Dakota: North Dakota State Water Conserv. Comm., Ground-water Studies 54, 57 p., 1963. LARRABEE, D. M. 1-63. Geologic map and section of Kellyland and Vanceboro quadrangles, Maine: U.S. Geol. Survey Mineral Inv. Field Studies Map MF-269, 1963. LARRABEE, D. M.--Continued 2-63. (and SPENCER, C. W.) Bedrock geology of the Dan-forth quadrangle, Maine: U.S. Geol. Survey Geol. Quad. Map GQ-221, 1963. 1- 64. Bedrock reconnaissance map of the Forest quadrangle, Maine: U.S. Geol. Survey open-file report, map, 1964. 2- 64. Bedrock reconnaissance map of the Mattawamkeag quadrangle, Maine: U.S. Geol. Survey open-file report, map, 1964. 3- 64. Bedrock reconnaissance map of the Nicatous Lake quadrangle, Maine: U.S. Geol. Survey open-file report, 2 maps, 1964. 4- 64. Bedrock reconnaissance map of the northern one-third of Wesley quadrangle, Maine: U.S. Geol. Survey open-file report, map, 1964. 5- 64. Bedrock reconnaissance map of the Scraggly Lake quadrangle, Maine: U.S. Geol. Survey open-file report, map, 1964. 6- 64. Bedrock reconnaissance map of the Springfield quadrangle, Maine: U.S. Geol. Survey open-file report, map, 1964. 7- 64. Bedrock reconnaissance map of the Waite quadrangle, Maine: U.S. Geol. Survey open-file report, map and 1 p., 1964. 8- 64. Bedrock reconnaissance map of the Winn quadrangle, Maine: U.S. Geol. Survey open-file report, map, 1964. 9- 64. Bedrock reconnaissance map of the Wytopitlock quadrangle, Maine: U.S. Geol. Survey open-file report, map, 1964. 10- 64. (SPENCER, C. W., and SWIFT, D. J. P.) Bedrock geology of the Grand Lake area, Maine: U.S. Geol. Survey open-file report, map, 1964. LaSALA, A. M., Jr. 1- 64. (HARDING, W. E., and ARCHER, R. J.) Water resources of the Lake Erie-Niagara area--A preliminary appraisal: U.S. Geol. Surey open-file report, 64 p., 1964. 2- 64. (and MEIKLE, R. L.) Records and logs of selected wells and test borings and chemical analyses of water in the Bristol-Plainville-Southington area, Connecticut: U.S. Geol. Survey open-file report, 18 p., 1964. LATHRAM, E. H. 1- 64. Apparent right-lateral separation on ChathamStrait fault, southeastern Alaska: Geol. Soc. America Bull., v. 75, no. 3, p. 249-251, 1964. 2- 64. Apparent right-lateral separation on ChathamStrait fault, southeastern Alaska: Geol. Soc. America Bull., v. 75, no. 3, p. 249-252, 1964. LAURENCE, R. A. 1- 63'! (and PALMER, A. R.) Age of the Murray Shale and Hesse Quartzite on Chilhowee Mountain, Blount County, Term.: U.S. Geol. Survey Prof. Paper 475-C, p. C53-C54, 1963. 2- 63. Some "lost" Tennessee mineral localities: Tennessee Acad. Sci. Jour., v. 38, no. 4, p. 156-158, 1963. 1-64. Rediscovery of the Murray Gap fossil locality, Blount County, Tennessee [abs.]: Geol. Soc. America Spec. Paper 76, p. 248-249, 1964. LEACH, S. D. 1-63. (and SHERWOOD, C. B.) Hydrologic studies in the Snake Creek Canal area, Dade County, Florida: Florida Geol. Survey Rept. Inv. 24, pt. 3, 33 p., 1963. LEE, D. E. 1-63. (COLEMAN, R. G., and ERD, R. C.) Garnet types from the Cazadero area, California: Jour. Petrology, v. 4, no. 3, p. 460-492, 1963. * 1-64. (THOMAS, H. H., MARVIN, R. F., and COLEMAN, R. G.) Isotopic ages of glaucophane schists from the area of Cazadero, Calif.: U.S. Geol. Survey Prof. Paper 475-D, p. D105-D107, 1964. LEGGAT, E. R. 1-63. (LOWRY, M. E., and HOOD, J. W.) Ground-water resources of the lower Mesilla Valley, Texas and NewA304 PUBLICATIONS IN FISCAL YEAR 1964 LEGGAT, E. R.—Continued Mexico: U.S. Geol. Survey Water-Supply Paper 1669-AA, p. AA1-AA49, 1963 [1964]. LeGRAND, H. E. 1-64. Hydrogeologic framework of the Gulf and Atlantic Coastal Plain: Geol. Soc. America, Southeastern Sec., 1964 Ann. Mtg., Baton Rouge, April 1964, Program, p. 25, 1964. LEONARD, R. B. 1-64. A method for evaluating oil-field-brine pollution of the Walnut River in Kansas, in Geol. Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B173-B176, 1964. LEOPOLD, E. B. 1-64. Review of "Spores and pollen of the Potomac Group" by G. J. Brenner: Science, v. 143, no. 3608, p. 795, 1964. LEOPOLD, L. B. 1-63. Lands of little water, Preface to Aridity and man: Am. Assoc. Adv. Science Pub. 74, p. ix-xii, 1963. 1-64. Water in the world: U.S. Geol. Survey open-file report, 6 p., 1964. LEPP, Henry 1- 63. (GOLDICH, S. S., and KISTLER, R. W.) A Gren- ville cross section from Port Cartier to Mt. Reed, Quebec, Canada: Am. Jour. Sci., v. 261, p. 693-712, 1963. 2- 63. (GOLDICH, S. S., and KISTLER, R. W.) A Grenville cross section from Port Cartier to Mt. Reed, Quebec, Canada: Econ. Geology, v. 261, p. 693-712, 1963. LeROUX, E. F. 1-63. Geology and ground-water resources of Rock County, Wis.: U.S. Geol. Survey Water-Supply Paper 1619-X, p. X1-X50, 1963. LeROY, L. W. 1-64. Smaller Foraminifera from the late Tertiary of southern Okinawa: U.S. Geol. Survey Prof. Paper 454-F, p. F1-F58, 1964. LESURE, F. G. 1-63. (KIILSGAARD, T. H., BROWN, C. E., and MROSE, M. E.) Beryllium in the tin deposits of Irish Creek, Va.: U.S. Geol. Survey Prof. Paper 475-B, p. B12-B15, 1963. LEVE, G. W. 1-64. Analysis of current meter data from wells by flow -distribution curves: Ground Water, v. 2, no. 2, p. 12-17, 1964; abs., Water Well Jour., v. 17, no. 9, p. 58-59, 1963. LEWIS, D. D. 1-63. A report on southern Arizona floods of September 1962: Arizona State Land Dept. Water Resources Rept. 13, 30 p., 1963. LEWIS, G. E. 1-63. Memorial to Barnum Brown, 1873-1963: Soc* Vert. Paleont. News Bull., no. 68, p. 29-32, 1963. 1- 64. Miocene vertebrates of the Barstow Formation in southern California: U.S. Geol. Survey Prof. Paper 475-D, p. D18-D23, 1964. 2- 64. Memorial to Barnum Brown (1873-1963): Geol. Soc. America Bull., v. 75, no. 2, p. 19-28, 1964. LEWIS, R. Q., Sr. 1- 63. (and THADEN, R. E.) Geology of the Columbia quadrangle, Kentucky: U.S. Geol. Survey Geol. Quad. Map GQ-249, 1963. 2- 63. Geologic features of the Mississippian Plateau, south-central Kentucky: Geol. Soc. Kentucky Field Trip, 28 p., 1963. LEWIS, R. W., Jr. 1-64. The geology, mineralogy, and paragenesis of the Castrovirreyna lead-zinc-silver deposits, Peru: U.S. Geol. Survey open-file report, 265 p., 1964. LICHTLER, W. F. 1-64. (ANDERSON, Warren, and JOYNER, Boyd) Interim report on the water resources of Orange County, Florida: Florida Geol. Survey Inf. Circ. 41, 50 p., 1964. LINDBERG, M. L. 1-64. (and INGRAM, Blanche) Rare-earth silicatian apatite from the Adirondack Mountains, N. Y., in Geol. Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B64-B65, 1964. LIPMAN, P. W. 1- 64. A welded-tuff dike in southern Nevada, in Geol. Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B79-B81, 1964. 2- 64. Structure and petrology of Canyon Creek pluton. Trinity Alps, northern California [abs.]: Geol. Soc. America Spec. Paper 76, p. 280-281, 1964. 3- 64. Two contrasting groups of Alpine-type ultramafic intrusions in northwestern California [abs.]: Geol. Soc. America Spec. Paper 76, p. 103, 1964. 4- 64. (and CHRISTIANSEN, R. L.) Zonal features of an ash-flow sheet in the Piapi Canyon Formation, southern Nevada, in Geol. Survey Research 1964: U.S. Geol.Survey Prof. Paper 501-B, p. B74-B78, 1964. 5- 64. (and McKAY, E. J.) Geologic map of the Topopah Spring SW quadrangle, Nevada: U.S. Geol. Survey Rept. TEI-846 (open-file report), map, 1964. LOCKWOOD, W. N. 1-64. Report on water-well drilling at Angoon, Alaska: U.S. Geol. Survey open-file report, 20 p., 1964. LOELTZ, O. J. 1-63. Ground-water conditions in the vicinity of Lake Mead Base, Las Vegas Valley, Nev.: U.S. Geol. Survey Water-Supply Paper 1669-Q, p. Q1-Q17, 1963. LOFGREN, B. E. 1- 63. Map--Land subsidence in the Arvin-Maricopa area, California, 1959-62: U.S. Geol. Survey open-file report, 1963. 2- 63. Land subsidence in the Arvin-Maricopa area, San Joaquin Valley, Calif.: U.S. Geol. Survey Prof. Paper 475-B, p. B171-B175, 1963. LOHMAN, S. W. 1- 63. Geologic map of the Grand Junction area, Colorado: U.S. Geol. Survey Misc. Geol. Inv. Map 1-404, 1963. 2- 63. Method for determination of the coefficient of storage from straight-line plots without extrapolation, in Shortcuts and special problems in aquifer tests, compiled by Ray Bentall: U.S. Geol. Survey Water-Supply Paper 1545-C, p. C33-C37, 1963. 1-64. (and ROBINOVE, C. J.) Photographic description and appraisal of water resources: Photogrammetria, v. 19, no. 3, p. 83-103, 1964. LONEY, R. A. 1-63. (BERG, H. C., POMEROY, J. S., and BREW, D. A.) Reconnaissance geologic map of Chichagof Island and northwestern Baranof Island, Alaska: U.S. Geol. Survey Hydrol. Inv. Atlas 1-388, 1963. 1-64. (POMEROY, J. S., BREW, D. A., and MUFFLER, L. J. P.) Reconnaissance geologic map of Baranof and Kruzof Islands, Alaska: U.S. Geol. Survey Misc. Geol. Inv. Map 1-411, 1964. LONGWELL, C. R. 1-63. Reconnaissance geology between Lake MeadandDa-vis Dam, Arizona-Nevada: U.S. Geol. Survey Prof. Paper 374-E, p. E1-E51, 1963. LOTSPEICH, F. B. 1-63. (and MARKWARD, E. L.) Minor elements in bedrock soil, and vegetation at an outcrop of the Phosphoria Formation on Snowdrift Mountain, southeastern Idaho: U.S. Geol. Survey Bull. 1181-F, p. F1-F42, 1963. LOVE, J. D. 1-64. Large uraniferous springs and associated uranium minerals, Shirley Mountains, Carbon County, Wyoming--A preliminary report: U.S. Geol. Survey open-file report, 23 p., 1964.LIST OF PUBLICATIONS A305 LOVERING, T. G. 1-63. Use of nonparametric statistical tests in the interpretation of geological data: Soc. Mining Engineers Trans., p. 137-140, 1963. LOVERING, T. S. 1- 63. (and GOODE, H. D.) Measuring geothermal gradients in drill holes less than 60 feet deep. East Tintic district Utah: U.S. Geol. Survey Bull. 1172, 48 p., 1963. 2- 63. (McCarthy, J. H., and FRIEDMAN, Irving) Significance of 0-18/0-16 and C-13/C-12 ratios in hydro-thermally dolomitized limestones and manganese carbonate replacement ores of the Drum Mountains, Juab County, Utah: Art. 1 in U.S. Geol. Survey Prof. Paper 475-B, p. B1-B9, 1963. LUBKE, E. R. 1-64. Hydrogeology of the Huntington-Smithtown area, Suffolk County, N. Y.: U.S. Geol. Survey Water-Supply Paper 1669-D, p. D1-D68, 1964. LUEDKE, R. G. 1-64. (and BURBANK, W. S.) Tertiary volcanic stratigraphy in the western San Juan Mountains, Colo.: U.S. Geol. Survey Prof. Paper 475-C, p. C39-C44, 1964. LUGN, R. V. 1-64. Photogrammetric mapping of experimental craters: Photogrammetric Eng., v. 30, no. 1, p. 55, 1964. LUSBY, G.C. 1-63. (TURNER, G. T., THOMPSON, J. R., and REID, V. H.) Hydrologic and biotic characteristics of grazed and ungrazed watersheds of the Badger Wash basin in western Colorado, 1953-58: U.S. Geol. Survey Water-Supply Paper 1532-B, p. B1-B73, 1963 [1964], LUSCZYNSKI, N. J. 1-64. (and SWARZENSKI, W. V.) Salt-water encroachment in southern Nassau and southeastern Queens Counties, Long Island, New York: U.S. Geol. Survey open-file report, 141 p., 1964. LUSTIG, L. K. 1- 63. Competence of transport on alluvial fans: U.S.Geol. Survey Prof. Paper 475-C, p. C126-C129, 1963. 2- 63. Distribution of granules in a bolson environment: U.S. Geol. Survey Prof. Paper 475-C, p. C130-C131, 1963. 1- 64. Sediment yield of the Castaic watershed, western Los Angeles County, California--A quantitative geomor-phic approach: U.S. Geol. Survey open-file report, 101 p., 1964. 2- 64. Uniformitarianism of the earth-moon system [abs.]: Geol. Soc. America Spec. Paper 76, p. 105, 1964. LUZIER, J. E. 1- 64. Ground-water data for southwestern King County, Washington: U.S. Geol. Survey open-file report, 200 p., 1964. 2- 64. Ground-water supply for Mount Rainier National Park headquarters site near Ashford, Washington: U.S. Geol. Survey open-file report, 35 p., 1964. MABEY, D. R. 1-63. Complete Bouguer anomaly map of the Death Valley region, California: U.S. Geol. Survey Geophys. Inv. Map GP-305, 1963. 1- 64. Gravity map of Eureka County and adjoining areas, Nevada: U.S. Geol. Survey Geophys. Inv. Map GP-415, 1964. 2- 64. Regional gravity and magnetic anomalies in southeastern Idaho and western Wyoming [abs.]: Geol. Soc. America Spec. Paper 76, p. 212, 1964. 3- 64. (CRITTENDEN, M. D., Jr. MORRIS, H. T„ ROBERTS, R. J., and TOOKER, E. W.) Aero magnetic and generalized geologic map of part of north-central Utah: U.S. Geol. Survey Geophys. Inv. Map GP-422, 1964. McADOO, G. D. 1-64. (LEGGAT, E. R., and LONG, A. T.) Geology and ground-water resources of Carson County and part of Gray County, Texas, progress report 2: Texas Water Comm. Bull. 6402, 27 p., 1964. mcallbter, j. f. 1-64. Preliminary geology of the Furnace Creek borate area. Death Valley, California: U.S. Geol. Survey open-file report, map, 1964. McCALL, J. E. 1-63. (and LENDO, A. C.) Surface water supply of New Jersey, streamflow records October 1, 1955 to September 30, 1960: New Jersey Div. Water Policy and Supply Special Rept. 20, 425 p., 1963. 1-64. Drought in a humid area: U.S. Geol. Survey open-file report, 13 p., 1964. McCARREN, E. F. 1-64. Chemical quality of surface water in the West Branch Susquehanna River basin, Pennsylvania: U.S. Geol.Survey Water-Supply Paper 1779-C, p. C1-C40, 1964. McCarthy, l. t„ Jr. 1-63. (and KEIGHTON, W. B.) Quality of Delaware River water at Trenton, New Jersey: U.S. Geol. Survey open-file report, 91 p., 1963. McCARTNEY, David 1-63. Test of a continuous dissolved-oxygen recorder, in Selected techniques in water resources investigations, compiled by G. N. Mesnier and K. T. Iseri: U.S. Geol. Survey Water-Supply Paper 1669-Z, p. Z33-Z44, 1963. McClelland, e. j. 1-63. Methods of estimating ground-water pumpage in California: U.S. Geol. Survey open-file report, 1963. McCOLLUM, M. J. 1- 63. Underground accumulation of refined gasoline--Savannah, Georgia: Georgia Mineral Newsletter, v. 16, nos. 3-4, p. 81-86, 1963. 2- 63. (and COUNTS, H. B.) Relation of salt-water encroachment to the major aquifer zones, Savannah, Georgia and South Carolina area: U.S. Geol. Survey open-file report, 62 p., 1963. McCONAGHY, J. A. 1-64. (CHASE, G. H., BOETTCHER, A. J., and MAJOR, T. J.) Hydrogeologic data of the Denver Basin, Colorado: Colorado Conserv. Board Ground Water Basic-Data Rept. 15, 224 p., 1964. McCULLOH, T. H. 1-64. Factors controlling subsurface density variations in post-Oligocene sedimentary rocks [abs.]: Geol. Soc. America Spec. Paper 76, p. 112, 1964. MCDONALD, C. C. 1-64. Progress report for the Lower Colorado River area: U.S. Geol. Survey open-file report, 8 p., 1964. MacDONALD, G. A. 1-63. Geology of the Manzanita Lake quadrangle, California: U.S. Geol. Survey Geol. Quad. Map GQ-248, 1963. 1-64. (and EATON, J. P.) Hawaiian volcanoes during 1955: U. S. Geol. Survey Bull. 1171, 170 p., 1964. McGILL, J. T. 1-64. Growing importance of urban geology: U.S. Geol. Survey Circ. 487, 4 p., 1964; [abs.]; Geol. Soc. America Spec. Paper 76, p. 112-113, 1964. McGovern, h. e. 1-63. (and COFFIN, D. L.) Potential ground-water development in the northern part of the Colorado High Plains: Colorado Water Conserv. Board Ground-Water Ser. Circ. 8, p. 9, 1963. McGREEVY, L. J. 1-64. (and GORDON, E. D.) Ground water east of Jackson Lake, Grand Teton National Park, Wyoming: U.S. Geol. Survey open-file report, 71 p., 1964. McGREW, L. W. 1-63. Geology of the Fort Laramie area, Platte and Goshen Counties, Wyo.: U.S. Geol. Survey Prof. Paper 1141-F, p. F1-F39, 1963. McGUINNESS, C. L. 1-63. The role of ground-water in the national water situation: U.S. Geol. Survey Water-Supply Paper 1800, 1121 p., 1963.A306 PUBLICATIONS IN FISCAL YEAR 1964 McGUINNESS, C. L. — Continued 1-64. The USGS and the driller: The Driller, v. 38, no. 6, p. 12-19, 22-23, 1964. MACK, F. K. 1-64. (PAUSZEK, F. H., and CRIPPEN, J. R.) Geology and hydrology of the West Milton area, Saratoga County, N. Y.: U.S. Geol. Survey Water-Supply Paper 1747, 110p., 1964. McKAY, E. J. 1-64. (and WILLIAMS, W. P.) Geology of the Jackass Flats quadrangle, Nevada Test Site, Nevada: U.S. Geol. Survey Rept. TEI-843 (open-file report), map, 1964. McKEE, E. D. 1- 63. Nomenclature for lithologic subdivisions oftheMis-sissippian Redwall Limestone, Arizona: U.S. Geol.Survey Prof. Paper 475-C, p. C21-C22, 1963. 2- 63. Triassic uplift along the west flank of the Defiance positive element, Arizona: U.S. Geol. Survey Prof. Paper 475-C, p. C28-C29, 1963. 3- 63. Origin of the nubian and similar sandstones: Geol. Rundschau (Wurzburg, Germany, special African volume), v. 52, no. 2, p. 551-587, 1963. 1- 64. (and TIBBITTS, G. C., Jr.) Primary structures of a seif dune and associated deposits in Libya: Jour. Sed. Petrology, v. 34, no. 1, p. 5-17, 1964. 2- 64. (and TIBBITTS, G. C., Jr.) Primary structures of a seif dune and associated deposits in Libya: Jour. Sed. Petrology, v. 34, no. 1, p. 5-17, 1964. McKELVEY, V. E. 1-63. Geology as the study of complex natural experiments, in C. C. Albritton, Jr., ed., The fabric of geology: Addi-son-Wesley Pub. Co., Reading, Mass., p. 69-74, 1963. McKenzie, m. l. 1-64. Adjustment of elevations derived from instrumen-tally bridged aerial photographs: Photogramm. Eng., v. 30, no. 2, p. 272-278, 1964. MacKEVETT, E. M., Jr. 1- 63. Geology and ore deposits of the Bokan Mountain uranium-thorium area, southeastern Alaska: U.S. Geol. Survey Bull. 1154, 125 p., 1963 [1964]. 2- 63. Preliminary geologic map of the McCarthy C-5 quadrangle, Alaska: U.S. Geol. Survey Misc. Geol. Inv. Map 1-406, 1963 [1964], 3- 63. (and BERG, H. C.) Geology of the Red Devil quicksilver mine Alaska: U.S. Geol. Survey Bull. 1142-G, p. G1-G16, 1963. 4- 63. (and BLAKE, M. C., Jr.) Geology oftheNorth Brad-field River iron prospect, southeastern Alaska: U.S. Geol. Survey Bull. 1108-D, p. D1-D21, 1963. 1-64. (BERG, H. C., PLAFKER, George, and JONES, D. L.) Preliminary geologic map of the McCarthy C-4 quadrangle, Alaska: U.S. Geol. Survey Misc. Geol. Inv. Map 1-423, 1964. MacLACHLAN, M. E. 1-64. The Anadarko Basin (of parts of Oklahoma, Texas, Kansas, and Colorado): U.S. Geol. Survey Rept. TEI-831, 75 p„ 1964. McLaughlin, t. g. 1-64. Ground water in Huerfano County, Colorado: U.S. Geol. Survey open-file report, 161 p., 1964. McMASTER, W. M. 1- 63. Geology and ground-water resources of the Athens area, Alabama: Alabama Geol. Survey Bull. 71, 45 p., 1963. 2- 63. (and HARRIS, W. F., Jr.) General geology and ground-water resources of Limestone County, Alabama: Alabama Geol. Survey County Rept. 11, 43 p., 1963. MacNEIL, F. S. 1-64. Book review of "Late Eocene Zoogeography of the Eastern Gulf Coast region" by A. H. Cheetham: Science, v. 144, no. 3619, p. 717-718, 1964. McQUEEN, I. S. 1-63. Development of a hand portable rainfall-simulator infiltrometer: U.S. Geol. Survey Circ. 482, 16 p., 1963. McQUEEN, I. S.--Continued . 2-63. (and MILLER, R. F.) Temperature and humidity control in the centrifuge moisture equivalent test [abs.]: Am. Soc. Agronomy Mtg., 1963, Agronomy Abs. 1963, p. 64, 1963. MADDOX, G. E. 1-64. Artificial recharge of aquifers overlain by relatively impermeable sediments [abs.]: Geol. Soc. AmericaSpec. Paper 76, p. 282, 1964. MADERAK, M. L. 1-63. Quality of waters, Minnesota—A compilation, 1955-62: Minnesota Div. Waters Bull. 21, 104 p., 1963. MAEVSKY, Anthony 1-63. (and DRAKE, J. A.) Records and logs of selected wells and test holes and chemical analyses of water in southeastern Massachusetts: Massachusetts Water Resources Comm. Basic-Data Rept. 7, Ground-water Ser., 55 p., 1963. MAGNESS, M. G. 1-63. (and CAHILL, J. M.) Details of a hydraulic experiment on an uncemented sand model simulating the movement of radioactive waste injected into the aquifer system at the N.R.T.S., Arco, Idaho. An animated theoretical comparison is included: Time-lapse, 16 mm., color movie, 30 min., on file, Phoenix Research Office, 1963. MALDE, H. E. 1- 63. (POWERS, H. A., and MARSHALL, C. H.) Reconnaissance geologic map of west-centralSnake River Plain, Idaho: U.S. Geol. Survey Misc. Geol. Inv. Map 1-373, 1963. 2- 63. Early man in arid America [abs.]: Assoc. Am. Geographers Ann. Meeting, 59th, Denver, Colo.,Sept., Program, p. 93-94, 1963. 1- 64. Patterned ground in the western Snake River Plain, Idaho, and its possible cold-climate origin: Geol. Soc. America Bull., v. 75, no. 3, p. 191-207, 1964. 2- 64. Patterned ground in the western Snake River Plain, Idaho, and its possible cold-climate origin: Geol. Soc. America Bull., v. 75, no. 3, p. 191-208, 1964. MALMBERG, G. T. 1-63. Las Vegas Valley, Nevada, in Effects of drought in the Colorado River basin, by H. E, Thomas and others: U.S. Geol. Survey Prof. Paper 372-F, p. F9-F11, 1963. 1- 64. Land subsidence in Las Vegas Valley, Nevada, 1935-63: Nevada Dept. Conserv. and Nat. Resources, Ground-Water Resources--Inf. Ser. Rept. 5, 18 p., 1964. 2- 64. (and EAKIN, T. E.) Relation of fluoride content to recharge and movement of ground water in Oasis Valley, southern Nevada: U.S. Geol. Survey Prof. Paper 475-D, p. D189-D191, 1964. MANGER, G. E. 1-63. Porosity and bulk density of sedimentary rocks: U.S. Geol. Survey Bull. 1144-E, p. E1-E55, 1963. MAPEL, W. J. 1-63. (and PILLMORE, C. L.) Geology of the Newcastle area, Weston County, Wyo.:U.S. Geol. Survey Bull. 1141-N, p. N1-N85, 1963. 1-64. (CHISHOLM, W. A., and BERGENBACK, R. E.) Nonopaque heavy minerals in sandstone of Jurassic andCre-taceous age in the Black Hills, Wyoming and South Dakota: U.S. Geol. Survey Bull. 1161-C, p. C1-C59, 1964. MARCHER, M. V. 1- 63. Geologic map of the Ovilla quadrangle, Tennessee: Tennessee Div. Geology Geol. Map, GM 42-SE, 1963. 2- 63. Geologic map of the Westpoint quadrangle, Tennessee: Tennessee Div. Geology Geol. Map, GM43-NE, 1963. 3- 63. Geologic map of the Whitten quadrangle, Tennessee: Tennessee Div. Geology Geol. Map, GM 43-SW, 1963. 4- 63. (and BARNES, R. H.) Geologic map of the Collinwood quadrangle, Tennessee: Tennessee Div. Geology Geol. Map, GM 43-NW, 1963. 5- 63. (and WILSON, C. W., Jr.) Geologic map of the Negro Hollow quadrangle, Tennessee: Tennessee Div. Geology Geol. Map, GM 42-SW, 1963.LIST OF PUBLICATIONS A307 MARCHER, M. V.--Continued 1- 64. (and NYMAN, D. J.) Geologic map of the Burns quadrangle, Tennessee: Tennessee Div. Geology Geol. Map GM 48-SE, 1964. 2- 64. (and NYMAN, D. J.) Geologic map of the Dickson quadrangle, Tennessee: Tennessee Div. Geology Geol. Map GM 48-SW, 1964. MARINE, I. W. 1-63. (and PRICE, Don) Geology and ground-water resources of the Jordan Valley, Utah: U.S. Geol. Survey open-file report, 171 p., 1963. MARSH, O. T. 1-64. Deep-lying salt deposits in Florida panhandle suggested by faulting and gravity anomalies: Geol. Soc. America, Southeastern Sec., 1964 Ann. Mtg., Baton Rouge, April 1964, Program, p. 26-27, 1964. MARTINEZ, Prudencio 1-64. (SENFTLE, F. E„ and PAGE, M.) Trapping levels and thermoluminescence of Csl doped with various activators: Phys. Rev. Letters, v. 12, p. 369-371, 1964. MARVIN, R. F. 1-63. (SHAFER, G. H., and DALE, O. C.) Ground-water resources of Victoria and Calhoun Counties, Texas: Texas Board Water Engineers Bull. 6202, 147 p., 1963. MASON, C. C. 1-63. Ground-water resources of Refugio County, Texas: Texas Water Comm. Bull. 6312, 122 p., 1963. MAUGHAN, E. K. 1-63. Mississippian rocks in the Laramie Range, Wyo., and adjacent areas: U.S. Geol. Survey Prof. Paper 475-C, p. C23-C27, 1963. ,1-64. The Goose Egg Formation in the Laramie Range and adjacent parts of southeastern Wyoming, in Geol. Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B53-B60, 1964. MAXWELL, C. H. 1-64. Geology of the Knifley quadrangle, Kentucky: U.S. Geol. Survey Geol. Quad. Map GQ-294, 1964. MAY, H. G. 1-63. A simplified time-and distance-drawdown graph, in Shortcuts and special problems inaquifer tests, compiled by Ray Bentall: U.S. Geol. Survey Water-Supply Paper 1545-C, p. C29-C32, 1963. MAY, Irving 1-64. Book review of "Detection and analysis of rare elements" ed. by A. P. Vinogradov and D. I. Ryabchikov: Geochim. et Cosmochim. Acta, v. 28, no. 5,p. 751, 1964. MAY, J. R. 1-63. Arkansas wells show path of nuclear pressure wave: Arkansas Gazette, p. 6E, Sunday, Mar. 31, 1963. 1-64. (and EMMETT, L. F.) Logs and water-level measurements of selected wells and test holes in the alluvium of the Arkansas River Valley between Little Rock and FortSmith, Arkansas: U.S. Geol. Survey open-file report, 653 p., 1964. MEADE, R. H. 1- 63. Factors influencing the pore volume of fine-grained sediments under low-to-moderate overburden loads: Sedimentology, v. 2, p. 235-242, 1963. 2- 63. Removal of water and rearrangement of particles during the compaction of clayey sediments—Review: U.S. Geol. Survey open-file report, 87 p., 1963. MEIER, M. F. 1-63. Glaciers, in U. S. Natl. Rept., 1960-1963, Thirteenth General Assembly, Internat. Union Geodesy and Geophysics: Am. Geophys. Union Trans., v. 44, no. 2, p. 581-585, 1963. MEISLER, Harold 1-63. Hydrogeology of the carbonate rocks of the Lebanon Valley, Pennsylvania: Pennsylvania Geol. Survey,4th Ser., Bull. W 18, 81 p., 1963. MELLO, J. F. 1-64. (MINARD, J. P., and OWENS, J. P.) Foraminifera from the Exogyra ponderosa zone of the Marshalltown Formation at Auburn, N. J., in^ Geol. Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B61-B63, 1964. MENDIETA, H. B. 1-63. (and BLAKEY, J. F.) Brazos River basin reservoir studies, progress report, May 1962—Chemical quality and stratification of Belton, Whitney, and Possum Kingdom Reservoirs: Texas Water Comm. Memo. Rept. 63-01, 24 p., 1963. MEREWETHER, E. A. 1-63. (HALEY, B. R., and FREZON, S. E.) The Chester, Morrow, and Atoka Series in Western Arkansas and Eastern Oklahoma [abs.j: Shale Shaker, v. 14, no. 2, p. 4, 1963. MERRIAM, C. W. 1-63. Geology of the Cerro Gordo mining district, Inyo County, Calif.: U.S. Geol. Survey Prof. Paper 408, 83 p., 1963 [1964]. MERRILL, C. W. 1-63. Selected bibliography of talc in the United States: U.S. Geol. Survey Bull. 1182-C, p. C1-C26, 1963. MESNIER, G. N. 1-63. (and ISERI, K. T., compilers) Selected techniques in water resources investigations: U.S. Geol. Survey Water-Supply Paper 1669-Z, p. Z1-Z64, 1963. MESSINGER, Harry 1-63. Dissipation of heat from a thermally loaded stream: U.S. Geol. Survey Prof. Paper 475-C, p. C175-C178, 1963. METZGER, D. G. 1-64. Progress report on geohydrologic investigations in the Parker-Blythe-Cibola and Needles areas: U.S. Geol. Survey open-file report, 18 p., 1964. MEUSCHKE, J. L. 1- 63. (JOHNSON, R. W., and KIRBY, J. R.) Aeromagnetic map of the southwestern part of Custer County, S. Dak.: U.S. Geol. Survey Geophys. Inv. Map GP-362, 1963. 2- 63. (and ZANDLE, G. L.) Aeromagnetic map of the Ash-field quadrangle, Franklin and Hampshire Counties, Mass.: U.S. Geol. Survey Geophys. Inv. MapGP-429, 1963. 3- 63. (and ZANDLE, G. L.) Aeromagnetic map of the Greenfield quadrangle, Franklin County, Massachusetts: U.S. Geol. Survey Geophys. Inv. Map GP-432, 1963. 4- 63. (and ZANDLE, G. L.) Aeromagnetic map of the Plain-field quadrangle, Franklin, Hampshire, and Berkshire Counties, Mass.: U.S. Geol. Survey Geophys. Inv. Map GP-436, 1963. 5- 63. (and ZANDLE, G. L.) Aeromagnetic map of the Shelburne Falls quadrangle, Franklin County, Massachusetts: U.S. Geol. Survey Geophys. Inv. Map GP-438, 1963. MEYER, Gerald 1-64. (GRIFFIN, W. C., and WARK, J. W.) Surface-, ground-, and quality-of-water investigations in West Virginia, in Water research symposium, Morgantown, Nov. 1963, Proc.: West Virginia Univ., p. 13-17, 1964. MEYROWITZ, Robert 1-63. (ROSS, D. R., and WEEKS, A. D.) Synthesis of liebi-gite: U.S. Geol. Survey Prof. Paper 475-B, p. B162-B163, 1963. 1- 64. The direct spectrophotometric microdetermination of high level magnesium in silicate minerals—A Clayton Yellow procedure: Am. Mineralogist, v. 49, no. 5-6, p. 769-777, 1964. 2- 64. (ROSS, D. R., and ROSS, Malcolm) Anewuranyl tricarbonate, K2Ca3(UO2)2(CO3>0-9 —IOH2O, in Geol. Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B82-B83, 1964. MIESCH, A. T. 1-63. Distribution of elements in Colorado Plateau uranium deposits--A preliminary report: U.S. Geol. Survey Bull. 1147-E, p. E1-E57, 1963.A308 PUBLICATIONS IN FISCAL YEAR 1964 MIESCH, A. T.— Continued 1- 64. (and CONNOR, J. J.) Investigation of sampling-error effects in geochemical prospecting: U.S. Geol. Survey Prof. Paper 475-D, p. D84-D88, 1964. 2- 64. (CONNOR, J. J., and EICHER, R. N.) Investigations of geochemical sampling problems by computer simulation [abs.], in Abstracts and biographies, internat. symposium on applications of statistics, operations research, and computers in the mineral industry: Colorado School of Mines pamphlet, April 20-24, 1964. 3- 64. (and EICHER, R. N.) A system of statistical computer programs for geologic research [abs.], in Abstracts and biographies, internat. symposium on applications of statistics, operations research and computers in the mineral industry: Colorado School of Mines pamphlet, April 20-24, 1964. 4- 64. Effects of sampling and analytical error in geochemical prospecting: Computers in the Mineral Industries, Part 1: Stanford Univ. Pub., Geol. Sci., v. 9, no. 1, p. 156-170, 1964. MILICI, R. C. 1-64. (and WEDOW, Helmuth, Jr.) Geologic features related to the post-Knox unconformity inSequatchie Valley, Tennessee [abs.]: Tennessee Acad. Sci. Jour., v. 39, no. 2, p. 66-67, 1964. MILLER, C. H. 1-63. Gravity survey in the Rampart Range area, Colorado: U.S. Geol. Survey Prof. Paper 475-C, p. C110-C113, 1963. MILLER, D. J. 1-64. (and MacCOLL, R. S.) Geologic map and sections of the northern part of the McCarthy A-4 quadrangle, Alaska: U.S. Geol. Survey Misc. Geol. Inv. Map 1-410, 1964. MILLER, G. A. 1-63. Ground-water conditions, U. S. Naval Missile Facility, Point Arguello, California, July 1962-June 1963: U.S. Geol. Survey open-file report, 21 p., 1963. MILLER, J. P. 1-63. (and LEOPOLD, L. B.) Simple measurements of morphological changes in river channels and hill slopes, in Changes of climate: Arid Zone Research, v. 20, p. 421-427, 1963. MILLER, R. E. 1-63. Maps and geologic sections from "Subsurface geology of the water-bearing deposits in the Los Banos-Kettleman City area, Merced, Fresno, and King Counties, California": U.S. Geol. Survey open-file report, 1963. MILLER, R. F. 1-63. (and RATZLAFF, K. W.) Chemistry of soil profiles indicates recurring patterns and modes of moisture migration: Western Soc. of Soil Sci. Mtg., Stanford Univ., Palo Alto, Calif., June 17-20, 1963, Program, p. 17, 1963. MILLER, R. L. 1- 64. The Little Stone Gap Member of the Hinton Formation (Mississippian) in southwest Virginia, in Geol. Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B39-B42, 1964. 2- 64. (HARRIS, L. D., and ROEN, J. B.) The Wildcat Valley Sandstone (Devonian) of southwest Virginia, in Geol. Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B49-B52, 1964. MILLER, T. P. 1- 64. Geology of the Dunmor quadrangle, Kentucky: U.S. Geol. Survey Geol. Quad. Map GQ-290, 1964. 2- 64. Geology of the Kelly quadrangle, Kentucky: U.S. Geol. Survey Geol. Quad. Map GQ-307, 1964. MILLS, W. B. 1-63. Annotated bibliography of surface-water publications and open-file reports of the Texas Water Commission and the U.S. Geological Survey for Texas through June 1962: Texas Water Comm. Circ. 63-04, 38 p., 1963. MILLS, W. B.--Continued 2-63. Use of plastic tubes for peak-stage gages on reservoirs, in Selected techniques in water resources investigations, compiled by G. N. Mesnier and K. T. Iseri: U.S. Geol. Survey Water-Supply Paper 1669-Z, p. Z27-Z28, 1963. 1-64. (and RAWSON, J.) Quantity and quality of base flow of Lampasas River, Texas, June 3-6, 1963: U.S. Geol. Survey open-file report, 31 p., 1964. MILTON, Charles 1-63. Review of "Ore microscopy" by E. N. Cameron: Am. Geophys. Union Trans., v. 44, no. 2, p. 601, 1963. 1-64. (and MEYROWITZ, Robert) Ferroan northupite in the Green River Formation of Wyoming, in Geol. Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B66-B68, 1964. MINARD, J. P. 1-63. (and OWENS, J. P.) Pre-Quaternary geology of the Browns Mills quadrangle, New Jersey: U.S. Geol. Survey Geol. Quad. Map GQ-264, 1963 [1964], 1-64. (OWENS, J. P.,andNICHOLS,T.C.) Pre-Quaternary geology of the Mount Holly quadrangle. New Jersey: U.S. Geol. Survey Geol. Quad. Map GQ-272, 1964. MITCHELL, W. D., Jr. 1- 63. Discussion of "Analysis of synthetic unit-graph methods", by Paul E. Morgan and Stanley M. Johnson: Am. Soc. Civil Engineers Proc.,v. 89, Jour. Hydraulics Div., no. HY3, pt. 1, p. 349-354, 1963. 2- 63. (and REPENNING, C. A.) The chronologic and geographic range of desmostyleans: Los Angeles County Mus., Contr. Sci., no. 78, p. 1-20, 1963. MOENCH, R. H. . 1- 63. Geologic map of the Laguna quadrangle. New Mexico: U.S. Geol. Survey Geol. Quad. Map GQ-208, 1963. 2- 63. Geologic map of the Seboyeta quadrangle, New Mexico: U.S. Geol. Survey Geol. Quad. Map GQ-207, 1963. 3- 63. (and PUFFETT, W. P.) Geologic map of the Arch Mesa quadrangle. New Mexico: U.S. Geol. Survey Geol. Quad. Map GQ-211, 1963. 4- 63. (and PUFFETT, W. P.) Geologic map of the Mesa Gigante quadrangle. New Mexico: U.S. Geol. Survey Geol. Quad. Map GQ-212, 1963. 1-64. (and MEYROWITZ, R. L,) Goldmanite, a vanadium garnet from Laguna, New Mexico: Am. Mineralogist, v. 49, no. 5-6, p. 644-655, 1964. MONROE, W. H. 1- 63. Geology of the Camuy quadrangle, Puerto Rico: U.S. Geol. Survey Geol. Quad. Map GQ-197, 1963. 2- 63. Geology of the Vega Alta quadrangle, Puerto Rico: U.S. Geol. Survey Geol. Quad. Map GQ-191, 1963. 1- 64. Large retrogressive landslides in north-central Puerto Rico, in Geol. Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B123-B125, 1964. 2- 64. Memorial to Lloyd William Stephenson (1876-1962): Geol. Soc. America Bull., v. 75, no. 5,p. P83-P89, 1964. 3- 64. The zanjon, a solution feature of karst topography in Puerto Rico, in Geol. Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B126-B129, 1964. MOORE, E. J. 1-63. Miocene marine mollusks from the Astoria Fbrmation in Oregon: U.S. Geol. Survey Prof. Paper 419, 109 p., 1963 [1964], MOORE, F. B. 1-64. Geology of the Summit quadrangle, Kentucky: U.S. Geol. Survey Geol. Quad. Map GQ-298, 1964. MOORE, G. E., Jr. 1-63. Bedrock geology of the Coventry Center quadrangle, Rhode Island: U.S. Geol. Survey Bull. 1158-A,p. A1-A24, 1963. MOORE, G. W. 1-64. (and NICHOLAS, Brother G.) Out-of-phase seasonal temperature fluctuations in Cathedral Cave, Kentucky [abs.]: Geol. Soc. America Spec. Paper 76, p. 313, 1964.LIST OF PUBLICATIONS A309 MOORE, H. J. 1-63. (MacCORMACK, R. W., and GAULT, D. E.) Fluid impact craters and hypervelocity impact experiments in metals and rocks: U.S. Army, U.S. Air Force,U.S. Navy, Symposium on hypervelocity impact, 6th, Proc., v. 2, pt. 2, N/A, p. 367-399, 1963. 1-64. (MacCORMACK, R. W„ and GAULT, D. E.) Fluid impact craters and hypervelocity--High velocity impact experiments in metals and rocks: U.S. Geol. Survey open-file report, 29 p., 1964. MOORE, J. E. 1-63. (DOYLE, A. C., WALKER, G. E., and YOUNG, R. A.) Ground-water test well 2, Nevada Test Site, Nye County, Nevada--A summary of lithologic data, aquifer tests, and well construction, with a section on Geophysical logs, by R. D. Carroll: U.S. Geol. Survey Report TEI-836, 73 p., 1963. MOORE, J. G. 1-63. (and REED, R. K.) Pillow structures of submarine basalts east of Hawaii: U.S. Geol. Survey Prof. Paper 475-B, p. B153-B157, 1963. 1-64. (and KRIVOY, H. L.) The 1962 eruption of Kilauea Volcano and structure of the east rift zone [abs.]: Jour. Geophys. Research, v. 69, no. 10, p. 2033-2045, 1964. MOORE, R. H. 1-64. (SPEERT, J. L., and BENTLEY, L. E.) Discussion of paper "Control traverses and their adjustment," by Everett D. Morse: Am. Soc. Civil Engineers Proc., v. 90, Jour. Surveying and Mapping Div., no. SU1, p. 81-84, 1964. MOORE, S. L. 1- 63. Geology of the Allen Springs quadrangle, Kentucky: U.S. Geol. Survey Geol. Quad. Map GQ-285, 1963 [1964], 2- 63. Geology of the Drake quadrangle, Kentucky: U.S. Geol. Survey Geol. Quad. Map GQ-277, 1963. MOREY, G. W. 1- 64. (FOURNIER, R. O., and ROWE, J. J.) The solubility of amorphous silica at 25°C: Jour. Geophys. Research, v. 69, no. 10, p. 1995-2002, 1964. 2- 64. (ROWE, J. J., and FOURNIER, R. O.) The system K2Mg2(S04>3 (Langbeinite)-K2Ca2(S04)3 (Calcium- langbeinite): Jour. Inorganic and Nuclear Chemistry, v. 26, no. 1, p. 53-58, 1964. MOREY, George 1-63. Review of "The constitution of glass. A dynamic interpretation. Vol. I, Fundamentals of the structure of inorganic liquids and solids," by W. A. Weyl and E. C. Marboe: Chem. and Eng. News, v. 41, no. 26, p. 50, 1963. MORGAN, C. O. 1-63. Ground-water resources of East Feliciana and West Feliciana Parishes, Louisiana: Louisiana Dept. Public Works, 58 p., 1963. 1-64. (and WINNER, M. D., Jr.) Salt-water encroachment in aquifers of the Baton Rouge area--Preliminary report and proposal: Louisiana Dept. Public Works, 37 p., 1964. MORRIS, H. T. 1- 64. Geology of the Eureka quadrangle, Utah and Juab Counties, Utah: U.S. Geol. Survey Bull. 1142-K, p. Kl-K29, 1964. 2- 64. Geology of the Tintic Junction quadrangle, Tooele, Juab, and Utah Counties, Utah: U.S. Geol. Survey Bull. 1142-L, p. L1-L23, 1964. MORRIS, R. H. 1-63. Geologia general das quadriculas de Gravatai, Taquara, y Rolante, Rio Grande do Sul, Brasil: Escola de Geologia, Univ. do Rio Grande do Sul, Porto Alegre, Brazil, Pub. Especial No. 5, 38 p., 1963. MORRISON, R. B. 1-64. Lake Lahontan—Geology of southern Carson Desert, Nevada: U.S. Geol. Survey Prof. Paper 401, 156 p., 1964. MOULDER, E. A. 1-63. Locus circles as an aid in the location of a hydro-geologic boundary, in Shortcuts and special problems in MOULDER, E. A.—Continued aquifer tests, compiled by Ray Bentall: U.S. Geol.Survey Water-Supply Paper 1545-C, p. C110-C112, 1963. 2- 63. (JENKINS, C. T., MOORE, J. E., and COFFIN, D. L.) Effects of water management on a reach of the Arkansas Valley, La Junta to Las Animas, Colorado: Colorado Water Conserv. Board Ground Water Circ. 10, 20 p., 1963. 3- 63. (and KLUG, M. L.) Jetting method of installing small-diameter wells, in Methods of collecting and interpreting ground-water data, compiled by Ray Bentall: U.S. Geol. Survey Water-Supply Paper 1544-H, p. H14-H-30, 1963. MOUNT, Priscilla 1-63. Occurrence of bismuth at the Brewer mine, Chesterfield County, South Carolina: South Carolina State Devel. Board, Div. of Geology, Geol. Notes, v. 7, no. 3-4, p. 19-23, 1963. MOURANT, W. A. 1-63. Water resources and geology of the Rio Hondo drainage basin, Chaves, Lincoln, and Otero Counties, New Mexico: New Mexico State Engineer Tech. Rept. 28, 85 p., 1963. 1-64. (and HAVENS, J. S.) Rattlesnake Springs test drilling, Eddy County, New Mexico: U.S. Geol. Survey open-file report, 11 p., 1964. MOWER, R. W. 1- 63. Ground-water resources of Pavant Valley, Utah: U.S. Geol. Survey open-file report, 154 p., 1963. 2- 63. Selected hydrologic data, Pavant Valley, Millard County, Utah: U.S. Geol. Survey and Utah State Engineer Basic-Data Rept. 5, 20 p., 1963. 1-64. (HOOD, J. W., CUSHMAN, R. L., BORTON, R. L„ and GALLOWAY, S. E.) An appraisal of potential ground-water salvage along the Pecos River between Acme and Artesia, New Mexico: U.S. Geol. Survey Water-Supply Paper 1659, 98 p., 1964. MOXHAM, R. M. 1-64. Radioelement dispersion in a sedimentary environment and its effect on uranium exploration: Econ. Geology, v. 59, no. 2, p. 309-321, 1964. MOYLE, W. R., Jr. 1-63. Data on water wells in Indian Wells Valley area, Inyo, Kern, and San Bernardino Counties, California: California Dept. Water Resources Bull. 91-9, 243 p., 1963. MROSE, M. E. 1-63. (and FLEISCHER, Michael) The probable identity of magnioborite with suanite: Am. Mineralogist, v. 48, no. 7-8, p. 915-924, 1963. MUEHLBERGER, W. R. 1-63. (and GOLDICH, S. S.) Age determinations on the buried basement rocks of the midcontinent region, USA [abs.]: Internat. Union Geodesy and Geophysics, General Assembly, 13th, Berkeley, Calif., Aug. 1963, Abs. Papers, v. 7, p. 76, 1963. MUIR, K. S. 1-63. Water levels in observation wells in Santa Barbara County, California, in 1962: U.S. Geol. Survey open-file report, 55 p., 1963. 1-64. Geology and ground water of San Antonio Creek valley, Santa Barbara County, Calif.: U.S. Geol. Survey Water-Supply Paper 1664, 53 p., 1964. MULLENS, T. E. 1-64. (and LARAWAY, W. H.) Geology of the Devils Slide quadrangle, Morgan and Summit Counties, Utah: U.S. Geol. Survey Mineral Inv. Field Studies Map MF-290, 1964. MULLINEAUX, D. R. 1-64. Extensive Recent pumice lapilli and ash layers from Mount St. Helens Volcano, southern Washington [abs.]: Geol. Soc. America Spec. Paper 76, p. 285, 1964. MUNDORFF, M. J. 1-63. (and SISCO, H. G.) Ground water in the Raft River basin, Idaho, with special reference to irrigation use.A310 PUBLICATIONS IN FISCAL YEAR 1964 MUNDORFF, M. J.—Continued 1956-60: U.S. Geol. Survey Water-Supply Paper 1619-CC, p. CC1-CC23, 1963. 1-64. Geology and ground-water conditions of Clark County, Wash., with a description of a major alluvial aquifer along the Columbia River: U.S. Geol. Survey Water-Supply Paper 1600, 268 p., 1964. MURATA, K. J. 1-63. (AULT, W. U., and WHITE, D. E.) Halogen acids in fumarolic gases of Kilauea volcano [abs.]: Internat. Union Geodesy and Geophysics, General Assembly, 13th, Berkeley, Calif., Aug. 1963, Abstracts of Papers, v. 7, p. 43, 1963. MUSGROVE, R. H. 1-63. Accuracy of three nonstandard rain gages, in Selected techniques in water resources investigations, compiled by G. N. Mesnier and K. T. Iseri: U.S. Geol. Survey Water-Supply Paper 1669-Z, p. Z45-Z47, 1963. MUSSER, J. J. 1-63. Description of physical environment and of stripmining operations in parts of Beaver Creek basin, Kentucky: U.S. Geol. Survey Prof. Paper 427-A, p. A1-A25, 1963 [1964]. MYERS, A. T. 1-64. (HAVENS, R. G., and CONKLIN, N. M.) Application of direct-reading spectrography for the trace-element analysis of silicate rocks [abs.]: Geol. Soc. AmericaSpec. Paper 76, p. 286-287, 1964. MYRICK, R. M. 1-63. (and LEOPOLD, L. B.) Hydraulic geometry of a small tidal estuary: U.S. Geol. Survey Prof. Paper 422-B, p. Bl-B18, 1963. NACE, R. L. 1-63. (and TISON, L. J.) International cooperation in scientific hydrology: Internat. Council Sci. Unions Review World Sci., v. 5, no. 2, p. 116-123, 1963. 1- 64. Water for the world: Nat. History, v. 73, no. 1, p. 10-19, 1964. 2- 64. (and PLUHOWSKI, E. J.) Drought of the 1950's, with special reference to the midcontinent: U.S. Geol. Survey open-file report, 169 p., 1964. NELSON, W. B. 1-63. Escalante Valley, Utah, in Effects of drought in basins of interior drainage, by H. E. Thomas and others: U.S. Geol. Survey Prof. Paper 372-E, p. E29-E35, 1963. NELSON, W. H. 1-63. Geology of the Meador quadrangle, Kentucky: U.S. Geol. Survey Geol. Quad. Map GQ-288, 1963 [1964]. 1-64. Geology of the Adolphus quadrangle, Kentucky-Ten-nessee: U.S. Geol. Survey Geol. Quad. MapGQ-299, 1964. NEUMAN, R. B. 1-63. Caradocian (Middle Ordovician) fossiliferous rocks near Ashland, Maine: U.S. Geol. Survey Prof. Paper 475-B, p. B117-B119, 1963. 1-64. Ordovician brachiopods in Maine [abs.]: Geol. Soc. America Spec. Paper 76, p. 121, 1964. NEUSCHEL, S. K. 1-64. Correlation of aeroradioactivity and areal geology in District of Columbia and parts of Maryland, Virginia, and West Virginia [abs.]: Geol.Soc. AmericaSpec. Paper 76, p. 252, 1964. NEWCOMB, R. C. 1-63. Ground water in the Orchard Syncline, Wasco County, Oregon: Ore Bin, v. 25, no. 8, p. 133-148, 1963. NEWCOME, Roy, Jr. 1- 63. Simplified method of altimeter surveying, in. Selected techniques in water resources investigations, compiled by G. N. Mesnier and K. T. Iseri: U. S. Geol. Survey Water-Supply Paper 1669-Z, p. Z59-Z64, 1963. 2- 63. (PAGE, L. V., and SLOSS, R.) Water resources of Natchitoches Parish, Louisiana: Louisiana Geol. Survey Dept. Conserv. and Louisiana Dept. Public Works, Water Resources Bull.4, 189 p., 1963. NEWCOME, Roy, Jr.—Continued 1-64. (and CALLAHAN, J. A.) Water for industry in the Corinth area, Mississippi: Mississippi Board Water Comm. Bull. 64-2, 24 p., 1964. NEWPORT, T. G. 1-63. (and HADDOR, Yousef) Ground-water exploration in A1 Marj area, Cyrenaica, United Kingdom of Libya: U.S. Geol. Survey Water-Supply Paper 1757-A, p. A1-A24, 1963. NILES, W. W. 1-64. Determination of total iron in hematitic ironoresby X-ray fluorescence spectrometry: U.S. Geol. Survey Prof. Paper 475-D, p. D174-D175, 1964. NOBLE, D. C. 1- 64. Mathematical rotation of orientation data: Geol. Soc. America Bull., v. 75, no. 3, p. 247-248, 1*964. 2- 64. Rapid procedure for determining plagioclase with the five axis universal stage [abs.]: Geol. Soc. America Spec. Paper 76, p. 217, 1964. 3- 64. Structural state of metamorphosed volcanic plagioclase from west-central Nevada [abs.]: Geol. Soc. America Spec. Paper 76, p. 122-123, 1964. 4- 64. (ANDERSON, R. E., EKREN, E. B., andO'CONNOR, J. T.) The Thirsty Canyon Tuff of Nye and Esmeralda Counties, Nev.: U.S. Geol. Survey Prof. Paper 475-D, p. D24-D27, 1964. 5- 64. Mathematical rotation of orientation data: Geol.Soc. America Bull., v. 75, no. 3, p. 247-248, 1964. NOEHRE, A. W. 1- 63. Floods in Wadsworth quadrangle, Illinois: U.S. Geol. Survey open-file report, 10 p., 1963. 2- 63. (and WALTER, G. L.) Floods in Geneva quadrangle, Illinois: U.S. Geol. Survey open-file report, 9 p., 1963. 1-64. (ELLIS, D. W., and LONG, D. E.) Floods in Liberty-ville quadrangle, Illinois: U.S. Geol. Survey Hydrol. Inv. Atlas HA-88, 1964. NORDIN, C. F., Jr. 1- 63. A preliminary study of sediment transport parameters, Rio Puerco near Bernardo, N. Mex.: U.S. Geol. Survey Prof. Paper 462-C, p. C1-C21, 1963. 2- 63. (and DEMPSTER, G. R., Jr.) Vertical distribution of velocity and suspended sediment. Middle Rio Grande, New Mexico: U.S. Geol. Survey Prof. Paper 462-B, p. Bl-B20, 1963. 1- 64. Aspects of flow resistance and sediment transport, Rio Grande near Bernalillo, New Mexico: U.S. Geol.Survey Water-Supply Paper 1498-H, p. H1-H41, 1964. 2- 64. (and BEVERAGE, J. P.) Discussion of "An expression for bed-load transportation", by M. Selim Yalin: Am. Soc. Civil Engineers Proc., v. 90, Jour. Hydraulics Div., HY 1, pt. 1, p. 303-313, 1964. 3- 64. (and BEVERAGE, J. P.) Temporary storage of fine sediments in islands and point bars and alluvial channels of the Rio Grande, New Mexico andTexas: U.S. Geol. Survey Prof. Paper 475-D, p. D138-D140, 1964. NORTON, J. J. 1-64. (and others) Geology and mineral deposits of some pegmatites in the southern Black Hills, South Dakota: U.S. Geol. Survey Prof. Paper 297-E, p. 293-341, 1964. NORVITCH, R. F. 1-63. (SCHNEIDER, Robert, and GODFREY, R. G.) Geology and hydrology of the Elk River Minnesota nuclear-reactor site: U.S. Geol. Survey Bull. 1133-C, p. C1-C25, 1963. OAKES, E. L. 1-64. Bedrock topography of the eastern and central Me-sabi Range, northeastern Minnesota: U.S. Geol. Survey Misc. Geol. Inv. Map 1-389, 1964. OBORN, E. T. 1-63. Effectiveness of common aquatic organisms in removal of dissolved lead from tap water: U.S. Geol. Survey Prof. Paper 475-C, p. C220, 1963. 1-64. Intracellular and extracellular concentration of manganese and other elements by aquatic organisms: U.S.LIST OF PUBLICATIONS A311 OBORN, E. T.—Continued Geol. Survey Water-Supply Paper 1667-C, p. C1-C18, 1964. O'CONNOR, J. T. 1-63. Petrographic characteristics of some welded tuffs of the Piapi Canyon Formation, Nevada Test Site, Nev.: U.S. Geol. Survey Prof. Paper 475-B, p. B52-B55, 1963. 1-64. (and HONEA, R. M.) An X-ray study of some volcanic alkali feldspars from southern Nevada [abs.]: Geol. Soc. America Spec. Paper 76, p. 123-124, 1964. OGATA, Akio 1-63. Effect of the injection scheme on thespreadof tracers in ground-water reservoirs: U.S. Geol. Survey Prof. Paper 475-B, p. B199-B202, 1963. OGILBEE, William 1-63. (and VORHIS, R. C.) Ground-water resources of the Az Zawiyak area, Tripolitania, United Kingdom of Libya: U.S. Geol. Survey open-file report, 77 p., 1963. 1- 64. Ground water in the Sirte area, Tripolitania, United Kingdom of Libya: U.S. Geol. Survey Water-Supply Paper 1757-C, p. C1-C14, 1964. 2- 64. (and TARHUNI, H. A.) Ground-water resources of the Tarahbulli area, Tripolitania, United Kingdom of Libya: U.S. Geol. Survey open-file report, 93 p., 1964. 3- 64. (VORHIS, R. C., and DEGHAIES, Fituri) Ground-water resources of A1 Mayah area, Tripolitania, United Kingdom of Libya: U.S. Geol. Survey open-file report, 74 p., 1964. OLDALE, R. N. 1-64. (and TUTTLE, C. R.) Seismic investigations on Cape Cod, Mass.: U.S. Geol. Survey Prof. Paper 475-D, p. D118-D122, 1964. OLIVE, W. W. 1-63. Geology of the Lynn Grove quadrangle in Kentucky: U.S. Geol. Survey Geol. Quad. Map GQ-268, 1963. OLIVER, H. W. 1- 63. (and MABEY, D. R.) Anomalous gravity field in east-central California: Geol. Soc. America Bull., v. 74, no. 10, p. 1293-1298, 1963. 2- 63. (and MABEY, D. R.) Regional gravity anomalies in central California [abs.]: Am. Assoc. Petroleum Geologists Bull., v. 47, no. 9, p. 1774, 1963. OLIVER, W. A., Jr. 1-63. The Onondaga Limestone, in Stratigraphy, facies changes, and paleoecology of the Lower Devonian Helder-berg Limestones and the Middle Devonian Onondaga Limestone: Geol. Soc. America Guidebook—Field Trip No. 1, Mohawk and Central Hudson Valleys, New York, p. 11-16, 1963. 1- 64. New occurrences of the rugose coral Rhizophvllum in North America: U.S. Geol. Survey Prof. Paper 475-D, p. D149-D158, 1964. 2- 64. Ontogeny in a species of Nalivkinella from the Middle Devonian of eastern Pennsylvania [abs.]: Geol. Soc. America Spec. Paper 76, p. 124-125, 1964. 3 - 64. The Devonian colonial coral genus Billingsastraea aid its earliest known species: U.S. Geol. Survey Prof. Paper 483-B, p. B1-B5, 1964. OLMSTED, F. H. 1- 64. Relation of percent sodium to source and movement of ground water, National Reactor Testing Station, Idaho: U.S. Geol. Survey Prof. Paper 475-D, p. D186-D188, 1964. 2- 64. (and ROBISON, J. H.) Progress report on geologic investigation of the Yuma area and the East Mesa area of Imperial Valley: U.S. Geol. Survey open-file report, 31 p., 1964. OLTMAN, R. E. 1-64. (STERNBERG, H. O'R., AMES, F. C., and DAVIS, L. C., Jr.) Amazon River investigations, reconnaissance measurements of July 1963: U.S. Geol. Survey Circ.486, 15 p., 1964. OREM, H. M. 1-63. Base flow and summary of streamflow conditions in the Pacific Northwest since October 1, 1962: Columbia Basin Water Forecast Comm. Ann. Mtg., 25th, Portland, Oregon, April 15, 1963, Proc., p. 12-17, 1963. ORKILD, P. P. 1-63. Geologic map of the Tippipah Spring quadrangle, Nye County, Nev.: U.S. Geol. Survey Geol. Quad. Map GQ-213, 1963. O'SULLIVAN, R. B. 1-63. (and BEIKMAN, H. M.) Geology, structure, and uranium deposits of the Shiprock quadrangle, New Mexico and Arizona: U.S. Geol. Survey Misc. Geol. Inv. Map I-345, 1963. OTTON, E. G. 1- 64. (and LAUGHLIN, C. P.) Ground-water conditions in gabbroic rocks near Harford Furnace, Maryland: U.S. Geol. Survey open-file report, 17 p., 1964. 2- 64. (MARTIN, R. O. R., and DURUM, W. H.) Water resources of the Baltimore area, Maryland: U.S. Geol.Survey Water-Supply Paper 1499-F, p. F1-F105, 1964. OTTS, L. E., Jr. 1-63. Water requirements of the petroleum refining industry: U.S. Geol. Survey Water-Supply Paper 1330-G, p. 287-340, 1963. OVERSTREET, W. C. 1- 63. (YATES, R. G., and GRIFFITTS, W. R.) Geology of the Shelby quadrangle, North Carolina: U.S. Geol.Survey Misc. Geol. Inv. Map 1-384, 1963. 2- 63. (YATES, R. G., and GRIFFITTS, W. R.) Heavy minerals in the saprolite of the crystalline rocks in the Shelby quadrangle. North Carolina: U.S. Geol. Survey Bull. 1162-F, p. F1-F31, 1963. 3- 63. Regional heavy-mineral reconnaissance as a guide to ore deposits in areas underlain by deeply weathered crystalline rocks, in Proceedings of the seminar on geochemical prospecting methods and techniques, Bangkok, 1963: New York, United Nations Econ. Comm. Asia and Far East (ECAFE), Mineral Resources Devel. Ser. no. 21, p. 57-66, 1963. OWEN, Vaux, Jr. 1- 63. Geology and ground-water resources of Lee and Sumter Counties, southwest Georgia: U.S. Geol. Survey Water-Supply Paper 1666, 70 p., 1963. 2- 63. Geology and ground-water resources of Mitchell County, Georgia: Georgia Geol. Survey Inf. Circ. 24, 39 p., 1963. OWENS, J. P. 1-64. (and MINARD, J. P.) Pre-Quaternary geology of the Pemberton quadrangle, New Jersey: U.S. Geol. Survey Geol. Quad. Map GQ-262, 1964. PAGE, H. G. 1-63. Water regimen of the inner valley of the San Pedro River near Mammoth, Arizona (A pilot study): U.S. Geol. Survey Water-Supply Paper 1669-1, p. 11-122, 1963. PAGE, L. R. 1-63. Summary of geologic investigations in New England [abs.]: Northern New England Acad. Sci. Bull., p. 10, Oct. 1963’. PAGE, L. V. 1- 63. Water-supply characteristics of Louisiana streams: Louisiana Dept. Public Works Tech. Rept. 1, 109 p., 1963. 2- 63. (NEWCOME, Roy, Jr., and GRAEFF, G. D„ Jr.) Water resources of Sabine Parish, Louisiana: Louisiana Dept. Conserv., Geol. Survey, and Louisiana Dept, of Public Works Water Resources Bull. 3, 146 p., 1963. 3- 63. (and SEABER, P. R.) Water-resources investigations and reports in the Susquehanna River basin: U.S. Geol. Survey open-file report, 1 map, 1963. PAGE, R. W. 1-63. Geology and ground-water appraisal of the Naval Air Missile Test Center area, Point Mugu, Calif.: U.S. Geol. Survey Water-Supply Paper 1619-S, p. S1-S40, 1963. 746-002 0-64- 21A312 PUBLICATIONS IN FISCAL YEAR 1964 PAKISER, L. C. 1- 63. Structure of the crust and upper mantle in the western United States: Jour. Geophys. Research, v. 68, no. 20, p. 5747-5756, 1963. 2- 63. (and HILL, D. P.) Crustal structure in Nevada and southern Idaho from nuclear explosions: Jour. Geophys. Research, v. 68, no. 20, p. 5757-5766, 1963. 1- 64. A gravity study of Long Valley, in Rinehart, C. D., and Ross, D. C., Geology and mineral deposits of the Mount Morrison quadrangle, Sierra Nevada, California: U.S. Geol. Survey Prof. Paper 385, p. 85-89,1964. 2- 64. Reply to comments on papers by L. C. Pakiser, "Structure of the crust and upper mantle in the western United States": Jour. Geophys. Research, v. 69, p. 2162, 1964. PAMPEYAN, E. H. 1-63. Geology and mineral deposits of Mt. Diablo, Contra Costa County, California: Calif. Div. Mines Spec. Rept. 80, 31 p., 1963. 1-64. Franciscan and related rocks of the Mount Diablo piercement, Contra Costa County, California: Geol. Soc. Sacramento (Calif.) Guidebook, Ann. Field Trip, p. 1-8, 1964. PANKEY, Titus 1-63. (and SENFTLE, F. E., and CUTTITTA, F.) Antiferromagnetism of UC>2-2H20: Jour. Chem. Physics, v. 39, no. 7, p. 1702-1706, 1963. PAPADOPULOS, I. S. 1-63. Preparation of type curves for calculating T/S of a wedge-shaped aquifer: U.S. Geol. Survey Prof. Paper 475-B, p. B196-B198, 1963. PARKER, G. G. 1-64. (SHOWN, L. M., and RATZLAFF, K. W.) Officer's cave, a pseudokarst feature in altered tuff and volcanic ash of the John Day formation in eastern Oregon: Geol. Soc. America Bull., v. 75, no. 5, p. 393-402, 1964. PARKER, J. M., 3d 1-63. Geologic setting of the Hamme tungsten district. North Carolina and Virginia: U.S. Geol. Survey Bull. 1122-G, p. G1-G69, 1963. PARKER, R. L. 1- 63. (and HAVENS, R. G.) Thortveitite associated with fluorite, Ravalli County, Mont.: U.S. Geol. Survey Prof. Paper 475-B, p. B10-B11, 1963. 2- 63. (SALAS O., Raul, and PEREZ R., Gabriel) Geologia de los distritos mineros Checo de Cobre, Pampa larga, y parte norte de Cabeza de Vaca, Provincia de Atacama, Chile: [Chile) Inst. Investigaciones Geol. Bol. 14, 46 p., 1963. PASHLEY, E. F., Jr. 1-63. A reinterpretation of the anticlinal structure exposed in the northwest face of Pusch Ridge, Santa Catalina Mountains, Arizona: Arizona Geol. Soc. Digest, v. 6, p. 49-53, 1963. 1-64. Folds in the Tanque Verde, Rincon, and southern Santa Catalina Mountains, Pima County, Arizona [abs.]: Geol. Soc. America Spec. Paper 76, p. 289, 1964. PATTERSON, E. D. 1- 63. Coal resources of Beaver County, Pa.: U.S. Geol. Survey Bull. 1143-A, p. A1-A33, 1963 [1964]. 2- 63. Geologic map of the Roscoe NE quadrangle, Stillwater and Carbon Counties, Mont.: U.S. Geol. Survey Mineral Inv. Field Studies Map MF-267, 1963. PATTERSON, J. L. 1-63. Floods in Texas, magnitude and frequency of peak flows: Texas Water Comm. Bull. 6311, 173 p., 1963. 1-64. Magnitude and frequency of floods in the United States--Pt. 7, Lower Mississippi River basin: U.S. Geol. Survey Water-Supply Paper 1681, 636 p., 1964. PATTERSON, S. H. 1-63. Estimates of world bauxite reserves and potential resources: U.S. Geol. Survey Prof. Paper 475-B, p. B158-B159, 1963. PATTERSON, S. H.™Continued 2-63. Halloysitic underclay deposits and an occurrence of an alumina-silica gel and an allophane-like mineraloid in Hawaii [abs.]: Natl. Clay Conf., 12th, Program and Abstracts, p. 31, 1963. PAVLIDES, Louis 1-64. (and CANNEY, F. C.) Geological and geochemical reconnaissance, southern part of the Smyrna Mills quadrangle, Aroostook County, Maine: U.S. Geol. Survey Prof. Paper 475-D, p. D96-D99, 1964. PAYNE, J. N. 1-64. Hydrogeology of the Sparta Sand in north-central Louisiana [abs.]: Geol. Soc. America, Southeastern Sec., 1964 Ann. Mtg., Baton Rouge, April 1964, Program, p. 29, 1964. PEACE, R. R., Jr. 1-63. Geology and ground-water resources of Franklin County, Alabama: Alabama Geol. Survey Bull. 72, 55 p., 1963. PEARRE, N. C. 1-64. Mining for copper and related minerals in Maryland: Maryland Historical Mag., v. 59, no. 1, p. 15-33, 1964. PECK, D. L. 1-64. Geologic reconnaissance of the Antelope-Ashwood area, north-central Oregon, with emphasis on the John Day Formation of late Oligocene and early Miocene age: U.S. Geol. Survey Bull. 1161-D, p. D1-D26, 1964. PECK, L. C. 1-64. Systematic analysis of silicates: U.S. Geol. Survey Bull. 1170, 89 p„ 1964. PEPPER, J. F. 1-63. (and EVERHART, G. M.) The Indian Ocean, the geology of its bordering lands and the configuration of its floor: U.S. Geol. Survey Misc. Geol. Inv. Map 1-380, 1963. PERLMUTTER, N. M. 1- 63. (and DeLUCA, F. A.) Availability of fresh ground water, Montauk Point area, Suffolk County, Long Island, N. Y.: U.S. Geol. Survey Water-Supply Paper 1613-B, p. B1-B39, 1963. 2- 63. (LIEBER, Maxim, and FRAUENTHAL, H. L.) Movement of waterborne cadmium and hexavalent chromium wastes in South Farmingdale, Nassau County, Long Island, N. Y.: U.S. Geol. Survey Prof. Paper 475-C, p. C179-C184, 1963. PESELNICK, Louis 1-63. (and ROBIE, Richard) Elastic constants of calcite: Jour. Appl. Physics, v. 34, no. 8, p. 2494-2495, 1963. PETERMAN, Z. E. 1-64. (and HEDGE, C. E.) Age of basement rocks from the Williston basin of North Dakota and adjacent areas: U.S. Geol. Survey Prof. Paper 475-D, p. D100-D104, 1964. PETERSON, D. W. 1-63. (and ROBERTS, R. J.) Relation between the crystal content of welded tuffs and the chemical composition: Bull. Volcanol., v. 26, p. 113-123, 1963. PETERSON, N. P. 1-63. Geology of the Pinal Ranch quadrangle, Arizona: U.S. Geol. Survey Bull. 1141-H, p. H1-H18, 1963. PETERSON, W. L. 1- 64. Geology of the Big Spring quadrangle, Kentucky: U.S. Geol. Survey Geol. Quad. Map GQ-261, 1964. 2- 64. Geology of the Platte Canyon quadrangle, Colorado: U.S. Geol. Survey Bull. 1181-C, p. C1-C23, 1964. PETRI, L. R. 1-64. (LANE, C. W., and FURNESS, L. W.) Water resources of the Wichita area, Kansas: U.S. Geol. Survey /Wa/ter-Supply Paper 1499-1, p. 11-169, 1964. PEWE, T. L. 1-64. Ice wedges in Alaska—Classification, distribution and climatic significance [abs.]: Geol.Soc. AmericaSpec. Paper 76, p. 129, 1964.LIST OF PUBLICATIONS A313 PHIBBS, E. J., Jr. 1- 64. (compiler) Chemical and physical character of municipal water supplies in North Carolina: North Carolina Dept. Water Resources, Div. Stream Sanitation and Hydrology Bull. 2, supp. 2, 36 p., 1964. 2- 64. Chemical and physical character of surface waters of North Carolina, 1961-62: North Carolina Dept. Water Resources, Div. Stream Sanitation Bull. 1, v. 6, 218 p., 1964. PHILBIN, P. W. 1-64. (and VARGO, J. L.) Aeromagnetic map of central Gogebic County, Michigan, and vicinity: U.S. Geol. Survey open-file report, map, 1964. PHOENIX, D. A. 1-63. Geology of the Lees Ferry area, Coconino County, Ariz.: U.S. Geol. Survey Bull. 1137, 86 p., 1963. PIERCE, A. P. 1-64. (GOTT, G. B„ and MYTTON, J. W.) Uranium and helium in the Panhandle gas field, Texas, and adjacent areas, with contributions by Henry Faul, G. E. Manger, A. B. Tanner, A. S. Rogers, Rosemary Staatz, and Betty Skipp: U.S. Geol. Survey Prof. Paper 454-G, p. G1-G57, 1964. PIERCE, W. G. 1-63. Reef Creek detachment fault, northwestern Wyoming: Geol. Soc. America Bull., v. 74, no. 10, p. 1225-1236,1963. PLATT, L. B. 1-63. (and CARSWELL, L. D.) Stratigraphy and structure of the Martinsburg formation near Harrisburg, Pennsylvania [abs.]: Geol. Soc. America Spec. Paper 76, p. 131, 1963. PLUHOWSKI, E. J. 1-63. (and KANTROWITZ, I. H.) Influence of land-surface conditions on ground-water temperatures in southwestern Suffolk County, Long Island, N. Y.: U.S. Geol. Survey Prof. Paper 475-B, p. B186-188, 1963. POMERENE, J. B. 1-63. Hand-made map pattern made easily: GeoTimes, v. 8, no. 4, p. 19, 1963. 1- 64. Geology and ore deposits of the Belo Horizonte, Ibiritfe, and Macacos quadrangles, Minas Gerais, Brazil: U.S. Geol. Survey Prof. Paper 341-D, p. D1-D84, 1964. 2- 64. Geology of the Whitley City quadrangle, Kentucky and the Kentucky part of the Winfield quadrangle: U.S. Geol. Survey Geol. Quad. Map GQ-260, 1964. POMEROY, J. S. 1-64. Recognition criteria of igneous and metamorphic rocks on aerial photographs of Chichagof and Kruzof Islands, southeastern Alaska: U.S. Geol. Survey Bull. 1043-E, p. 87-110, 1964. POMMER, A. M. 1-63. Relation between dual acidity and structure of H-montmorillonite: U.S. Geol. Survey Prof. Paper 386-C, p. C1-C23, 1963. POOLE, F. G. 1-64. Geologic map of the Frenchman Flat quadrangle, Nye, Lincoln, and Clark Counties, Nevada: U.S. Geol. Survey Rept. TEI-848 (open-file report), map, 1964. POOLE, J. L. 1-63. Saline ground water—A little used and unmapped resource: Ground Water, v. 1, no. 3, p. 18-20, 1963. POPENOE, Peter 1- 63. (and ZANDLE, G. L.) Aeromagnetic map of the Heath quadrangle, Franklin County, Massachusetts, and Windham County, Vermont: U.S. Geol. Survey Geophys. Inv. Map GP-433, 1963. 2- 63. (and ZANDLE, G. L.) Aeromagnetic map of the Millers Falls quadrangle, Franklin County, Massachusetts: U.S. Geol. Survey Geophys. Inv. Map GP-434, 1963. 3- 63. (and ZANDLE, G. L.) Aeromagnetic mapof the Rowe quadrangle, Franklin and Berkshire Counties, Mass., and Windham and Bennington Counties, Vt.: U.S. Geol. Survey Geophys. Inv. Map GP-437, 1963. POPENOE, Peter—Continued 1- 64. (BOYNTON, G. R., and ZANDLE, G. L.) Aeromagnetic map of the Beckett quadrangle, Berkshire, Hampshire, and Hampden Counties, Massachusetts: U.S. Geol. Survey Geophys. Inv. Map GP-448, 1964. 2- 64. (BOYNTON, G. R„ and ZANDLE, G. L.) Aeromagnetic map of the Berlin quadrangle, Berkshire County, Massachusetts, Rensselaer County, New York, and Bennington County, Vermont: U.S. Geol. Survey Geophys. Inv. Map GP-449, 1964. 3- 64. (BOYNTON, G. R., and ZANDLE, G. L.) Aeromag- netic map of part of the Canaan quadrangle, Berkshire County, Massachusetts, and Columbia and Rensselaer Counties, New York: U.S. Geol. Survey Geophys. Inv. Map GP-450, 1964. 4- 64. (BOYNTON, G. R., and ZANDLE, G. L.) Aeromagnetic map of the Cheshire quadrangle, Berkshire County, Massachusetts: U.S. Geol. Survey Geophys. Inv. Map GP-451, 1964. 5- 64. (BOYNTON, G. R., and ZANDLE, G. L.) Aeromagnetic map of the Hancock quadrangle, Berkshire County, Massachusetts, and Rensselaer County, New York: U.S. Geol. Survey Geophys. Inv. Map GP-453, 1964. 6- 64. (BOYNTON, G. R., and ZANDLE, G. L.) Aeromagnetic map of the Peru quadrangle, Berkshire and Hampshire Counties, Massachusetts: U.S. Geol. Survey Geophys. Inv. Map GP-455, 1964. 7- 64. (BOYNTON, G. R., and ZANDLE, G. L.) Aeromagnetic map of the Pittsfield East quadrangle, Berkshire County, Massachusetts: U.S. Geol. Survey Geophys. Inv. Map GP-456, 1964. 8- 64. (BOYNTON, G. R., and ZANDLE, G. L.) Aeromagnetic map of the Pittsfield West quadrangle, Berkshire County, Massachusetts and Columbia County, New York: U.S. Geol. Survey Geophys. Inv. Map GP-457, 1964. 9- 64. (BOYNTON, G. R„ and ZANDLE, G. L.) Aeromagnetic map of the State Line quadrangle, Berkshire County, Mass., and Columbia County, N. Y.: U.S. Geol. Survey Geophys. Inv. Map GP-458, 1964. 10- 64. (BOYNTON, G. R„ and ZANDLE, G. L.) Aeromagnetic map of the Stockbridge quadrangle, Berkshire County, Mass.: U.S. Geol. Survey Geophys. Inv. Map GP-459, 1964. 11- 64. (BOYNTON, G. R., and ZANDLE, G. L.) Aeromagnetic map of the Williamstown quadrangle, Berkshire County, Mass., and Bennington County, Vt.: U.S. Geol. Survey Geophys. Inv. Map GP-460, 1964. 12- 64. (BOYNTON, G. R., and ZANDLE, G. L.) Aeromagnetic map of the Windsor quadrangle, Berkshire County, Mass.: U.S. Geol. Survey Geophys. Inv. MapGP-461, 1964. 13- 64. (PETTY, A. J., and TYSON, N. S.) Aeromagnetic map of western Pennsylvania and parts of eastern Ohio, northern West Virginia, and western Maryland: U.S. Geol. Survey Geophys. Inv. Map GP-445, 1964. 14- 64. Aeroradioactivity of parts of east-central New York and west-central New England: U.S. Geol. Survey Geophys. Inv. Map GP-358, 1964. PORTERFIELD, George 1-64. (and DUNHAM, C. A.) Sedimentation of Lake Pills-bury. Lake County, California: U.S. Geol. Survey Water-Supply Paper 1619-EE, p. EE1-EE46, 1964. POST, E. V. 1- 63. (and HITE, J. B.) Heavy metals in stream sediment, west-central Maine: U.S. Geol. Survey Mineral Inv. Field Studies Map MF-278, 1963. 2- 63. (and DENNEN, W. H.) Geochemical mapping in Maine [abs.]: Mining Eng., v. 16, no. 1, p. 67, 1963. POTH, C. W. 1-63. Geology and hydrology of the Mercer quadrangle, Mercer, Lawrence, and Butler Counties, Pennsylvania: Pennsylvania Geol. Survey, 4th ser., Ground Water Rept. W 16, 149 p., 1963.A314 PUBLICATIONS IN FISCAL YEAR 1964 POTH, C. W.--Continued 2-63. The ground-water observation-well program in Pennsylvania: Pennsylvania Geol. Survey, 4th ser., Ground Water Rept. W 20, 18 p., 1963. POWELL, W. J. 1-63. (CARROON, L. E., and AVRETT, J. R.) Water problems associated with oil production in Alabama: Alabama Geol. Survey Circ. 22, 63 p., 1963. POWERS, H. A. 1-64. (and WILCOX, R. E.) Volcanic ash from Mount Ma-zama (Crater Lake) and from Glacier Peak: Science, v. 144, p. 1334-1336, 1964. PRESCOTT, G. C., Jr. 1- 63. Geologic map of the surficial deposits of part of southwestern Maine and their water-bearing characteristics: U.S. Geol. Survey Hydrol. Inv. Atlas HA-76, 1963. 2- 63. Reconnaissance of ground-water conditions in Maine: U.S. Geol. Survey Water-Supply Paper 1669-T, p. Tl-T52, 1963. 1-64. Records of wells, springs, and test borings in the lower Penobscot River basin, Maine: U.S. Geol. Survey open-file report, 13 p., 1964. PRICE, Don 1-63. (HART, D. H., and FOXWORTHY, B. L.) Artificial recharge in Oregon and Washington: U.S. Geol. Survey open-file report, 161 p., 1963. PRICE, W. E., Jr. 1-63. Geology and hydrology of alluvial deposits along the Ohio River between South Portsmouth and the Manchester Islands, Ky.: U.S. Geol. Survey Hydrol. Inv. Atlas HA-73, 1963. 1- 64. Geology and hydrology of alluvial deposits along the Ohio River between Ethridge and the Twelvemile Island, Ky.: U.S. Geol. Survey Hydrol. Inv. Atlas HA-97, 1964. 2- 64. Geology and hydrology of alluvial deposits along the Ohio River between Newport and Warsaw, Ky.: U.S. Geol. Survey Hydrol. Inv. Atlas HA-98, 1964. 3- 64. Geology and hydrology of alluvial deposits along the Ohio River between the Manchester Islands and Silver Grove, Kentucky: U.S. Geol. Survey Hydrol. Inv. Atlas HA-94, 1964. PRILL, R. C. 1-64. (JOHNSON, A. I., and MORRIS, D. A.) Specific yield--Laboratory experiments showing the effect of time on column drainage: U.S. Geol. Survey open-file report, 55 p.. 1964. QUINN, A. W. 1- 63. Bedrock geology of the Crompton quadrangle, Rhode Island: U.S. Geol. Survey Bull. 1158-B, p. B1-B17, 1963. 2- 63. Geologic sketch mapof Newport, Rhode Island, vicinity, in New England Intercollegiate Geol. Conf. Guidebook, 55th Ann. Mtg., Providence, R. I., Oct. 4-6, 1963. 1-64. Geology of the Narragansett Bay area, Rhode Island: U.S. Geol. Survey open-file report, map, 1964. RADBRUCH, D. H. 1-64. Engineering geology in the San Francisco Bay area, California [abs.]: Geol. Soc. America Spec. Paper 76, p. 133-134, 1964. RADER, L. F. 1-63. (SWADLEY, W. C., HUFFMAN, Claude, Jr., and LIPP, H. H.) New chemical determinations of zinc in basalts and rocks of similar composition: Geochim. et Cosmochim. Acta, v. 27, no. 6, p. 695-714, 1963. RAINEY, H. C., 3d 1-63. Geology of the Hadley quadrangle, Kentucky: U.S. Geol. Survey Geol. Quad. Map GQ-237, 1963. 1-64. Geology of the Rockfield quadrangle, Kentucky: U.S. Geol. Survey Geol. Quad. Map GQ-309, 1964. RAMIREZ, L. F. 1-63. (ELBERG, E. L., Jr., and HELLEY, H. H.) Geologic map of the south central Rub A1 Khali quadrangle. Kingdom of Saudi Arabia: U.S. Geol. Survey Misc. Geol. Inv. Map I-219A, 1963. RAMIREZ, L. F.—Continued 2-63. (ELBERG, E. L., Jr., and HELLEY, H. H.) Geologic map of the southeastern Rub A1 Khali quadrangle, Kingdom of Saudi Arabia: U.S. Geol. Survey Misc. Geol. Inv. Map I-220A, 1963. RANDALL, A. D. 1-64. Geology and ground water in the Farmington-Granby area, Connecticut: U.S. Geol. Survey Water-Supply Paper 1661, 129 p., 1964. RANDICH, P. G. 1- 64. Geology and ground-water resources of Burleigh County, North Dakota-Pt. 2, Ground-water basic data: U.S. Geol. Survey open-file report, 449 p., 1964. 2- 64. Map of Burleigh County, North Dakota, showing the location of aquifers and potential yields: U.S. Geol. Survey open-file report, 1964. RANDOLPH, W. J. 1-64. (and FRYE, P. M.) Floods on Mill Creek near Antioch, Tennessee: U.S. Geol. Survey open-file report, 20 p., 1964. RANTZ, S. E. 1- 63. An empirical method of determining momentary discharge of tide-affected streams: U.S. Geol. Survey Water-Supply Paper 1586-D, p. D1-D28, 1963. 2- 63. Annual runoff in the Santa Margarita River basin, California, 1925-62: U.S. Geol. Survey open-file report, 16 p., 1963. 3- 63. Optimum discharge for king salmon spawning as related to hydrologic characteristics in northern California Coast Ranges: U.S. Geol. Survey open-file report, 38 p., 1963; abs., Am. Geophys. Union Trans., v. 45, no. 2, p. 357, 1964. 4- 63. (and HARRIS, E. E.) Floods of January-February 1963 in California and Nevada: U.S. Geol. Survey open-file report, 74 p., 1963. 5- 63. Snowmelt hydrology of the North Yuba River basin, California: U.S. Geol. Survey Prof. Paper 475-C, p. C191-C193, 1963. 1- 64. Snowmelt hydrology of a Sierra Nevada stream: U.S. Geol. Survey Water-Supply Paper 1779-R, p. R1-R36, 1964. 2- 64. Surface-water hydrology of coastal basins of northern California: U.S. Geol. Survey Water-Supply Paper 1758, 77 p., 1964. RATTE, J. C. 1-64. (and STEVEN, T. A.) Magmatic differentiation in a volcanic sequence related to the Creede caldera, Colorado: U.S. Geol. Survey Prof. Paper 475-D, p. D49-D53, 1964. RAU, W. W. 1-63. Foraminifera from the upper part of the Poul Creek Formation of southeastern Alaska: Cushman Found. Foram. Research Contr., v. 14, pt. 4, p. 135-145, 1963. 1-64. Foraminifera from the northern Olympic Peninsula, Washington: U.S. Geol. Survey Prof. Paper 374-G,p. Gl-G33, 1964. RAWSON, Jack 1- 63. Quality of water from test wells in the Castolon area. Big Bend National Park, Brewster County, Texas: U.S. Geol. Survey open-file report, 12 p., 1963. 2- 63. Solution of manganese dioxide by tannic acid: U.S. Geol. Survey Prof. Paper 475-C, p. C218-C219, 1963. RAY, H. A. 1-63. (and YOUNG, L. E.) Areas of potential flood inundation, San Luis Rey River basin, California: U.S. Geol. Survey open-file report, 25 p., 1963. RAY, L. L. 1-63. Quaternary events along the unglaciated lower Ohio River valley: U.S. Geol. Survey Prof. Paper 475-B, p. B125-B128, 1963. 1-64. The Charleston, Mo., alluvial fan, jrj Geol. Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B130-B134, 1964.LIST OF PUBLICATIONS A315 READ, C. B. 1-64. (and MAMAY, S. H.) Upper Paleozoic floral zones and floral provinces of the United States, witha Glossary of stratigraphic terms by G. C. Keroher: U.S.Geol. Survey Prof. Paper 454-K, p. K1-K35, 1964. REDDEN, J. A. 1- 63. Diamond drilling exploration of the Beecher No. 3-Black Diamond pegmatite, Custer County, S. Dak.: U.S. Geol. Survey Bull. 1162-E, p. El-Ell, 1963. 2- 63. Geology and pegmatites of the Fourmilequadrangle, Black Hills, S. Dak.: U.S. Geol.Survey Prof. Paper 297-D, p. D199-D291, 1963. REED, J. C., Jr. 1- 63. (and JOLLY, Janice) Crystalline rocks of the Potomac River gorge near Washington, D. C.: U.S. Geol. Survey Prof. Paper 414-H, p. H1-H16, 1963. 2- 63. Structure of Precambrian crystalline rocks in the northern part of Grand Teton National Park, Wyo.: U.S. Geol. Survey Prof. Paper 475-C, p. C1-C6, 1963. 3- 63. (BRYANT, Bruce, and HACK, J. T.) Origin of some intermittent ponds on quartzite ridges in western North Carolina: Geol. Soc. America Bull., v. 74, no. 9, p. 1183-1188, 1963. 1- 64. Geologic maps of part of the Grandfather Mountain window, North Carolina: Sheet 1, Linville Falls 15'quadrangle, Sheet 2, Southwestern extension of the window, by J. C. Reed, Jr., and Bruce Bryant: U.S. Geol. Survey open-file report, 2 maps, 1964. 2- 64. Geology of the Lenoir quadrangle. North Carolina: U.S. Geol. Survey Geol. Quad. Map GQ-242, 1964. 3- 64. Map of the lower portion of the Teton Glacier, Grand Teton National Park, Wyoming: U.S. Geol. Survey open-file report, map, 1964. 4- 64. (BRYANT, Bruce, LEOPOLD, E. B., and WEILER, Louise) A Pleistocene section at Leonards Cut, Burke County, N. C.: U.S. Geol. Survey Prof. Paper 475-D, p. D38-D42, 1964. REEDER, H. O. 1-63. (BJORKLUND, L. J., and DINWIDDIE, G. A.) Quantitative analysis of water resources in the Albuquerque area, New Mexico: U..S. Geol. Survey open-file report, 55 p., 1963. REESIDE, J. B., Jr. 1-64. Fossils from lower part of the Mancos Shale, Disappointment Valley, San Miguel County, Colorado (Introduction by Daniel R. Shawe): U.S. Geol. Survey open-file report, 1 sheet, 1964. RICHARDSON, R. M. 1-63. Significance of climate in relation to the disposal of radioactive waste at shallow de-’th below ground, in Comptes Rendu du Colloque International sur la Retention et la Migration des Ions Radioactifs dans les Sols, Saclay, 1962: Paris, Presses Universitaires de France, p. 207-211, 1963. RICHMOND, G. M. 1-63. High level erosion surfaces in the Rocky Mountains--age and origin [abs.]: Assoc. Am. Geographers Annals, v. 53, no. 4, p. 618, 1963. RICHTER, D. H. 1-63. Volcano observations: Am. Geophys. Union Trans., v. 44, no. 2, p. 505-507, 1963. RIGGS, H. C. 1-63. Discussion of "Reservoir mass analysis by low-flow series", by John B. Stall: Am. Soc. Civil Engineers Proc., Jour. Sanitary Eng. Div., v. 89, no. SA 2, pt. 1, p. 122-125, 1963. 1-64. The relation of discharge to drainage area in the Rappahannock River basin, Virginia, iri Geol. Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B165-B168, 1964. RIMA, D. R. 1-64. (COSKERY, O. J., and ANDERSON, P. W.) Ground-water resources of southern New Castle County, Del.: U.S. Geol. Survey Water-Supply Paper 1756, 54 p., 1964. RINEHART, C. D. 1-64. (and ROSS, D. C.) Geology and mineral deposits of the Mount Morrison quadrangle. Sierra Nevada, California, with a section on A gravity study of Long Valley, by L. C. Pakiser: U.S. Geol. Survey Prof. Paper 385, 106 p., 1964. ROBERSON, C. E. 1-63. (FETH, J. H., SEABER, P. R., and ANDERSON, Peter) Differences between field and laboratory determinations of pH, alkalinity, and specific conductance of natural water: U.S. Geol. Survey Prof. Paper 475-C, p. C212-C215, 1963. 1-64. Carbonate equilibria in selected natural waters: Am. Jour. Sci., v. 262, no. 1, p. 56-65, 1964. ROBERTS, A. E. 1-63. The Livingston Group of south-central Montana: U.S. Geol. Survey Prof. Paper 475-B, p. B86-B92, 1963. 1- 64. Geologic map of the Bozeman Pass quadrangle, Montana: U.S. Geol. Survey Misc. Geol. Inv. Map 1-399, 1964. 2- 64. Geology of the Bnsbin quadrangle, Montana: U.S. Geol. Survey Geol. Quad. Map GQ-256, 1964. 3- 64. Geology of the Chimney Rock quadrangle, Montana: U.S. Geol. Survey Geol. Quad. Map GQ-257, 1964. 4- 64. Geologic map of the Fort Ellis quadrangle, Montana: U.S. Geol. Survey Misc. Geol. Inv. Map 1-397, 1964. 5- 64. Geology of the Hoppers quadrangle, Montana: U.S. Geol. Survey Geol. Quad. Map GQ-258, 1964. 6- 64. Geology of the Livingston quadrangle, Montana:U.S. Geol. Survey Geol. Quad. Map GQ-259, 1964. 7- 64. Geologic map of the Maxey Ridge quadrangle, Montana: U.S. Geol. Survey Misc. Geol. Inv. Map 1-396, 1964. 8- 64. Geologic map of the Mystic Lake quadrangle, Montana: U.S. Geol. Survey Misc. Geol. Inv. Map 1-398, 1964. ROBERTS, R. J. 1- 64. Exploration targets in north-central Nevada: U.S. Geol. Survey open-file report, 10 p., 1964. 2- 64. (and THOMASSON, M. R.) Comparisonof late Paleozoic depositional history of northern Nevada and central Idaho: U.S. Geol. Survey Prof. Paper 475-D, p. D1-D6, 1964. ROBERTSON, E. C. 1-63. Review of "Theory of flow and fracture of solids", vol. 2, by A. Nadai: Am. Geophys. Union Trans., v. 44, no. 4, p. 1021-1023, 1963. 1-64. Time-dependent strain in rocks and metals [abs.]: Geol. Soc. America Spec. Paper 76, p. 137-138, 1964. ROBERTSON, J. F. 1-63. Geology of the lead-zinc deposits in the Municipio de Januaria, State of Minas Gerais, Brazil: U.S. Geol. Survey Bull. 1110-B, p. 35-110, 1963 [1964], ROBIE, R. A. 1-64. Equilibrium of talc with enstatite and quartz: Science, v. 143, no. 3610, p. 1057, 1964. ROBINOVE, C. J. 1- 63. Photography and imagery—A clarification of terms: Photogramm. Eng., v. 29, no. 5, p. 880-881, 1963. 2- 63. What's happening to water?: Smithsonian Inst. Rept. 1962, p. 375-389, 1963. 3- 63. (and CUMMINGS, T. R.) Ground-water resources and geology of the Lyman-Mountain View area, Uinta County, Wyo.: U.S. Geol. Survey Water-Supply Paper 1669-E, p. E1-E43, 1963. ROBINSON, C. S. 1- 64. (CARROLL, R. A., and LEE, F. T.) Preliminary report on the geologic and geophysical investigations of the Loveland Basin landslide. Clear Creek County, Colorado: U.S. Geol. Survey open-file report, 5 p., 1964. 2- 64. (and LEE, F. T.) Research in the engineering geology of the Straight Creek tunnel site, Colorado [abs.]: Geol. Soc. America Spec. Paper 76, p. 291, 1964. ROBINSON, G. D. 1-64. (WANEK, A. A., HAYS, W. H., and McCALLUM, M. E.) Philmont Country, the rocks and landscape of aA316 PUBLICATIONS IN FISCAL YEAR 1964 ROBINSON, G. D.--Continued famous New Mexico ranch, illustrated by J. R. Stacey: U.S. Geol. Survey Prof. Paper 505, 152 p., 1964. RODIS, H. G. 1- 63. Geology and occurrence of ground-water in Lyon County, Minn.: U.S. Geol. Survey Water-Supply Paper 1619-N, p. N1-N41, 1963. 2- 63. (and ISKANDER, Wilson) Ground water in the Nahud outlier of the Nubian Series, Kordofan Province, Sudan: U.S. Geol. Survey Prof. Paper 475-B, p. B179-B181, 1963. ROEDDER, Edwin 1- 64. Evidence from fluid inclusions as to the nature of the ore-forming fluids [abs.]: Fortschr. fur Mineral-ogie, v. 41, p. 190, 1964. 2- 64. Metastable "superheated" ice in fluid inclusions under high negative pressure [abs.]: Geol. Soc. America Spec. Paper 76, p. 139-140, 1964. ROEN, J. B. 1-64. (MILLER, R. L., and HUDDLE, J. W.) The Chattanooga Shale (Devonian and Mississippian) in the vicinity of Big Stone Gap, Va., in Geol. Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B43-B48, 1964. ROGERS, C. L. 1-63. (van VLOTEN, Roger, RIVERA, J. O., AMEZCUA, E. T., and de CSERNA, Zoltan) Plutonic rocks of northern Zacatecas and adjacent areas, Mexico: U.S. Geol.Survey Prof. Paper 475-C, p. C7-C10, 1963. ROGERS, W. B. 1-63. Geology of the Eddyville quadrangle, Kentucky: U.S. Geol. Survey Geol. Quad. Map GQ-255, 1963. ROHRER, Wr. L. 1-63. (and LEOPOLD, E.BJFenton Pass Formation (Pleistocene?), Bighorn Basin, Wyo.: U.S. Geol. Survey Prof. Paper 475-C, p. C45-C48, 1963. 1- 64. Geology of the Sheep Mountain quadrangle, Wyoming: U.S. Geol. Survey Geol. Quad. Map GQ-310, 1964. 2- 64. Geology of the Tatman Mountain quadrangle, Wyoming: U.S. Geol. Survey Geol. Quad. Map GQ-311, 1964. ROLLER, J. C. 1- 63. New results on crustal thickness and upper-mantle velocities from seismic-refraction measurements [abs.]: Am. Geophys. Union Trans., v. 44, no. 4, p. 890, 1963. 2- 63. (and HEALY, J. H.) Seismic-refraction measurements of crustal structure between Santa Monica Bay and Lake Mead: Jour. Geophys. Research, v. 68, no. 20, p. 5837-5850, 1963. 1-64. Crustal structure in the vicinity of Las Vegas, Nev., from seismic and gravity observations: U.S. Geol. Survey Prof. Paper 475-D, p. D108-D111, 1964. ROMAN, Irwin 1-64. Controlled quadrature: Mathematics of Computation, v. 18, no. 86, p. 254-263, 1964. RORABAUGH, M. I. 1-63. Streambed percolation in development of water supplies, in Methods of collecting and interpreting ground-water data, compiled by Ray Bentall: U.S. Geol. Survey Water-Supply Paper 1544-H, p. H47-H62, 1963. 1-64. Estimating changes in bank storage and ground-water contribution to streamflow: Internat. Assoc. Sci. Hydrology Pub. 63, Symposium Surface Waters, p. 432-441, 1964. ROSE, H. J., Jr. 1- 63. (ADLER, Isidore, and FLANAGAN, F. J.) X-ray fluorescence analysis of the light elements in rocks and minerals: Jour. Applied Spectroscopy, v. 17, no. 4, p. 81-85, 1963. 2- 63. (and BROWN, Robena) X-ray fluorescence analysis of niobate-tantalate ore concentrates [abs.], in Program: 12th Ann. Conf. on Application of X-ray Analysis, Denver, p. 33-34, 1963. 3- 63. Semimicro X-ray fluorescence analysis of minerals, rocks, and ores [abs.],_in Program, 11th Ann. Conf.: Assoc. Anal. Chemists, Detroit, p. 92, 1963. ROSE, H. J., Jr.--Continued 1-64. (CUTTITTA, Frank, CARRON, M. K., and BROWN, Robena) Semimicro X-ray fluorescence analysis of tek-tites using 50-milligram samples: U.S. Geol. Survey Prof. Paper 475-D, p. D171-D173, 1964. ROSEN, A. A. 1-64. (and RUBIN, Meyer) Natural carbon-14 activity of organic substance in streams: Science, v. 143, no. 3611, p. 1163-1164, 1964. ROSENSHEIN, J. S. 1-63. Recharge rates of principal aquifers in Lake County, Indiana: Ground Water, v. 1, no. 4, p. 13-20, 1963. 1- 64. (and HUNN, J. D.) Ground-water hydrology, development, and potential of rock units. Lake County, Indiana, with special emphasis on Geohydrology of rocks of Silurian and Quaternary ages: U.S. Geol. Survey open-file report, 54 p., 1964. 2- 64. (and HUNN, J. D.) Ground-water hydrology, development, and potential of rock units of Quaternary age, Porter and La Porte Counties, Indiana: U.S. Geol. Survey open-file report, 41 p., 1964. ROSHOLT, J. N. 1-64. (GARNER, E. L., and SHIELDS, W. R.) Fractionation of uranium isotopes and daughter products in weathered granite and uranium-bearing sandstone, Wind River basin, Wyoming, m Geol. Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B84-B87, 1964. ROSS, C. P. 1- 63. The Belt series in Montana, with a geologic map compiled by B. A. L.Skipp. and a gg£ti£>n an Paleontologic criteria by Richard Rezak: U.S. Geol. Survey Prof. Paper 346, 122 p., 1963 [1964]. 2- 63. Modal composition of the Idaho batholith: U.S. Geol. Survey Prof. Paper 475-C, p. C86-C90, 1963. ROSS, C. S. 1-64. Volatiles in volcanic glasses and their stability relations: Am. Mineralogist, v. 40, no. 3-4, p. 258-271, 1964. ROSS, D. C. 1-63. New Cambrian, Ordovician, and Silurian formations in the Independence quadrangle, Inyo County, Calif.: U.S. Geol. Survey Prof. Paper 475-B, p. B74-B85, 1963. ROSS, Malcolm 1-63. The crystallography of meta-autunite (I): Am. Mineralogist, v. 48, no. 11-12, p. 1389-1393, 1963. 1-64. Crystal chemistry of beryllium: U.S. Geol. Survey Prof. Paper 468, 30 p., 1964. ROWE, J. J. 1-63. Releasing-addition method for the flame photometric determination of calcium in thermal waters: Geochim. et Cosmochim. Acta, v. 27, p. 915-923, 1963. RUBIN, Jacob 1-63. (and STEINHARDT, R.) Soil water relations during rain infiltration-[Pt.] 1, Theory: Soil Sci. Soc. America Proc., v. 27, no. 3, p. 246-251, 1963. RUBIN, Meyer 1-63. (and TAYLOR, D. W.) Radiocarbon activity of shells from living clams and snails: Science, v. 141, no. 3581, p. 637, 1963. RUGGLES, F. H., Jr. 1-64. Frequency and extent of flooding on Lower White Rock Creek at Dallas, Texas: U.S. G eol. Survey and City of Dallas open-file report 69, 23 p., 1964. RUPPEL, E. T. 1-63. Geology of the Basin quadrangle, Jefferson, Lewis and Clark, and Powell Counties, Mont.: U.S. Geol. Survey Bull. 1151, 121 p„ 1963. RUSH, F. E. 1-63. (and EAKIN, T. E.) Ground-water appraisal of Lake Valley in Lincoln and White Pine Counties, Nevada: Nevada Dept. Conserv. and Nat. Resources Ground-Water Resources--Reconn. Ser. Rept. 24, 29 p., 1963.LIST OF PUBLICATIONS A317 RUTLEDGE, D. H. 1-63. (and GESSEL, C. D.) Closing discussion of paper "Large scale mapping of Lake Powell," by Clyde D. Ges-sel and Dwight H. Rutledge: Am. Soc. Civil Engineers Proc., v. 89, Jour. Surveying and Mapping Div., no. SU3, p. 179, 1963. RYALL, Allan 1-63. (and STUART, D. J.) Traveltimes and amplitudes from nuclear explosions: Nevada Test Site to Ordway, Colorado: Jour. Geophys. Research, v. 68, no. 20, p. 5821-5835, 1963. 1- 64. (and STUART, D. J.) Travel times and amplitudes from nuclear explosions: Nevada Test Site to Ordway, Colorado [abs.]: Geol. Soc. America Spec. Paper 76, p. 221-222, 1964. 2- 64. Improvement of array seismic recordings by digital processing: Seismol. Soc. America Bull., v. 54, no. 1, p. 277-294, 1964. SACHET, Marie-Helene 1-63. History of change in the biota of Clipperton Island, in J. Linsley Gressitt, ed.. Pacific basin biogeography, a symposium: Bishop Mus. Press, Honolulu, p. 525-534, 1963. SAINSBURY, C. L. 1-63. Beryllium deposits of the western Seward Peninsula, Alaska: U.S. Geol. Survey Circ. 479, 18 p., 1963. 1- 64. Geology of Lost River mine area, Alaska: U.S. Geol. Survey Bull. 1129, 80 p., 1964. 2- 64. Preliminary geologic map and structure sections of the central York Mountains, Seward Peninsula, Alaska: U.S. Geol. Survey open-file report, map, 1964. SAINT-AMAND, Pierre 1-64. (and ERICKSEN, G. E.) Las Melosas-El Volcan, Chile, earthquake swarm of August and September 1958 [abs.]: Geol. Soc. America Spec. Paper 76, p. 222-223, 1964. SAKAKURA, A. Y. 1-64. Solution of the gamma-ray transport equation for two media, the ground source and air, in airborne radioactivity surveying: U.S. Geol. Survey open-file report, 244 p., 1964. SAMMEL, E. A. 1-63. Surficial geology of the Ipswich quadrangle, Massachusetts: U.S. Geol. Survey Geol. Quad. MapGQ-189, 1963. SANDBERG, C. A. 1- 63. Dark shale unit of Devonian and Mississippian age in northern Wyoming and southern Montana: U.S. Geol. Survey Prof. Paper 475-C, p. C17-C20, 1963. 2- 63. Spirorbal limestone in the Souris River(?) Formation of Late Devonian age at Cottonwood Canyon, Bighorn Mountains, Wyo.: U.S. Geol. Survey Prof. Paper 475-C, p. C14-C16, 1963. SANDBERG,G. W. 1-63. Ground-water data, Beaver, Escalante, Cedar City, and Parowan Valleys, parts of Washington, Iron, Beaver, and Millard Counties, Utah: U.S. Geol. Survey and Utah State Engineer Basic-Data Rept. 6, 26 p., 1963. SANDO, W. J. 1-63. New species of colonial rugose corals from the Mississippian of northern Arizona: Jour. Paleontology, v. 37, no. 5, p. 1074-1079, 1963. SARGENT, K. A. 1-63. The grooved plate, a simple petrographic aid for size measurements of elongate minerals: Am. Mineralogist, v. 48, no. 11-12, p. 1403-1405, 1963. SAUER, V. B. 1-63. Spur dikes in Louisiana: U.S. Geol. Survey open-file report, 4 p., 1963. SAWYER, R. M. 1-63. Effect of urbanization on storm discharge and ground-water recharge in Nassau County, N. Y.: U.S. Geol. Survey Prof. Paper 475-C, p. C185-C187, 1963. SAYRE, W. W. 1- 63. (and.CHAMBERLAIN, A. R.) Exploratory laboratory study of lateral turbulent diffusion at the surface of an alluvial channel: U.S. Geol. Survey open-file report, 36 p., 1963. 2- 63. (and HUBBELL, D. W.) Dispersal of bed sediments, in Transport of radionuclides in fresh water systems: U.S. Atomic Energy Comm. Rept. TID-7664, p. 327-352, 1963. 3- 63. (and HUBBELL, D. W.) Transport and dispersion of labeled bed material. North Loup River, Nebraska: U.S. Geol. Survey open-file report, 112 p., 1963. SCHAFER, J. P. 1-63. Trip C, Glacial geology, Providence to Point Judith, in New England Intercollegiate Geol. Conf., Guidebook, 55th Ann. Mtg., Providence, R. I., Oct. 4-6, p. 34-38, 1963. SCHEIDEGGER, A. E. 1- 63. Discussion of "On the statistics of fault plane solutions of earthquakes", by A. J. de Witte: Jour. Geophys. Research, v. 68, no. 18, p.5231-5232, 1963. 2- 63. Dynamical similarity in erosional processes: Geo-fisica Pura e Appl., v. 56, no. 3, p. 58-66, 1963^ 1- 64. Comments on "The determination of tectonic stresses through analysis of hydraulic well fracturing", by R.O. Kehle: Jour. Geophys. Research, v. 69, no. 10, p. 2155-2156, 1964. 2- 64. Lithologic variations in slope development theory: U.S. Geol. Survey Circ. 485, 8 p., 1964. 3- 64. Some implications of statistical mechanics in geomorphology: Internat. Assoc. Sci. Hydrology Bull., v. 9, no. 1, p. 12-16, 1964. SCHELL, E. M. 1-64. (and GERE, W. C.) Preliminary report on the phosphate deposits and stratigraphy of Permian rocks in Dry Bread Hollow, Weber County, Utah: U.S. Geol. Survey open-file report, 36 p., 1964. SCHINER, G. R. 1-63. Ground-water exploration and test pumping in the Halma-Lake Bronson area, Kittson County, Minn.: U.S. Geol. Survey Water-Supply Paper 1619-BB, p. BB1-BB38, 1963. SCHLANGER, S. O. 1-63. Subsurface geology of Eniwetok Atoll, with sections on Carbonate mineralogy by D. L. Graf and J. R. Goldsmith; Petrography of the basalt beneath the limestones, by G. A. Macdonald; Dating of carbonate rocks by ionium-uranium ratios, by W. M. Saclfett and H.A. Potratz: U.S. Geol. Survey Prof. Paper 260-BB, p. 991-1066, 1963. SCHLEE, J. S. 1- 63. (and MOENCH, R. H.) Geologic map of the Mesita quadrangle. New Mexico: U.S. Geol. Survey Geol. Quad. Map GQ-210, 1963. 2- 63. (and MOENCH, R. H.) Geologic map of the Moquino quadrangle. New Mexico: U.S. Geol. Survey Geol. Quad. Map GQ-209, 1963. 3- 63. Texture of sediments: Woods Hole Oceanog. Inst. Summ. Inv. Conducted 1962, Reference no. 63-18, Chemistry-Geology, p. 21-22, 1963. 1-64. (UCHUPI, Elazar, and TRUMBULL, J. V. A.) Size parameters of Cape Cod beach and eolian sands [abs.]: Geol. Soc. America Spec. Paper 76, p. 144, 1964. SCHMIDT, D. L. 1-63. (FORD, A. B., DOVER, J. H„ and BROWN, R. D.) Preliminary geology and structure of the Patuxent Mountains, Antarctica [abs.]: Polar Record, v. 11, no. 75, p. 760, 1963. 1-64. Reconnaissance petrographic cross section of the Idaho batholith in Adams and Valley Counties, Idaho: U.S. Geol. Survey Bull. 1181-G, p. G1-G50, 1964. SCHMIDT, R. A. M. 1-63. Pleistocene microfauna of the Bootlegger Cove Clay: Science, v. 141, p. 350-351, 1963.A318 PUBLICATIONS IN FISCAL YEAR 1964 SCHMIDT, Robert George 1-64. (SWANSON, D. A., andZUBOVIC, Peter) Preliminary-geologic map and sections of the Hogan 4 Northeast quadrangle, Lewis and Clark, and Cascade Counties, Mont.: U.S. Geol. Survey Misc. Geol. Inv. Map 1-409, 1964. SCHMIDT, Robert Gordon 1- 63. Geology and ore deposits of the Cuyuna North Range, Minnesota: U.S. Geol. Survey Prof. Paper 407, p. 1-96, 1963. 2- 63. (and ASAD, S. A.) A reconnaissance survey of radioactive beach sand at Cox's Bazar, East Pakistan: Geol. Survey of Pakistan Interim Geol. Report no. 3, 13 p., 1963. SCHNEIDER, Robert 1-64. Relation of temperature distribution to ground-water movement in carbonate rocks of central Israel: Geol. Soc. America Bull., v. 75, no. 3, p. 209-215, 1964. SCHNEIDER, W. J. 1-63. Variability of low flows in an area of diverse geologic units [abs.]: Am. Geophys. Union Trans., v. 44, no. 4, p. 870, 1963. 1-64. (and CONOVER, W. J.) Tree growth proves nonsensitive indicator of precipitation in central New York, in Geol. Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B185-B187, 1964. SCHNEPFE, M. M. 1-64. (MAY, Irving, andNAESER, C. R.) Cesium and strontium sorption studies on glauconite, in Geol. Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B95-B99, 1964. SCHOEN, Robert 1-63. Clay mineralogy of the Clinton ironstones [abs.]: Geol. Soc. America Spec. Paper 73, p. 235, 1963. 1-64. (and LEE, D. E.) Successful separation of silt-size minerals in heavy liquids, ic Geol.Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B154-B157, 1964. SCHOFF, S. L. 1-64. (and MOORE, J. E.) Chemistry and movement of ground water, Nevada Test Site: U.S. Geol. Survey Rept. TEI-838 (open-file report), 75 p., 1964. SCHOPF, J. M. 1-63. Nomenclature for fossil plants: Taxon, v. 12, no. 8, p. 279-282, 1963. 1-64. Paleobotanical studies in Antarctica [abs.]: Geol. Soc. America Spec. Paper 76, p. 317, 1964. SCHULTZ, C. B. 1-63. (TANNER, L. G., WHITMORE, F. C., Jr., RAY, L. L., and CRAWFORD, E. C.) Paleontologic excavations at Big Bone Lick State Park, Kentucky--A preliminary report: Science, v. 142, no. 3596, p. 1167- 1169, 1963. SCHULTZ, L. G. 1-63. Clay minerals in Triassic rocks of the Colorado Plateau: U.S. Geol. Survey Bull. 1147-C, p. C1-C71, 1963. SCHUMM, S. A. 1- 63. A tentative classification of alluvial river channels: U.S. Geol. Survey Circ. 477, 10 p., 1963. 2- 63. The disparity between present rates of denudation and orogeny: U.S. Geol. Survey Prof. Paper 454-H, p. H1-H13, 1963. 3- 63. (and LICHTY, R. W.) Channel widening and flood-plain construction along Cimarron River in southwestern Kansas: U.S. Geol. Survey Prof. Paper 352-D, p. 71-88, 1963. SCHWOB, H. H. 1-63. Cedar River basin floods: Iowa Highway Research Board Bull. 27, 57 p., 1963. SCOTT, G. R. 1- 63. Nussbaum Alluvium of Pleistocene(?) ageatPueblo, Colo.: U.S. Geol. Survey Prof. Paper 475-C, p. C49-C52, 1963. 2- 63, (and COBBAN, W. A.) Apache Creek Sandstone Member of the Pierre Shale of southeastern Colorado: U.S. SCOTT, G. R.—Continued Geol. Survey Prof. Paper 475-B, p. B99-B101, 1963; abs., Geol. Soc. America Spec. Paper 76, p. 293, 1964. 1-64. Geology of the Northwest and Northeast Pueblo quadrangles, Colorado: U.S. Geol. Survey Misc. Geol. Inv. Map 1-408, 1964. SCOTT, J. H. 1-63. Two nomographs for computation of standard equations in earth-resistivity interpretation: U.S. Geol. Survey Prof. Paper 475-B, p. B71-B73, 1963. SEABER, P. R. 1- 63. Chloride concentration of water from wells in the Atlantic Coastal Plain of New Jersey, 1923-61: New Jersey Dept. Consej-v. and Econ. Devel., Div. Water Policy and Supply Spec. Rept. 22, 250 p., 1963. 2- 63. (and VECCHIOLI, John) Stratigraphic section at Island Beach State Park, N. J.: U.S. Geol. Survey Prof. Paper 475-B, p. B102-B105, 1963. SEGERSTROM, Kenneth 1-63. (CASERTANO, Lorenzo,andGALLI O., Carlos)Erup-tions of water and sand resulting from an earthquake near Concepcion, Chile: U.S. Geol. Survey Prof. Paper 475-B, p. B131-B134, 1963. 1- 64. (CASTILLO U., Octavio, and FALCON M„ Eduardo) Quaternary mudflow deposits near Santiago, Chile: U.S. Geol. Survey Prof. Paper 475-D, p. D144-D148, 1964. 2- 64. Quaternary geology of Chile: brief outline: Geol. Soc. America Bull., v. 75, no. 3, p. 157-170, 1964. SENFTLE, Frank E. 1- 64. (THORPE, A. N„ and LEWIS, R. R.) Magnetic properties of nickel-iron spherules in tektites from Isabela, Philippine Islands: Jour. Geophys. Research, v. 69, no. 2, p. 317-324, 1964. 2- 64. (and HOYTE, A. F.) Resistivity and viscosity of tektites [abs.]: Am. Geophys. Union Trans., v. 45, no. 1, p. 112, 1964. SEVER, C. W. 1-63. Ground-water resources of Bainbridge Air Base, Decatur County, Georgia: Georgia Mineral Newsletter, v. 16, nos. 1-2, p. 39-43, 1963. 1-64. Relation of economic deposits of attapulgite and fuller's earth to geologic structure in southwestern Georgia, in Geol. Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B116-B118, 1964. SHACKLETTE, H. T. 1-63. Variation in element content of American elm tissue with a pronounced change in the chemical nature of the soil: U.S. Geol. Survey Prof. Paper 475-C, p. C105-C106, 1963. 1- 64. (and CUTHBERT, M. E.) Iodine content of plant groups as influenced by variation in rock and soil type [abs.]: Geol. Soc. America Spec. Paper 76, p. 147, 1964. 2- 64. Flower variation of Epilobium angustifolium L. growing over uranium deposits: The Canadian Field-Naturalist, v. 78, no. 1, p. 32-42, 1964. SHAFER, G. H. 1-64. Ground-water resources of Gonzales County, Texas: U.S. Geol. Survey open-file report, 138 p., 1964. SHAPIRO, Leonard 1-63. (and CURTIS, E. L.) Percent-constituent printing accessory and flow-through cell for a spectrophotometer: U.S. Geol. Survey Prof. Paper 475-C, p. C171-C174, 1963. SHARP, W. N. 1-64. (and GIBBONS, A. B.) Geology and uranium deposits of the southern part of the Powder River Basin, Wyoming: U.S. Geol. Survey Bull. 1147-D, p. D1-D60, 1964. SHARPS, J. A. 1-63. Geologic map of the Malvado quadrangle, Terrell and Val Verde Counties, Tex.: U.S. Geol. Survey Misc. Geol. Inv. Map 1-382, 1963. 1-64. Geologic map of the Dryden Crossing quadrangle, Terrell County, Texas: U.S. Geol. Survey Misc. Geol. Inv. Map 1-386, 1964.LIST OF PUBLICATIONS A319 SHAW, H. R. 1- 63. Obsidian-H20 viscosities at 1000 and 2000 bars in the temperature range 700°-900°C: Jour. Geophys. Research, v. 68, no. 23, p. 6337-6343, 1963. 2- 63. The four-phase curve sanidine-quartz-liquid-gas between 500 and 4,000 bars: Am. Mineralogist, v. 48, no. 7-8, p. 883-896, 1963. 1-64. Viscosity measurements on synthetically hydrated obsidian labs.]: Geol. Soc. America Spec. Paper 76, p. 149, 1964. SHAWE, D. R. "" 1-63. Possible wind-erosion origin of linear scarps on the Sage Plain, southwestern Colorado: U.S. Geol. Survey Prof. Paper 475-C, p. C138-C141, 1963. 1- 64. A late Tertiary low-angle fault in western Juab County, Utah, in Geol. Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B13-B15, 1964. 2- 64. (and BERNOLD, Stanley) Distribution of beryllium in igneous rocks, in Geol. Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B100-B104, 1964. SHAWE, F. R. 1- 63. Geology of the Bowling Green North quadrangle, Kentucky: U.S. Geol. Survey Geol. Quad. Map GQ-234, 1963. 2- 63. Geology of the Bowling Green South quadrangle, Kentucky: U.S. Geol. Survey Geol. Quad. Map GQ-235, 1963. 3- 63. Geology of the Franklin quadrangle, Kentucky-Ten-nessee: U.S. Geol. Survey Geol. Quad. MapGQ-281, 1963. 4- 63. Geology of the Woodburn quadrangle, Kentucky: U.S. Geol. Survey Geol. Quad. Map GQ-280, 1963. SHELDON, R. P. 1-63. Physical stratigraphy and mineral resources of Permian rocks in western Wyoming: U.S. Geol. Survey Prof. Paper 313-B, p. B49-B273, 1963. 1-64. Relation between specific gravity and iron content of rocks from the Red Mountain Formation, Alabama: U.S. Geol. Survey Bull. 1182-D, p. D1-D17, 1964. SHELL, J. D. 1-63. Floods on Pearl River at Jackson, Mississippi: U.S. Geol. Survey open-file report, 9 p., 1963. SHEPARD, A. O. 1-64. (and STARKEY, H. C.) Effect of cation exchange on the thermal behavior of heulandite and clinoptilolite: U.S. Geol. Survey Prof. Paper 475-D, p. D89-D92, 1964. SHEPPARD, R. A. 1- 64. Geologic map of the Husum quadrangle, Washington: U.S. Geol. Survey Mineral Inv. Field Studies Map MF-280, 1964. 2- 64. Geology of the Tygarts Valley quadrangle, Kentucky: U.S. Geol. Survey Geol. Quad. Map GQ-289, 1964. SHERWOOD, C. B. 1-64. (and KLEIN, Howard) Surface- and ground-water relation in a highly permeable environment: Internat. Assoc. Sci. Hydrology Pub. 63, p. 454-468, 1964. SHIELDS, W. R. 1-63. (GARNER, E. L., MURPHY, T. J., and GOLDICH, S. S.) Natural variations of copper isotopes [abs.]: Internat. Union Geodesy and Geophysics, General Assembly, 13th, Berkeley, Calif., Aug. 1963, Abs. Papers, v. 9, p. 49, 1963. SHOEMAKER, E. M. 1-63. (GAULT, D. E., MOORE, H. J., and LUGN, R. V.) Hypervelocity impact of steel into Coconino Sandstone: Am. Jour. Sci., v. 261, p. 668-682, 1963. SIEVER, Raymond 1-63. (and SCOTT, R. A.) Organic geochemistry of silica, in Breger, Irving, ed., Organic Geochemistry: London, Pergamon Press, p. 579-595, 1963. SIMMONS, G. C. 1-64. Leucophosphite, a new occurrence in the Quadri-latero Ferrifero, Minas Gerais, Brazil: Am. Miner- alogist, v. 49, nos. 3-4, p. 377-386, 1964. SIMMONS, M. G. 1-64. Gravity data collected in New York by the U.S. Geological Survey during June 1963: U.S. Geol. Survey open-file report, 12 p., 1964. SIMONS, D. B. 1-64. (RICHARDSON, E. V., and HAUSHILD, W. L.) Closure to discussion of "Depth-discharge relations in alluvial channels": Am. Soc. Civil Engineers Proc., v. 90, Jour. Hydraulics Div., no. HY 1, pt. 1, p. 249-252, 1964. SIMONS, F. S. 1- 63. A composite dike of andesite and rhyolite at Klondyke, Arizona: Geol. Soc. America Bull., v. 74, no. 8, p. 1049-1055, 1963. 2- 63. (and MUNSON, Elaine) Johannsenite from the Ara-vaipa mining district Arizona: Am. Mineralogist, v. 48, no. 9-10, p. 1154-1158, 1963. SIMONS, W. D. 1-64.,Estimated streamflow modifications by historic irrigation, Columbia River Basin: U.S. Geol. Survey open-file report, 26 p., 1964. SIMPSON, T. A. 1- 63. Geology and hydrologic studies in the Birmingham red iron ore district, Alabama: U.S. Geol. Survey open-file report, 163 p., 1963. 2- 63. Structural geology of the Birmingham red iron ore district, Alabama: Alabama Geol. Survey Circ. 21, 17 p., 1963. SIMS, P. K. 1- 63. (DRAKE, A. A., JR., and TOOKER, E. W.) Economic geology of the Central City district, Gilpin County, Colo.: U.S. Geol. Survey Prof. Paper 359, 231 p., 1963. 2- 63. (and others) Geology of uranium and associated ore deposits, central part of the Front Range mineral belt, Colorado: U.S. Geol. Survey Prof. Paper 371, 119p., 1963. 3- 63. (and GABLE, D. J.) Cordierite-bearing mineral assemblages in Precambrian rocks. Central City quadrangle, Colorado: U.S. Geol. Survey Prof. Paper 475-B, p. B35-B37, 1963. SINCLAIR, W. C. 1- 63. Ground-water appraisal of Duck Lake Valley, Washoe County, Nevada, with a section on Soils of Duck Lake Valley, by R. L. Malchow: Nevada Dept. Conserv. and Nat. Resources, Ground-Water Resources--Reconn. S e r. Rept. 17, 19 p., 1963. 2- 63. Ground-water appraisal of the Black Rock Desert area, northwestern Nevada: Nevada Dept. Conserv. and Nat. Resources, Ground-Water Resources--Reconn. Ser. Rept. 20, 32 p., 1963. 3- 63. Ground-water appraisal of the Long Valley-Massacre Lake Region, Washoe County, Nevada, with a section on Soils of Long Valley, by R. L. Malchow: Nevada Dept. Conserv. and Nat. Resources, Ground-Water Resources--Reconn. Ser. Rept. 15, 26 p., 1963. 4- 63. Ground-water appraisal of the Pueblo Valley— Continental Lake region, Humboldt County, Nevada: Nevada Dept. Conserv. and Nat. Resources, Ground-Water Resources--Reconn. Ser. Rept. 22, 25 p., 1963. SISCO, H. G. 1-63. (and LUSCOMBE, R. W.) Ten-year summary of records of observation wells and water-level fluctuations in the Aberdeen-Springfield area, Bingham and Power Counties, Idaho, through December 1962: U.S. Geol. Survey open-file report, 122 p., 1963. SKIBITZKE, H. E. 1- 63. Determination of the coefficient of transmissibility from measurements of residual drawdown in a bailed well, in Methods of determining permeability, transmissibility, and drawdown: U.S. Geol. Survey Water-Supply Paper 1536-1, p. 293-298, 1963. 2- 63. (BROWN, R. H., and HARSHBARGER, J. W.) Water and its use, Chap. 6, in Aridity and man: Am. Assoc. Adv. Sci. Pub. 74, p. 145-172, 1963.A320 PUBLICATIONS IN FISCAL YEAR 1964 SKINNER, B. J. 1- 63. Sulfides deposited by the Salton Sea geothermal brine [abs.]: Mining vEng., v. 15, no. 11, p. 60-61, 1963. 2- 63. (and FAHEY, J. J.) Observations on the inversionof stishovite to silica glass: Jour. Geophys. Research, v. 68, no. 19, p. 5595-5604, 1963. 1- 64. (ADLER, Isidore, and MEAD, C. W.) Phase relations among the copper arsenides and their application to geologic thermometry [abs.]: Geol: Soc. America Spec. Paper 76, p. 152, 1964. 2- 64. (ERD, R. C., and GRIMALDI, F. S.) Greigite, the thio-spinel of iron—A new mineral: Am. Mineralogist, v. 49, p. 543-555, 1964. SKIPP, B. A. L. 1-64. Zonation of Mississippian rocks in the North American Cordillera using Tournayellinae, calcareous Foram-inifera [abs.]: Geol. Soc. America Spec. Paper 76, p. 152-153, 1964. SKOUGSTAD, M. W. 1-63. (and FISHMAN, M. J.) Water analysis: Anal. Chemistry, v. 35, no. 5, p. 179R-204R, 1963. SLACK, K. V. 1-64. Effect of tree leaves on water quality in the Cacapon River, W. Va.: U.S. Geol. Survey Prof. Paper 475-D, p. D181-D185, 1964. SLAUGHTER, T. H. 1-62. The ground-water resources of Allegheny andWash-ington Counties, Maryland, in The Water Resources of Allegheny and Washington Counties: Maryland Dept. Geology, Mines and Water Resources Bull. 24, p. 1-243, 1962. SLOSS, Raymond 1-63. Use of ponds to measure rates of storm runoff in Louisiana: U.S. Geol. Survey open-file report, 69 p., 1963. SMART, R. L. 1-64. Geodetic control diagrams: Surveying and Mapping, v. 24, no. 2, p. 241-242, 1964. SMITH, F. A. 1-64. (EMERY, P. A., and SOUDERS, V. L.) Saline County: Nebraska Water Survey Test Hole Rept. 6, 82 p., 1964. SMITH, H. L. 1-63. Geologic map of the Castagne quadrangle. Carbon County, Mont.: U.S. Geol. Survey MineralInv. FieldStud-ies Map MF-264, 1963. SMITH, J. F., Jr. 1-63. (HUFF, L. C., HINRICHS, E. N., and LUEDKE, R. G.) Geology of the Capitol Reef area, Wayne and Garfield Counties, Utah: U.S. Geol. Survey Prof. Paper 363, 102 p., 1963. SMITH, J. H. 1-63. Geology of the Cumberland Falls quadrangle, Kentucky: U.S. Geol. Survey Geol. Quad. Map GQ-274, 1963 [1964]. SMITH, P. B. 1-63. Possible Pleistocene-Recent boundary in the Gulf of Alaska, based on benthonic Foraminifera: U.S. Geol. Survey Prof. Paper 475-C, p. C73-C77, 1963. SMITH, R. E. 1- 63. Estancia Valley, New Mexico, in. Effects of drought in basins of interior drainage, by H. E. Thomas and others: U.S. Geol. Survey Prof. Paper 372-E, p. E8-E12, 1963. 2- 63. (and GATES, J. S.) Ground-water conditions in the southern and central parts of the East Shore area, Utah, 1953-1961: Utah Geol. and Mineralog. Survey, Water-Resources Bull. 2, 48 p., 1963. SMITH, R. L. 1-63. Ash-flow problems--a synthesis based on field and laboratory studies [abs.]: Bull. Volcanol. v. 25, p. 109-110, 1963. 1-64. (and BAILEY, R. A.) Resurgent cauldrons—Their relation to granitic ring complexes and voluminous rhyolitic ash-flow fields [abs.]: Geol.Soc. AmericaSpec. Paper 76, p. 294, 1964. SMITH, R. O. 1-64. (SCHNEIDER, P. A., Jr„ and PETRI, L. R.) Ground-water resources of the South Platte River basin in western Adams and southwestern Weld Counties, Colo.: U.S. Geol. Survey Water-Supply Paper 1658, 132 p., 1964. SMITH, R. P. 1-64. Floods of April-May 1958 in Louisiana and adjacent states: U.S. Geol. Survey Water-Supply Paper 1660-A,p. A1-A149, 1964. SMITH, W. C. 1-64. Memorial to William Clement Putnam (1908-1963): Geol. Soc. America Bull., v. 75, no. 5,p. P79-P82, 1964. SMITH, W. O. 1-64. (and SAYRE, A. N.) Turbulence in ground-water flow: U.S. Geol. Survey Prof. Paper 402-E, p. E1-E29, 1964. SMITH, Winchell 1-63. (and BAILY, G. F.) Closure to discussion of "Optical current meter": Am. Soc. Civil Engineers Proc., v. 89, Jour. Hydraulics Div.,no. HY 4, pt. 1, p. 223-224, 1963. 1-64. Acoustic velocity meter [abs.]: Am. Geophys. Union Trans., v. 45, no. 2, p. 356, 1964. SNIEGOCKI, R. T. 1- 63. Geochemical aspects of artificial recharge in the Grand Prairie region, Arkansas: U.S. Geol. Survey Water-Supply Paper 1615-E, p. E1-E41, 1963. 2- 63. Problems in artificial recharge through wells in the Grand Prairie region, Arkansas: U.S. Geol. Survey Water-Supply Paper 1615-F, p. F1-F25, 1963. 3- 63. (and REED, J. E.) Principles of siphons with respect to the artificial-recharge studies in the Grand Prairie region, Arkansas: U.S. Geol. Survey Water-Supply Paper 1615-D, p. D1-D19, 1963. 1-64. Hydrogeology of a part of the Grand Prairie region, Arkansas: U.S. Geol. Survey Water-Supply Paper 1615-B, p. B1-B72, 1964. SNYDER, G. L. 1-64. Geology of the Tyner quadrangle, Kentucky: U.S. Geol. Survey Geol. Quad. Map GQ-247, 1963. SOHL, N. F. 1-63. New gastropod genera from the late Upper Cretaceous of the east Gulf Coastal Plain: Jour. Paleontology, v. 37, no. 4, p. 747-757, 1963. SOHN, I. G. 1- 63. Middle Triassic marine ostracodes in Israel: U.S. Geol. Survey Prof. Paper 475-C, p. C58-C59, 1963. 2- 63. (and MORRIS, R. W.) Chaikella. a new fresh-water ostracode genus, and Telekia, a new name for a homonym: Micropaleontology, v. 9, no. 3, p. 327-331, 1963. 1- 64. Review of "Faunes d'Ostracodes...": Micropaleon- tology, v. 10, no. 2, p. 264-265, 1964. 2- 64. (and ANDERSON, F. W.) The ontogeny of Therio-svnoecum fittoni (Mantell): Palaeontology, v. 7, pt. 1, p. 72-84, 1964. 3- 64. (and REISS, Zeev) Conodonts and Foraminifera from the Triassic of Israel: Nature, v. 201, no. 4925, p. 1209, 1964. SOREN, Julian 1-63. The ground-water resources of Delaware County, New York: New York Dept. Conserv. Water Resources Comm. Bull. GW-50, 59 p., 1963. SPEER, P. R. 1- 64. (and GAMBLE, C. R.) Magnitude and frequency of floods in the United States-Pt. 2-A, South Atlantic slope basins, James River to Savannah River: U.S. Geol.Survey Water-Supply Paper 1673, 329 p., 1964. 2- 64. (and GAMBLE, C. R.) Magnitude and frequency of floods in the United States—Pt. 3-B, Cumberland and Tennessee River basins: U.S. Geol. Survey Water-Supply Paper 1676, 340 p., 1964. 3- 64. (PERRY, W. J., McCABE, J. A., LARA, O. G., and others) Low-flow characteristics of streams in the Mississippi Embayment in Tennessee, Kentucky, and Illinois, with _a section on Quality of the water, by H. G. Jeffery: U.S. Geol. Survey open-file report, 130 p., 1964.LIST OF PUBLICATIONS A321 SPEERT, J. L. 1-64. (MOORE, R. H., and BENTLEY, L. E.) Discussion of paper "Control traverses and their adjustment," by Everett D. Morse: Am. Soc. Civil Engineers Proc., v. 90, Jour. Surveying and Mapping Div., no. SU1, p. 81-84, 1964. SPENCER, F. D. 1-63. Geology of the Pellville quadrangle, Kentucky: U.S. Geol. Survey Geol. Quad. Map GQ-284, 1963 [1964]. SPICER, H. C. 1- 63. Tables of the ascending exponential function ex: Summary in Mathematics of Computation, v. 17, no. 83, p. 305-306, 1963. 2- 63. Tables of the inverse probability integral P=2 imr-B2ag; Summary in Mathematics of Computation, v. 17, no. 83, p. 320-321, 1963. 3- 63. Tables of the descending exponential function e-x: Summary in Mathematics of Computation, v. 17, no. 83, p. 306, 1963. SPIEGEL, Zane 1-63. (and BALDWIN, Brewster) Geology and water resources of the Santa Fe area. New Mexico, with contributions by F. E. Kottlowski and E. L. Barrows, and a section on Geophysics by H. A. Winkler: U.S. Geol. Survey Water-Supply Paper 1525, 258 p., 1963. STAATZ, M. H. 1-63. (PAGE, L. R., NORTON, J.J., and WILMARTH, V. R.) Exploration for beryllium at the Helen Beryl, Elkhorn and Tin Mountain pegmatites, Custer County, South Dakota: U.S. Geol. Survey Prof. Paper 297-C, p. 129-197, 1963. STAKA, G. C. 1-63. (and MILLER, W. A.) Graphs of ground-water levels in Minnesota, 1957-1961: Minnesota Dept. Conserv., Div. Waters Bull. 18, 58 p., 1963. STALLMAN, R. W. 1- 63. Computation of ground-water velocity from temperature data, in Methods of collecting and interpreting ground-water data, compiled by Ray Bentall: U.S. Geol. Survey Water-Supply Paper 1544-H, p. H36-H46, 1963. 2- 63. Type curves for solution of single-boundary problems, m. Shortcuts and special problems in aquifer tests, compiled by Ray Bentall: U.S. Geol. Survey Water-Supply Paper 1545-C, p. C45-C47, 1963. 1-64. Multiphase fluids in porous media—A review of theories pertinent to hydrologic studies: U.S. Geol. Survey Prof. Paper 411-E, p. E1-E51, 1964. STARK, J. T. 1-63. Petrology of the volcanic rocks of Guam .with a section on Trace elements in the volcanic rocks of Guam, by J. I. Tracey, Jr., and J. T. Stark: U.S. Geol. Survey Prof. Paper 403-C, p. C1-C32, 1963. STARKEY, H. C. 1-64. Determination of the ion-exchange capacity of a zeo-litic tuff: U.S. Geol. Survey Prof. Paper 475-D, p. D93-D95, 1964. STAUDER, W. V. 1-64. (DOWLING, John, and JACKSON, Wayne) Billiken "calibration shot" in southeast Missouri [abs.]: Seis- mol. Soc. America, 60th Ann. Mtg., Mar. 27-28, 1964, Program, p. 60, 1964. STEAD, F. W. 1-63. Tritium distribution in ground water around large underground fusion explosions: Science, v. 142, no. 3596, p. 1163-1165, 1963. STEINHART, J. S. 1-64. The Lake Superior seismic experiment [abs.]: Am. Geophys. Union Trans., v. 45, no. 1, p. 93, 1964. STERMITZ, Frank 1-63. (HANLY, T. F., and LANE, C; W.) Water resources, in Mineral and water resources of Montana: U.S. Cong., 88th, 1st sess., Comm. Print, p. 137-166, 1963. STERN, T. W. 1-64. Isotopic ages of zircon and allanite from the Minnesota River Valley and La Sal Mountains, Utah [abs.]: Am. Geophys. Union Trans., v. 45, no. 1, p. 116, 1964. STEVEN, T. A. 1- 64. Geologic setting of the Spar City district, San Juan Mountains, Colo.: U.S. Geol. Survey Prof. Paper 475-D, p. D123-D127, 1964. 2- 64. (and RATTE, J. C.) Revised Tertiary volcanic sequence in the central San Juan Mountains, Colo.: U.S. Geol. Survey Prof. Paper 475-D, p. D54-D63, 1964. STEVENS, H. H., Jr. 1-64. (and DEMPSTER, G. R., Jr.) An electric powered vehicle for large river measurements: Civil Eng., v. 34, no. 6, p. 74, 1964. STEVENS, P. R. 1-63. Examination of drill cuttings and application of resulting information to solving of field problems on the Navajo Indian Reservation. 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Geology of the Gamaliel quadrangle, Kentucky: U.S. Geol. Survey Geol. Quad. Map GQ-253, 1963. TRUESDELL, A. H. 1-63. (and POMMER, A. M.) Phosphate glass electrode with good selectivity for alkaline-earth cations: Science, v. 142, p. 1292-1294, 1963. 1- 64. Theory of divalent-cation exchange selectivity [absj: Geol. Soc. America Spec. Paper 76, p. 170, 1964. 2- 64. (and CHRIST, C. L.) Use of sodium-sensitive glass electrodes for solubility determinations: U.S. Geol. Survey Prof. Paper 475-D, p. D167-D170, 1964. TRUMBULL, J.V.A. 1-63. Coarse fraction of sediments: Woods Hole Oceanog. Inst. Summ. Inv. Conducted 1962, Reference no. 63-18, Chemistry-Geology, p. 22-23, 1963. TWENTER, F. R. 1-63. (and METZGER, D. G.) Geology and ground water in Verde Valley—The Mogollon Rim region, Arizona: U.S. Geol. Survey Bull. 1177, 132 p„ 1963. TWETO, Ogden 1-63. (and SIMS, P. K.) Precambrian ancestry of the Colorado mineral belt: Geol. Soc. America Bull., v. 74, no. 8, p. 991-1014, 1963. 1-64. 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Survey Water-Supply Paper 1734, 318 p., 1963 [1964], 4- 63. Compilation of records of surface waters of the United States, October 1950 to September 1960--Pt. 13, Snake River Basin: U.S. Geol. Survey Water-Supply Paper 1737, 282 p., 1963 [1964], 5- 63. Compilation of records of surface waters of the United States, October 1950 to September 1960—Pt. 14, Pacific Slope basins in Oregon and Lower Columbia River basin: U.S. Geol. Survey Water-Supply Paper 1738, 372 p., 1963 [1964], 6- 63. Contributions to economic geology of Alaska: U.S. Geol. Survey Prof. Paper 1155, 93 p., 1963. 7- 63. Drainage areas of Texas streams, San Antonio River basin: Texas Water Comm. Circ. 63-07, 11 p., 1963.A324 PUBLICATIONS IN FISCAL YEAR 1964 UNITED STATES GEOLOGICAL SURVEY--Continued 8- 63. Ground-water levels in the United States, 1956-60, Northwestern States: U.S. Geol. Survey Water-Supply Paper 1760, 222 p., 1963. 9- 63. Ground-water levels in the United States, 1956-60, Southeastern States: U.S. Geol. Survey Water-Supply Paper 1770, 160 p., 1963. 10- 63. Map of Pompano Beach area, Broward County, Florida, showing contours on water table, January 25, 1963: U.S. Geol. Survey open-file map, 1963. 11- 63. Quality of surface waters for irrigation. Western States, 1959: U.S. Geol. Survey Water-Supply Paper 1699, 147 p., 1963 [1964]. 12- 63. Quality of surface waters of the United States, 1958- -Pts. 7-8, Lower Mississippi River basins and Western Gulf of Mexico basins: U.S. Geol. Survey Bull. 1573, 588 p., 1963. 13- 63. Quality of surface waters of the United States, 1959- -Pts. 5-6, Hudson Bay and Upper Mississippi River basins, and Missouri River basin: U.S. Geol. Survey Bull. 1643, 247 p., 1963. 14- 63. Short papers in geology and hydrology, articles 1-59, Geological Survey research 1963: U.S. Geol.Survey Prof. Paper 475-B, p. B1-B219, 1963. 15- 63. Short papers in geology and hydrology, articles 60-121, Geological Survey research 1963: U.S. Geol. Survey Prof. Paper 475-C, p. 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Compilation of records of surface waters of the United States, October 1950 to September 1960--Pt. 3-A, Ohio River basin except Cumberland and Tennessee River basins: U.S. Geol. Survey Water-Supply Paper 1725, 560 p., 1964. 2- 64. Compilation of records of surface waters of the United States, October 1950 to September 1960--Pt. 8, Western Gulf of Mexico basins, prepared under the direction of E. L. Hendricks: U.S. Geol. Survey Water-Supply Paper 1732, 574 p., 1964. 3- 64. Floods of January-February 1957 in southeastern Kentucky and adjacent areas: U.S. Geol. Survey Water-Supply Paper 1652-A, p. A1-A195, 1964. 4- 64. Floods of January-February 1959 in Ohio and adjacent states, prepared under the direction of E. L. Hendricks: U.S. Geol. Survey Water-Supply Paper 1750-A, p. A1-A296, 1964. 5- 64. Geological Survey research 1964, Chap. B: U.S. Geol. Survey Prof. Paper 501-B, p. B1-B191, 1964. 6- 64. Index to water resources data-collection stations in Florida, 1961: Florida Geol. Survey Spec. Pub. 11, 166 p., 1964. 7- 64. Long range plan for resource surveys, investigations, and research programs of the United States Geological Survey: U.S. Geol. Survey Misc. Rept., 75 p., 1964. 8- 64. Mineral and water resources of Alaska: U.S. Cong., 88th, 2d sess., U.S. Senate Comm, on Interior and Insular UNITED STATES GEOLOGICAL SURVEY--Continued Affairs Rept., 179 p., 1964. (Prepared in coop, with State of Alaska, Department of Natural Resources.) (U.S. Geological Survey contributors were G. D. Eberlein, principal author, and also F. F. Barnes, H. C. Berg, G. O. Gates, G. C. Giles, Arthur Grantz, E. M. MacKevett, Jr., W. W. Patton, Jr., George Plafker, A. O. Waananen, and Clyde Wahrhaftig.) 9- 64. Mineral and water resources of Utah: U.S. Cong., 88th, 2d sess., U.S. Senate Comm, on Interior and Insular Affairs Rept., 275 p., 1964. (Prepared in coop, with Utah Geological and Mineralogical Survey and Utah Water and Power Board.) (U.S. Geological Survey contributors were L. S. Hilpert, principal author, and also J. W. Adams, Ted Arnow, Paul Averitt, M. H. Bergendahl, D. A. Brobst, W. B. Cashion, M. D. Crittenden, Jr., M. D. Dasch, R. P. Fischer, W. C. Gere, W. R. Griffitts, W. R. Hansen, J. N. Harstead, A. V. Heyl, R. J. Hite, G. W. Horton, Arthur Johnson, R. B. Ketner, T. H. Kiilsgaard, R. U. King, R. H. Langford, D. M. Lemmon, H. T. Morris, Priscilla Mount, R. L. Parker, S. H. Patterson, R. G. Reeves, R. J. Roberts, D. F. Russell, W. C. Senkpiel, J. H. Stewart, E. W. Tooker, Richard Van Horn, J. D. Vine, R. A. Weeks, M. T. Wilson, and C. F. Withington.) 10- 64. Preliminary report on recent surface movements through July 1962 in the Baldwin Hills, Los Angeles County, California: U.S. Geol. Survey open-file report, 30 p., 1964. 11- 64. Quality of surface waters of the United States, 1958--Pts. 9-14, Colorado River basin to Pacific slope basins in Oregon and lower Columbia River basin: U.S. Geol. Survey Water-Supply Paper 1574, 487 p., 1964. 12- 64. Short papers in geology and hydrology, articles 122-172, Geological Survey research 1963: U.S. Geol. Survey Prof. Paper 475-D, p. D1-D223, 1964. 13- 64. Summary of floods in the United States during 1956: U.S. Geol. Survey Water-Supply Paper 1530, 85 p., 1964. 14- 64. The Hebgen Lake, Montana, earthquake of August 17, 1959: U.S. Geol. Survey Prof. Paper 435, 242 p., 1964. UPSON, J. E. 1- 64. Relationships of fresh and salty ground water along the northern Atlantic Coast [abs.]: Geol. Soc. America Spec. Paper 76, p. 171, 1964. 2- 64. (LEOPOLD, E. B., and RUBIN, Meyer) Postglacial change of sealevel in New Haven harbor, Connecticut: Am. Jour. Sci., v. 262, p. 121-132, 1964. VAN HYLCKAMA, T. E. A. 1-64. Growth, development and water use by saltcedar (Tamarix pentandra) under different conditions of weather and access to water: Internat. Assoc. Sci. Hydrology Pub. 62, p. 75-86, 1964. VANLIER, K. E. 1- 63. Ground-water resources of the Alma area, Michigan: U.S. Geol. Survey Water-Supply Paper 1619-E, p. El-E-66, 1963. 2- 63. Reconnaissance of the ground-water resources of Alger County, Michigan: Michigan Geol. Survey Water Inv. 1, 55 p., 1963. VAN SICKLE, G. H. 1-64. (DENNEN, W. H., and POST, E. V.) Heavy metals in stream sediment, southeastern Maine: U.S. Geol. Survey open-file report, map, 1964. VAUDREY, W. C. 1-63. Floods of March-May 1963 in Hawaii: U.S. Geol. Survey open-file report, 65 p., 1963. 1-64. An investigation of floods in Hawaii through June 30, 1963: U.S. Geol. Survey, Water Resources Div., Surface Water Branch, Honolulu Dist. Prog. Rept. 6, 145 p., 1964. VECCHIOLI, John 1-62. (and PALMER, M. M.) Ground-water resources of Mercer County, New Jersey: New Jersey Dept. Conserv. and Econ. Devel., Div. Water Policy and Supply Spec. Rept. 19, 71 p., 1962.LIST OF PUBLICATIONS A325 VEDDER, J. G. 1-63. (and NORRIS, R. M.) Geology of San Nicolas Island, California: U.S. Geol. Survey Prof. Paper 369, 65 p., 1963. VICE, R. B. 1-64. Sedimentology program of the Geological Survey: U.S. Geol. Survey open-file report, 9 p., 1964. VISHER, F. N. 1-64. (and MINK, J. F.) Ground-water resources in southern Oahu, Hawaii: U.S. Geol. Survey Water-Supply Paper 1778, 133 p., 1964. VITALIANO, C. J. 1-63. (and CALLAGHAN, Eugene) Geology of the Paradise Peak quadrangle, Nevada: U.S. Geol. Survey Geol. Quad. Map GQ-250, 1963 [1964], VOEGELI, P. T., Sr. 1- 63. Ground water in Colorado--Its importance during an emergency: Colorado Water Conserv. Board, Ground-Water Circ. 9, 10 p., 1963. 2- 63. Water for the proposed West Side Campground site. Rocky Mountain National Park, Colorado: U.S. Geol. Survey open-file report, 22 p., 1963. 1-64. Ground-water resources of North Park and Middle Park, Colorado—A reconnaissance investigation: U.S. Geol. Survey open-file report, 90 p., 1964. von HUENE, Roland 1-63. (BATEMAN, P. C., and ROSS, D. C.) Indian Wells Valley, Owens Valley, Long Valley, and Mono Basin, Pt. 4 of International Union of Geology and Geophysics, 1963 Meeting, Guidebook for seismology study tour: China Lake, Calif., U.S. Naval Ordnance Test Station, p. 57-110, 1963. VORHIS, R. C. 1-64. Relationship of the Suwannee Limestone to the Flint River Formation, Mitchell County, Georgia [abs.]: Geol. Soc. America, Southeastern Sec., 1964 Ann. Mtg., Baton Rouge, April 1964, Program, p. 33, 1964. WAANANEN, A. O. 1-64. Urban development and hydrology: U.S. Geol. Survey open-file report, 19 p., 1964. WAHLSTROM, E. E. 1-64. The validity of geologic projection—A case history: Econ. Geology, v. 59, no. 3, p. 465-474, 1964. WAIT, R. L. 1-63. (and McCOLLUM, M. J.) Contamination of freshwater aquifers through an unplugged oil-test well in Glynn County, Georgia: Georgia Mineral Newsletter, v. 16, nos. 3-4, p. 74-80, 1963. WAITE, H. A. 1-63. (and THOMAS, H. E.) Cedar City Valley, Utah, in Effects of drought in basins of interior drainage, by H. E. Thomas and others: U.S. Geol. Survey Prof. Paper 372-E, p. E23-E29, 1963. WALKER, E. H. 1- 63. Ground water in the upper Star Valley, Wyoming: U.S. Geol. Survey open-file report, 37 p., 1963. 2- 63. Relative rates of erosion under grass and forest in a valley of western Wyoming: Northwest Sci., v. 37, no. 3, p. 104-111, 1963. 1- 64. Subsurface geology of the National Reactor Testing Station, Idaho: U.S. Geol. Survey Bull. 1133-E, p. E1-E22, 1964. 2- 64. (and SISCO, H. G.) Ground water in the Midvale and Council areas, upper Weiser River basin, Idaho: U ,S. Geol. Survey Water-Supply Paper 1779-Q, p. Q1-Q26, 1964. WALKER, G. W. 1-63. (OSTERWALD, F. W., and ADAMS, J. W.) Geology of uranium-bearing veins in the conterminous United States: U.S. Geol. Survey Prof. Paper 455-A—F, 120 p., 1963 [1964]. WALKER, H. D. 1-64. (and SMALL, J. B.) Cooperative control projects: Surveying and Mapping, v. 24, no. 1, p. 107-112, 1964. WALLER, R. M. 1-63. Data on wells in the Homer area, Alaska: Alaska Dept. Health and Welfare Water-Hydrol. Data Rept. 23, 24 p„ 1963. WALTERS, K. L. 1-63. Geologic reconnaissance and test-well drilling, Cordova, Alaska: U.S. Geol. Survey Water-Supply Paper 1779-A, p. Al-All, 1963. WALTON, W. C. 1-63. (and DRESCHER, W. J.) Composite type curve for analyzing aquifer-test data, ija Shortcuts and special problems in aquifer tests, compiled by Ray Bentall: U.S. Geol. Survey Water-Supply Paper 1545-C, p. Cl-C3, 1963. WANEK, A. A. 1- 63. Geologic map of the Rapids quadrangle. Carbon and Stillwater Counties, Mont.: U.S. Geol. Survey Mineral Inv. Field Studies Map MF-270, 1963. 2- 63. Geology and fuel resources of the southwestern part of the Raton coal field, Colfax County, N. Mex.: U.S. Geol. Survey Coal Inv. Map C-45, 1963 [1964], 1-64. (READ, C. B., ROBINSON, G. D., HAYS, W. H., and McCALLUM, Malcolm) Geologic map and sections of the Philmont Ranch region. New Mexico: U.S. Geol. Survey Misc. Geol. Inv. Map 1-425, 1964. WARD, P. E. 1- 63. Geology and ground-water features of salt springs, seeps, and plains in the Arkansas and Red River basins of western Oklahoma and adjacent parts of Kansas and Texas: U.S. Geol. Survey open-file report, 71 p., 1963. 2- 63. (and JORDAN, D. G.) Water resources of the Virgin Islands, a preliminary appraisal, 1963: U.S. Geol. Survey open-file report, 44 p., 1963. 1-64. (and TRUXES, L. S.) Water wells in Puerto Rico: Puerto Rico Water-Resources Bull. 3, 248 p., 1964. WARING, C. L. 1-64. Determination of hafnium content and Hf/Zr ratios in zircon with the direct-reading emission spectrometer, in Geol. Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B146-B147, 1964. WARK, J. W. 1-61. (KELLER, F. J., and FELTZ, H. R.) Reconnaissance of sedimentation and chemical quality of surface water in the Potomac River basin, in. Potomac River Basin Rept., Sediment studies: U.S. Army Engineer District, Baltimore, v. 7, app. H, 75 p., 1961 [1963], 1-63. (and KELLER, F. J.) Preliminary study of sediment sources and transport in the Potomac River basin: Interstate Comm. Potomac River Basin Tech. Bull. 1963-11, 28 p., 1963. WARMAN, J. C. 1-63. (and CAUSEY, L. V.) Relation of springs to thrust faults in Calhoun County, Alabama: Alabama Geol.Survey Reprints Ser.3,8p,,1963. (Reprinted from Alabama Acad. Sci. Jour., v. 32, no. 2, p. 87-94, Apr. 1961.) WARNER, L. A. 1-64. (and ROBINSON, C. S.) Fracture patterns in the Harold D. Roberts Tunnel, Colorado Front Range [abs.]: Geol. Soc. America Spec. Paper 76, p. 231, 1964. WARREN, C. R. 1-63. Origin and nature of the probable skeletal fuzz on the Moon: U.S. Geol. Survey Prof. Paper 475-B, p. B148-B152, 1963. WARREN, M. A. 1-63. Graphic shortcuts in applying the nonequilibrium formula to ground-water problems, in Shortcuts and special problems in aquifer tests, compiled by Ray Bentall: U.S. Geol. Survey Water-Supply Paper 1545-C, p. C19-C28, 1963. WASSERBURG, Gerald J. 1-63. (MAZOR, E., and ZARTMAN, R. E.) Isotopic and chemical composition of some terrestrial natural gases.A326 PUBLICATIONS IN FISCAL YEAR 1964 WASSERBURG, Gerald J.--Continued in Earth Science and Meteoritics: Amsterdam, North - Holland Publishing Co., p. 219-240, 1963. WASSON, B. E. 1-64. Aquifer test at West Point, Mississippi: Mississippi Indus, and Technol. Research Comm. Water Research Bull. 64-2, 8 p., 1964. WATKINS, F. A., Jr. 1- 63. (and JORDAN, D. G.) Ground-water resources of west-central Indiana--Preliminary report, Owen County: Indiana Div. Water Resources Bull. 18, 99 p., 1963. 2- 63. (and JORDAN, D. G.) Ground-water resources of west-central Indiana--Preliminary report, Vigo County: Indiana Div. Water Resources Bull. 17, 358 p., 1963. 3- 63. (and ROSENSHEIN, J. S.) Ground-water geology and hydrology of Bunker Hill Air Force Base and vicinity, Peru, Ind.: U.S. Geol. Survey Water-Supply Paper 1S19-B, p. B1-B32, 1963. 1- 64. Ground-water appraisal of the Clifty Creek Basin and Clifty Creek Reservoir site, Indiana: U.S. Geol. Survey open-file report, 7 p., 1964. 2- 64. Ground-water appraisal of the Patoka River basin and Patoka Reservoir site, Indiana: U.S. Geol. Survey open-file report, 5 p., 1964. 3- 64. Wabash Basin comprehensive study, ground-water appraisal of the Embarrass River basin and Lincoln Reservoir site, Illinois: U.S. Geol. Survey open-file report, 8 p., 1964. WATKINS, J. S. 1- 64. (and SPIEKER, A. M.) Seismic refraction survey in the Great Miami River Valley and vicinity, Montgomery, Warren, and Butler Counties, Ohio: U.S. Geol. Survey open-file report, 6 p., 1964. 2- 64. (and GEDDES, W. H.) Magnetic anomaly and possible orogenic significance of geologic structure of the Atlantic Shelf [abs.]: Am. Geophys. Union Trans., v. 45, no. 1, p. 35, 1964. 3- 64. Basement depths from widely spaced aeromagnetic profiles in Kansas and Nebraska: Geophysics, v. 29, no. 1, p. 80-86, 1964. WAYMAN, C. H. 1- 63. Determination of total sulfur in water by neutron activation analysis: Anal. Chemistry, v. 35, no. 6, p. 768-769, 1963. 2- 63. Surfactant sorption on heteroionic clay minerals: Internat. Clay Conf., Stockholm, Sweden, Aug. 1963, Proc., v. 1, p. 329-342, 1963. 3- 63. (and ROBERTSON, J. B.) Biodegradation of anionic and nonionic surfactants under aerobic and anaerobic conditions: Biotechnology and Bioengineering, v. 5, p. 367-384, 1963. 4- 63. (PAGE, H. G., and ROBERTSON, J. B.) Adsorption of the surfactant ABS35 on illite: U.S. Geol. Survey Prof. Paper 475-C, p. C221-C223, 1963. 5- 63. (PAGE, H. G., and ROBERTSON, J. B.) Effect of detergents on the viscosity of water containing bacteria and clay in suspension: U.S. Geol. Survey Prof. Paper 475-B, p. B209-B212, 1963. 6- 63. (and ROBERTSON, J. B.) Biodegradation of surfactants in synthetic detergents under aerobic and anaerobic conditions at 10°C: U.S. Geol. Survey Prof. Paper 475-C, p. C224-C227, 1963. 7- 63. (ROBERTSON, J. B., and PAGE, H. G.) Adsorption of the surfactant ABS35 on montmorillonite: U.S. Geol. Survey Prof. Paper 475-B, p. B213-B216, 1963. 8- 63. (ROBERTSON, J. B., and PAGE, H. G.) Factors influencing the survival of Escherichia coli in detergent solutions: U.S. Geol. Survey Prof. Paper 475-B, p. B205-B208, 1963. WAYMAN, C. H.~Continued 1-64. (and PAGE, H. G., and ROBERTSON, J. B.) Behavior of surfactants and other detergent components in water and soil-water environments: U.S. Geol. Survey open-file report, 266 p., 1964. WEDOW, Helmuth, Jr. 1-64. (and MARIE, J. R.) Statistical analysis of solution-collapse structures [abs.]: Geol. Soc. America Spec. Paper 76, p. 262, 1964. WEEKS, Alice D. 1-63. (and ROSS, D. R., and MARVIN, R. F.) The occurrence and properties of barnesite Na2V60ig.3H20,a new hydrated sodium vanadate mineral from Utah: Am. Mineralogist, v. 48, p. 1187-1195, 1963. WEEKS, E. P. 1-63. (HANSON, G. F., and HOLT, C. L. R., Jr.) Movie on Little Plover River project--A study in sand-plains hydrology: U.S. Geol. Survey open-file movie, 16 mm., 35 minutes, color, sound, 1963. 1-64. Use of water-level recession curves to determine the hydraulic properties of glacial outwash in Portage County, Wis., in,Geol. Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B181-B184, 1964. WEIGLE, J. M. 1-63. Ground-water favorability map of the Nashua-Merrimack area. New Hampshire: U.S. Geol. Survey open-file report, 1963. WEIR, J. E., Jr. 1- 63. Ground-water inventory for 1962, Edwards Air Force Base, California: U.S. Geol. Survey open-file report, 42 p., 1963. 2- 63. (and BADER, J. S.) Ground water and related geology of Joshua Tree National Monument, California: U.S. Geol. Survey open-file report, 101 p., 1963. 1-64. Geology and availability of groundwater in the northern part of the White Sands Missile Range and vicinity, New Mexico: U.S. Geol. Survey open-file report, 174 p., 1964. WEIST, W. G., Jr. 1- 63. Geology and occurrence of ground water in Otero County and the southern part of Crowley County, Colorado, with sections by E. D. Jenkins and C. A. Horr: U.S. Geol. Survey open-file report, 158 p., 1963. 2- 63. Water in the Dakota and Purgatoire Formations in Otero County and the southern part of Crowley County, Colo.: U.S. Geol. Survey Water-Supply Paper 1669-P, p. P1-P17, 1963. 1- 64. Geology and ground-water resources of Yuma County, Colo.: U.S. Geol. Survey Water-Supply Paper 1539-J, p. J1-J56, 1964. 2- 64. Hydrogeologic data from parts of Larimer, Logan, Morgan, Sedgwick, and Weld Counties, Colorado: Colorado Water Conserv. Board Ground Water Basic-Data Rept. 16, 30 p., 1964. WELD, B. A. 1-63. (ASSELSTINE, E. S., and JOHNSON, Arthur) Reports and maps of the Geological Survey released only in the open files: U.S. Geol. Survey Circ. 473, 15 p., 1963. WELDER, F. A. 1-64. (and REEVES, R. D.) Geology and ground-water resources of Uvalde County, Tex.: U.S. Geol. Survey Water-Supply Paper 1584, 49 p., 1964. WELDER, G. E. 1-63. (and WEEKS, E. P.) Hydrologic conditions near Glendo, Platte County, Wyoming: U.S. Geol. Survey open-file report, 150 p., 1963. WESSELMAN, J. B. 1-64. Geology and ground-water resources of Orange County, Texas: U.S. Geol. Survey open-file report, 1964LIST OF PUBLICATIONS A327 WEST, S. W. 1- 63. Water levels. New Mexico, January to April 1963: Ground Water, v. 1, no. 3, p. 26, 1963. 2- 63. (and KILBURN, Chabot) Ground water for irrigation in part of the Fort Hall Indian Reservation, Idaho: U.S. Geol. Survey Water-Supply Paper 1576-D, p. D1-D33, 1963. WESTFALL, A. O. 1- 63. Surface water of Little River basin in southeastern Oklahoma, with a section on Quality of water, by R. P. Orth: U.S. Geol. Survey open-file report, 66 p., 1963. 2- 63. Surface water of Muddy Boggy River basin in south-central Oklahoma, with a section cn Quality of water, by T. R. Cummings: U.S. Geol. Survey open-file report, 78 p., 1963. 1-64. (and PATTERSON, J. L.) Floods in Oklahoma, magnitude and frequency: U.S. Geol. Survey open-file report, 44 p., 1964. WETTERHALL, W. S. 1- 64. Geohydrologic reconnaissance of Pasco and southern Hernando Counties, Florida: Florida Geol. Survey Rept. Inv. 34, 28 p., 1964. 2- 64. Reconnaissance of springs and sinks in west-central Florida: U.S. Geol. Survey open-file report, 78 p., 1964. WHETSTONE, G. W. 1-63. (DRAKE, P. G., and COLLIER, C. R.) Discussion of "Billion-dollar river clean-up", by Edward J. Cleary: Am. Soc. Civil Engineers Proc., v. 89, Jour. Sanitary Eng. Div., no. SA 3, pt. 1, p. 95-97, 1963. WHITCOMB, H. A. 1-64. (and GORDON, E. D.) Availability of ground water at Devils Tower National Monument, Wyoming: U.S. Geol. Survey open-file report, 61 p., 1964. WHITE, A. M. 1-63. (STROMQUIST, A. A.,STERN, T. W., andWESTLEY, Harold) Ordovician age for some rocks of the Carolina slate belt in North Carolina: U.S. Geol. Survey Prof. Paper 475-C, p. C107-C109, 1963. WHITE, D. E. 1- 63. Summary of studies of thermal waters and volcanic emanations of the Pacific region, 1920 to 1961, in Macdonald, G. A., chm., Geology and solid earth geophysics of the Pacific basin: Pacific Sci. Cong., 10th, Honolulu, 1961 (Rept. Ser.), p. 161-169, 1963. 2- 63. The Salton Sea geothermal brine, an ore-transporting fluid [abs.]: Mining Eng., v. 15, no. 11, p. 60, 1963. 3- 63. Fumaroles, hot springs, and hydrothermal alteration: Am. Geophys. Union Trans., v. 44, no. 2, p. 508-511, 1963. WHITE, N. D. 1- 63. Ground-water conditions in the Rainbow Valley and Waterman Wash areas, Maricopa and Pinal Counties, Ariz.: U.S. Geol. Survey Water-Supply Paper 1669-F, p. F1-F50, 1963 [1964]. 2- 63. (STULIK, R. S., MORSE, E. K., and others) Annual report on ground water in Arizona, spring 1962 to spring 1963: Arizona State Land Dept. Water Resources Rept. 15, 136 p., 1963. WHITLOW, J. W. 1-63. (and BROWN, C. E.) The Ordovician-Silurian contact in Dubuque County, Iowa: U.S. Geol. Survey Prof. Paper 475-C, p. C11-C13, 1963. WHITMAN, H. M. 1-63. (and KILBURN, Chabot) Ground-water conditions in southwestern Louisiana, 1961 and 1962, with a discussion of the Chicot aquifer in the coastal area: Louisiana Dept. Conserv., Geol. Survey and Louisiana Dept. Public Works, Water Resources Pamph. 12, 32 p., 1963. WHITMORE, F. C., Jr. 1-63. Review of "In prehistoric seas "by Carroll L. Fenton and Mildred A. Fenton: Atlantic Naturalist, v. 18, no. 3, p. 193-196, 1963. WHITMORE, F. C., Jr.—Continued 2-63. Review of "Fossils" by F. H. T. Rhodes et al,: Atlantic Naturalist, v. 18, no. 4, p. 259, 1963. WIITALA, S. W. 1-63. (VANLIER, K. E., and KRIEGER, R. A.) Water resources of the Flint area, Michigan: U.S. Geol. Survey Water-Supply Paper 1499-E, p. E1-E86, 1963 [1964], WILCOX, R. E. 1- 64. Immersion liquids of relatively strong dispersion in the low refractive index range (1.46 to 1.52): \m. Mineralogist, v. 49, nos. 5-6, p. 683-688, 1964. 2- 64. (and POWERS, H. A.) Petrographic characteristics of Recent pumice from volcanoes in the Cascade Range [abs.]: Geol. Soc. America Spec. Paper 76, p. 232, 1964. WILLIAMS, J. R. 1-63. Ground water in permafrost regions—An annotated bibliography of publications through 1960, with glossary of terms: U.S. Geol. Survey open-file report, 2,608 p., 1963. 1-64. Geologic reconnaissance of the Yukon Flats Ceno-zoic basin, Alaska: U.S. Geol. Survey open-file report, 21 p., 1964. WILLIAMS, R. B. 1-64. Bedrock geology of the Wickford quadrangle, Rhode Island: U.S. Geol. Survey Bull. 1158-C, p. C1-C15, 1964. WILSHIRE, H. G. 1- 63. Geology of the Crutchfield quadrangle in Kentucky: U.S. Geol. Survey Geol. Quad. Map GQ-270, 1963. 2- 63. Geology of the Kirksey quadrangle, Kentucky: U.S. Geol. Survey Geol. Quad. Map GQ-246, 1963. WILSON, C. W., Jr. 1- 63. (and MARCHER, M. V.) Geologic map of the St. Joseph quadrangle, Tennessee: Tennessee Div. Geology Geol. Map GM 43-SE, 1963. 2- 63. (and MARCHER, M. V.) Geologic map of the Topsy quadrangle, Tennessee: Tennessee Div. Geology Geol. Map GM 42-NW, 1963. WILSON, H. D., Jr. 1-63. Hydrologic bench marks to distinguish the effects of climate vs. man: Ground Water, v. 1, no. 3, p. 13-14, 1963. WILSON, K. V. 1-63. Floods of 1960 in Mississippi: Mississippi Board Water Commissioners Bull. 63-9, 9 p., 1963. WINNER, M. D., Jr. 1-63. The Florida Parishes--An area of large, undeveloped ground-water potential in southeastern Louisiana: Louisiana Dept. Public Works and Louisiana Geol. Survey, Dept. Conserv., 50 p., 1963. WEMOGRAD, I. J. 1-63. A summary of the ground-water hydrology of the area between Las Vegas Valley and the Amargosa Desert, Nevada: U.S. Geol. Survey Rept. TEI-840 (open-file report), 76 p., 1963. WINSLOW, J. D. 1-64. (NUZMAN, C. E., and FADER, S. W.) Water-level changes in Grant and Stanton Counties, 1939-1964: Kansas Geol. Survey Spec. Distrib. Pub. 10, 11 p., 1964. WINTERS, H. A. 1-63. Geology and ground-water resources of Stutsman County, North Dakota-Pt. 1, Geology: North Dakota Geol. Survey Bull. 41, and North Dakota State Water Conserv. Comm., County Ground Water Studies 2, 84 p., 1963. WITHINGTON, C. F. 1- 64. Joints in clay and their relation to the slope failure at Greenbelt, Maryland, December 28, 1962: U.S. Geol. Survey open-file report, 7 p., 1964; abs., Geol. Soc. America Spec. Paper 76, p. 180-181, 1964. 2- 64. Map showing gravel resources in the Patuxent Formation of Cretaceous age in the Beltsville quadrangle. Prince Georges and Montgomery Counties, Maryland: U.S. Geol. Survey open-file report, map, 6 p., 1964. 746-002 0—64 -22A328 PUBLICATIONS IN FISCAL YEAR 1964 WITHINGTON, C. F.--Continued 3-64. (and COULTER, H. W.) Engineering geology in metropolitan Washington, D. C.: GeoTimes, v. 8, no. 5, pt. 1, p. 12-14, 1964. WITKIND, I. J. 1- 64. Preliminary geologic map of the Tepee Creek quadrangle, Montana-Wyoming: U.S. Geol. Survey Misc. Geol. Inv. Map 1-417, 1964. 2- 64. Age of the grabens in southeastern Utah: Geol. Soc. America Bull., v. 75, no. 2, p. 63-80, 1964. WOLFE, E. W. 1-63. Geology of the Dexter quadrangle, Kentucky: U.S. Geol. Survey Geol. Quad. Map GQ-244, 1963. WONES, D. R. 1- 63. Physical properties of synthetic biotites on the join phlogopite-annite: Am. Mineralogist, v. 48, no. 11-12, p. 1300-1321, 1963. 2- 63. Experimental petrology at moderate pressures: Am. Geophys. Union Trans., v. 44, no. 2, p. 542-548, 1963. WOOD, G. H., Jr. 1-63. (ARNDT, H. H., and HOSKINS, D. M.) Geology of the southern part of the Pennsylvania Anthracite region: Geol. Soc. America Guidebook--Field Trip No. 4, 84 p., 1963. WOOD, L. A. 1-63. (GABRYSCH, R. K., and MARVIN, Richard) Reconnaissance investigation of the ground-water resources of the Gulf Coast region, Texas: Texas Water Comm. Bull. 6305, 114 p., 1963. 1-64. (and GABRYSCH, R. K.) An analog model study of ground water in the Houston district, Texas, with a section on Design, construction, and use of analog models, by Eugene P. Patten, Jr.: U.S. Geol. Survey open-file report, 106 p., 1964. WOOD, P. R. 1-63. (and STACY, B. L.) Preliminary report on the geology and ground-water resources of Woodward County, Oklahoma: Oklahoma Water Resources Board Rept., 45 p., 1963. 1-64. (and MOELLER, M. D.) Ground-water levels in observation wells in Oklahoma, 1961-62: U.S. Geol. Survey open-file report, 132 p., 1964. WOODARD, T. H. 1-64. (and HEIDEL, S. G.) Inventory of published and unpublished chemical analyses of surface waters in the continental United States and Puerto Rico, 1961: U.S. Geol. Survey Water-Supply Paper 1786, 490 p., 1964. WOODCOCK, Alfred H. 1-63. (and FRIEDMAN, I.) The deuterium content of raindrops: Jour. Geophys. Research, v. 68, no. 15, p. 4477-4483, 1963. WOODRING, W. P. 1-64. Geology and paleontology of Canal Zone and adjoining parts of Panama: U.S. Geol. Survey Prof. Paper 306-C, p. 241-297, 1964. WORTS, G. F., Jr. 1- 63. A brief appraisal of ground-water conditions in the coastal artesian basin of British Guiana, South America: U.S. Geol. Survey Water-Supply Paper 1663-B, p. 1-44, 1963. 2- 63. Effect of ground-water development on the pool level in Devil's Hole, Death Valley National Monument, Nye County, Nevada: U.S. Geol. Survey open-file report, 27 p., 1963. 3- 63. Report of the U.S. Geological Survey, Water Resources Division, in. Nevada Water Conference, 16th, Carson City, Sept. 26-27, 1963, Proc.: p. 96-101, 1963. WRIGHT, J. C. 1-63. (and DICKEY, D. D.) Block diagram of the San Rafael Group and underlying strata in Utah and partof Colorado: U.S. Geol. Survey Oil and Gas Inv. Map OC-63, 1963. WRIGHT, T. L. 1-64. X-ray determination of composition and structural state of alkali feldspar: Am. Geophys. Union Trans., v. 45, no. 1, p. 127, 1964. YEN, T. P. 1-64. (and ROSENBLUM, Sam) Potassium-argon ages of micas from the Tananso schist terrane of Taiwan--A preliminary report: Geol. Soc. China Proc. 1964, no. 7, p. 80-81, 1964. YERKES, R. F. 1-64. (CAMPBELL, R. H., and SCHOELLHAMER, J. E.) Preliminary geologic map and sections of the southwest part of the Topanga quadrangle, Los Angeles County, California: U.S. Geol. Survey open-file report, map, 1964. YOCHELSON, E. L. 1- 63. Paleoecology of the Permian Phosphoria Formation and related rocks: U.S. Geol. Survey Prof. Paper 475-B, p. B123-B124, 1963. 2- 63. Problems of the early history of the Mollusca [abs.]: Internat. Congress Zoology, 16th, Washington, D. C., Aug. 20-27, 1963, Proc., v. 2, p. 187, 1963. 1-64. Book review of "Speciation in the sea" ed. by J. P. Harding and Norman Tebble: Systematic Zoology, v. 13, no. 1, p. 54-56, 1964. YOUNG, E. J. 1-64. (and LOVERING, T. G.) Productive and barren jas-peroids at Lake Valley, Sierra County, New Mexico [abs.]: Geol. Soc. America Spec. Paper 76, p. 182, 1964. YOUNG, K. B. 1-63. Flow characteristics of Wisconsin streams--Flow-duration, high-flow, and low-flow tables for selected streams through water year 1960: U.S. Geol. Survey open-file report, 151 p., 1963. YOUNG, L. E. 1-63. Floods near Fortuna, California: U.S. Geol. Survey Hydrol. Inv. Atlas HA-78, 1963. 1-64. (and RAY, H. A.) Flood inundation mapping, San Diego County, Calif., in,Geol. Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B163-B164, 1964. YOUNG, L. L. 1- 63. (COLBERT, J. L., NEAL, D. W., and FLAHERTY, G. M.) Gross theoretical waterpower, developed and undeveloped, Snake River basin, Wyoming, Idaho, Nevada, Oregon, and Washington: U.S. Geol. Survey open-file report, 52 p., 1963. 2- 63. (COLBERT, J. L., NEAL, D. W., and FLAHERTY, G. M.) Gross theoretical waterpower, developed and undeveloped, State of Oregon—Pt. 1, Basin summaries, 10 p.; Pt. 2, Lists of powersites: U.S. Geol. Survey open-file report, 42 p., 1963. 3- 63. (WAYLAND, R. G.,and GASKILL, D. L.) Waterpower resources in Trask River basin, Oregon: U.S. Geol.Survey Water-Supply Paper 1610-B, p. B1-B44, 1963. YOUNG, R. A. 1-63. (and CARPENTER, C. H.) Ground-water conditions and storage in the central Sevier Valley, Utah: U.S. Geol. Survey open-file report, 170 p., 1963. YUVAL, Zvi 1-64. Gravity observations and Bouguer anomalies in the Albemarle, Denton, Mt. Pleasant, and Salisbury quadrangles, North Carolina: U.S. Geol. Survey open-file report, 21 p., 1964. ZARTMAN, Robert E. 1-63. Comparison of Rb-Sr ages on biotites from Llano, Texas, in Nuclear Geophysics: Natl. Acad. Sci.—Natl. Research Council, Nuclear Sci. Ser. Rept. 38, p. 43-51, 1963. 1-64. The isotopic composition of lead in microclines from the Llano Uplift, Texas [abs.]: Am. Geophys. Union Trans., v. 45, no. 1, p. 109, 1964.LIST OF PUBLICATIONS A329 ZELLER, H. D. 1-63. Geologic map of the Roberts quadrangle. Carbon County, Mont.: U.S. Geol. Survey Mineral Inv. Field Studies Map MF-266, 1963. ZEN, E-an 1- 63. Structural relations in the southern taconic region— an interpretation, in. Geol. Soc. America Guidebook — Field Trip No. 3, 1963: Albany, State Univ. of New York, Dept. Earth Sciences, p. 1-4, 1963. 2- 63. Components, phases, and criteria of chemical equilibrium in rocks: Am. Jour. Sci., v. 261, no. 10, p. 929-942, 1963. 1-64. Subdivision of the Stockbridge Limestone in southwestern Massachusetts and adjacent Connecticut [abs.]: ZEN, E-an—Continued Geol. Soc. America Spec. Paper 76, p. 183-184, 1964. 2- 64. Taconic stratigraphic names—Definitions and synonyms: U.S. Geol. Survey Bull. 1174, 95 p., 1964. 3- 64. (ROSS, Malcolm, and BEARTH, Peter) Paragonite from Tasch Valley near Zermatt, Switzerland: Am. Mineralogist, v. 49, no. 1-2, p. 183-190, 1964. ZIETZ, Isidore 1- 64. A magnetic anomaly of possible economic significance in southeastern Minnesota: U.S. Geol. Survey Circ. 489, 5 p., 1964. 2- 64. (and GRISCOM, Andrew) Geology and aeromagnetic expression of the midcontinent gravity high [abs.]: Geol. Soc. America Spec. Paper 76, p. 184, 1964. INDEX TO LIST OF PUBLICATIONS Absolute age, dates Franconia Sandstone Zircon and feldspar concentrates: Tatsumoto, Mitsunobu, 1-64. General listing Antarctica, Thiel Mountains: Aaron, J. M. , 1-64. Glaucophane schist Cazadero area, California: Lee, D. E., 1-64. Granitic rocks California, Sierra Nevada-Inyo Mountains: Kistler, R. W. , 1-64. Igneous rocks Alaska Talkeetna Mountains Grantz, Arthur, 2-63. Precambrian rocks Williston basin: Peterman, Z. E., 1-64. Quartzite Red Creek quartzite, Precambrian: Hansen, W. R. , 1-64. Absolute age, methods Carbon-14 Preparation of water samples: Feltz, H. R. , 1-63. Obsidian dating: Friedman, Irving, 4-63. Africa Stratigraphy Northern, Nubian Sandstone :Mc-Kee, E. D. , 3-63. Alabama Areal geology Athens area: McMaster, W. M., 1-63. Birmingham red iron ore district: Simpson, T. A., 1-63. Colbert County: Harris, H. B., 1- 63. Franklin County: Peace, R. R., Jr., 1-63. Lauderdale County: Harris, H. B. 2- 63. Limestone County: McMaster, W. M. , 2-63. Montgomery County: Knowles, D. B. , 2-63. Morgan County: Dodson, C. L. , 1-63. Saint Clair County: Causey, L. V., 1-63. Economic geology Copper: Espenshade, G. H., 1-63. Iron, Birmingham district: Simpson, T. A., 1-63. Iron, Red Mountain Formation, relation of specific gravity to iron content: Sheldon, R. P.,1-64 Hydrogeology Athens area: McMaster, W. M. , 1-63. Alabama (Continued) Hydrogeology (Continued) Birmingham red iron ore district: Simpson, T. A., 1-63. Colbert County: Harris, H. B. , 1-63. Franklin County, geologic and ground-water: Peace, R. R., Jr., 1-63. Lauderdale County: Harris, H. B., 2-63. Limestone County: McMaster, W. M., 2-63. Montgomery County: Knowles, D. B. , 2-63. Morgan County: Dodson, C. L. , 1-63. Oil field brine disposal: Knowles, D. B., 2-64. Saint Clair County: Causey, L. V. , 1-63. Streams, temperature: Avrett, J. R., 1-63. Water problems associated with oil production: Powell, W. J., 1-63. Structural geology Birmingham red iron ore district: Simpson, T. A., 2-63. Relation of springs to thrust faults: Warman, J. C., 1-63. Alaska Absolute age Igneous rocks, Talkeetna Mountains: Grantz, Arthur, 2-63. Paleozoic intrusive rocks, southwestern, K-Ar: Lan-phere, Marvin A., 1-64. Areal geology Bokan Mountain uranium-thorium area: MacKevett, E. M., Jr., 1-63. Chandler River region: Detter-man, R. L., 1-63. Chichagof and Kruzof Islands: Pomeroy, J. S., 1-64. Iliamna quadrangle: Detterman, R. L. , 1-64. Imuruk Lake area: Hopkins, D. M. , 1-63. Kenai Lowland:Karlstrom, T. N. V., 1-64. Killik-Etivluk Rivers region: Chapman, R. M. , 1-64. North Bradfield iron prospect: MacKevett, E. M., Jr. ,4-63. Red Devil quicksilver mine: MacKevett, E. M., Jr. ,3-63. Shumagin Island: Grantz, Arthur, 1-63. Test-well drilling: Walters, K. L. , 1-63. Yukon Flats Cenozoic basin: Williams, J. R., 1-64. Alaska (Continued) Earthquakes March 27, 1964: Grantz, Arthur, 2- 64. Economic geology: U. S. Geol. Survey, 6-63. Beryllium, Seward Peninsula: Sainsbury, C. L., 1-63. Gold, placer deposits: Cobb, E. H., 1-64. Oil shale, northern: Tailleur, I. L. , 1-64. Resources: U. S. Geol. Survey, 8-64. Tin and tungsten, Lost River area: Sainsbury, C. L. , 1-64. Engineering geology Water power: Johnson, Arthur, 1-63. Geochemistry Radionuclides, absorption equilibria: Baker, J. H. , 1-64. Stream sediments, Juneau area: Berg, H. C., 1-64. Geomorphology Ogotorak Creek area, valley asymmetry: Currey, D. R., 1-64. Structural effect on topography, Baranof Island: Brew, D. A., 1-63 Glacial geology Cook Inlet region: Karlstrom, T. N. V., 1-64. Glaciolacustrine deposits,Copper River Basin: Ferrians, O. J., Jr., 1-63. Hydrogeology Angoon, water-well drilling: Lockwood, W. N., 1-64. Homer area, well data: Waller, R. M., 1-63. King Salmon area: Feulner, A. J. , 1-63. Northwestern, chemical quality of ground water: Feulner, A. J., 3- 63. Ohlson Mountain area: Feulner, A. J., 2-63. Resources: U. S. Geol. Survey 8-64. Test-well drilling: Walters, K. L., 1-63. Maps Baranof and Kruzof Islands, geologic: Loney, R. A., 1-64. Chandalar quadrangle, geologic: Brosge, W. P., 1-64. Chichagof and Baranof Islands, geologic: Loney, R. A., 1-63. McCarthy A-4 quadrangle, geologic: Miller, D. J., 1-64. McCarthy C-4 quadrangle, geologic: MacKevett, E. M., Jr., 1-64. A331A332 Alaska (Continued) Maps (Continued) McCarthy C-5 quadrangle, geologic: MacKevett, E, M., Jr., 2-63. Tanana Lowland, aeromagnetic: Andreasen, G. E., 4-64. York Mountains, geologic: Sainsbury, C. L. , 2-64. Paleontology Brachiopoda, Ordovician, east-central: Dutro, J. T., Jr., 1-64. Cephalopoda, Cretaceous, ammonites: Jones, D. L., 1-63. Foraminifera, Pleistocene-Recent, Gulf of Alaska: Smith, P. B., 1-63. Foraminifera, Poul Creek Formation: Rau, W. W., 1-63. Microfauna of Bootlegger Cove Clay: Schmidt, R. A. M., 1-63. Permafrost, ice wedges: P6w£, T. L., 1-64. Stratigraphy Gubik Formation, Quaternary: Black, R. F., 1-64. McCarthy A-4 quadrangle, sections: Miller, D. J., 1-64. Matanuska Formation, Matanus-ka Valley: Grantz, Arthur, 1-64. Pleistocene-Recent boundary. Gulf of Alaska: Smith, P. B., 1-63. Tuxedni Group, Cook Inlet region: Detterman, R. L., 2-63. Structural geology Chatham Strait fault: Lathram, E. H. , 1-64, 2-64. Volcanology Katmai, book review: Davies, W. E. , 2-63. Alluvial fans California Fresno County: Bull., W. B., 1-64. Missouri Charleston: Ray, L. L. 1-64. Sediment transport: Lustig, L. K, 1-63. Antarctica Absolute age Thiel Mountains: Aaron, J. M., 1-64. Areal geology Patuxent Mountains: Schmidt, D. L., 1-63. Glacial geology Thiel Mountains: Andersen, B. G., 1-63. Paleontology Paleobotanical studies: Schopf, J. M., 1-64. Petrology Differentiated diabase sheet: Hamilton, Warren, 6-63. Thiel Mountains, cordierite-bearing hypersthene quartz monzonite: Ford, A. B., 1-63. PUBLICATIONS IN FISCAL YEAR 1964 Antarctica (Continued) Stratigraphy Beacon Sandstone: Hamilton, Warren, 3-63. Anthozoa Devonian, Billingsastraea: Oliver, W. A., Jr., 3-64. Appalachian region General Isotopic ages, crustal heating, and sedimentation: Hadley, J. B., 1-64, 2-64. Geophysical surveys Basement depths: Griscom, Andrew, 1-64. Weathering Bauxitization: Knechtel, M. M., 1-63. Arabia Maps Arabian Peninsula, geologic: U. S. Geol. Survey, 21-63. Arctic Ocean Basin Geomorphology Genesis of basin: King, E. R., 1-64. Heat flux: Lachenbruch, A. H. , 1-64. Arctic Region Biological research: Davies, W. E., 1-64. Arizona Areal geology Cenozoic history: Cooley, M. E , 1-64. Lake Mead to Davis Dam: Long-well, C. R., 1-63. Lees Ferry area: Phoenix, D. A., 1-63. McMullen Valley: Kam, William, 1- 64. Pinal Ranch quadrangle: Peterson, N. P., 1-63. Verde Valley-Mogollon River region: Twenter, F. R., 1-63. Yuma area: Olmsted, F. H., 2- 64. Economic geology Uranium, Shiprock quadrangle: O'Sullivan, R. B., 1-63. Hydrogeology Annual report on ground water, spring 1962 to spring 1963: White, N. D., 2-63. McMullen Valley: Kam. William, 1-64. Maricopa County, water salvage: Thomsen, B. W., 1-63. Prescott area, floods, 1963: Aldridge, B. N., 1-63. Rainbow Valley and Waterman Wash areas: White, N. D. , 1-63. San Francisco Plateau, ground water: Akers, J. P., 1-63. San Pedro River, water regimen; Page, H. G., 1-63. Southern, floods, 1962: Lewis, D. D., 1-63. Arizona (Continued) Hydrogeology (Continued) Verde Valley-Mogollon Rim region: Twenter, F. R., 1-63. Willcox Basin: Brown, S. G., 1-63. Yuma, evapotranspiration tanks: Hughes, G. H., 1-64. Maps Bagdad area, aeromagnetic: Dempsey, W. J., 1-63. Cochise quadrangle, aeromagnetic: Dempsey, W. J., 2-63, 6-63. Los Gigantes Buttes quadrangle, aeromagnetic: Frischknecht, F. C., 1-63. Mammoth quadrangle, aeromagnetic: Dempsey, W. J., 7-63. Maricopa County, aeromagnetic: Dempsey, W. J., 5-63. Shiprock quadrangle, geologic, structural: O'Sullivan, R. B., 1-63. Twin Buttes area, aeromagnetic: Andreasen, G. E., 5-63. Yavapai County, central, aeromagnetic: Dempsey, W. J., 4-63. Yellowstone Canyon quadrangle, aeromagnetic: Frischknecht, F. C., 2-63. Mineralogy Johannsenite, Aravaipa district: Simons, F. S., 1-63. Paleontology Corals, Mississippian, new species: Sando, W. J., 1-63. Petrology Andesite and rhyolite dike, Klon-dyke: Simons, F. S., 1-63. Stratigraphy Dripping Spring Quartzite: Granger, H. C., 1-64. Mogollon Highlands, influence on erosion and sedimentation: Cooley, M. E., 1-63. Redwall Limestone: McKee, E. D. , 1-63. Southeastern: Davidson, E. S., 1-64. Structural geology Defiance positive element: McKee, E. D., 2-63. Pusch Ridge, Santa Catalina Mountains: Pashley, E. F. ,Jr.. 1-63. Southeastern:Davidson, E. S. ,1-61 Tanque Verde, Rincon, and southern Santa Catalina mountains :Pashley, E. F. , Jr. , 1-64. Arkansas Areal geology Bradley, Calhoun, and Ouachita Counties: Albin, D. R. , 1-64. Paris quadrangle: Haley, B. R., 1-64. General Geological interpretations: Glick, E. E., 2-63.INDEX TO LIST OF PUBLICATIONS A333 Arkansas (Continued) Hydrogeology Arkansas River, valley:Bedinger, M. S., 1-64, 2-63; Cordova, R. M. , l-63;May, J. R., 1-64. Bradley, Calhoun, and Ouachita Counties:Albin, D. R., 1-64. Eastern, ground-water: Hahl-berg, H. N., 1-63. Floods :Smith, R. P., 1-64. Grand Prairie region: Engler, Kyle, 1-63; Sniegocki, R. T., 1- 63, 2-63, 3-63, 1-64. Hot Springs area, floods: Gilstrap, R. C., 1-64. Ouachita Mountains: Albin, D. R., 2-64. Maps Bauxite, Mississippi embay-ment, aeromagnetic:Jesper-son, Anna, 1-64. Malvern quadrangle, geologic: Danilchik, Walter, 1-64. Paleontology Cambarus (Decapoda, Astacidae): Hobbs, H. H., Jr., 1-64. Seismology Nuclear pressure wave in wells: May, J. R., 1-63. Stratigraphy Chester, Morrow, and Atoka Series:Merewether, E. A., 1-63. Chester and Morrow rocks: Gordon, Mackenzie, Jr. , 1-63. Morrow Series: Henbest, L. G., 2- 63. Asbestos Ve rmont Missisquoi Valley: Cady, W. M., 1-63. Atlantic Coastal Plain Hydrogeology:LeGrand, H. E., 1-64. Bacteria Unmineralized fossil: Bradley, W. H., 1-63. Basalt Arsenic content :Bartel, A. J., 1-63. Bauxite Reserves and potential resources of world:Patterson, S. H., 1-63. Beryllium Crystal chemistry:Ross, Malcolm, 1-64. Igneous rocks :Shawe, D. R., 2-64. Volcanic rocks: Bernold, Stanley, 1-64. Bibliography Hydrology: Johnson, A. I., 1-64. Permafrost regions: Williams, J. R. , 1-63. Ross, C. S. : Hooker, Marjorie, 1- 63. Schaller, W. T. : Hooker, Marjorie, 1-63. Talc United States: Merrill, C. W., 2- 63. Texas: Mills, W. B., 1-63. Biography Brown, Barnum: Lewis, G. E., 1- 63, 2-64. Gilbert, G. K. : Gilluly, James, 2- 63. Pepper, James Franklin:DeWitt, Wallace, Jr., 1-64. Putnam, William C. : Smith, W. C., 1-64. Stephenson, Lloyd W. : Monroe, W. H., 2-64. Zapp, A. D. : Gill, J. R., 1-63. Boron Geochemistry Hydrous Na-Ca borate: Han-shaw, B. B., 1-63. Halite rocks:Grimaldi, F. S., 1-63. Brachiopoda Camerophoriacea:Grant, R. E., 1-64. Chonetoidea Morphology and classification: Dutro, J. T. ,Jr. , 3-63. Composita Morphologic studies: Grinnel, R. S., Jr., 1-64. Ordovician Alaska, east-central: Dutro, J. T., Jr., 1-64. Permian Texas, Glass Mountains :Cooper, G. A., 1-64. Brazil Areal geology Belo Horizonte, Ibiritg, and Macacos quadrangles: Pomerene, J. B., 1-64. Itabira District: Dorr, J. V. N., 2d, 1-63. Rio Grande do Sul: Morris, R. H. , 1-63. Economic geology Belo Horizonte, Ibiritfe and Macacos quadrangles :Pomerene, J. B. , 1-64. Iron, Minas Gerais: Dorr, J. V. N. ,2d, 1-64. Itabira District: Dorr, J. V. N., 2d, 1-63. Lead-zinc deposits, Minas Gerais:Robertson, J. F., 1-63. Hydrogeology Amazon River: Davis, L. C., Jr., 1-64; Oltman, R. E., 1-64. Mineralogy Leucophosphite, Minas Gerais: Simmons, G. C., 1-64. Brines Subsurface formations Mechanism for concentration: Bredehoeft, J. D., 2-63. British Guiana Hydrogeology Coastal artesian basin: Worts, G. F., Jr. , 1-63. California Absolute age Glaucophane schist, Cazadero area: Lee, D. E., 1-64. California (Continued) Absolute age (Continued) Sierra Nevada-Inyo Mountains, granitic rocks: Kistler, R. W., 1- 64. Areal geology Cerro Gordo mining district: Merriam, C. W., 1-63. Cosio Knob quadrangle :Durham, D. L., 1-64. East Mesa area:01msted, F. H., 2- 64. Edwards Air Force Base: Dutcher, L. C., 2-63. Espinosa Canyon quadrangle: Durham, D. L., 1-64. French Gulch quadrangle :Albers, J. P., 1-64. Indian Wells Valley, Owens Valley, Long Valley, and Mono Basin: von Huene, Roland, 1-63. Mission Creek Indian Reservation: Giessner, F. W., 1-64. Mount Diablo, Contra Costa County:Pampeyan, E. H., 1-63. Mount Morrison quadrangle: Rinehart, C. D., 1-64. Naval Air Missile Test Center area: Page, R. W., 1-63. Puente Hills area: Durham, D. L., 2-64. Reliz Canyon quadrangle :Durham, D. L., 1-63. San Antonio Creek Valley: Muir, K. S., 1-64. San Bernardino area: Dutcher, L. C., 1-63. San Lucas quadrangle:Durham, D. L., 1-63. San Nicolas Island: Vedder, J. G., 1-63. Thompson Canyon quadrangle: Durham, D. L., 1-63. Ecology Fresh water clams, erroneous records: Taylor, D. W., 2-63. Economic geology Mercury, New Almaden: Bailey, E. H., 2-64. Mount Morrison quadrangle: Rinehart, C. D., 1-64. Nickeliferous laterites: Hotz, P. E., 2-64. Oil, Puente Hills area: Durham, D. L., 2-64. Panamint Butte quadrangle and Modoc district, Inyo County: Halle, W. E. , 2-63. Salton Sea brine, ore-transporting fluid: White, D. E., 2-63. Engineering geology Impact shock absorption of rocks: DeBuchananne, G. D., 1-63. Land subsidence, San Joaquin Valley: Lofgren, B. E. , 2-63. Recent surface movements, Baldwin Hills, Los Angeles County: U. S. Geol. Survey, 10-64.A334 California (Continued) Engineering geology (Continued) San Francisco Bay area: Rad-bruch, D. H., 1-64. Test drilling, Naval Missle Facility, Point Arguello: Even-son, R. E., 1-64. Waterpower: Doolittle, R. N., 1-64. Geochemistry Argon retention in granitic xen-olith from basalt: Dalrymple, G. B., 1-63. Hafnium in zircon, southern California batholith: Gottfried, David, 1-64. Isotopes, brine and obsidian, near Niland: Doe, B. R., 1-63. Ge omorphology Alluvial fans, Fresno County: Bull, W. B., 1-64. Channel trenching, Fresno County: Bull, W. B., 2-64. Ridges, differential subsidence of peatlands: Davis, G. H., 3- 63. Geophysical surveys Central, gravity: Oliver, H. W., 1-63, 2-63. Long Valley, gravity: Rinehart, C. D., 1-64. Mount Morrison quadrangle, gravity: Pakiser, L. C. ,1-64. Hydrogeology Castaic watershed, sediment yield: Lustig, L. K., 1-64. Central Valley, water utilization: Thomas, H. E., 2-63. Coast Ranges, optimum discharge: Rantz, S. E., 3-63. Death Valley National Monument, Furnace Creek Wash area: Kunkel, F., 1-63. Drought effects: Thomas, H. E., 4- 63. Edwards Air Force Base: Dutcher, L. C., 2-63; Weir, J. E., Jr., 1-63. Floods, January-February 1963: Rantz, S. E., 4-63. Ground-water pumpage: McClelland, E. J., 1-63. Indian Wells Valley, well data: Moyle, W. R. , Jr., 1-63. Joshua Tree National Monument: Weir, J. E., Jr. ,2-63. Lake Pillsbury, sedimentation: Porterfield, George, 1-64. Lower Mojave Valley: Dyer, H. B. , 1-63. Mission Creek Indian Reservation: Giessner, F. W., 1-64. Naval Air Missle Test Center area: Page, R. W., 1-63. North Fork Feather River: Cobb, E. D., 1-64. North Yuba River basin, snow-belt: Rantz, S. E., 1-63, 5-63. Northern, coastal basins:Rantz, S. E. . 2-64. PUBLICATIONS IN FISCAL YEAR 1964 California (Continued) Hydrogeology (Continued) Pai ker-Blythe-Cibola and Needles areas: Metzger, D. G., 1-64. Permanente Creek, streamflow regimen: Harris, E. E., 1-63. Point Arguello area: Miller, G. A., 1-63. Rice and Vidal Valley areas, well data: Giessner, F. W., 2-63. Riverside County, well data: Giessner, F. W., 1-63. Saline ground water: Bader, J. S., 1-64. San Antonio Creek Valley: Muir, K. S. , 1-64. San Bernardino area: Dutcher, L. C., 1-63. San Diego County, flood-inundation mapping: Young, L. E., 1-64. San Joaquin Valley, drought: Davis, G. H., 1-63. San Joaquin Valley, ground storage of surface water: Davis, G. H. , 1-64. San Luis Rey River basin, potential flood areas: Ray, H. A., 1- 63. Santa Barbara County, well data: Muir, K. S., 1-63. Santa Margarita River basin, annual runoff: Rantz, S. E., 2- 63. Sierra Nevada, stream snowmelt: Rantz, S. E., 1-64. Southern, mountain basins: Crippen, J. R., 1-63. Twentynine Palms Marine Corps Base: Johnston, P. M., 2-64. United States Geological Survey activities during fiscal 1964: U. S. Geol. Survey, 1-63. Upper Salinas River Basin, drought effects: Gatewood, J. S., 1- 63. Water from granitic rocks: Feth, J. H. , 1-64. Maps Arvin-Maricopa area, subsidence: Lofgren, B. E., 1-63. Death Valley National Monument, aeromagnetic: Andreasen, G. E., 2- 63. Death Valley region, gravity: Mabey, D. R., 1-63. Fortuna, floods: Young, L. E. , 1-63. French Gulch quadrangle, geologic: Albers, J. P. , 3-64. Furnace Creek borate area, geologic: Me Allister, J. F. ,1-64. Garlock area, aeromagnetic: Bromery, R. W., 2-64. Kramer area, aeromagnetic: Frischknecht, F. C., 2-64. California (Continued) Maps (Continued) Los Angeles area, aeromagnetic: Andreasen, G. E., 2-64. Los Banos-Kettleman City area, geologic: Miller, R. E., 1-63. Manzanita Lake quadrangle, geologic: MacDonald, G. A., 1-63. Oxidized zinc districts: Heyl, A. V., 1-64. Oxnard area, aeromagnetic: Andreasen, G. E., 3-64. San Andreas quadrangle, geologic: Clark, L. D., 1-63. San Francisco South quadrangle, geologic: Bonilla, M. G., 1-64. Topanga quadrangle, geologic: Yerkes, R. F., 1-64. Weaverville quadrangle, geologic: Irwin, W. P., 1-63. Mineralogy Apatitized wood and leucophos-phite, Moreno Formation: Gul-brandsen, R. A., 1-63. Deep Spring Lake, saline mineral sequence: Jones, B. F,, 1-64. Garnet, Cazadero area: Lee, D. E., 1-63. Sulfides deposited by Salton Sea brine: Skinner, B. J., 1-63. Paleontology Bristlecone pines: LaMarche, V. C., Jr., 1-63. Jurassic: Imlay, R. W., 1-64. Miocene veriebrates: Lewis, G. E., 1-64. Pale ot empe rature Mollusca, late Miocene: Addicott, W. O., 1-63. Petrology Alpine-type ultramafic intrusions: Lipman, P. W., 3-64. Canyon Creek pluton: Lipman, P. W., 2-64. Glaucophane-bearing metamorphic rocks, Cazadero area: Coleman, R. G., 1-63. Mount Diablo piercement, Franciscan and related rocks: Pam-peyan, E. H., 1-64. Sierra Nevada batholith: Bateman, P. C., 1-63. Sierra Nevada plutonic rocks, Sr-87/Rb-87 relationships: Hurley, P. M., 1-64. Sedimentation Lake Pillsbury: Dunnam, C. A., 1-64. Stratigraphy Franciscan Formation: Bailey, E. H., 1-63. Los Banos-Kettleman City area, sections: Miller, R. E., 1-63. Paleozoic, Independence quadrangle: Ross, D. C., 1-63. Pliocene, San Joaquin Valley: Klausing, R. L., 1-64. Topanga quadrangle, sections: Yerkes, R. F., 1-64.INDEX TO LIST OF PUBLICATIONS A335 California (Continued) Stratigraphy- Upper Cretaceous, Berkeley and San Leandro Hills: Case, J. E., < 2-64. Structural geology Canyon Creek pluton: Lipman, P. W., 2-64. Coast Ranges, thrust faults: Brown, R. D., Jr., 1-64. Crust, coastal area: Healy, J. H., 1-63. Crust, San Francisco to Eureka, Nevada: Eaton, J. P., 1-64. Crust, Santa Monica Bay to Lake Mead: Roller, J. C., 2-63. Crustal section: Eaton, J. P., 1-63. San Andreas fault, sphenoclastic rifting: Bailey, E. H., 1-64. Southeastern, nappes: Hamilton, Warren, 1-64. Cartography Arizona Lake Powell, large-scale mapping: Rutledge, D. H., 1-63. Control traverses: Moore, R. H., 1-64. Control traverses and adjustment: Speert, J. L. , 1-64. Cooperative control project: Walker, H. D., 1-64. Maximum bridging distance: Kennedy, Daniel, 1-64. Cephalopoda Ammonites Wyoming, Late Cretaceous: Cobban, W. A., 1-63. Haresiceras Late Cretaceous: Cobban, W. A., 1- 64. Chemical analyses Techniques Phosphate glass electrode for alkaline-earth cations: Trues-dell, A. H., 1-63. Chile Areal geology Provincia de Atacama: Parker, R. L. , 2-63. Quaternary: Segerstrom, Kenneth, 2- 64. Earthquakes Concepcion, water and sand eruption: Segerstrom, Kenneth, 1-63. Las Melosas-El Volcan, August-September 1958: Saint-Amand, Pierre, 1-64. Economic geology Salt, northern: Ericksen, G. E., 1- 64. Hydrogeology Arica area: Doyel, W. W., 1-64. Santiago area: Doyel, W. W. , 3- 64. Tierra del Fuego: Doyel, W. W., 2- 64. Chile (Continued) Paleontology Pleistocene, Arica area, diatoms: Dingman, R. J., 1-63. Petrology Batholith emplacement, Tierra Amarilla: Tilling, Robert, 1-64. Stratigraphy Mudflow, Quaternary, Santiago: Segerstrom, Kenneth, 1-64. China Economic geology Coal production, trends :Averitt, Paul, 1-64. Clay mineralogy Adsorption on illite: Wayman, C. H, 4-63. Adsorption in montmorillonite: Wayman, C. H. , 7-63. Areal studies Upper Mississippi Valley: Heyl, A. V., 2-64. Clinton ironstones: Schoen, Robert, 1-63. Experimental studies Cation exchange, solution theory: Christ, C. L., 1-64. Mineral descriptions Alteration of montmorillonite to kaolinite: Altschuler, Z. S.,1-63. H-montmorillonite: Pommer, A. M., 1-63. Surfactant sorption: Wayman, C. H., 2-63. Coal Alabama Resources and geology of coalbearing rocks: Culbertson, W. C. , 1-64. Weathering: Breger, I. A., 1-64. Colorado Areal geology Black Canyon area: Hansen, W.R., 4-64. Glenwood Springs quadrangle: Bass, N. W., 1-63. Lake George beryllium area: Hawley, C. C., 2-64. Otero and Crowley Counties: Weist, W. G., Jr., 1-63. Platte Canyon quadrangle Peterson, W. L. , 2-64. Tenmile Range: Bergendahl, M. H., 1-63. Yuma County: Weist, W. G. ,Jr., 1-64. Economic geology Base metal and barite. Spar City district: Steven, T. A., 1-64. Colorado mineral belt: Tweto, Ogden, 1-63. Gold, silver, uranium, and base metals, Central City district: Sims, P. K., 1-63. Malachite mine, copper, prospecting methods: Huff, L. C. , 1-63. Colorado (Continued) Economic geology (Continued) Uranium and associated ores. Front Range mineral belt: Sims, P. K., 2-63. Engineering geology Loveland Basin landslide: Robinson, C. S., 1-64. Straight Creek tunnel site:Robin-son, C. S., 2-64. Geochemistry Crude oils, composition: Bass, N. W., 1-64. Geomorphology Sage Plain, linear scarps, wind erosion origin: Shawe, D. R. , 1- 63. Geophysical surveys Loveland Basin landslide: Robinson, C. S., 1-64. Rampart Range area, gravity: Miller, C. H., 1-63. Hydrogeology Arkansas Valley: Moulder, E. A. , 2- 63. Badger Wash basin: Lusby, G. C. , 1-63. Cache la Poudre River basin: Hershey, L. A., 1-64. Denver Basin: McConaghy, J. A., 1-64. Floods, Longmont area:Jenkins, C. T. , 1-63. Fountain and Jimmy Camp Valleys: Jenkins, E. D., 1-64. High Plains: McGovern, H. E. , 1-63. Huerfano County: McLaughlin, T. G. , 1-64. Importance during emergency: Voegeli, P. T., Sr., 1-63. Larimer, Logan, Morgan, Sedgwick, and Weld CountiestWeist, W. G., Jr., 2-64. North Park and Middle Park: Voegeli, P. T., Sr., 1-64. Otero and Crowley Counties: Weist, W. G., Jr., 1-63,2-63. Rocky Mountain National Park: Voegeli, P. T., Sr., 2-63. South Platte River Basin:Smith, R. O. , 1-64. Yuma County: Weist, W. G. ,Jr., 1-64. Maps Grand Junction area, geologic: Lohman, S. W., 1-63. Hot Sulphur Springs SE quadrangle, geologic: Izett, G. A., 1-63. Mount Wilson quadrangle, geologic: Bromfield, C. S. , 1-63. Pueblo quadrangle, geologic: Scott, G. R., 1-64. San Rafael Group, stratigraphic: Wright, J. C., 1-63.A336 Colorado (Continued) Paleontology Mancos Shale, Disappointment Valley: Reeside, J. B., Jr., 1- 64. Miocene vertebrates: Izett, G. A., 2- 63. Petrology Beryllium-bearing greissens, Lake George area: Hawley, C. C., 1-63. Black Canyon, Curecanti pluton: Hansen, W. R., 2-64. Central City quadrangle, Pre-cambrian rocks, cordierite-bearing mineral assemblages: Sims, P. K., 3-63. Creede caldera, magmatic differentiation: Ratte, J. C., 1-64. Front Range mineral belt, altered wall rock: Tooker, E. W., 1-63. Lake George area: Hawley, C. G, 1-64. Sawatch Range, St. Kevin Granite: Tweto, Ogden, 1-64. Walsen composite dike, Walsen-burg: Johnson, R. B. , 1-64. Stratigraphy Kirtland and Fruitland Formations, Upper Cretaceous, San Juan Basin: Fassett, J. E., 1- 64. Nussbaum Alluvium, Pleistocene (?), Pueblo: Scott, G. R. , 1-63. Ohio Creek Formation, Paleo-cene: Gaskill, D. L., 1-63. Pierre shale, Apache Creek Sandstone Member: Scott, G. R., 2- 63. San Juan Mountains, Tertiary volcanics: Luedke, R. G., 1-64; Steven, T. A., 2-64. Structural geology Black Canyon, repeated movements on conjugate faults: Hansen, W. R., 3-64. Eastern, crustal structure, seismic survey: Jackson, W. H. , 1-63. Fracture patterns in Harold D. Roberts Tunnel: Warner, L. A., 1-64. Gypsum Valley salt anticline: Cater, F. W., 1-64. Colorado Plateau Geochemistry Element distribution, uranium deposits: Miesch, A. T. ,1-63. Stratigraphy Chinle Formation, tuffaceous sandstones: Cadigan, R. A., 1-63. Triassic, clay minerals: Schultz, L. G. , 1-63. Colorado River Basin Hydrogeology Drought effects: Cushman, R. L. , 1-63. PUBLICATIONS IN FISCAL YEAR 1964 Connecticut Areal geology Farmington-Granby area: Randall, A. D., 1-64. Middletown area: Baker, J. A., 1- 63. Hydrogeology Bristol -Plainville -Southington area: LaSala, A. M. , Jr., 2- 64. Farmington-Granby area: Randall, A. D., 1-64. Hartford-New Britain area: Cushman, R. V., 3-64. Middletown area: Baker, J. A., 1-63. North-central: Cushman, R. V., 1- 64. North-central, well data:Cushman, R. V., 2-64. Maps Ashley Falls quadrangle, materials: Holmes, G. W., 1-64. Bashbish Falls quadrangle, geologic: Hartshorn, J. H., 1-64. Broad Brook quadrangle, bedrock surface: Cushman, R. V., 2- 63. Eastern, geologic: Goldsmith, Richard, 2-64. Hartford North quadrangle, geologic: Cushman, R. V., 1-63. Manchester quadrangle, bedrock surface: Colton, R. B., 6-63. Mount Carmel quadrangle, geologic: Fritts, C. E., 1-63. South Sandisfield quadrangle, materials: Holmes, G. W. ,7-64. Southern quadrangle, geologic: Fritts, C. E., 2-63. Petrology Ashaway quadrangle: Feininger, Tomas, 1-64. Voluntown quadrangle :Feininger, Tomas, 1-64. Westerly Granite: Feininger, T. G. , 2-63. Post-glacial sea-level changes New Haven harbor: Upson, J. E., 2-64. Stratigraphy Stockbridge Limestone: Zen, E-an, 1-64. Conodonts Bibliography, 1959-61: Ash, S. R., 2-63. Nomenclature problems: Huddle, J. W., 1-64. Contact metamorphism Reaction between mafic magma and pelitic schist: Barker, Fred, 2-64. Continental drift Antarctic tectonics: Hamilton, W. B., 5-63. General discussion: Bradley,W.H., 2-63. Stable continents suggested by fossil flora: Hamilton, Warren, 2-64. Continental shelf Atlantic Ocean Program for study: Emery.K.O., 1-63. Sedimentation and erosion: Gilluly, James, 1-64. Sediments: Uchupi, Elazar, 1-63. Structure and magnetic anomaly: Watkins, J. S., 2-64. Topography: Uchupi, Elazar,l-64. Copper Isotopes Natural variations: Shields,W.R., 1-63. Cratering Fluid impact craters: Moore,H.J., 1-63, 1-64. Impact of steel into Coconino Sandstone: Shoemaker, E. M. , 1-63. Photogrammetric mapping: Lugn, R. V., 1-64. Crust Electrical properties: Keller, G. V., 1-63. Structure Basin and Range province: Eaton, J. P., 2-64. Velocities Refraction measurements: Roller, J. C., 1-63. Cryptoexplosion structures Kentucky Versailles: Black, D. F.B.,1-64. Crystal chemistry Hydrated calcium borates:Clark, J. R., 2-63. Proustite-pyrargyrite: Toulmin, Priestley, 3d, 1-63. Crystal structure Meta-autunite: Ross, Malcolm, 1-63. Unit cell dimensions Computer determination: Evans, H. T., Jr., 1-63. Delaware Hydrogeology Delaware River basin: Hardison, C. H., 2-63; Hely, A. G.,2-63. New Castle County, ground water resources: Rima, D.R., 1-64. Maps Bethany Beach area, ground water: Boggess, D.H., 2-63. Burrsville area, ground water: Boggess, D. H., 7-63. Dover area, ground water: Adams, J. K., 2-63. Frankford area, ground water: Adams, J. K., 3-63. Frederica area, ground water: Davis, C. F„ 1-63. Harrington area, ground water: Davis, C. F., 2-63. Kenton area, ground water: Boggess, D. H., 3-63. Laurel area, ground water: Boggess, D. H., 4-63. Little Creek area, ground water: Boggess, D. H., 5-63.INDEX TO LIST OF PUBLICATIONS A337 Delaware (Continued) Maps (Continued) Marydel area, ground water: Davis, C. F., 3-63. Middletown area, ground water: Boggess, D. H., 1-64. Milford area, ground water: Boggess, D. H., 8-63. Millsboro area, ground water: Boggess, D. H., 6-63. Mispillion River area, ground water: Davis, C. F., 4-63. Newark area, ground water: Boggess, D. H., 1-63. Saint Georges area, ground water: Adams, J. K., 1-63. Sharptown area, ground water: Adams, J. K., 4-63. Smyrna area, ground water: Boggess, D. H„ 2-64. Taylors Bridge area, ground water: Adams, J. K., 2-64. Trap Pond area, ground water: Adams, J. K., 5-63. Wilmington area, ground water: Adams, J. K., 1-64. Wyoming area, ground water: Boggess, D. H., 9-63. Density Tuff: Dickey, D. D., 2-64. Desert varnish Minor-element content: Lakin, H. W., 1-63. Detergents Survival of Escherichia coli: Wayman, C. H., 8-63. Deuterium Hydrologic cycle: Friedman, Irving, 3-64. Rainwater:Woodcock,Alfred H., 1-63. District of Columbia Areal geology: Johnston, P. M., 1-64; Coulter, H. W., 1-64. Engineering geology: Withington, C. F., 3-64. Radioactivity Correlation with areal geology: Neuschel, S. K., 1-64. Dolomite Solubility Ground water: Barnes, Ivan, 2-64. Drainage patterns Reservoir storage on streams: Hardison, C. H., 1-64. Earthquakes Fault plane solutions: Scheidegger, A. E., 1-63. Ecology Barred marine basin: Breger, I. A., 63. General: Fosberg, F. R., 2-64. Economic geology Developments in 1963: Guild, P. W., 1-63. Ore microscopy Book review: Milton, Charles, 1-63. Education United States Geological Survey's training program: Andrews, D. A., 1-63. Egypt Hydrogeology Corrosion of desert wells:Clarke, F. E., 1-63. Elastic properties Calcite: Peselnick, Louis, 1-63. Elastic waves Nuclear explosions Traveltimes and amplitudes: Ryall, Alan, 1-63. Electrical exploration Resistivity, nomograms: Scott, J. H., 1-63. Electrical properties Deep crust: Keller, G. V., 1-63. Electron probe analysis (Zn,Fe)S:Adler,Isidore, 1-63, 1-64. Emission spectrometry Silicate rocks Trace elements:Myers,A.T., 1-64. Zircon, hafnium content and Hf/Zr ratios: Waring, C. L., 1-64. Gas jet for d-c arc:Helz,A.W.,l-64. Mineral and rocks:Helz,A.W.,2-64. Engineering geology General: Benson, M. A., 1-63. Industrial development Surveys and maps: Fennell, E. J., 1-63. Photogrammetry Reservoir planning: Kennedy, Daniel, 1-63. Surveys and maps for industrial growth: Kennedy, Daniel, 2-64. Urban geology:McGill, J.T., 1-64. Eniwetok Atoll Petrology Carbonates and basalt: Schlanger, S. O., 1-63. Erosion Dynamic similarity: Scheidegger, A. E., 2-63. Estuaries Hydraulic geometry: Langbein, W. B., 1-63. Evaporites Boron content:Grimaldi, F.S.,1-63. Faults Bannock thrust zone Idaho, southeastern:Armstrong, F. C., 1-64. Sphenoclastic rifting California, San Andreas fault: Bailey, E. H., 1-64. Strike slip Western United States cordillera: Albers, J. P., 2-64. Flame photometry Releasing-addition method Calcium in thermal waters: Rowe, J. J., 1-63. Floods Distribution and magnitude: Alexander, G. N., 1-64. Florida Areal geology Glades and Hendry Counties: Klein, Howard, 1-64. Economic geology Chicora quadrangle: Cathcart, J. B„ 1-63. Plant City quadrangle: Cathcart, J. B., 2-63. Florida (Continued) Geochemistry Water: Back, William, 1-63. Geomorphology Lake depths, maps: Kenner, W. E., 1-64. Hydrogeology Alachua, Bradford, Clay, and Union Counties: Clark, W.E., 2-64. Biscayne aquifer, Pompano Beach area:Tarver,G.R.,l-64. Brooklyn Lake:Clark,W.E„ 1-63. Dade County:Leach, S.D., 1-63. Data-collection stations: U.S. Geol. Survey, 6-64. Glades and Hendry Counties: Klein, Howard, 1-64. Orange County: Lichtler, W.F., 1- 64. Pasco and Hernando Counties: Wetterhall, W. S., 1-64. Polk County: Stewart, H. G., Jr., 1-63. Saint Johns, Flagler, and Putnam Counties:Kenner, W.E., 1-63. Salt-water leakage, intracoastal waterway: Clark, W.E., 1-64. Snake Creek Canal: Kohout, F. A., 1-64. Water resources: Conover, C. S., 1-63. West-central: Wetterhall,W.S., 2- 64. Maps Melbourne area, aeromagnetic: Dempsey, W. J., 3-63. Pompano Beach area, ground water: U.S. Geol.Survey, 10-63. Paleontology Eocene and Paleocene microfauna: Applin, E. R., 1-64. Petrology Paleozoic sandstones and shales: Carroll, Dorothy, 1-63. Structural geology Panhandle area, deep-lying salt deposits: Marsh.O.T., 1-64. Fluorine Ground water Conterminous United States: Fleischer, Michael, 1-64. Silicic volcanic rocks Western United States: Coats, R. R„ 1-63. Folds Oroclinal Western United States cordillera: Albers, J. P., 2-64. Foraminifera Nomenclature: Todd, Ruth, 1-63. Paleozoic Mineralogy and diagenesis: Henbest, L. G., 1-63. Frost penetration Influence of snow cover:Krinsley, D. B., 1-63. Galapagos Islands Botanical studies:Svenson,H.K, 1-63. Gas chromatography Effluent collector: Goerlitz, D.F., 1-64.A338 Gastropoda Hinkleyia, western United States: Taylor, D. W., 1-63. General Computer programs for geologic research:Miesch,A.T., 3-64. Geologic laws:Bradley,W.H.,3-63. Geologic projection: Wahlstrom, E. E., 1-64. Geology as complex natural ex-periments:McKelvey,V.E„l-63. Open-file reports and maps of U.S. Geological Survey: Weld, B. A., 1-63. Orientation data Mathematical rotation: Noble, D. C., 5-64. Research:U.S.Geologicai Survey, 18-63; 5-64; 7-64; 12-64. Geochemical prospecting Sampling-error effects: Miesch, A. T., 1-64; 4-64. Sampling problems Computer analysis:Miesch,A.T., 2-64. Uranium deposits Flora variations: Shacklette, H. T., 2-64. Utah Rocky Range: Connor, J.J., 1-64. Geochemistry Aqueous solutions: Hem,J.D., 1-63. Carbonate equilibria Natural waters: Roberson.C.E., 1-64. Desert varnish Minor-element content:Lakin, H. W., 1-63. Glauconite, sorption studies: Schnepfe, M. M., 1-64. Ground water Mine drainage:Barnes,Ivan,3-64. Mg and Ca carbonate minerals in natural waters: Hostetler, P. B., 3-63. Nutritional problems: Cannon, H. L., 2-63. Preliminary relations in hydrous Na-Ca borate: Hanshaw, B. B„ 1-63. Rare elements Detection and analysis: May, Irving, 1-64. Soil control of vegetation:Shack-lette, H. T., 1-63; 1-64. Technique Divalent-cation exchange selectivity: Truesdell,A.H.,l-64. Tellurium separated from iron and gold:Thompson,C.E.,l-6 3. Trace elements in fertilizers: Fleischer, Michael, 1-62. Water: Durum, W. H., 1-63. Alkalinity and pH; Barnes, Ivan, 1-64. Carbonate studies:Back,William, 1-63. Zeolitic tuffs, ion-exchange capacity: Starkey, H. C., 1-64. Geodetic surveys Control diagrams: Smart, R.L., 1-64. PUBLICATIONS IN FISCAL YEAR 1964 Geologic maps Technique for coloring:Pomerene, J. B., 1-63. Geologic thermometry Copper arsenides:Skinner, B.J., 1-64. G eomo rphology Alluvial river channels:Schumm, S. A., 1-63. Estuaries Hydraulic geometry: Myrick, R. M., 1-63. River channels and hill slopes Measurement of changes: Miller, J. P., 1-63. Slope theory, lithologic variations: Scheidegger, A. E., 2-64. Statistical mechanics :Scheidegger, A. E., 3-64. Geophysical exploration Book review:Keller,G.V., 2-63. Instrumentation Acoustic velocity meter: Smith, Winchell, 1-64. Geophysical research Controlled quadrature: Roman, Irwin, 1-64. Tables of ascending exponential function ex:Spicer,H.C., 1-63. Tables of descending exponential function e :Spicer,H,D.,3-63. Tables of inverse probability integral P 2//iff B~-B a b: Spicer, H. C.,J2-63. Geophysics Geophysical Abstracts: Clarke, J. W., 1-63 thru 6-63, 1-64 thru 6-64. Georgia Areal geology Bartow County:Croft,M.G.,l-63. Catoosa County: Cressler.C.W., 1-63. Chattooga County: Cressler, C. W., 1-64. Coastal plain: Herrick, S. M., 1- 63; 2-64. Dade County: Croft,M.G., 1-64. Lee and Sumter Counties: Owen, Vaux, Jr., 1-63. Mitchell County, Owen, Vaux, Jr., 2-63. Walker County:Cressler, C.W., 2- 64. Economic geology Fuller's earth and attapulgite: Sever, C. W., 1-64. Engineering geology Underground accumulation of gasoline:McCollum,M.J., 1-63. Geochemistry Crystalline rock: Stewart, J. W., 2-63. Hydrogeology Aquifer contamination, oil-test well: Wait, R. L., 1-63. Atlanta area, emergency water supplies:Stewart, J.W., 1-63. Bainbridge Air Base: Sever, C. W., 1-63. Bartow County: Croft,M.G., 1-63. Catoosa County:Cressler, C.W., 1-63. Georgia (Continued) Hydrogeology (Continued) Chattooga County: Cressler, C. W., 1-64. Crystalline rocks, permeability: Stewart, J. W., 1-64. Dade County: Croft,M.G., 1-64. Ground water quality:Callahan, J. T., 1-63. Iron content of ground water: Joyner, B. F., 1-63. Lee and Sumter Counties: Owen, Vaux, Jr., 1-63. Mitchell County, Owen, Vaux, Jr., 2-63. Salt-water encroachment: Counts, H. B., 1-63; McCollum, M. J., 2-63. Sediment transport: Kennedy, V. C., 1-64. Southwest, solution subsidence of limestone terrane: Herrick, S. M., 3-64. Subsidence due to decline in Artesian pressure: Davis, G. H., 2-63. Walker County: Cressler, C.W., 2-64. Paleontology Foraminifera, Miocene: Herrick, S. M., 1-64. Stratigraphy Suwannee Limestone and Flint River Formation: Vorhis, R. C. , 1-64. Glacial geology Antarctica Thiel Mountains: Andersen,B.G., 1-63. North Dakota Map: Colton, R. B., 7-63. Washington Olympic Peninsula: Crandell, D. R„ 1-64. Glaciers Current research, review:Meier, M. F., 1-63. Glass Dynamic interpretation of constitution: Morey, George, 1-63. Glass, Natural Hydration and devitrification: Friedman, Irving, 2-64. Glossary Stratigraphic terms Paleozoic: Read, C. B., 1-64. Taconic stratigraphic names Definitions and synonyms: Zen, E-an, 2-64. Greenland Areal geology North Star Bay area: Davies, W. E., 1-63. Ground water Aquifers Artificial recharge: Maddox, G. E., 1-64. Curve for analyzing test data; Walton, W. C., 1-63. Multiple-regression analysis: Jenkins, C. T., 3-63. Nonequilibrium formula:Warren, M. A., 1-63.Ground water (Continued) Aquifers (Continued) Permeability: Jacob, C.E., 2-63. Plotting test data: LaRocque, G. A., Jr., 1-63. Sea water in coastal areas: Cooper, H. H., Jr., 1-64. Single-boundary problems: Stallman, R. W„ 2-63. Storage coefficient: Lohman, S. W„ 2-63. Slug injection:Ferris, J.G., 2-63. Transmissibility: Theis,C.V,7-63. Type curves for calculating T/S: Papadopulos, I. S., 1-63. Water-level fluctuations:Ferris, J. G„ 1-63. Artesian-pressure decline: Green, J. H., 1-64. Chemical analyses: Krieger, R.A., 2-63. Coastal aquifers Relation of carbon concentrations to saline-water contamination: Hanshaw, B. B., 1-64. C ontamination Hydrologic factors: Brown, R. H., 1-64. Shallow aquifers: Deutsch, Morris, 1-64. Correction of drawdowns: Jacob, C. E., 1-63. Cyclic discharge Drawdowns: Brown, R.H., 1-63. Depression cone: Brown,R.H,3-63. Diffusion zone: Cooper, H.H.,Jr., 1-63. Drawdown patterns: Lang, S.M., 1-63. Drawdowns Cyclic rates of discharge:Theis, C. V., 3-63. Chart for computing: Theis, C.V., 1- 63. Well discharging under equilibrium conditions: Theis, C.V., 2- 63. Drillers, U.S. Geological Survey relationship to: McGuinness, C. L., 1-64. Flow variability Area of diverse geologic units: Schneider, W. J., 1-63. Geochemistry Chemical equilibrium: Hem, J. D., 3-63. Magnesium and calcium carbonate minerals in natural waters:Hostetler, P. B., 1-63. Instrumentation Television:Callahan, J.T., 2-63. Measurement of temperatures by "lazy" thermometers: Heath, R. C„ 2-64. Movements Flood stages: Cooper, H.H., Jr., 3- 63, 4-63. Rectangular aquifer: Brown,R.H., 2-63. Nonequilibrium formula, slide rule: Theis, C. V., 6-63. Radial flow Leaky aquifer: Cooper, H. H., Jr., 2-63. INDEX TO LIST OF PUBLICATIONS Ground water (Continued) Reverse water-level fluctuations: Andreasen, G. E., 1-63. Review: da Costa, J. A., 1-63. Saline Little used resource: Poole, J. L., 1-63. Tracers Effect of injection method:Ogata, Akio, 1-63. Transmissibility: Jacob,C.E.,3-63. Turbulence in flow:Smith, W. O., 1- 64. Velocity from temperature data: Stallman, R. W., 1-63. Water-level changes Drawdown scales: Conover.C.S., 2- 63. Well spacing: Theis, C.V., 5-63. Wells Jetting method:Moulder, E. A., 3- 63. Guam Geochemistry Volcanic rocks, trace elements: Stark, J. T., 1-63. Paleontology Algae, fossil, Recent: Johnson, J. Harlan, 1-64. Petrology Volcanic rocks:Stark,J.T., 1-63. Gulf Coastal Plain Hydrogeology: LeGr and,H .E., 1 - 64. Paleontology New gastropod genera, Upper Cretaceous:Sohl, N. F., 1-63. Hafnium Zircon Southern California batholith: Gottfried, David, 1-64. Hawaii Earthquakes Underwater nuclear explosion, May 11, 1962: Krivoy, H. L., 1-64. Geochemistry Lead isotopes in volcanic rocks: Tatsumoto, Mitsunobu, 2-64. Geophysical surveys Gravity: Kinoshita.W.T., 1-63. Hydrogeology Floods, 1963: Vaudrey, W. C., 1-63, 1-64. Kohala Mountain and Mauna Kea: Davis, D. A., 2-63. Oahu, Haiku-Kahaluu area: Hirashima, G. T., 1-63. Oahu, southeastern: Visher, F. N., 1-64. Mineralogy Clay minerals: Patterson, S. H., 2-63. Petrology Pillow structures, submarine basalts: Moore, J. G., 1-63. Volcanism Kilauea, 1962 eruption: Moore, J. G., 1-64. Seismic events 1962:Koyanagi, R. Y., 1-64. Volcanology Activity during 1955:MacDonald, G. A., 1-64. A339 Hawaii (Continued) Volcanology (Continued) Kilauea, halogen acids in fum-erolic gases:Murata,K.J.,l-63. Observations during 1960-62: Richter, D. H., 1-63. Heat flow Washington, D. C., area: Diment, W. H., 3-64. Heavy minerals Technique Separation of silt-size minerals: Schoen, Robert, 1-64. Hydraulics Flow and movement: Bentall, Ray, 2-63. Hydrogeology Alluvial channels Depth-discharge relations: Simons, D. B., 1-64. Aquifer tests Flow and movement: Bentall,Ray, 1- 64. Bibliography:Johnson, A.I., 1-64. Coefficient of transmissibility: Skibitzke, H. E., 1-63. Culvert discharge: Jenkins, C.T., 2- 63. Detergent effects on viscosity: Wayman, C. H., 5-63. t Deuterium variation Hydrologic cycle: Friedman, Irving, 3-64. Drainage density Steam flow:Carlston, C.W., 1-63. Drought, humid areas: McCall, J. E., 1-64. Embankment-shaped weirs Discharge characteristics: Kinds-vater, C. E., 1-64. Flow Shear in open-channel: Davidian, Jacob, 1-63. Shear in rectangular channels: Davidian, Jacob, 2-63. Flow-duration curve measurements: Hunt, O. P., 1-63. General:Leopold, L.B., 1-63,1-64; Robinove, C.J., 2-63; U.S. Geological Survey, 14-63, 15-63. Radiation from water surface: Koberg, G. E., 1-64. Uses of water: Skibitzke, H. E., 2-63. Geochemistry of water: Durum, W. H., 1-63. Geophysical logging: Johnson, A. I., 4-63. Ground water Stream-induced fluctuations: Bedinger, M. S., 2-64. Ground water data Methods and techniques: Bentall, Ray, 1-63. Ground water movements Methods and techniques of measurement of movement: Bentall, Ray, 2-63. Ground-water resources:Johnston, P. M., 1-64. Highly permeable environment Surface- and ground-water relation: Sherwood, C. B., 1-64.A340 Hydrogeology (Continued) History: Hackett, O. M., 1-64. Hydrologic bench marks: Wilson, H. D., Jr., 1-63. Hydraulics Flow and movement: Bentall,Ray, 2-63. Industrial use Petroleum industry requirements: Otts, L. E., Jr., 1-63. Instrumentation Altimeter surveying: Newcome, Roy, Jr„ 1-63. Centrifuge moisture equivalent test: McQueen, I. S., 2-63. Crest-stage gages: Frye, P.M., 1-63. Current-meter data analysis: Leve, G. W., 1-64. Current meters:Carter,R.W.,l-63; Colby, B.R., 1-64. Digital computer, streamflow records: Kennedy, E. J., 1-63. Dissolved-oxygen recorder: McCartney, David, 1-63. Field filtering unit: Drake,P.G., 1- 63. High altitude glacial basin, water budget records: Tangborn.W.V., •1-64. Optical current meter: Smith, Winchell, 1-63. Peak-stage gages: Mills, W. B., 2- 63. Rain gages:Musgrove, R.H., 1-63. Rainfall-simulator infiltrometer: McQueen, I. S., 1-63. Streamflow records automated: Carter, R. W., 2-63. Tipping-Bucket rain-gage attachment: Brice, H. D., 1-63. Vehicle for river measurements: Stevens, H. H., Jr., 1-64. Water-level sensing device: Barron, E. G., 1-64. Water-stage recorder: Isherwood, W. L., 1-63. Water-storage recorder:Koopman, F. C., 1-63. International cooperation in scientific hydrology: Nace.R.L., 1-63. Laboratory experiments Lateral turbulent diffusion: Sayre, W. W., 1-63. Specific yield of column drainage: Prill, R. C., 1-64. Lead removal by aquatic organism: Oborn, E. T., 1-63. Limestone aquifers: Swenson, F. A., 1-64. Manganese concentration by aquatic organisms: Oborn,E.T,1-64. Mean annual runoff Areal variations: Hely,A.G.,l-63. Permeability: Johnson, A. I.,2-63, 6-63. Photographic appraisal: Lohman, S. W., 1-64. Prairie potholes: Eisenlohr.W.S., Jr., 1-63. Runoff compilation: Casey, D.J., 1-63. PUBLICATIONS IN FISCAL YEAR 1964 Hydrogeology (Continued) Saline waters Chemistry:Krieger, R.A., 1-63. Sand transport studies: Hubbell, D. W., 1-64. Soil profiles Moisture migration: Miller, R. F., 1-63. Specific yield for various materials: Johnson, A.I., 3-63, 7-63. Streams Dissolved and suspended material: Glover, R. E., 1-64. Surface water Methods and techniques:Barron, E. G., 1-63. Surfactant activity: Wayman, C.H., 1-64. Technique: Dalrymple,Tate,1-64; Johnson, A. I., 1-63; Mesnier, G. N., 1-63. Chart, pumped water from stream: Theis, C. V., 8-63. Determinations of pH, alkalinity, and specific conductance: Roberson, C. E., 1-63. Estimation of bank storage and contribution to streamflow: Rorabaugh, M. I., 1-64. Locus circles:Moulder,E.A.,l-63. Momentary discharge of tide-affected streams: Rantz, S.E., 1-63. Reservoir mass analysis:Riggs, H. C., 1-63. Time- and distance-drawdown graph: May, H. G., 1-63. Unit-graph method: Harbaugh, T. E., 1-63; Mitchell, W. D., 1-63. Water hammer analysis:Streeter, V. L., 1-63. Textbook: Baldwin, H. L., 1-63. Training aids:Johnson,A.I.,5-63. Tritium research: Carlston.C.W., 1-64. Urban development: Waananen, A. O., 1-64. Vegetation dependence on water environment: Van Hylckama, T.E.A., 1-64. Water analysis: Skougstad.M.W., 1-63. Water quality networks: Swenson, H. A., 1-63. Water resource report of U.S. Geological Survey: Worts,G.F., Jr., 3-63. Water supply, abundance:Drescher, W. J., 1-63. Water supply development Streambed percolation:Rorabaugh, M. I., 1-63. World, water: Nace, R. L., 1-64. Iceland Geochemistry Deuterium content: Friedman, Irving, 3-63. Idaho Areal geology Clark Fork quadrangle:Harrison, J. E., 1-63. Idaho (Continued) Areal Geology (Continued) Georgetown Canyon-Snowdrift Mountain area: Cressman, E. R., 1-64. Jarbidge quadrangle: Coats,R.R., 1-64. National Reactor Testing Station: Walker, E. H., 1-64. Geochemistry Minor elements, Phosphoria Formation: Lotspeich, F. B., 1-63. Geomorphology Patterned ground, Snake River Plain: Malde, H. E., 1-64,2-64. Geophysical surveys Gravity and magnetic: Mabey, D. R., 2-64. Hydrogeology Aberdeen-Springfield area: Sisco, H. G., 1-63. Floods, Boise:Thomas,C.A.,l-62. Fort Hall Indian Reservation: West, S. W., 2-63. Midvale and Council areas: Walker, E. H., 2-64. National Reactor Testing Station waste disposal: Jones, P. H., 1-63. Raft River basin: Mundorff, M. J., 1-63. Snake River Plain: Jones,P.H., 1-64. Sodium as tracer: Olmsted,F.H., 1-64. Southeastern: Hadley.R.F., 1-63. Teton Valley:Kilburn, Chabot, 1-63. Weiser River basin, waterpower withdrawals: Colbert,J.L„ 1-64. Maps Garns Mountain NE quadrangle, geologic: Albee, H. F., 1-64. Snake River Plain, geologic: Malde, H. E., 1-63. Thompson Peak quadrangle, geologic:Jobin,D.A., 1-64. Petrology Belt series in Elk River-Clarkia area: Hietanen, Anna, 3-63. Boehls Butte quadrangle,anorthosite and associated rocks: Hietanen, Anna, 1-63. Idaho batholith, Adams and Valley Counties: Schmidt, D. L., 1-64. Idaho batholith, modal composition: Ross, C. P., 2-63. Pierce and Bungalow,batholith: Hietanen, Anna, 2-63. Western, metamorphism in the Riggins region: Hamilton, Warren, 2-63. Stratigraphy Belt Series: Harrison,J.E., 2-63. Graptolite beds, correlation with Nevada: Churkin, Michael,Jr., 1-64. Mississippian, Chesterfield Range: Dutro, J.T., Jr., 3-63. Paleozoic, central: Roberts, R. J., 2-64.'INDEX TO LIST OF PUBLICATIONS A341 Idaho (Continued) Structural geology Bannock thrust zone: Armstrong, F. C., 1-64. Crustal structure from nuclear explosions:Pakiser,L.C., 2-63. Snake River Plain, gravity and crustal structure: Hill, D. P., 2-63. Igneous petrology Silicates Systematic analysis: Peck, L.C., 1-64. Volcanic glasses, volatiles: Ross, C. S., 1-64. Igneous rocks Beryllium: Shawe, D. R., 2-64. Illinois Geochemistry Fluid inclusions, composition, cave-in-rock:Hall, W.E., 1-63. Illinois Hydrogeology Argonne National Laboratory: Knowles, D. B., 1-63. Aurora North quadrangle,floods: Ellis, D. W„ 1-63. Embarrass River basin and Lincoln reservoir site: Watkins, F. A., Jr., 3-64. Elmhurst quadrangle, floods: Ellis, D. W., 2-63. Geneva quadrangle, floods: Noehre, A. W., 2-63. Highland Park quadrangle,floods: Ellis, D. W., 3-63. Hinsdale quadrangle, floods: Ellis. D. W.. 1-64. Harvey quadrangle, floods:Allen, H. E., 1-63. Joliet quadrangle, floods: Allen, H. E., 3-63. Libertyville quadrangle, floods: Noehre, A. W., 1-64. Lombard quadrangle, floods: Allen, H. E., 2-63. Low-flow characteristics of streams: Speer, P. R., 3-64. Naperville quadrangle, floods: Allen, H. E., 2-64. Palatine quadrangle, floods: Allen, H. E., 1-64. Park Ridge quadrangle, floods: Ellis, D. W., 2-64. Wadsworth quadrangle, floods: Noehre, A. W., 1-63. Wheeling quadrangle, floods: Ellis, D. W., 4-63. Inclusions Metastable "superheated" ice in fluid inclusions: Roedder, Edwin, 2-64. Nature of ore-forming fluids: Roedder, Edwin, 1-64. India Hydrogeology Kerala, artesian water: Taylor, G. C., Jr., 1-64. Kutch, Cretaceous sandstone: Taylor, G. C., Jr., 1-63. Indian Ocean Maps Geologic and topographic: Pepper, J. F., 1-63. Indiana Hydrogeology Bunker Hill Air Force Base area: Watkins, F. A., Jr.,3-63. City Creek basin and reservoir site:Watkins,F.A.,Jr., 1-64. Clifty Creek basin and reservoir site: Watkins, F.A., Jr., 1-64. Lake County: Rosenshein, J.S., 1- 64. Lake County, recharge rates of aquifers:Rosenshein,J.S.,l-63. Owen County: Watkins, F. A., Jr., 1-63. Patoka River basin and reservoir site: Watkins,F.A., Jr., 2-64. Porter and La Porte Counties: Rosenshein, J. S., 2-64. Vigo County: Watkins, F. A.,Jr., 2- 63. Iowa Geophysical surveys Central and southwestern, aero-magnetic :Hender son, J.R., 1-63. Hydrogeology Cedar River basin: Schwob.H.H., 1-63. Stratigraphy Ordovician-Silurian contact, Dubuque County: Whitlow,J.W., 1-63. Iron Brazil Minas Gerais:Dorr,J.V.N„2d,l-64. Isostasy Rates of denudation and orogeny: Schumm, S. A., 2-63. Viscosity of earth Pleistocene loading of Lake Bonneville-.Crittenden, M.D., Jr.,3-63. Israel Hydrogeology Carbonate rocks, temperature: Schneider, Robert, 1-64. Paleontology Conodonts and Foraminifera, Triassic: Sohn, I.G., 3-64. Ostracoda, Middle Triassic: Sohn, I. G.,1-63. Italy Petrology Sapphirine-bearing rocks, Valle Codera: Barker, Fred, 3-64. Iwo Jima Geochemistry Lead isotopes in volcanic rocks: Tatsumoto, Mitsunobu, 2-64. Japan Geochemistry Lead isotopes in volcanic rocks: Tatsumoto, Mitsunobu, 2-64. Kansas Areal geology Wallace County:Hodson,W.G.,l-63. Geophysical surveys Basement depths: Watkins, J. S., 3- 64. Southeastern, gravity: Cook.K.L., 1-64. Hydrogeology Cimarron River: Schumm, S. A., 3-63. Grant and Stanton Counties:Fader. S. W., 1-64. Kansas (Continued) Hydrogeology (Continued) Grant and Stanton Counties,water-level changes, 1939-1964: Winslow, J. D., 1-64. Ground-water levels: Broeker, M. E., 1-63. Quality of water: Culbertson, D. M., 1-63. Saline River basin: Jordan, P.R., 2-64. Salt springs and seeps: Ward, P. E., 1-63. Wallace County:Hodson,W.G.,l-63. Walnut River, oil-field-brine pollution: Leonard, R.B., 1-64. Wichita area, floods: Ellis, D.W., 5-63. Wichita area, water resources: Petri, L. R., 1-64. Maps Tri-state mining district, aero-magnetic:Keller, Fred,Jr.,1-63. Stratigraphy Correlations of wells: Adkison, W. L., 1-63. Pleistocene and Pliocene, southwestern: Gutentag, E. D., 1-64. Karst Georgia Southwest: Herrick, S.M., 3-64. Puerto Rico: Monroe,W.H., 3-64. Wyoming, Gros Ventre Mountains: Keefer, W. R., 1-63. Kentucky Areal geology Mississippian Plateau: Lewis, R. Q., Sr., 2-63. Mississippian Plateau, Mammoth Cave and Elizabethtown area: Kepferle, R. C., 1-64. Caves Seasonal temperature fluctuations, Cathedral Cave:Moore,G.W,l-64. Economic geology Strip mining: Musser, J. J., 1-63. Geomorphology Mammoth Cave, fluvial sedimentation: Collier, C. R., 1-64. Geophysical surveys Bluegrass region, gamma-ray logs: Black, D.F.B., 2-64. Hydrogeology Beaver Creek basin, strip mining effect: Collier, C. R., 2-64. Floods, 1957: U.S. Geological Survey, 3-64. Louisville area: Bell, E.A., 1-63. Low-flow characteristics of streams: Speer, P. R., 3-64. Maps Adair, Casey, Clinton, Cumberland, Pulaski, Russell, Taylor, and Wayne Counties-.Lambert, T. W., 1-63. Adolphus quadrangle, geologic: Nelson, W. H., 1-64. Allen Springs quadrangle,geologic: Moore, S. L., 1-63. Ashland quadrangle, geologic: Dobrovolny, E., 1-63. Big Spring quadrangle, geologic: Peterson, W. L., 1-64.A342 Kentucky (Continued) Maps (Continued) Bowling Green North quadrangle, geologic: Shawe, F. R., 1-63. Bowling Green South quadrangle, geologic: Shawe, F. R., 2-63. Breeding quadrangle, geologic: Taylor, A. R., 1-64. Canton quadrangle, geologic: Fox, K. F., Jr., 1-63. Catlettsburg quadrangle .geologic: Dobrovolny, E., 1-63. Cecilia quadrangle, geologic: Kepferle, R. C., 1-63. Clarkson quadrangle, geologic: Glick, E. E., 1-63. Columbia quadrangle, geologic: Lewis, R. Q., Sr., 1-63. Crutchfield quadrangle,geologic: Wilshire, H. G., 1-63. Cumberland Falls quadrangle, geologic: Smith,J.H., 1-63. Dexter quadrangle, geologic: Wolfe, E. W., 1-63. Drake quadrangle, geologic: Moore, S. L., 2-63. Dunmore quadrangle, geologic: Miller, T. P., 1-64. Eddyville quadrangle,geologic: Rogers, W. B., 1-63. Fountain Run quadrangle, geol.: Hamilton, Warren, 1-63. Franklin quadrangle, geologic: Shawe, F. R., 3-63. Gamaliel quadrangle, geologic: Trimble, D. E., 2-63. Gradyville quadrangle, geologic: Taylor, A. R., l“-63. Hadley quadrangle, geologic: Rainey, H. C., 3d, 1-63. Hazel Green quadrangle,geologic: Cashion, W. B„ 1-63. Hazel quadrangle, geologic: Blade, L. V., 1-63. Hawesville and Cloverport areas, geologic and hydrologic: Gallaher, J. T., 1-63. Howe Valley quadrangle,geologic: Kepferle, R. C., 2-63. Kelly quadrangle, geologic: Miller, T. P., 2-64. Kirksey quadrangle, geologic: Wilshire, H. G„ 2-63. Knifley quadrangle, geologic: Maxwell, C. H., 1-64. Lewisport and Owensboro areas, geologic and hydrologic: Gallaher, J. T., 2-63. London quadrangle, geologic: Hatch, N. J., Jr., 1-63. Lynn Grove quadrangle,geologic: Olive, W. W., 1-63. Lucas quadrangle, geologic: Haynes, D. D., 1-63. Madisonville East quadrangle, geologic: Kehn, T.M., 1-63. Meador quadrangle, geologic: Nelson, W. H., 1-63. Middlesboro North quadrangle, geologic: Englund, K.J.,2-64. New Madrid S.E. and Hubbard Lake quadrangles, geologic: Baker, L. N., 1-63. PUBLICATIONS IN FISCAL YEAR 1964 Kentucky (Continued) Maps (Continued) Ohio River between Ethridge and Twelvemile Island,geologic and hydrologic: Price, W.E., Jr., 1-64. Ohio River between Manchester Islands and Silver Grove, geologic and hydrologic: Price, W. E., Jr., 3-64. Ohio River between Newport and Warsaw, geologic and hydrologic: Price, W. E., Jr., 2-64. Ohio River between South Portsmouth and Manchester Islands, geologic and hydrologic: Price, W. E., Jr., 1-63. Olive Hill Clay Bed, structure-contour:Hosterman,J.W., 1-63. Parrot quadrangle, geologic: Crowder, D. F., 1-63. Pellville quadrangle, geologic: Spencer, F. D., 1-63. Philpot quadrangle, geologic: Calvert, R. H., 1-64. Quicksand quadrangle, geologic: Donnell, J. R., 1-63. Rockfield quadrangle, geologic: Rainey, H. C., 3d, 1-64. Salyersville North quadrangle, geologic: Adkison, W.L., 1-64. Shopville quadrangle, geologic: Hatch, N. L., Jr., 1-64. South Union quadrangle,geologic: Klemic, Harry, 1-63. Spottsville and Reed areas, geologic and hydrologic: Gallaher, J. T„ 3-63. Summit quadrangle, geologic: Moore, F. B., 1-64. Tygarts Valley quadrangle,geologic: Sheppard, R. A., 2-64. Tyner quadrangle, geologic: Snyder, G. L., 1-64. Water Valley quadrangle,geologic: Finch, W. I., 1-63. Waterview quadrangle, geologic: Cattermole, J. M., 1-63. Whitley City and Winfield quadrangles, geologic: Pomerene, J. B., 2-64. Wolf Creek and West Point areas, geologic and hydrologic: Gallaher, J. T., 1-64. Woodburn quadrangle,geologic: Shawe, F. R., 4-63. Mineralogy Central mineral districts, para-genesis: Jolly, J.L., 1-64. Central mineral districts,zoning: Jolly, J. L., 2-64. Paleontology Big Bone Lick State Park, esca-vations: Schultz, C. B., 1-63. Foraminifera, Paleocene:Browne, Ruth, 1-63. Stratigraphy Lee Formation, Cumberland Mountains: Englund, K.J., 1-64. Structural geology Cryptoexplosion structures, Versailles: Black,D.F.B.,1-64. Lake Superior Geophysical surveys Seismic: Jackson, W.H. ,1-64. Seismic experiments: Steinhart, J. S., 1-64. Lava flows Direction of flow Eddies in rhyolite: Cummings, David, 1-64. Nevada Rhyolite, Fortymile Canyon: Christiansen, R. L., 2-64. Lead Isotopes Basalts: Tilton, G. R., 1-64. Granites, provincial aspects: Doe, B. R., 2-64. Microline, Llano Uplift, Texas: Zartman, R. E., 1-64. Preparation of samples: Ant-weiler, J. C., 1-63. Reference sample: Delevaux, M. H., 1-63. Variations in growth zoning of galena: Cannon, R. S., 1-63. Volcanic rocks, Japan, Iwo Jima, and Hawaii: Tatsumoto, Mitsunobu, 2-64. Ocean waters and snow: Tatsumoto, Mitsunobu, 1-63, 2-63. Leveling Precision of instrument: Isto, R. E., 1-63. Libya Geomorphology Seif dunes, primary structure: McKee, E. D., 1-64, 2-64. Hydrogeology Agedabia: Jones, J. R., 1-64. A1 Marj area, ground-water exploration: Newport, T.G., 1-63. A1 Mayah area, Tripolitania: Ogilbee, William, 3-64. Azzahra-Annasira-Al Amiria area: Bertaiola, Maria, 1-64. Az Zawiyak area, Tripolitania: Ogilbee, William, 1-63. Ground water resources: Doyel, W. W., 4-64. Sirte area, Tripolitania Ogilbee, William, 1-64. Tarahbulli area, Tripolitania: Ogilbee, William, 2-64. Tripoli area: Cederstron, D. J., 1-64. Tripolitania, decline in ground-water levels: Stuart, W.T., 1-64. Maps Geologic: Conant, L. C.,1-64. Louisiana Hydrogeology Baton Rouge area: Cardwell, G. T., 1-63; Morgan, C. O., 1-64. Chemistry of surface water: Kapustka, S. F., 1-64.Louisiana (Continued) Hydrogeology (Continued) East Feliciana and West Feliciana Parishes: Morgan,C.O., 1-63. Floods: Smith, R. P., 1-64. Floods near Baton Rouge:Camp, J. D., 1-63. Florida Parishes: Winner, M.EI, Jr., 1-63. Lake Charles area, gas and brackish water in fresh-water aquifers: Hodges, A.L., Jr., 1- 63. Measurement of storm runoff: Sloss, Raymond, 1-63. Natchitoches Parish, water resources: Newcome,Roy, Jr., 2- 63. Sabine Parish,water resources: Page, L. V., 2-63. Sabine River basin, surface waters: Hughes, L. S. ,2-64. Southwestern, Chicot aquifer: Whitman, H. M. , 1-63. Sparta Sand: Payne, J. N., 1-64. Spur dikes: Sauer, V. B., 1-63. Water-supply characteristics of streams: Page, L.V.,1-63. Magnesium Complexing with bicarbonate: Hostetler, P. B., 2-63 Magnetic anomalies Electromagnetic survey of: Frischknecht, F. C., 1-64. Polar charts for calculating three-dimensional bodies: Henderson, R. G., 1-64. Magnetic field of the earth Field behavior: Cox, Allan, 3-64. Secular variations in eastern Pacific: Doell, R. R., 1-63. Magnetic properties Antife r romagnetis m UC^^HgO: Pankey, Titus, 1-63. Inhomogeneous laccolith Computer analysis: Henderson, R. G., 2-64. Remanent magnetization Igneous rocks: Doell, R. R., 1-64. Susceptibility Bedded iron-formation: Jahren, C. E., 1-63. Maine Areal geology Presque Isle quadrangle: Boucot, A. J., 1-64. Smyrna Mills quadrangle: Pav-lides, Louis, 1-64. Geochemistry Mapping: Post, E. V., 2-63. Smyrna Mills quadrangle: Pav-lides, Louis, 1-64. Geophysical surveys Gravity: Kane, M. F., 1-64. Hydrogeology Ground-water conditions: Prescott, G. C., Jr., 2-63. Penobscot River basin, wells, springs, and test borings: Prescott, G. C., Jr., 1-64. INDEX TO LIST OF PUBLICATIONS Maine (Continued) Maps Cupsuptic quadrangle, aeromag-netic: Boynton, G. R. 1-64. Danforth area, geologic and aero-magnetic: Griscom, Andrew, 1-63. Danforth quadrangle, geologic: Larrabee, D. M., 2-63. Forest quadrangle, geologic: Larrabee, D. M., 1-64. Grand Lake area, geologic: Larrabee, D. M., 10-64. Kellyland and Vanceboro quadrangles, geologic: Larrabee, D. M., 1-63. Mattawamkeag quadrangle, geologic: Larrabee, D. M., 2-64. Nicatous Lake quadrangle, geologic: Larrabee, D. M., 3-64. Oquossoc quadrangle, aeromag-netic: Boynton, G. R., 2-64. Phillipps quadrangle, aeromag-netic: Boynton, G. R., 3-64. Rangeley quadrangle, aeromag-netic: Boynton, G. R., 4-64. Scraggly Lake quadrangle, geologic: Larrabee, D. M., 5-64. Southeastern, heavy metals in stream sediments: Van Sickle, G. H., 1-64. Southwestern, geologic and hydrologic: Prescott,G.C., Jr., 1-63. Springfield quadrangle, geologic: Larrabee, D. M., 6-64. Squaretown area, geochemical and geologic: Canney,F.C.,3-64, Waite quadrangle, geologic: Larrabee, D. M., 7-64. Wesley quadrangle, geologic: Larrabee, D. M., 4-64. West-central, heavy metals in stream sediment: Post, E. V., 1- 63. Winn quadrangle, geologic: Larrabee, D. M., 8-64. Wytopitlock quadrangle, geologic: Larrabee, D. M., 9-64. Paleontology Caradocian (Middle Ordovician), Ashland: Neuman, R. B., 1-63. Ordovician, Brachiopoda: Neuman, R. B., 1-64. Stratigraphy Kellyland and Vanceboro quadrangles, section: Larrabee, D. M., 1-63. Mammals Desmosty leans Chronologic and geographic range: Mitchell, W. D., Jr., 2- 63. Man, fossil North America: Malde, H.E., 2-63. Manganese , Geochemistry Chemical equilibria affecting behavior in natural water: Hem, J. D., 2-63. Deposition and solution: Hem, J. D., 1-64. Oxidation at contact with feldspar grains: Hem, J. D., 4-63. A343 Mantle Velocities Refraction measurements: Roller, J. C., 1-63. Mapping Special subject maps Technical problems: Gerlach, A. C., 1-64. Maryland Economic geology Copper mining: Pearre, N. C., 1-64. •Engineering geology Greenbelt, joints in clay and slope failure: Withington, C.F., 1-64. Residential construction and sedimentation: Guy, H. P., 1-63. Hydrogeology Allegheny and Washington Counties: Slaughter, T. H., 1-62. Baltimore area: Otton,E.G., 2-64. Harford Furnace area, gabbroic rocks: Otton, E. G., 1-64. Montgomery County: Johnston, P. M., 1-63. Potomac River basin: Wark.J.W., 1-61, 1-63. Salisbury well field, geochemistry of water: Heidel, S.G., 1-63. Maps Beltsville quadrangle, gravel resources: Withington,C.F., 2-64. Western, aeromagnetic: Popenoe, Peter, 13-64. Marine ecology Attached macro-organisms, Patuxent River estuary: Cory, R. L., 1-64. Petrology Potomac River gorge, crystalline rocks: Reed, J.C., Jr., 1-63. Radioactivity Correlation with areal geology: Neuschel, S. K., 1-64. Massachusetts Areal geology Salem quadrangle and vicinity: Toulmin, Priestley,3d, 1-64. Geomorphology Recent sea-level changes,Boston: Kaye, C. A.., 4-64. Geophysical surveys Cape Cod, seismic: Oldale.R.N., 1-64. Glacial geology Boulder train,Paleozoic silicified wood:Kaye,C.A.,l-64, 4-64. Concord, glacial lakes: Koteff, Carl, 1-63. Martha's Vineyard, Pleistocene: Kaye, C. A., 2-64. Hydrogeology Lowell area: Baker,J. A., 1-64. Springfield-Holyoke area: Kam-merer, J. C., 1-63. Well logs and water analysis: Maevsky, Anthony, 1-63. Maps Ashfield quadrangle, aeromagnetic: Meuschke, J. L., 2-63. Ashley Falls quadrangle, materials: Holmes, G. W., 1-64. 746-002 0-64- -23A344 Massachusetts (Continued) Maps (Continued) Bashbish Falls quadrangle, geologic: Hartshorn, J. H., 1-64. Beckett quadrangle, aeromag-netic: Popenoe, Peter, 1-64. Berlin quadrangle, aeromagnet-ic: Popenoe, Peter, 2-64. Bernardston quadrangle, aero-magnetic: Andreasen, G. E., 6-63. Canaan quadrangle, aeromagnet-ic: Popenoe, Peter, 3-64. Cheshire quadrangle, aeromag-netic: Popenoe, Peter, 4-64. Colrain quadrangle, aeromag-netic: Andreasen, G. E., 7-63. Egremont quadrangle, materials: Holmes, G. W., 2-64. Great Barrington quadrangle, materials: Holmes, G.W.,6-64. Greenfield quadrangle, aero-.magnetic: Meuschke,J.L.,3-63. Hancock quadrangle, aeromag-netic: Popenoe, Peter, 5-64. Heath quadrangle; aeromagnet-ic: Popenoe, Peter, 1-63. Hydrogeologic: Knox, C.E.,1-64. Ipswich quadrangle, geologic: Sammel, E. A., 1-63. Millers Falls quadrangle, aero-magnetic: Popenoe,Peter,2-63. Monterey quadrangle,materials: Holmes, G. W„ 4-64. Northfield quadrangle, aeromag-netic: Andreasen, G. E., 8-63. Peru quadrangle, aeromagnetic: Popenoe, Peter, 6-64. Pittsfield East quadrangle,aeromagnetic: Popenoe,Peter,7-64. Pittsfield West quadrangle,aeromagnetic : Popenoe, Peter, 8 - 64. Plainfield quadrangle,aeromagnetic: Meuschke, J. L., 4-63. Howe quadrangle, aeromagnetic: Popenoe, Peter, 3-63. Shelburne Falls quadrangle, aeromagnetic: Meuschke, J.L., 5-63. South Sandisfield quadrangle, materials: Holmes,G.W.,7-64. State Line quadrangle, aeromagnetic: Popenoe, Peter, 9-64. State Line quadrangle,materials: Holmes, G. W., 3-64. Stockbridge quadrangle, aeromagnetic: Popenoe, Peter, 10-64. Stockbridge quadrangle,materials: Holmes, G. W., 5-64. Williamstown quadrangle, aeromagnetic : Popenoe, Peter, 11 - 64. Windsor quadrangle, aeromagnetic: Popenoe,Peter, 12-64. Sedimentation Statistical analyses, Cape Cod sands: Schlee, J. S., 1-64. Stratigraphy Martha's Vineyard,Cretaceous-Recent: Kaye, C. A., 3-64. Stockbridge Limestone: Zen, E-an, 1-64. PUBLICATIONS IN FISCAL YEAR 1964 Mercury California New Almaden: Bailey, E. H.,2-64 Metasomatism Hydrogen Silicate rocks: Jones,W.R., 1-63. Mexico Petrology Zacatecas, plutonic rocks: Rogers, C. L., 1-63. Michigan Areal geology Florence area: Dutton,C.E.,1-64. Economic geology Marquette district and Republic Trough: Gair, J. E., 3-64. Geophysical surveys Marquette iron range and Republic trough, aeromagnetic: Case, J. E„ 1-64. South Haven, gravity: Klasner, J. S„ 1-64. Hydrogeology Alger County: Vanlier, K. E., 2-63. Alma area: Vanlier, K.E., 1-63. Flint area: Wiitala.S.W., 1-63. Ground-water contamination: Deutsch, Morris, 1-63. Ground-water summary: Giroux, P. R., 1-63. Maps Gogebic County, aeromagnetic: Philbin, P. W„ 1-64. Marquette, Dickinson Baraga, Alger and Schoolcraft Counties, aeromagnetic: Balsley, J.R., 1-64. Palmer quadrangle, geologic and magnetic:Gair,J.E.,2-64. White Pine quadrangle, aeromagnetic : Bals ley, J.R., 2 - 64. Stratigraphy Animikie rocks, east of Teal Lake:Fritts, C. E., 1-64. Structural geology Marquette synclinorium: Gair, J. E., 1-64. Mineral deposits, genesis Equilibrium: Barton, P.B., Jr., 2-6 3. Facies and hydrothermal alteration: Hemley, J. J., 1-63. Nature of ore-forming fluids: Roedder, Edwin, 1-64. Mineral descriptions Aksaite: Clark, J. R., 2-64. Bar ne site New hydrated sodium vanadate, Utah: Weeks,Alice D., 1-63. Biotite Synthetic, physical properties: Wones, D. R., 1-63. Calcite Elastic constants: Peselnick, Louis: 1-63. Chlorite Water content: Foster, M. D., 1-64. C linoptilolite :Shepard, A.O., 1- 64. Feldspar X-ray study of composition and structural state: Wright, T. L., 1-64. Mineral descriptions (Continued) Galena Lead isotope variation in growth zoning: Cannon, R.S., 1-63. Goldmanite: Moench.R.H., 1-64. Greigite Thio-spinel of iron: Skinner, B. J., 2-64. Heulandite:Shepard,A.O., 1-64. Leucophosphite Minas Gerais, Brazil:Simmons, G. C., 1-64. Liebigite, synthetic: Meyrowitz, Robert, 1-63. Lithiophorite: Fleischer,Michael, 1-63. Mackina wite :E vans, H.T., Jr., 1-64. Magnioborite probably suanite: Mrose, M. E., 1-63. Manganese oxides Tellurium content: Lakin.H.W., 3-63. Mica Water content:Foster,M.D.,l-64. Northupite, Green River Forma-tion;Milton, Charles, 1-64. Plagioclase:Stewart,D.B., 2-64. Proustite- pyrar gyr ite: Toulmin, Priestley, 3d, 1-63. Pyrite Thermodynamic study:Toulmin, Priestley, 3d, 2-64. Pyrrhotite Thermodynamic study: Toulmin, Priestley, 3d, 2-64. Stishovite Inversion to silica glass:Skinner, B. J., 2-63. Tune Hite Boron-oxygen polyanion in crystal structure: Clark, J. R.,1-63. Uranyl tricarbonate:Meyrowitz, Robert, 2-64. Valleriite: Evans,H.T., Jr., 1-64. Mineral exploration Heavy-mineral reconnaissance: Overstreet, W. C., 3-63. Mineralogy Boron-oxygen polyanion: Clark, J. R., 1-64. Immersion liquids Strong dispersion in low refractive index range: Wilcox, R. E., 1-64. Research at Woods Hole Oceanog. Inst., 1962: Hathaway, J. C., 1-63. Silicates Chain, book review: Stewart, D. B., 1-63. Minnesota Areal geology Camp Ripley Military Reservation: Jones, J. R., 1-63. Elk River nuclear-reactor site: Norvitch, R. F., 1-63. Lyon County: Rodis, H.G.,1-63. Economic geology Iron, Cuyuna North Range: Schmidt, Robert Gordon, 1-63. Geophysical surveys Southeastern, magnetic: Zietz, Isidore, 1-64.INDEX TO LIST QF PUBLICATIONS A345 Minnesota (Continued) Hydrogeology Camp Ripley Military Reservation: Jones, J. R., 1-63. Elk River nuclear-reactor site: Norvitch, R. F., 1-63. Ground-water levels: Staka, G. C„ 1-63. Halma-Lake Bronson area: Schiner, G. R., 1-63. Lyon County: Rodis, H. G., 1-63. Mesabi and Vermilion Iron Range area: Cotter, R. D., 1-63. Quality of water: Maderak.M.L., 1-63. Maps Mesabi Range, bedrock topography: Oakes, E. L., 1-64. Wilkin, Otter Tail, Grant, and Traverse Counties, aeromag-netic: Anderson, L. A., 1-64. Mississippi Hydrogeology Adams, Claiborne, Jefferson,and Warren Counties: Callahan, J. A., 1-64. Aquifer test at West Point: Wasson, B. E., 1-64. Cockfield Formation: Harvey, E. J„ 1-63. Corinth area, water for industry: Newcome, Roy, Jr., 1-64. Floods: Smith, R. P., 1-64. Floods,1959: Humphreys, C. P., Jr., 1-63. Floods, 1960: Wilson,K.V., 1-63. Hinds, Madison, and Rankin Counties: Harvey, E. J., 1-64. Jackson County: Kapustka, S. F., 1-63. Jackson, floods: Shell, J. D., 1-63. Northeastern: Boswell, E. H., 1-63. Observation wells: Ellison, B.E., Jr., 1-63. Salt-water encroachment: Lang, J. W., 1-64. Radioactivity Project Dribble, subsurface natural gamma activity: Bunker, Carl M., 3-63. Stratigraphy Core samples, southeastern: Eargle, D. H., 2-64. Surface and subsurface sequence, southeastern: Eargle,D.H., 1-64. Structural geology Seismic refraction measurements: Healy, J. H., 1-64. Mississippi embayment Areal geology: Cushing,E.M.,l-64. Mississippi Valley Economic geology Clay alteration in lead-zinc district: Heyl, A. V., 2-63. Geochemistry Fluid inclusions, composition: Hall, W. E., 1-63. Mississippian Utah Brachiopods: Gordon, Mackenzie, Jr., 1-64. Missouri Geomorphology Charleston, alluvial fan: Ray, L.L., 1-64. Geophysical surveys Billiken calibration shot: Stauder, W. V., 1-64. Crustal structure, refraction surveys: Stewart, S. W., 1-64. Maps Bauxite, Mississippi embayment, aeromagnetic: Jespersen,Anna, 1-64. Tri-state mining district, aeromagnetic: Keller,Fred, Jr.,1-63. Stratigraphy Mississippi River at St. Louis: Jordan, P. R., 1-64. Mollusca Early history, problems: Yochel-son, E. L., 2-63. Molybdenum Trends in supply: Fischer, R. P., 1-63. Monazite Washington, Spokane County: Hos-terman, J. V/., 1-64. Montana Areal geology Basin quadrangle: Ruppel, E. T., 1-63. Clark Fork quadrangle: Harrison, J. E., 1-63. Fort Peck area: Jensen,F.S.,1-64. Jefferson City quadrangle,geologic: Becraft, G. E„ 1-63. Winnett-Mosby area: Johnson, W. D., Jr., 1-64. Earthquakes August 17, 1959,Hebgen Lake: U.S. Geological Survey, 14-64. Economic geology Missouri River valley:Erdmann, C. E., 1-63. Glacial geology Glacier National Park: Johnson, Arthur, 1-64. Hydrogeology Missoula Valley: Brietkrietz,A„ 1-64. Water resources: Stermitz, Frank, 1-63. Maps Baylor, Larslan West Fork, Police Creek, Kahle, and Lundville quadrangles,geologic: Colton, R. B., 2-64. Belt Series: Ross, C. P., 1-63. Boulder batholith area,geologic: Knopf, Adolph, 1-63. Bozeman Pass quadrangle, geologic: Roberts, A. E., 1-64. Brisbin quadrangle,.geologic: Roberts, A. E., 2-64. Brockton quadrangle,geologic: Colton, R. B., 1-63. Canyon Ferry quadrangle, gravity, aeromagnetic, geologic: Davis, W. E., 1-63. Carbon and Stillwater Counties, geologic: Wanek, A. A., 1-63. Castagne quadrangle, geologic: Smith, H. L., 1-63. Montana (Continued) Maps (Continued) Chelsea quadrangle, geologic: Colton, R. B., 2-63. Chimney Rock quadrangle, geologic: Roberts, A. E., 3-64. East Helena quadrangle, gravity, aeromagnetic, geologic: Davis, W. E., 1-63. Fort Ellis quadrangle, geologic: Roberts, A. E,, 4-64. Hogan 4 NE quadrangle, geologic: Schmidt, Robert George, 1-64. Hoppers quadrangle, geologic: Roberts, A. E., 5-64. Livingston quadrangle, geologic: Roberts, A. E., 6-64. Maxey Ridge quadrangle, geologic: Roberts, A. E., 7-64. Mystic Lake quadrangle,geologic: Roberts, A. E., 8-64. Oswego quadrangle,geologic: Colton, R. B., 3-63. Poplar quadrangle, geologic: Colton, R. B., 4-63. Roberts quadrangle, geologic: Zeller, H. D., 1-63. Roscoe NE quadrangle,geologic: Patterson, E. D., 2-63. Tepee Creek quadrangle, geologic: Witkind, I. J., 1-64. Todd Lakes quadrangle,geologic: Colton, R. B., 5-63. Townsend and Duck Creek Pass quadrangles, gravity, aeromagnetic, and geologic: Kinoshita, W. T„ 1-64. Wolf Point area, construction materials: Colton, R. B., 1-64. Mineralogy Thortveitite, Ravalli County, associated with fluorite: Parker, R. L., 1-63. Paleontology Belt Series: Ross, C. P., 1-63. Petrography Stillwater complex, stratigraoh-ic and lateral variation of chromite composition: Jack -son, E. D., 1-63. Stratigraphy Belt Series: Harrison.J.E.,2-63; Ross, C. P., 1-63. Devonian-Mississippian shale: Sandberg, C. A., 1-6 3. Hogan 4 NE quadrangle, section: Schmidt, Robert George, 1-64. Livingston Group: Roberts, A. E., 1-63. Post-Madison rocks: Dutro, J.T, Jr., 1-63. Mudflows Glacial and fluvioglacial land forms: Fahnestock,R.K.,2-64. Moon Surface Skeletal fuzz: Warren,C.R.,1-63. Natural gases Isotopic and chemical composition: Wasserburg,Gerald J., 1-63.A346 Nebraska Areal geology Richardson County: Emery, P.A„ 1-63. Geomorphology Loup Rivers, channels and terraces: Brice, J. C., 1-64. Geophysical surveys Basement depths: Watkins, J.S., 3-64. Hydrogeology Frenchman Creek basin: Card-well, W. D. E., 1-63. Mirage Flats: Keech, C. F.,1-63. North Loup River: Sayre, W.W., 3-63. Observation wells: Emery.P.A., 1-64. Richardson County: Emery,P.A., 1-63. Saline County: Smith,F.A.,l-64. Salt Creek basin: Kister, L. R., 1-63. Neutron activation analysis Sulfur in water; Wayman, C. H., 1-63. Nevada Areal geology Carson Desert, Lake Lahontan: Morrison, R. B., 1-64. Jarbidge quadrangle: Coats, R. R., 1-64. Lake Mead to Davis Dam: Longwell, C. R., 1-63. Nevada Test Site: Bowers,W.E., 1-64; Davis, R. E., 1-64. Nevada Test Site, Pluto Site: Johnson, R. B., 2-64. Osgood Mountains quadrangle: Hotz, P. E., 1-64. Railroad mining district:Ketner, K. B., 1-63. Timber Mountain caldera, Nevada Test Site: Byers,F.M., Jr., 2-64. Economic geology Barite, Shoshone Range: Ketner, K. B., 2-63. Bullfrog Hills and related ore deposits: Cornwall, H. R.,1-63. North-central, exploration: Roberts, R. J., 1-64. Engineering geology Las Vegas Valley, land subsidence: Malmberg, G. T., 1-64. Geochemistry Roberts thrust near Cortez: Erickson, R. L„ 1-64. Geophysical surveys Las Vegas, crustal structure: Roller, J. C., 1-64. Nevada Test Site, gravity: Healey, D. L., 1-63. Hydrogeology Antelope and Middle Reese River valleys: Crosthwaite.E.G., 1-63. Black Rock Desert area: Sinclair, W. C., 2-63. Churchill County: Everett,D.E., 1-64. Coyote Spring and Kane Spring Valleys: Eakin, T. E., 1-64. PUBLICATIONS IN FISCAL YEAR 1964 Nevada (Continued) Hydrogeology (Continued) Death Valley National Monument Worts, G. F., Jr., 2-63. Dixie-Fairview Valley area: Cohen, Philip, 3-63. Dry Lake and Delamar Valleys: Eakin, T. E., 1-63. Duck Lake Valley: Sinclair, W. C., 1-63. Floods, January-February 1963: Rantz, S. E., 4-63. Fluorine content, movement of ground water: Malmberg.G.T., 2-64. Garden and Coal Valleys:Eakin, T. E., 2-63. Geochemical aspects: Cohen, Philip, 2-64. Humbolt River Valley: Cohen, Philip, 1-63, 1-64. Lake Mead Base: Loeltz.O.J., 1-63. Lake Valley: Rush, F. E., 1-63. Las Vegas Valley and Amargosa Desert: Winograd, I. J., 1-63. Las Vegas Valley, drought effects: Malmberg, G. T., 1-63. Long Valley-Massacre Lake region: Sinclair, W. C., 3-63. Lower Humboldt River basin: Bredehoeft, J. D., 1-63. Muddy River Springs area: Eakin, T. E., 1-64. Nevada Test Site: Schoff.S. L., 1-64. Nevada Test Site, well data: Moore, J. E., 1-63. Pahranagat and Pahroc Valleys: Eakin, T. E., 3-63. Pueblo Valley—Continental Lake region: Sinclair, W. C., 4-63. Southern: Eakin, T. E., 4-63. Water from granitic rocks:Feth, J. H., 1-64. Maps Cane Spring quadrangle, aero-magnetic: Boynton, G. R.,3-63. Eureka County area, gravity: Mabey, D. R., 1-64. Frenchman Flat quadrangle, geologic: Poole, F. G., 1-64. Jackass Flats quadrangle, geologic: McKay, E. J., 1-64. Oak Spring quadrangle,geologic: Barnes, Harley, 1-63. Oxidized zinc districts: Heyl, A. V., 1-64. Painte Range, geologic: Byers, F. M., Jr., 1-64. Paradise Peak quadrangle: Vitaliano, C. J., 1-63. Rainier Mesa quadrangle, geologic: Gibbons, A. B., 1-63. Skull Mountain quadrangle, geologic: Ekren, E. B., 1-64. Timber Mountain quadrangle, aeromagnetic: Boynton,G.R., 1- 63. Tippipah Spring quadrangle, aeromagnetic: Boynton, G. R., 2- 63. Nevada (Continued) Maps (Continued) Tippipah Spring quadrangle, geologic: Orkild, P. P., 1-63. Topopah Spring NW quadrangle, geologic: Christiansen, R. L., 1- 64. Topopah Spring quadrangle, aeromagnetic: Boynton,G. R., 4- 63. Topopah Spring SW quadrangle, geologic: Lipman, P. W., 5-64. Mineralogy Alkali feldspars, X-ray study: O'Connor, J. T., 1-64. Petrology Ash-flow in Piapi Canyon Formation: Lipman, P. W., 4-64. Nevada Test Site, Piapi Canyon Formation, welded tuffs: O'Connor, J. T., 1-63. Nye County, flow structures in welded tuff: Hoover,D.L.,1-64. Rhyolite flow, Fortymile Canyon, emplacement and thermal history: Christiansen, R.L., 2- 64. Siliceous mudstone, Carlin and Pine Valley quadrangles: Ketner, K. B., 3-63. Welded-tuff dike, southern: Lipman, P. W., 1-64. Radioactivity Nevada Test Site, preliminary measurements, reentry tunnel: Bunker, Carl M., 1-63. Nevada Test Site, rock samples: Bunker, Carl M., 2-63, 4-63, 5- 63, 6-63, 7-63. Stratigraphy Alluvium, Quaternary, particle size: Cohen, Philip, 2-63. Graptolite beds, correlation with Idaho: Churkin, Michael, Jr., 1-64. Mississippian, synorogenic sedimentation, Eureka quadrangle: Brew, D. A., 1-64. Nevada Test Site: Hansen, W.R., 1-63. Paleozoic, northern: Roberts, R. J., 2-64. Thirsty Canyon Tuff, Pliocene, Nye and Esmeralda Counties: Noble, D. C., 4-64. Structural geology Crustal section: Eaton, J. P., 1- 63. Crustal structure from nuclear explosions: Pakiser, L. C., 2- 63. Crustal study, Eureka to San Francisco, California: Eaton, J. P., 1-64. Las Vegas, crustal structure: Roller, J. C., 1-64. Schell Creek Range, thrust fault: Drewes, Harald, 1-64. Timber Mountain dome and caldera: Carr, W. J., 1-64. West-central metamorphosed volcanic plagioclase: Noble, D. C., 3-64.INDEX TO LIST QF PUBLICATIONS A347 New England Areal geology Summary of investigations: Page, L. R., 1-63. Geophysical surveys Radioactivity: Popenoe,Peter, 14-64. Hydrogeology Historical floods: Thomson, M. T., 1-64. Maps Geologic, metamorphic zones, and radiometric ages: Goldsmith, Richard, 1-64. New Guinea General Grazing animals and vegetation: Fosberg, F. R., 2-63. Humid tropics: Fosberg,F.R., 1-63. Origin of cocoanut:Fosberg,F.R. 4-64. Plant communities: Fosberg, F. R., 3-63. New Hampshire Maps Mashua-Merrimack area,ground water: Weigle, J. M., 1-63. Northfield quadrangle,aeromag-netic: Andreasen, G.E., 8-63. New Jersey Hydrogeology Atlantic Coastal Plain, chloride concentration in water wells: Seaber, P. R., 1-63. Camden County: Donsky,Ellis, 1-63. Delaware River, quality of water: McCarthy,L.T.,Jr.,1-63. Delaware River region: Hely, A. G., 2-63. Floods, height-frequency relations: Thomas, D. M., 1-64. Floods, Raritan and Millstone Rivers: Thomas, D. M., 2-64. Mercer County: Vecchioli,John, 1-62. Southern, aquifer test: Lang, S. M., 2-63. Southern and Delaware River basin: Hardison, C.H., 2-63. Streams, water quality: George, J. R., 1-63. Surface water supply:McCall, J. E., 1-63. Maps Browns Mills quadrangle,geologic: Minard, J. P„ 1-63. Mount Holly quadrangle,geologic: Minard, J. P., 1-64. Pemberton quadrangle,geologic: Owens, J. P., 1-64. Paleontology Foraminifera, Marshalltown Formation: Mello, J. F., 1-64. Stratigraphy Island Beach State Park,section: Seaber, P. R., 2-63. New Mexico Areal geology Philmont Country: Robinson, G. D., 1-64. Rio Hondo drainage basin: Mourant, W. A., 1-63. New Mexico (Continued) Areal geology (Continued) Sandoval County: Conover,C.S., 3-63. Santa Fe area: Spiegel,Zane, 1-63. White Sands Missile Range area: Weir, J. E., Jr., 1-64. Economic geology Uranium, Ambrosia Lake: Granger, H. C., 2-63. Uranium, Shiprock quadrangle: O'Sullivan, R. B., 1-63. Geochemistry Radium migration, uranium deposits at Ambrosia Lake: Granger, H. C., 1-63. Geophysical surveys Santa Fe area: Spiegel, Zane, 1-63. Hydrogeology Acoma and Laguna Indian Reservations: Dinwiddie, G. A., 3-64. Albuquerque area, quantity of water: Reeder, H. O., 1-63. Dona Ana County: Doty, G. C., 1-63. Elephant Butte Reservoir, effect of seiches and setup on elevation: Haynes,G.L.,Jr., 1-64. Estancia Valley: Smith, R. E., 1-63. Ground water levels, 1962: Bal-lance, W. C., 1-63. Lea County, ground water: Ash, S. R., 1-63. Los Alamos area: Cushman, R. L., 1-64. Lower Mesilla Valley: Leggat, E. R., 1-63. Municipal water supplies: Dinwiddie, G. A., 1-63, 2-64. Navajo Indian Reservation: Stevens, P. R., 1-63. Pecos River, ground-water salvage: Mower, R. W., 1-64. Rattlesnake Springs test drilling, Eddy County: Mourant, W. A., 1-64. Rio Grande: Culbertson, J. K., 1-64; Nordin, C. F., Jr., 2-63, 1-64, 3-64. Rio Hondo drainage basin: Mourant, W. A., 1-63. Rio Puerco, sediment transport parameters: Nordin, C.F.,Jr.', 1-63. Sandoval County: Conover,C.S., 3-63. Santa Fe area: Spiegel, Zane, 1-63. Santa Fe County: Dinwiddie, G. A., 1-64. Tularosa and Hueco Bolsons, drought effects in interior drainage basins: Hood, J. W., 1-63. Water levels, 1963: West.S.W., 1-63. White Sands Missile Range area: Weir, J. E., Jr., 1-64. New Mexico (Continued) Maps Arch Mesa quadrangle, geologic; Moench., R. H., 3-63. Laguna quadrangle, geologic: Moench, R. H., 1-63. Mesa Gigante quadrangle, geologic: Moench, R. H., 4-63. Mesita quadrangle,geologic: Schlee, J. S., 1-63. Moquino quadrangle, geologic: Schlee, J. S., 2-63. Philmont Ranch region,geologic: Wanek, A. A., 1-64. Raton coal field, geologic:Wanek, A. A., 2-63. Seboyeta quadrangle, geologic: Moench, R. H., 2-63. Shiprock quadrangle, geologic, structural: O'Sullivan,R. B., 1-63. Silver City mining region,geologic and aeromagnetic: Jones, W. R., 1-64. Torrance Station 4 NE quadrangle, geologic: Fischer, W. A., 1-64. Mineralogy Goldmanite from Laguna: Moench, R. H., 1-64. Petrology Lake Valley, productive and barren jasperoids: Young, E. J., 1-64. Philmont Country: Robinson, G. D., 1-64. Stratigraphy Philmont Ranch region,sections: Wanek, A. A., 1-64. Upper Cretaceous, Kirtland and Fruitland Formations, San Juan Basin: Fassett, J. E., 1-64. Structural geology San Juan Basin: Baltz,E.H,Jr., 1-64. New York Areal geology Brookhaven National Laboratory area: de Laguna,Wallace, 1-63. Nassau County: Isbister, J., 1-64. New York Nuclear Service Center: Broughton, J. G., 1-64. Penn Yan and Keuka Park quadrangles: Bergin.M. J.,. 1-64. Saratoga County:Mack,F.K„l-64. Suffolk County: Crandell, H.C., 1-63. General Albany, seasonal temperature fluctuations in surficial sand: Heath, R. C., 3-64. Tree growth as precipitation indicator: Schneider, W. J., 1-64. Geomorphology Surficial geology, Elmira-Williamsport region: Denny, C. S., 1-63. Geophysical surveys Gravity:Simmons, N-.G., 1-64.A348 New York (Continued) Geophysical surveys (Continued) Northeastern, gravity and magnetic anomalies: Diment, W.H., 1-64. Radioactivity: Popenoe, Peter, 14-64. Glacial geology Adirondack Mountains, lithology of drift: Denny, C.S., 1-64. Hydrogeology Albany-Schnectady-Troy area, water resources: Halberg, H. N., 1-64. Delaware County: Soren,Julian, 1-63. Ground water: Heath,R.C.,1-63. Huntington -Smithtown area: Lubke, E. R., 1-64. Jamestown area:Crain,L.J, 1-63. Lake Erie-Niagara area-.LaSala, A. M., Jr., 1-64. Long Island, salt-water encroachment: Lusczynski, N. J., 1-64. Montauk Point area, fresh ground water; Perlmutter, N. M., 1-63. Nassau County: Isbister,J., 1-64; Sawyer, R. M., 1-63. Nassau and Queens Counties: Swarzenski, W. V., 1-63. New York Nuclear Service Center: Broughton, J. G., 1-64. Rockland County, streams: Ayer, G. R., 1-63. Saratoga County: Mack, F. K., 1-64. South Farmingdale, cadmium and chromium wastes: Perlmutter, N. M., 2-63. Suffolk County: Crandell, H. C., 1-63; Pluhowski, E. J., 1-63. Maps Bashbish Falls quadrangle, geologic: Hartshorn, J. H., 1-64. Berlin quadrangle, aeromagnetic: Popenoe, Peter, 2-64. Canaan quadrangle, aeromagnetic: Popenoe, Peter, 3-64. Egremont quadrangle, materials: Holmes, G. W., 2-64. Ground water: Heath,R.C.,1-64. Hancock quadrangle, aeromagnetic: Popenoe, Peter, 5-64. Pittsfield West quadrangle, aeromagnetic: Popenoe, Peter, 8-64. State Line quadrangle, aeromagnetic: Popenoe, Peter, 9-64. State Line quadrangle,materials: Holmes, G. W., 3-64. Mineralogy Amphibolites, Adirondack Mountains: Engel, A. E. J., 1-64. Apatite, Adirondack Mountains: Lindberg, M. L., 1-64. Petrology Cortlandt complex, contact effects: Barker, Fred, 1-64. Long Island, sediments: Faust, G. T., 1-63. Stratigraphy Onondaga Limestone: Oliver, W. A., Jr., 1-63. PUBLICATIONS IN FISCAL YEAR 1964 New York (Continued) Structural geology Taconic region, southern: Zen, E-an, 1-63. Newfoundland Sedimentation Bay St. George: Carroll,Dorothy, 3-63. North America Hydrogeology Ground water: Thomas,H.E.,1-64 Paleontology Anthozoa, Rhizophyllum: Oliver, W. A., Jr., 1-64. Early man: Malde, H. E., 2-63. Foraminifera, Eocene, distribution: Cole, W. S., 1-63. Foraminifera, Mississippian, Tournayellinae: Skipp, B.A.L., 1-64. Radioactivity Tritium fallout, 1961 tests in U.S.S.R.: Thatcher,L.L.,1-63. Stratigraphy Silurian-Devonian boundary: Berdan, J. M., 1-64. Structural geology Tectonic map: King, P.B.,4-64. North Carolina Absolute age Little River Series, Albemarle quadrangle: White,A.M., 1-63. Areal geology Great Smoky Mountains: Hadley, J. B., 1-63. Hamme tungsten district:Parker, J. M., 3d, 1-63. Northeastern: Brown, P.M.,1-63. Economic geology Copper: Espenshade, G.H., 1-63. Ore Knob massive sulfide:Kinkel, A. R., 1-63. Geochemistry Harrisburg quadrangle, heavy minerals: Bell,Henry,III, 1-64. Kannapolis quadrangle, heavy minerals: Bell, Henry,III, 1-63. Sulfate and nitrate content of precipitation: Gambell, A. W., 1-63. Geomorphology Intermittent ponds on quartzite ridges: Reed, J. C., Jr., 3-63. Geophysical surveys Albemarle, Denton, Mt.Pleasant and Salisbury quadrangles, gravity: Yuval, Zvi, 1-64. Hydrogeology Cape Hatteras National Seashore Recreational area: Harris, W. H., 1-64. Chemical and physical character of municipal water supplies: Phibbs, E. J., Jr., 1-64. Chemical and physical character of surface waters: Phibbs,E.J., Jr., 2-64. Water-supply, streams: Goddard, G. C., Jr., 1-63. Maps Blowing Rock quadrangle, geologic: Bryant, Bruce, 1-63. Grandfather Mountain window, geologic: Reed, J. C., Jr.,1-64. North Carolina (Continued) Maps (Continued) Lenoir quadrangle, geologic: Reed, J. C., Jr., 2-64. Shelby quadrangle, geologic: Overstreet, W. C., 1-63. Petrology Carolina Slate Belt, lapilli: Sundelius, H. W., 1-63. Shelby quadrangle, heavy minerals in saprolite: Overstreet, W. C., 2-63. Stratigraphy Carolina Slate belt: White,A.M., 1-63. Leonards Cut, Pleistocene section: Reed, J. C., Jr., 4-64. Phosphorite unit, Beaufort County: Kimrey, J. O., 1-63. North Dakota Areal geology Burleigh County: Randich, P.G., 1-64. Stutsman County: Huxel, C. J., Jr., l-63;Winters,H.A„ 1-63. Glacial geology Late Pleistocene drainage: Aronow, Saul, 1-63. Hydrogeology Burleigh County: Randich, P. G., 1-64. Crosby-Mohall area: LaRocque, G. A., Jr., 2-63. Hillsboro area: Jensen, H. M., 1-63. Kidder County: Bradley, Edward, 1-63. Max area, ground water: Armstrong, C. A., 1-63. Stutsman County: Huxel, C. J., Jr., 1-63; Winters, H. A., 1-63. Maps Burleigh County, ground water: Randich, P. G., 2-64. Glacial: Colton, R. B., 7-63. Norway Glacial geology Ullsfjord, chronology: Holmes, G. W., 8-64. Nuclear explosions Effects on rock salt: Dickey,D.D., 1-64. Traveltimes and amplitudes: Ryall, Alan, 1-63, 1-64. Obsidian Viscosity measurement: Shaw, H. R., 1-63, 1-64. Oceanography Specialization of forms Book review: Yochelson, E. L., 1-64. Ohio Areal geology Belmont County: Berryhill, H. L., Jr., 1-63. Economic geology Coal, Belmont County: Berryhill, H. L., Jr., 1-63. Geophysical surveys Great Miami River Valley, seismic: Watkins, J. W., 1-64. Hydrogeology Floods, 1959: U.S. Geological Survey, 4-64.Ohio (Continued) Hydrogeology (Continued) Mad River basin: Cross, W. P., 1-64. Rivers, low-flow frequencies: Cross, W. P., 1-63. Maps Ashland quadrangle, geologic: Dobrovolny, E., 1-63. Eastern, aeromagnetic: Popenoe, Peter, 13-64. Ohio River valley Alluvial history: Ray, L. L., 1-63. Okinawa Paleontology Foraminifera: LeRoy, L. W., 1-64. Oklahoma Areal geology Woodward County: Wood, P. R., 1-63. Geomorphology Sandstone Creek, channel changes: Bergman, D.L.,1-63. Geophysical surveys Northeastern, gravity: Cook, K. L., 1-64. Hydrogeology Chemistry of surface waters: Cummings, T. R., 1-63, 1-64. Floods,magnitude and frequency: Westfall, A. O., 1-64. Ground-water levels in observation wells, 1961-1962: Wood, P. R., 1-64. Kiamchi River basin, surface water: Laine, L. L., 1-63. Little River basin: Westfall, A. O., 1-63. Muddy Boggy River basin: West-fall, A. O., 2-63. Rush Springs Sandstone, Caddo County: Tanaka, H. H., 1-63. Salt springs and seeps: Ward, P. E., 1-63. Washita River, ground water in alluvial deposits: Hart, D. L., Jr., 1-63. Woodward County: Wood, P. R., 1-63. Maps Northeastern, aeromagnetic: Andreasen, G. E., 1-64. Tri-state mining district,aeromagnetic: Keller, Fred, Jr., 1-63. Stratigraphy Chester, Morrow, and Atoka Series: Merewether, E. A., 1-63. Correlations of wells: Adkison, W. L., 1-63. Ontario Botany Buttressed elm: Fosberg,F.R., 9-63. Optical mineralogy Plagioclase determination Five axis universal stage: Noble, D. C., 2-64. Oregon Areal geology Antelope-Ashwood area, emphasizing John Day Formation: Peck, D. L., 1-64. INDEX TO LIST OF PUBLICATIONS Oregon (Continued) Areal geology (Continued) Portland area: Trimble, D. E., 1-63. Umatilla River basin: Hogenson, G. M., 1-64. Upper Grande Ronde River basin: Hampton, E. R., 1-64. Economic geology Nickeliferous laterites: Hotz, P. E., 2-64. Geomorphology Eastern, Officer's cave,pseudokarst: Parker, G. G., 1-64. Hydrogeology Artificial recharge: Price, Don, 1-63. Gross theoretical waterpower: Young, L. L., 2-63. Northern Willamette Valley: Hampton, E. R., 1-63. Orchard sync line, ground water: Newcomb, R. C., 1-63. Pacific slope and lower Columbia River basins, floods: Hulsing, Harry, 1-64. Resources: U.S. Geological Survey, 20-63. Trask River basin: Young,L.L., 3-63. Umatilla River basin: Hogenson, G. M., 1-64. Upper Grande Ronde River basin: Hampton, E. R., 1-64. Paleontology Miocene, Astoria Formation, mollusks: Moore, E. J., 1-63. Petrology Canyon Mountain Complex, mafic magma stem: Thayer, T. P., 1- 63, 1-64. Low-grade mineral facies: Brown, C. E., 1-63. Volcanism Crater Lake, volcanic ash; Powers, H. A., 1-64. Ostracoda Chaikella and Telekia: Sohn, I.G., 2- 63. Ontogeny: Sohn, I. G., 2-64. Review of "Faunes d'Ostracodes": Sohn, I. G., 1-64. Pacific Islands Areal geology Islands of western north: Johnson, C. G., 1-63. Ecology Clipperton Island, biota: Sachet, Marie-Helene, 1-63. General: Fosberg, F. R., 5-63. Island ecosystems: Fosberg, F. R., 7-63, 8-63. Plant dispersal: Fosberg, F. R. , 6-63. Mineralogy Guam, soils: Carroll, Dorothy, 2-63. Rubiacae: Fosberg, F. R., 1-64. Pacific Northwest Hydrogeology Columbia River Basin: Simons, W. D., 1-64. Streamflow: Orem, H.M.,1-63. A349 Pacific Ocean Volcanism Pacific basin, 1920 to 1961: White, D. E., 1-63. Pakistan Economic geology Manganese, Sanjro, Kalat Division: Bogue, R. G., 1-63. Radioactive beach sand, Cox's Bazar:Schmidt, R. G., 1-63. Paleobotany Cretaceous megaspores: Ellis, C. H., 1-64. Nomenclature: Schopf, J. M.,1-63. Paleozoic United States, floral zones and provinces: Read, C. B., 1-64. Spores and pollen of the Potomac Group: Leopold, E. B. ,1-64. Paleomagnetism Field reversals Radiometric ages, Pleistocene: Doell, R. R., 2-64. Polarity epochs:Cox, Allan, 2-63, 3-63. Reversals Radiometric dates: Cox, Allan, 1- 63. Reversals of field: Cox, Allan, 2- 64. Vectors Angular dispersion: Cox, Allan, 1- 64. Paleontology Book review: Whitmore, F. C., Jr., 1-63. General Marine life in geologic past: Witmore, F. C., Jr., 1-63. Orbitolinidae : Douglass, R. C., 2- 64. Paleotemperature Mollusca California, late Miocene: Addicott, W. O., 1-63. Panama Areal geology Canal Zone area:Woodring, W. P., 1-64. Paleontology Canal Zone area:Woodring, W. P., 1-64. Pegmatites Lithium Genesis: Stewart, D.B.,1-64. South Dakota Beecher No. 3-Black Diamond: Redden, J. A. , 1-63. Black Hills: Norton, J. J. ,1-64. Fourmile quadrangle:Redden, J. A., 2-63. Pennsylvania Areal geology Anthracite region: Wood, G. H., Jr., 1-63. Cedar Run quadrangle: Colton, G. W., 2-63. Klingerstown, Valley View, and Lykens quadrangles: Trexler, J. P. , 1-64.A350 Pennsylvania (Continued) Areal geology (Continued) Mercer quadrangle: Poth, C.W., 1-63. Neshannock quadrangle: Carswell, L. D. , 1-63. Economic geology Coal, Beaver County:Patterson, E. D., 1-63. Uranium, Leighton area:Klemic, Harry, 2-63. Geom orphology Surficial geology, Elmira-Williamsport region:Denny, C. S. , 1-63. Hydrogeology Ground-water observation-well program: Poth, C.W., 2-63. Lebanon Valley: Meisler, Harold, 1-63. Mercer quadrangle: Poth, C.W. , 1-63. Mine waters, anthracite fields: Barnes, Ivan, 4-64. Mine-water pools, northern anthracite field: Stuart, W. T. , 1-63. Susquehanna River, chemical character: Anderson, P. W., 1-63. Susquehanna River, quality of water:McCarren, E. F. ,1-64. Hydrology Neshannock quadrangle:Cars -well, L. D. , 1-63. Maps Amity quadrangle, geologic: Berryhill, H. L. , Jr. , 1-64. Susquehanna River Basin:Page, L. V., 3-63. Washington west quadrangle, geologic: Berryhill, H. L. , Jr., 2-64. Western, aeromagnetic: Popenoe, Peter, 13-64. Paleoecology Black shales: Ladd, H. S. , 1-64. Paleontology Anthozoa, Middle Devonian, NaKvkinella:Qliver, W. A., Jr., 2-64. Sedim entation Corey Creek and Elk River basins: Jones, B. L., 1-64. Stratigraphy Catskill Formation: Hoskins, D. M., 1-63. Devonian and Mississippian, north-central: Colton, G. W., 1- 63. Martinsburg formation, Harrisburg area: Platt, L. B., 1-63. Peridotite-gabbro Flow-layering: Thayer, T. P. , 2- 63. Permafrost Alaska Ice wedges: Pewe, T. L., 1-64. Bibliography: Williams, J. R., 1-63. PUBLICATIONS IN FISCAL YEAR 1964 Peru Areal geology, mineralogy, and economic geology Castrovirreyna deposits: Lewis, R. W., Jr., 1-64. Petrogenesis Lithium-rich pegmatites:Stewart, D. B., 1-64. Melting, transformation temperatures: Kracek, F. C., 1-63. Reaction between mafic magma and pelitic schist: Barker, Fred, 2-64. Petrology Experimental at moderate pressures: Wones, D. R. ,2-63. Staining technique: Laniz, R. V., 1-64. Technique Grooved plate, size measurement of elongate minerals: Sargent, K. A., 1-63. Phase equilibria Components, phases, and cri -teria: Zen, E-an, 1-63. Fe-Zn-S: Barton, P. B., Jr., 1-63, 1-64. K2 Mg2 (S04>3 - K2 Ca2 (804)3: Morey, G. W., 2-64. Mineral deposits: Barton, P. B., Jr., 2-63. Sani dine-qua rtz-liquid-gas: Shaw, H. R., 2-63. Sulfide systems Sulfur fugacity: Barton, P. B., Jr., 2-64. Talc with enstatite and quartz: Robie, R. A., 1-64. Photogeology Alaska Chichagof and Kruzof Islands, recognition criteria of igneous and metamorphic rocks: Pomeroy, J. S., 1-64. Infrared Soil-covered structures: Fischer, W. A., 1-63. Photography and imagery:Rob-inove, C. J., 1-63. Photoidentification of horizontal control: Halliday, James, 1-63. Photogramm etry Elevation adjustments:McKenzie, M. L., 1-64. Porosity Multiphase fluids in porous media: Stallman, R.W.,1-64. Tuff: Dickey, D. D., 2-64. Puerto Rico Areal geology Gr&nica-Guayanilla Bay area: Grossman, I. G. , 1-63. Ecology Lagunal: Arnow, Lois, 1-63. Geom orphology Karst topography: Monroe, W. H. , 3-64. Geophysical surveys Puerto Rico, gravity:Brornery, R. W., 1-64. Puerto Rico (Continued) Heat flow Mayaguez area: Diment, W.H., 2-64. Hydrogeology Chemical analyses of surface waters, 1961:Woodard, T. H., 1-64. Water wells: Ward.P. E., 1-64. Landslides North-central:Monroe, W. H., 1- 64. Maps Camuy quadrangle, geologic: Monroe, W. H., 1-63. Geologic: Briggs, R. P. ,1-64. Vega Alta quadrangle, geologic: Monroe, W. H., 2-63. Quebec Areal geology Grenville cross section, Port Cartier to Mt. Reed: Lepp, Henry, 1-63, 2-63. Radioactive waste disposal Deep wells: Drescher, W. J., 2- 63. Sand model: Magness, M. G. ,1-63. Shallow depth Climatic factors: Richardson, R. M., 1-63. Radioactivity Carbon-14 Organic matter in streams: Rosen, A. A., 1-64. Clams and snails Activity in living forms:Rubin, Meyer, 1-63. Radioactivity exploration Gamma-ray transport equation: Sakakura, A.Y., 1-64. Radioelement dispersion Sedimentary environment: Moxham, R.W., 1-64. Radium Determination in water: Barker, F. B., 1-64. Radon Diffusion Synthetic sandstones: Evans, H. B., 1-64. Rhode Island Areal geology Coventry Center quadrangle: Moore, G. E. , Jr., 1-63. Crompton quadrangle, bedrock geology: Quinn, A. W., 1-63. Wickford quadrangle:Williams, R. B. , 1-64. Glacial geology Providence to Point Judith: Schafer, J. P., 1-63. Hydrogeology Ground-water levels, 1960-62: Hansen, A. J. , Jr. , 2-63. Upper Pawcatuck River basin: Allen, W. B., 1-63. Maps Block Island, ground water: Hansen, A. J. , Jr. , 1-63.INDEX TO LIST OF PUBLICATIONS A351 Rhode Island (Continued) Maps (Continued) Narragansett Bay area, geologic: Quinn, A. W. , 1-64. Newport area, geologic:Quinn, A. W., 2-63. Petrology Ashaway quadrangle: Feininger, Tomas, 1-64. Voluntown quadrangle: Feininger, Tomas, 1-64. Westerly Granite: Feininger, T. G., 1-63, 2-63. Rhyolite Phenocrysts Water and deuterium content: Friedman, Irving, 1-64. Viscosity and water content Function of temperature and water pressure: Friedman, Irving, 2-63. Rivers Channel geometry: Langbein, W. B., 1-64, 3-64. Clean-up plan:Whetstone, G. W., 1-63. Profiles: Langbein, W. B., 2-64. Velocity in tide-affected:Craig, F. C., 1-63. Salt Effects of nuclear explosions:. Dickey, D. D., 1-64. Salt deposits Origin: Fleischer, Michael, 2-64. Salt tectonics Colorado Gypsum Valley salt anticline: Cater, F. W., 1-64. Samoa Hydrogeology Ground water reconnaissance: Davis, D. A., 1-63. Sandstones Tuffaceous Chinle Formation, Colorado Plateau: Cadigan, R.A., 1-63. Saudi Arabia Maps Darb Zubaydah quadrangle, geologic: Bramkamp, R. A., 3- 63. Hijaz quadrangle, geologic: Brown, G. F. , 1-63. Jawf-Sakakah quadrangle, geologic: Bramkamp, R.A., 4- 63. Northeastern Hijaz quadrangle: Brown, G. F., 3-63. South central Rub A1 Khali quadrangle, geologic: Ramirez, L. F., 1-63. Southern Hijaz quadrangle, geologic: Brown, G. F., 2-63. Southeastern Rub A1 Khali quadrangle, geologic:Ramirez, L. F., 2-63. Wadi As Sirhan quadrangle, geologic: Bramkamp, R.A., 1-63. Saudi Arabia (Continued) Maps (Continued Western Rub A1 Khali quadrangle, geologic:Bramkamp, R. A., 2-63. Scandium Volcanic rocks:Fryklind, V. C., Jr. 1-63. Sedimentary rocks Density Post-Oligocene rocks:McCulloh, T. H., 1-64. Porosity and bulk density: Manger, G. E., 1-63. Texture: Schlee, J. S., 3-63. Sedimentary structures Bedding, effect of base-level changes: Jopling, A. V., 2-63. Bedding, hydraulic studies: Jopling, A. V., 1-63. Islands and point bars Rio Grande, New Mexico and Texas: Nordin, C. F., Jr., 3-64. Ripple marks:Kennedy, J. F. J.-64. Sedimentation Bed-load transportation:Nordin, C. F., Jr., 2-64. Bolson environment Granule distribution: Lustig, L. K., 2-63. Coarse fractions: Trumbull, J.V.A., 1-63. Concept of sedimentation unit: Jopling, A. V., 1-64. Federal Inter-Agency project: Inter-Agency Sedimentation Project, 1-63. Fluvial Bed-material discharge:Colby, B.R., 3-64. Dispersal of bed sediments: Sayre, W.W. , 2-64. Scour and fill: Colby, B. R. ,4-64. Shear on stream-bed sediments: Colby, B. R., 3-63. Source, transportation and deposition: Colby, B. R., 1-63. Spatial and velocity-weighted sediment concentration: Guy, H. P., 2-64. Storm-period variables: Guy, H. P., 1-64. Transport in erodible channels: Colby, B. R., 2-64. Research in U. S. Geological Survey: Vice, R. B. , 1-64. Salt deposits, origin: Fleischer, Michael, 2-64. Scour and fill: Emmett, W.W. , 1-63. Techniques Sediment discharge computation Colby, B. R., 2-63. Sediments Cobalt content Determination by ammonium citrate: Canney, F. C., 1-64. Sediments (Continued) Compaction Water removal:Meade, R. H., 2-63. Porosity, low-to-moderate overburden: Meade, R.H., 1-63. Seismic exploration Array recordings:Ryall, Alan, 2-64. Refraction Computer processing: Healy, J. H., 2-64. Seismology Earthquake effects: Bonilla, M. G., 2-64. Instrum entation Unmanned ten-day recording system: Hoover, D. B., 1-64. Serpentine Minor elements: Faust, G. T., 2-63. Silica Organic geochemistry: Siever, Raymond, 1-63. Soil mechanics Book review: Kaye, C.A., 1-63. Soils Cobalt content Determination by ammonium citrate: Canney, F. C., 1-64. Heavy metals Citrate soluble: Canney, F. C., 2- 64. Nevada Long Valley: Sinclair, W. C., 3- 63. Soil-water relations:Rubin, Jacob, 1-63. Solid solutions (Zn, Fe) S Electron probe analysis: Adler, Isidore, 1-64. Solubility Dolomite Ground water: Barnes, Ivan, 2-64 Instrum entation Sodium-sensitive glass electrodes: Truesdell, A. H., 2-64. Manganese dioxide in natural waters: Rawson, Jack, 2-63. Silica at 25°C: Fournier, R. O., 1-64; Morey, G. W., 1-64. South Carolina Hydrogeology Salt-water encroachment: Counts, H. B., 1-63; McCollum, M. J., 2-63. Mineralogy Bismuth, Chesterfield County: Mount, Priscilla, 1-63. Paleontology Foraminifera, Miocene: Herrick, S. M., 1-64. South Dakota Areal geology Clifton quadrangle: Cuppels, N. P., 1-63. Fanny Peak quadrangle:Brobst, D. A. , 1-63.A352 South Dakota (Continued) Areal geology (Continued) Fourmile quadrangle: Redden, J. A., 2-63. Economic geology Beecher No. 3-Black Diamond exploration: Redden, J. A., 1-63. Beryllium, Helen Beryl, Elk-horn and Tin Mountain pegmatites: Staatz, M.H., 1-63. Black Hills, pegmatiticmineral deposits: Norton, J. J., 1-64. Pegmatite, South Dakota: Redden, J. A., 1-63. Hydrogeology Skunk Creek-Lake Madison drainage basin: Adolphson, D. G., 1-64. Maps Black Hills, gravity: Hazlewood, R. M. , 1-64. Custer County, aeromagnetic: Meuschke, J. L.; 1-63. Jewel Cave SW quadrangle, geologic: Braddock, W. A. ,1-63. Petrology Calcitization of dolomite, Min-nelusa Formation: Braddock, W.A., 1-63. Heavy minerals, Jurassic and Cretaceous sandstones: Mapel, W. J., 1-64. Stratigraphy Minnelusa Formation, solution breccias: Bowles, C. G., 1-63. Specific gravity Iron-bearing material Alabama, Red Mountain Formation: Sheldon, R. P. , 1-64. Statistics Nonparametric Interpretation of geological data: Lovering, T.G. , 1-63. Stratigraphy Pleistocene-Recent boundary Gulf of Alaska:Smith, P. B. ,1-64. Strength and plasticity Flow and fracture of solids Book review:Robertson, E. C., 1-63. Spectrophotom etry Instrumentation: Shapiro, Leonard, 1-63. Manganese in silicate minerals: Meyrowitz, Robert, 1-64. Strain Rocks and metals: Robertson, E. C., 1-64. Streams Heat dissipation: Messinger, Harry, 1-63. Strontium Isotopes Basalts: Tilton, G. R., 1-64. Sr-87 in crustal evolution: Hedge, Carl E., 1-63. PUBLICATIONS IN FISCAL YEAR 1964 Strontium (Continued) Radiogenic Volcanic lavas: Hedge, C. E., 1- 64. Structural geology General: Anderson, C. A., 1-63. Mathematical rotation of orientation data: Noble, D. C., 1-64. Solution-collapse structures: Wedow, Helmuth, Jr., 1-64. Sudan Hydrogeology Nahud outlier, Nubian Series: Rodis, H. G., 2-63. Sulfur Geochemistry Fugacity in sulfide systems: Barton, P. B., Jr. , 2-64. Surfactants Biodegredation: Wayman, C. H., 3-63, 6-63. Switzerland Mineralogy Paragonite, Zermatt: Zen, E-an, 3-64. Taiwan Absolute age Tananso schist terrane, micas: Yen, T. P., 1-64. Talc Bibliography United States: Merrill, C. W., 2- 63. United States Resources: Chidester, A.H., 1-64. Tectonic stress Analogy with hydraulic fracturing: Scheidegger, A. E. ,1-64. Tectonics Appalachian region: Hadley, J.B. , 1-64. Repeated movements on conjugate faults: Hansen, W. R., 3-64. Tektites Cesium, rubidium, and lithium contents: Annell, Charles, 1-64. Nickel-iron spherules Magnetic properties: Senftle, Frank E. , 1-64. Petrographic and chemical characteristics: Chao, E. C. T., 1-63. Physical properties and gas content: Friedman, Irving, 1-63. Resistivity and viscosity:Senftle, F. E., 2-64. Submicroscopic spherules and color: Thorpe, Arthur N., 1- 64. X-ray fluorescence analysis: Rose, H. J., Jr. , 1-64. Tellurium Marine manganese oxides: Lakin, H. W., 3-63. New sensitive test: Lakin, H. W., 2- 63. Tennessee Areal geology Great Smoky Mountains:Hadley, J. B., 1-63. Great Smoky Mountains,central: King, P. B. , 2-64. Heat flow Drill hole near Oak Ridge: Diment, W. H. , 1-63. Hydrogeology Ground-water levels, 1952-61: Bingham, R. H. , 1-63. Low-flow characteristics of streams: Speer, P. R. , 3-64. Mill Creek, floods: Randolph, W. J. , 1-64. Montgomery County, water wells: Bingham, R. H., 2-64. Springs: Sun, P.-C. P., 1-63. Maps Adolphus quadrangle, geologic: Nelson, W. H., 1-64. Burns quadrangle, geologic: Marcher, M. V., 1-64. Collinwood quadrangle, geologic: Marcher, M. V., 4-63. Dickson quadrangle, geologic: Marcher, M. V., 2-64. Fountain Run quadrangle, geologic: Hamilton, Warren, 1-63. Franklin quadrangle, geologic: Shawe, F. R., 3-63. Negro Hollow quadrangle, geologic: Marcher, M. V., 5-63. Ovilla quadrangle, geologic: Marcher, M. V., 1-63. St. Joseph quadrangle, geologic: Wilson, C. W. , Jr., 1-63. Topsy quadrangle, geologic: Wilson, C. W., Jr., 2-63. Westpoint quadrangle,geologic: Marcher, M. V. , 2-63. Whitten quadrangle, geologic: Marcher, M. V., 3-63. Military geology Tullahoma campaign: Brown, Andrew, 1-63. Mineralogy "Lost" localities: Laurence, R. A., 2-63. Paleontology Flynn Creek cryptoexplosive structures, conodonts: Huddle, J. W. , 1-63. Murray Gap fossil locality: Laurence, R. A. , 1-64. Stratigraphy Murray Shale and Hesse Quartzite, Chilhowee Mountain: Laurence, R. A., 1-63. Post-Knot unconformity, Sequatchie Valley: Milici, R. C. , 1-64. Rome Formation and Conasau-ga Group: Harris, L. D., 1-64. Structural geology Rocky Valley thrust fault, West New Market area: Bumgarner, J. G. , 1-64.INDEX TO LIST OF PUBLICATIONS A353 Tertiary Paleontology Miocene, Astoria Formation, mollusks: Moore, E. J., 1-63. Texas Absolute age Biotites, Llano, Rb-Sr ages: Zartman, Robert E., 1-63. Areal geology Carson and Gray Counties: Mc-Adoo, G. D., 1-64. Hardin County: Baker, E. T., Jr., 1-64. Orange County: Wesselman, J. B., 1-64. Uvalde County: Welder, F. A., 1-64. Economic geology Uranium, helium, Panhandle gas field: Pierce, A. P., 1-64. Geochemistry Castolon area, water quality: Raw son, Jack, 1-63. Lead, microcline, Llano Uplift: Zartman, R. E., 1-64. Hydrogeology Bexar County, ground water: Arnow, Ted, 1-63. Bibliography: Mills, W.B., 1-63. Blanco River, base flow: Buckner, H. D., 1-64. Brazos River Basin:Cronin, J. G., 1-63; Mendieta, H. B. , 1-63. Carson and Gray Counties: Mc-Adoo, G. D., 1-64. Castolon area, water quality: Rawson, Jack, 1-63. Cibolo Creek, base flow: Holland, P. H., 4-64. Dallas area, floods: Gilbert, C. R., 1-63. Dallas area, flooding: Ruggles, F. H., Jr., 1-64. De Witt County: Follett, C. R., 1-64. Drought effects: Thomas, H. E., 6-63. El Paso district: Davis, M.E., 1-64. Floods, magnitude and frequency of peak flows: Patterson, J. L., 1-63. Floods: Smith, R. P., 1-64. Galveston County: Anders, R. B., 1-63. Gonzales County: Shafer, G. H, 1-64. Guadalupe River; base flow: Holland, P. H., 1-64. Guadalupe, San Antonio, and Nueces River basins: Alexander, W. H., 1-63. Gulf Coast region: Wood, L. A., 1-63. Hardin County: Baker, E. T., Jr., 1-64. Texas (Continued) Hydrogeology (Continued) Houston district, analog model study of ground water: Wood, L. A., 1-64. Hubbard Creek watershed, quality of surface waters: Hembree, C. H. , 1-64. Lampasas River, base flow: Mills, W. B., 1-64. LaSalle and McMullen Counties: Harris, H. B., 1-64. Llano River, base flow:Holland, P. H., 3-64. Lower Mesilla Valley: Leggat, E. R., 1-63. Menard County: Baker, R. C., 1-64. Orange County:Wesselman, J. B., 1-64. Pedernales River, base-flow: Holland, P. H., 2-64. Red River, Sulphur River, and Cypress Creek basins:Baker, E. T., Jr., 1-63. Refugio County: Mason, C. C., 1-63. Rio Grande, bed form and flow: Fahnestock, R. K., 1-64. Rio Grande,, storage of sediments: Nordin, C. F., Jr., 3-64. Sabine River basin, surface waters: Hughes, L. S., 2-64. Salt Springs and seeps: Ward, P. E., 1-63. San Antonio, chemical analyses: Garza, Sergio, 1-64. San Antonio, ground-water discharge: Garza, Sergio, 1-63. San Antonio, precipitation and recharge: Garza, Sergio, 2-63. San Antonio River Basin, drainage areas: U. S. Geol. Survey, 7-63. Southern High Plains:Cronin, J. G., 1-64. Surface waters: Hughes, L. S., 1-63, 1-64. Tularosa and Hueco Bolsons, drought effects in interior drainage basins: Hood, J. W., 1-63. Uvalde County: Welder, F.A., 1-64. Victoria and Calhoun Counties: Marvin, R. F., 1-63. Maps Dryden Crossing quadrangle, geologic: Sharps, J. A., 1-64. Georgetown and vicinity, aero-magnetic: Andreasen, G. E., 3-63. Indian Wells quadrangle, geologic: Freeman, V. L., 1-64. Llano uplift, aeromagnetic: Andreasen,G. E., 4-63. Malvado quadrangle, geologic: Sharps, J.A., 1-63. Texas (Continued) Paleontology Amphibrians, Permian, Jones County: Dalquest, W. A., 1-63. Brachiopoda, Permian, Glass Mountains: Cooper, G. A., 1-64. Petrology Pennsylvanian limestone: Terriere, R. T., 1-63. Structural geology Garden Springs area: King, P. B., 3-64. Thailand Economic geology Phu Hin Lek Fai Loei-Chieng-karn area: Jacobson, H. S., 1-63. Thermal properties Plagioclase: Stewart, D. B., 2-64. Therm oluminescence Csl Doped with various activators: Martinez, Prudencio, 1-64. Thorium Washington, Spokane County: Hosterman, J. W., 1-64. Topographic mapping Control traverses: Bentley, L. E., 1- 64. Tritium Ground water Vicinity of underground fusion explosions: Stead, F.W.,1-63. Tuff Density and porosity: Dickey, D. D. , 2-64. Uniform itarianism Earth-Moon system:Lustig, L. K., 2- 64. U.S.S.R. Economic geology Coal production, trends:Averitt, Paul, 1-64. United States Absolute age Midcontinent region, buried basement rocks:Muehlberger, W. R., 1-63. Areal geology Anadarko Basin:MacLachlan, M. E., 1-64. Economic geology Long-range supply of minerals: Kirkemo, Harold, 1-63. Talc, resources:Chidester, A. H., 1-64. Uranium, vein deposits:Walker, G. W., 1-63. Geochemistry Fluorine, ground water: Fleischer, Michael, 1-64. Fluorine in silicic volcanic rocks: Coats, R. R., 1-63. Great Plains, Pierre Shale, cadmium: Tourtelot, H. A., 1-64. Upper Mississippi Valley zinc-lead district, clay mineral alterations: Heyl, A. V., 2-64.A354 United States (Continued) Geochemistry (Continued) Western beryllium and fluorine, silicic volcanic rocks: Grif-fitts, W. R,, 1-63. Geom orphology Meanders, free and incised: Carlston, C. W., 2-64. Rocky Mountains, high level erosion surfaces:Richmond, G. M., 1-63. Geophysical surveys Midcontinent, aeromagnetic: Zietz, Isidore, 2-64. Southern New England, seismic: Holt, R. J., 1-63. Western, crust and upper mantle: Pakiser, L. C., 2-64. Hydrogeology Chemical analyses of surface waters, 1961: Woodard, T. H., 1-64. Colorado River Basin, drought effects: Thomas, H. E., 7-63. Cumberland and Tennessee Rivers: Speer, P. R., 2-64. Delaware River basin, chemical character: Anderson, P. W., 2-63. Drought, 1950's, midcontinent: Nace, R. L., 2-64. Drought effects in basins of interior drainage: Thomas, H. E., 5-63. Eastern, stream-gaging stations: Hardison, C. H. ,1-63. Far Western States, floods in December 1955-January 1956: Hofmann, Walter, 1-63. Federal sources of data:Thom-son, M. T., 2-64. Floods: Barnes, H. H. Jr., 1-63; Benson, M. A. 1-64; Bodhaine, G. L., 2-64; Thomas, C. A., 1-63; U.S. Geol. Survey, 16-63, 17-63, 13-64. Great Basin, surface water: U.S. Geol. Survey, 3-63. Lower Mississippi River basin: Patterson, J. L., 1-64; U.S. Geol. Survey, 12-63. Mississippi embayment:Bos-well, E. H., 2-63. National Water Resources Data Network: U.S. Geol. Survey, 19-63. National water situation:Mc-Guinness, C. L., 1-63. Northern Atlantic Coast, fresh and salty ground water:Upson, J. E., 1-64. Northwest: Hackett, O.M., 1-63. Holmberg, G. D., 1-63; U. S. Geol. Survey, 8-63. Ohio River Basin, surface water: U. S. Geol. Survey, 1-64. Pacific Northwest, economic factor: Bodhaine, G. L., 1-64. PUBLICATIONS IN FISCAL YEAR 1964 United States (Continued) Hydrogeology (Continued) Pacific slope and lower Columbia River basins, floods: Hulsing, Harry, 1-64. Pacific slope, surface water: U.S. Geol. Survey, 5-63. Public water supply: Durfor, C. H., 1-64. River basin distribution: Giusti, E. V., 1-63. Sediment yield of streams: Swenson, H. A., 2-63. Snake River basin: U. S. Geol. Survey, 4-63; Young, L. L., 1- 63. South Atlantic slope, surface water: U.S. Geol. Survey, 2-63. Southeast: Callahan, J.T., 1-64, 2- 64; Kilpatrick, F. A., 1-64; Speer, P. R., 1-64; U.S. Geol. Survey, 9-63. Southwest: Gatewood, J. S., 1-64; Hackett, O. M., 2-63; Irelan, B., 1-64; McDonald, C. C., 1-64; Theis, C. V., 4-63; Thomas, H. E., 3-63. Tennessee River Basins, floods: Speer, P. R., 2-64. Upper Mississippi River Basins and Missouri River Basin, surface water: U. S. Geol. Survey, 13-63. Western, surface water:U. S. Geol. Survey, 11-63, 11-64. Western Gulf of Mexico Basins, surface water: U. S. Geol. Survey, 2-64. Yearly variations in runoff: Busby, M. W., 1-63. Mineralogy Chlorite, sediments off Atlantic Coast: Carroll, Dorothy, 1-64. Paleontology Eocene, eastern Gulf Coast region: MacNeil, F. S., 1-64. Paleozoic, floral zones and provinces:Read, C. B., 1-64. Western, Phosphoria and Park City Formations, and Shedhorn sandstone, paleoecology: Yochelson, E. L. ,1-63. Petrology Cascade Range, Recent pumice: Wilcox, R. E., 2-64. Petrography Lead isotopes in granites: Doe, B. R., 2-64. Stratigraphy Paleozoic, floral zones and provinces: Read, C. B. ,1-64. Structural geology Basin and Range province, crustal structure: Eaton, J. P. ,2-64. Eureka, Nevada, to Boise, Idaho, refraction study:Hill, D. P., 1-63. Jurassic folding and faulting, western cordillera:Albers, J. P., 2-64. United States (Continued) Structural geology (Continued) Southeastern: King, P. B. ,1-64, 5-64. Western, crust and upper mantle: Pakiser, L. C., 1-63, 2-64. Western, crustal study from seismic data: Stuart, D. J. ,1-64. Western, tectonic evolution: Gilluly, James , 1-63. U r anium Carbonate rocks:Bell, K. G., 1-63. Washington, Spokane County: Hosterman, J. W., 1-64. Utah Absolute age Zircon and allanite, Minnesota River Valley and La Sal Mountains: Stern, T.W., 1-64. Areal geology Capitol Reef area: Smith, J. F., Jr., 1-63 Jordan Valley: Marine, I. W., 1-63. Economic geology Oxidized zinc deposits:Heyl, A. V., 1- 63. Phosphate, Dry Bread Hollow: Schell, E. M., 1-6 4. Resources: U.S. Geol. Survey, 9-64. General Test drilling, Sevier River drainage basin: Feltis, R. D., 1-63. Geochemistry Crude oils, composition:Bass, N.W., 1-64. Juab County, beryllium and fluorine, mineralized tuff:Griffitts, W. R., 2-63. Oxygen and carbon isotopes, carbonate ores, Drum Mountains: Lovering, T.S. ,2-63. Rocky Range, prospecting:Con-nor, J. J. , 1-64. Trend analysis:Connor, J. J. , 2- 64. Geom orphology Lake Bonneville, isostatic deformation: Crittenden, M. D., Jr., 1-63. Geothermal gradients East Tintic district: Lovering, T.S., 1-63. Hydrogeology Beaver, Escalante, Cedar City and Parowan Valleys:Sand-berg, G.W., 1-63. Drought in basins of interior drainage:Waite, H. A., 1-63. East Shore area: Smith, R. E., 2-63. Escalante Valley, drought: Nelson, W. B. , 1-63. Great Salt Lake, brines:Hahl, D. C., 1-63, 2-63. Jordan Valley: Marine, I. W., 1-63. Middle Canyon, Oquirrh Mountains: Gates, J. S., 2-63.INDEX TO LIST OF PUBLICATIONS A355 Utah (Continued) Hydrogeology (Continued) Pavant Valley: Mower, R. W., 1-63, 2-63. Price River: Cordova, R. M., 1-64. Resources: U. S. Geol. Survey, 9-64. Sevier Valley: Young, R. A. , 1-63. Tooele County: Gates, J. S. ,3-63. Upper Sevier River drainage basin: Carpenter, C. H., 1-64. Water-level change maps:Arnow, T., 1-64. Water levels, observation wells: Butler, R. G. ,1-63. Weber County: Thomas, H.E., 1-63. Zion National Park:Gates, J. S., 1- 63. Maps Aspen Grove quadrangle, geologic: Baker, A. A., 1-64. Cowboy Pass NE quadrangle, geologic: Hose, R. K., 1-63. Cowboy Pass NW quadrangle, geologic: Hose, R. K., 3-63. Cowboy Pass SE quadrangle, geologic: Hose, R. K., 2-63. Cowboy Pass SW quadrangle, geologic: Hose, R. K., 1-64. Devils Slide quadrangle, geologic: Mullens, T. E. , 1-64. Eureka quadrangle, geologic: Morris, H. T., 1-64. Gandy NE quadrangle, geologic: Hose, R.K., 4-63. Gandy SE quadrangle, geologic: Hose, R.K., 2-64. North-central, aeromagnetic and geologic:Mabey, D.R. , 3-64. Orem quadrangle, geologic: Baker, A.A., 2-64. San Rafael Group, stratigraphic: Wright, J. C., 1-63. Tintic Junction quadrangle, geologic: Morris, H. T. , 2-64. Paleontology Ammonites, Permian aptychi: Closs, Darcy, 1-64. Brachiopods, Mississippian: Gordon, Mackenzie, Jr., 1-64. Stratigraphy Kelvin and Morrison(?formations, corrections: Crittenden, M.D., Jr., 2-63. Permian, Dry Bread Hollow: Schell, E.M., 1-64. Tertiary, upper, Iron County: Averitt, Paul, 1-63. Structural geology Age of grabens: Witkind, I. J., 2- 64. Juab County: Shawe, D. R., 1-64. Vanadium Biogeochemistry: Cannon, H. L., 1-63. Vanadium (Continued) Trends in supply: Fischer, R. P., 1-63. Verm ont Areal geology Missisquoi Valley:Cady, W. M., I- 63. Economic geology Asbestos, Missisquoi Valley: Cady, W.M., 1-63. Maps Berlin quadrangle, aeromagnetic: Popenoe, Peter, 2-64. Bernardston quadrangle, aeromagnetic: Andreasen, G. E., 6-63. Colrain quadrangle, aeromagnetic: Andreasen, G. E., 7-63. Heath quadrangle, aeromagnetic: Popenoe, Peter, 1-63. Northfield quadrangle, aeromagnetic: Andreasen, G. E., 8-63. Rowe quadrangle, aeromagnetic: Popenoe, Peter, 3-63. William stown quadrangle, aeromagnetic: Popenoe, Peter, II- 64. Virgin Islands Hydrogeology Resources: Ward, P. E. ,2-63. Saint Croix: Hendrickson, G. E., 1-63. Virginia Areal geology Hamme tungsten district: Parker, J. M., 3d, 1-63. Economic geology Beryllium, tin deposits, Irish Creek: Lesure, F. G., 1-63. Copper: Espenshade, G. H., 1-63. Geochemistry Sulfate and nitrate content of precipitation:Gambell, A. W., 1-63. Hydrogeology Potomac River basin:Wark, J.W., 1-61,1-63. Rappahannock River basin, discharge-drainage area re-lations:Riggs, H. C., 1-64. Maps Stickleyville quadrangle, geologic: Harris, L. D., 1-63. Petrology Potomac River gorge, crystalline rocks:Reed, J. C., Jr.,1-63. Radioactivity Correlation with areal geology: Neuschel, S. K., 1-64. Stratigraphy Chattanooga Shale, Big Stone Gap: Roen, J. B., 1-64. Little Stone Gap Member of Hinton Formation Mississippian: Miller, 'R. L., 1-64. Wildcat Valley Sandstone, Devonian: Miller, R. L., 2-64. Viscosity Obsidian-H20 High pressures and temperatures: Shaw, H. R., 1-63. Volcanic rocks Welded tuffs Crystal content and chemical composition: Peterson, D. W., 1-63. Volcanology Ash-flow problems:Smith, R. L., 1-63. Fumeroles, hot springs, and hydrothermal alteration:White, D. E., 3-63. Paleovolcanism:Bailey, R. A., 1-63. Resurgent cauldron Relation to granitic ring com -plexes and rhyolitic ash-flow fields: Smith, R. L., 1-64. Washington Areal geology:Crowder, D.F.,1-64, Clark County: Mundorff, M. J., 1-64. Mount Rainier National Park: Fiske, R. S. , 1-63. Geom orphology Lake Tapps quadrangle:Cran-dell, D. R. , 1-63. Paradise debris flow, Mount Rainier: Crandell, D.R.,2-63. Geophysical surveys Dunite, Twin Sisters:Thompson, G. A., 1-64. Glacial geology Olympic Peninsula:Crandell, D. R., 1-64. Hydrogeology Artificial recharge:Price, Don, 1-63. Clark County: Mundorff,M.J., 1-64. Floods, magnitude and fre-quency:Bodhaine, G. L., 2-64. Glacial stream, Mount Rainier: Fahnestock, R. K., 1-63. King County: Luzier, J. E., 1-64. Mount Rainier National Park: Luzier, J. E., 2-64. Puget Sound, ground water contamination: Kimmel, G. E., 1-63. Yakima River basin:Kinnison, H. B. , 1-63. Maps Cumberland quadrangle, geologic: Gower, H. D. ,1-63. Hunters quadrangle, geologic: Campbell, A.B., 1-64. Husum quadrangle, geologic: Sheppard, R.A., 1-64. Mount Rainier National Park: Fiske, R.S., 1-64. Wilmont Creek quadrangle, geologic :Becraft, G E., 1-64. Paleontology Foraminifera, Olympic Peninsula: Rau, W. W., 1-64.A356 Washington (Continued) Petrology Recent pumice and ash, Mount Saint Helens volcano: Mullineaux, D. R., 1-64. Radioactivity Spokane County, thorium and uranium in monazite: Hoster-man, J. W., 1-64. Volcanism Glacier Peak, volcanic ash: Powers, H.A., 1-64. Wells and drill holes Television apparatus: Eddy, J. E., 1-64. West Virginia Geochemistry Cacapon River, effect of leaves on water quality:Slack,K.V.,l-64. Hydrogeology Potomac River basin:Wark, J. W, 1-61, 1-63. Surface and ground water studies: Meyer, Gerald, 1-64. Water resources: Doll, W.L., 1-63. Maps Northern, aeromagnetic: Popenoe, Peter, 13-64. Radioactivity Correlation with areal geology: Neuschel, S. K., 1-64. Williston basin Absolute age Basement rocks:Peterman, Z. E., 1-64. Wisconsin Areal geology Dodgeville quadrangle:Alllng-ham, J.W., 1-63. Florence area: Dutton, C. E., 1-64. Mineral Point quadrangle: Allingham, J.W., 1-63. Platteville quadrangle:Agnew, A. F., 1-63. Rock County:LeRoux, E. F., 1-63. Hydrogeology Green Bay area: Knowles, D. B., 1-64, 3-64. Little Plover River project: Weeks, E. P., 1-63. Milwaukee - Waukesha area: Green, J. H., 2-64. Portage County: Holt, C. L. R., Jr., 1-63. Portage County, hydraulic properties in glacial outwash: Weeks, E. P. , 1-64. Rock County:LeRoux, E. F., 1-63. Selected stream flow characteristics, 1960: Young, K. B., 1-63. Waupaca County, ground water: Berkstresser, C. F., Jr. ,1-64. Waushara County:Summers, W. K., 1-63. Wyoming Areal geology Clifton quadrangle: Cuppels, N. P., 1-63. PUBLICATIONS IN FISCAL YEAR 1964 Wyoming (Continued) Areal geology (Continued) Fanny Peak quadrangle: Brobst, D. A. ,1-63. Fort Laramie area: McGrew, L. W., 1-63. Lyman-Mountain View area: Robinove, C. J., 3-63. Newcastle area:Mapel, W. J., 1-63. Powder River Basin: Sharp, W. N., 1-64. Shotgun Butte area: Keefer,W.R., 1-64. Economic geology Mineral resources: Sheldon, R. P., 1-63. Uranium, Powder River Basin: Sharp, W. N., 1-64. Uranium, Shirley Basin: Harshman, E. N., 1-63. Erosion Rates in grass and forest areas: Walker, E. H. 2-63. Geochemistry Uranium, Shirley Mountains: Love, J. D. , 1-64. Wind River basin, fractionation of uranium isotopes during weathering: Rosholt, J.N., 1-64. Geom orphology Gros Ventre Mountains: Keefer, W. R., 1-63. Geophysical surveys Gravity and magnetic: Mabey, D. R., 2-64. Hydrogeology Devils Tower National Monument: Whitcomb, H.A.,1-64. East of Jackson Lake: McGreevy L. J ., 1-64. Floods, magnitude and frequency: Carter, J. R., 1-63. Lyman-Mountain View area: Robinove, C. J., 3-63. Platte County: Welder, G. E., 1-63. Star Valley:Walker,E. H. , 1-63. Teton Valley: Kilburn, Chabot, 1-63. Maps Bates Creek quadrangle, geologic: Harshman, E. N. , 1-64. Chalk Hills quadrangle, geologic: Harshman, E.N., 2-64. Horse Peak quadrangle, geologic: Harshman, E. N., 3-64. Measel Spring Reservoir quadrangle, geologic: Harshman, E. N., 4-64. Moss Agate Reservoir quadrangle, geologic: Harshman, E. N., 5-64. Mud Springs quadrangle, geologic: Harshman, E.N., 6-64. Sheep Mountain quadrangle, geologic: Rohrer, W. L., 1-64. Squaw Spring quadrangle, geologic: Harshman, E. N., 7-64. Wyoming (Continued) Maps (Continued) Tatman Mountain quadrangle, geologic: Rohrer, W.L. ,2-64. Tepee Creek quadrangle, geologic: Witkind, I. J., 1-64. Teton Glacier: Reed, J. C., Jr. , 3-64. Thermopolis area, geologic: Horn, G. H. , 1-63. Wild Irish Reservoir quadrangle, geologic: Harshman, E. N., 8-64. Mineralogy Ferroan northupite, Green River Formation: Milton, Charles, 1-64. Paleontology Ammonites, Late Cretaceous: Cobban, W. A., 1-63. Fungi, Green River Formation: Bradley, W. H., 1-64. Petrology Calcitization of dolomite, Minne-lusa Formation: Braddock, W. A., 1-63. Grand Teton National Park Pre-cambrian crystalline rocks: Reed, J. C., Jr., 2-63. Heavy minerals, Jurassic and Cretaceous sandstones: Mapel, W. J., 1-64. Northwestern Yellowstone Plateau, rhyolite and basalt: Hamilton, Warren, 4-63. Stratigraphy Devonian-Mississippian shale: Sandberg, C. A., 1-63. Fenton Pass Formation (Pleistocene?), Bighorn Basin: Rohrer, W. L., 1-63. Goose Egg Formation: Maughan, E. K., 1-64. Green River Formation: Culbertson, W. C., 2-64. Minnelusa Formation, solution breccias: Bowles, C.G., 1-63. Mississippian rocks, Laramie Range: Maughan, E.K., 1-63. Permian: Sheldon, R. P., 1-63. Post-Madison rocks: Dutro, J.T., Jr., 1-63. Souris River (?) Formation, Late Devonian, Cottonwood Canyon: Sandberg, C. A., 2-63. Structural geology Reef Creek detachment fault: Pierce, W. G., 1-63. X-ray fluorescence analysis Hematitic iron ores, total iron determination: Niles, W.W.,1-64. Light elements: Rose, H. J. , Jr. , 1-63. Niobate-tantalate ores: Rose.H. J., Jr., 2-63. Rocks and ores: Rose, H. J., 3-63. Tektites: Rose, H. J., Jr. , 1-64. Zinc Basalts, chemical determinations: Rader, L. F., 1-63.INDEX [Some discussions cover more than one page, but only the number of the first page is given. Page numbers in italic refer to the list of investigations in progress (see p. A233- A267). See also Index to List of Publications] ABS, in ground water.......................... A58 Acid mine water, effect on streams............. 58 formation................................ 165 occurrence.............................. 25 Aeromagnetic anomalies, automatic contouring....................................... 153 Aeromagnetic surveys, district................ 113 investigations in progress_______________ 247 Aeroradioactivity surveys, investigations in progress. ...................... 247 Afghanistan, surface water................... 123 water resources. ...................... 267 Age determination. See Geochronology and various methods. Airborne Control (ABC) system, topographic mapping............................ 217 Alabama, coal.................................. 284 cooperating agencies...................... 221 flood studies...................... 66,286,287 geologic mapping.......................... 240 geomorphology.........................191,247 ground water....................... 33,178,260 petroleum and natural gas................. 255 quality of water______________________- 59,256 precipitation__________________________ 256 surface water_____________________________ 251 water resources___________________________ 257 water-temperature studies..--------------- 259 Alaska, beryllium.......................... 10,288 bibliography of literature................ 284 biology................................... 117 coal............................... 16,17,284 construction and terrain problems......... 285 cooperating agencies...................... 221 copper.................................. 286 earthquakes................................ 69 floods................................. 68 geochemical prospecting................... 288 geochemistry and petrology................ 289 geochronology......................... 119,289 geologic history..................... 116,117 geologic mapping..................... 289,240 geomorphology............................. 247 geophysics............................ 117,247 glacial geology.......................118,249 glaciology.............................. 249 gold.................................... 249 ground water................. 43,44,164,194,255 iron_____________________________________ 251 mineral and fuel resources, compilations and topical studies___________ 252 mineralogy............................... 117 nuclear test site....................... 54 oil shale______________________________ 116 paleontology--------------------------- 254 permafrost..__________________________ 194,255 petroleum and natural gas__________ 116,118,255 Alaska—Continued Page petrology............................... A117 quality of water_________________________ 164 quicksilver.............................5,266 sedimentation............................ 258 stratigraphy.................. 115,116,118,259 structural geology................ 117,119,259 surface water............................. 43 surficial and engineering geology________ 285 thorium................................ 269 tin...................................4,5,259 uranium............................... 259 vegetation............................... 260 volcanology.............................. 260 water resources.......................... 261 water use.........................:... 43 waterpower............................... 267 Algae, occurrence and age.................... 140 Alkali and alkaline-earth salt systems _ ..... 288 Amaranth, use in staining feldspar............ 200 Amazon River, measurement of flow............. 123 American Samoa, cooperating agencies.......... 225 water resources.......................... 261 Ammonites, occurrence and age................. 134 Analog models, hydrologic, investigations in progress.......................... 258 in analysis of ground-water flow__________ 42 in study of aquifers..................... 177 Analytical chemistry, investigations in progress.......................... 288 results of investigations________________ 195 See also Spectroscopy. Anhydrite-gypsum equilibria................... 161 Antarctica, geochronology..................... 122 geologic mapping......................... 24O glacial geology.......................... 249 glaciology............................... 121 meteorite------------------------------- 121 paleobotany-............................. 122 paleontology--------------------------- 264 petrology-............................... 122 relief model_____________________________ 215 stratigraphy............................. 121 topographic, mapping..................215,217 Antifouling, experiments in salt water________ 205 Antimony, in fern bush______________________ 201 Apatite, rare-earth, crystallography.......... 159 Appalachian region, geology and geophysics.. 81 Aquifers, artificial recharge, district studies.. 46 artificial recharge, investigations in progress.......................... 288 compaction______________________________ 63 contamination___________________________58,59 effects of nuclear explosions___________ 285 gas content...-------------------------- 164 mechanics.............................. 249 salt-water encroachment___________ 23,28,33,164 Arctic, geophysics--------------------------- 247 Arctic Ocean, geothermal studies______________ 151 Page Argentina, cryptoexplosion structures........ A143 Argon, occurrence in water well............... 40 Arid lands, soil moisture..................... 258 Arizona, asbestos............................ 288 coal______________________________________ 284 cooperating agencies...................... 221 copper................................... 236 evapotranspiration........................ 286 floods................................. 67,287 geochemical prospecting................... 288 geochemistry............................ 170 geologic mapping......................101,240 geomorphology......................... 108,247 geophysics!............................... 247 ground water........................... 40,43 land subsidence___________________________ 64 lead and zinc............................. 251 manganese................................... 5 meteorology............................. 204 mineralogy................................ 106 paleontology__________________________ 100,254 petroleum and natural gas................. 255 plant ecology.........................191,192 quality of water___________________________ 40 rockfall-impact studies.................. 143 sedimentation............................. 259 stratigraphy__________________ 100,104,106,269 structural geology....................104,106 surface water_________________________ 40,43 uranium................................... 269 water resources..................... 261 waterpower.............................- 267 Arkansas, artificial recharge.............. 288 barite________________-.................. 288 coal...................................... 284 cooperating agencies...................... 221 floods................................. 67,287 geologic mapping........................ 241 ground water............................ 34 hydrology_______________________________ 250 low-flow studies................-......- 252 paleontology.......................... 132,254 petroleum and natural gas----------------- 255 quality of water.......................... 288 sedimentation.............................. 34 stratigraphy.............................. 258 structural geology......................... 88 surface water.............................. 34 water resources___________________________ 261 water-temperature studies................ 259 Arkansas River basin, sedimentation studies, investigations in progress________ 257 Artificial recharge. See Aquifers, Artificial recharge. Arsenazo-III for thorium determination............ 195 Arsenic, in ground water....................61,165 Asbestos, investigations in progress......... 288 A357A358 INDEX Page Astrogeological studies. See Extraterrestrial studies. Astronauts, geologic-training program......... A236 Atlantic Coast, paleontology..................... 254 See also names of States. Atlantic Coastal Plain, ground water............. 249 stratigraphy and structure...............- 73,258 Atlas, Sino-Soviet terrain....................... 235 Atomic energy. See Nuclear energy, Radioactive materials, and subjects following these topics; Salt deposits. B Barite, district studies........................ 13 investigations in progress................ 233 Basalt, submarine, petrology................... 167 Base metals, investigations in progress...... 249 See also base-metals names. Basement rocks, age determinations............. 168 Bauxite, district studies..................... 11 investigations in progress................ 233 Bed forms................................... 187 Beryl, chemical composition.................... 197 Beryllium, content in volcanic rock............. 10 district studies........................ 8,52 investigations in progress........... 233,238 Bibliographies and abstracts, investigations in progress........................... 234 Bilby, Project, investigations in progress... 235 Biological studies, aquatic attachment organisms_________________........___-____-________ 140 effect of uranium on blueberries.......... 201 iodine in Spanish-moss.................... 200 mineralization of blood vessels........... 199 Biotite, physical and chemical properties____ 157 Black Hills, geologic studies................ 94 Black shale, minor elements.................. 238 Blood vessels, mineralization. .............. 199 Blueberries, effect of uranium deposits on... 201 Bolivia, investigations in progress............ 237 Boltwoodite, crystallography................... 159 Borates, crystal chemistry..................... 252 district studies......................... 12 investigations in progress................ 234 Boron, accumulation by phreatophytes......... 183 Botanical exploration, investigations in progress........................... 238 results of investigations................. 200 Bottom sediments, continental shelf............ 138 Bouguer anom alies.............................. 91 Brachiopods, evolution......................... 135 investigations in progress............ 253,254 occurrence and age......................... 76 use in defining Mississippian series.... 132 wall structure..........................131,132 Brazil, investigations in progress............. 237 mineral deposits.......................... 123 surface water............................. 123 water resources------------------------- 267 Brine, contaminant of ground water.............. 59 district studies........................... 12 isotopic composition...................... 171 Bromine, X-ray fluorescence determination.._ 198 Bryozoans, investigations in progress.......... 253 occurrence and age........................ 131 wall structure____________________________ 132 Bubbler method, evaporation suppression______ 65 Buddingtonite, occurrence...................... 158 c 156 152 Cadmium, occurrence_______ Calcite, elastic properties. See also Index to List of Publications Page California, borates.......................... A234 brines and evaporites______________________ 12 chromite.................................. 236 coal______________________________________ 234 construction and terrain problems...... 62,235 cooperating agencies...................... 221 evaporation studies_______________________ 236 evaporation suppression____________________ 65 flood studies............................. 237 geochemistry............... 155,161,171,238,239 geochronology....................... 112,113,114 geologic mapping............... 102,103,113,241 geomorphology..........................191,247 geophysics............. 112,113,114,153,247,248 glacial geology........................... 249 glaciology................................ 194 ground water............... 46,48,176,250,258 hydraulics................................ 249 hydrology................................. 249 lake deposits, geochemistry............... 165 land subsidence..................... 63,64,261 lead and zinc___________________________ 251 mineralogy________________________________ 199 nickel.................................... 236 nuclear-powerplant site.................... 57 paleontology............... 114,133,137,138,254 petroleum and natural gas_________________ 255 petrology___________________________ 154,155,239 phosphate............................... 7,255 quality of water............... 47,190,238,256 quicksilver_______________________________ 267 saline-water resources................... 48 salmon____________________________________ 175 sea-water intrusion_____________________ 47,58 sediemntation__________________ 184,267,268,259 Stratigraphy........... 101,103,107,113,114,259 structural geology..................112,114,269 sulfide deposits........................ 112 surface water___________________________ 46,176 thermal water............................. 156 tungsten.................................. 236 urban geology............................. 260 volcanism..............................113,114 water resources-------------------------- 261 waterpower________________________________ 267 zeolites.................................. 261 Carbon, organic, determination in water..... 202 Carbon dioxide, activity in salt lake......... 161 occurrence in water well------------------- 40 Carbon-14 analysis, investigations in progress. 239 sample preparation........................ 166 use in geochronology...................... 169 Carbonate rock, sites for nuclear experiments. 235 Carbonates, relation of interplanar spacing to composition....................... 159 Car rib bean area, paleontology............... 264 Cartography, research and development------- 219 Caves, paleohydrologic study.................. 191 sedimentation............................. 187 Cenosite, occurrence........................ 15,159 Central America, paleoecology................. 253 Central United States, aeromagnetic surveys. 247 Centrifuge, use in mineral separations-------- 200 Cephalopods, evolution........................ 136 investigations in progress................ 263 occurrence and age------------------------ 133 See also Ammonites. Cesium, determination in tektites............. 145 Cesium iodide, luminescence------------------- 153 Channel flow, factors affecting............... 174 chariot, Project, geologic and hydrologic studies............................ 54 Project, hydrology........................ 253 chariot—continued Page Project, investigations in progress.... A235 Charophytes, occurrence and age________________ 73 Chi-squared method, in rating of analysts_________ 195 Chile, ground water........................... 126 investigations in progress............... 237 Chitinozoans, investigations in progress.... 253 Chlorine, X-ray fluorescence determination... 198 Chromatography, gas, new effluent collector.. 202 Chromite, district studies...................3,128 investigations in progress............... 239 See also Ferro-alloy metals. Clay-water relations, investigations in progress. 234 Clays, district studies..................... 11,61 effect of heat on glycolation............ 159 investigations in progress............... 234 use in making membrane electrode............. 195 water movement in....................... 177 Clay mineralogy, relation to depositional environment........................ 75 Coal, district studies...............15,100,128 investigations in progress... 234,241,242,244,245 mine bumps............................. 62,236 mines, formation of acid water........... 165 minor-element content.................... 234 Coal-ball studies............................. 253 Cobalt, citrate-soluble, use in prospecting... 201 Coesite, physical chemistry................... 142 Coffinite, magnetic susceptibility............ 154 Colombia, investigations in progress.......... 237 mineral resources..................... 126 Colorado, base metals......................... 233 beryllium...............................9,234 coal..............................16,234 construction and terrain problems. 62,235 cooperating agencies..................... 222 copper.......................1......... 236 evaporites________________________________ 13 evapotranspiration studies............... 182 fluorspar..............................10,237 geochemistry________________________ 154,155,239 geochronology...........................95,97 geologic mapping.................. 101,240,241 geomorphology..................... 98,191 geophysics...................... 99,247,248 gold..................................... 249 ground water______________________________ 39 lead and zinc.._________________________ 4,251 mineralogy.....................94,101,171,199 niobium........................... 15,253 oil shale....................... 17,18,253 paleontology......................96,100 petroleum and natural gas................ 255 petrology............... 94,97,98,154,155,239 potash-------------------------------- 256 rare earths............................... 15 saline minerals__________________________ 257 sedimentation____________________ 257,258,259 soil moisture............................ 258 stratigraphy................. 95,96,97,100,269 structural geology......................94,95 thermal springs.......................... 164 thorium______________________-.........15,259 uranium.................................. 259 urban geology............................ 260 vanadium................................. 260 waterpower_______________________________ 267 Colorado Plateau, clay........................ 234 geologic mapping......................... 239 geomorphology............................ 191 heavy-mineral trends..................... 187 geophysics, regional..................... 247 stratigraphy and sedimentation........... 258 uranium.................................. 259INDEX A359 Page Colorado River basin, hydrology.............. A261 surface water........................... 42 Colorimetric analysis, determination of metal in stream sediment.................. 200 new equipment.........-................ 162 Columbia River basin, radioactive-waste disposal_____________________________ 55 sedimentation............................ 185,263 Compaction, caused by earthquake................. 70 relation to ground water.................... 63 Compaction recorders, use in subsidence areas. 64,65 Computers, use, contouring permeability data................................ 202 use, making mineralogical calculations... 156 processing stream data................. 202 processing water-quality data.......... 205 study of sampling methods.............. 163 See also Data processing. Connecticut, cooperating agencies............... 222 geochemistry............................... 239 geochronology.............................. 169 geologic mapping........................... 242 glacial geology........................... 80 ground water................................ 22 hydrology................................... Ml nuclear-powerplant site studies_____________ 57 petrology..............................80, 239 quality of water............................ 22 surface water............................... 22 water resources.......................... M2 Connecticut River basin, hydrology.............. 261 Conodonts, investigations in progress........... 262 occurrence and age.....................82.136 Construction and terrain problems, investigations in progress............................... 235 results of investigations.................. 61 See also under names of States. Contamination, water, investigations in progress........................- 23 4 water, results of investigations............ 57 See also Detergents, Radioactive-waste disposal. Continental Shelf, Atlantic, geochemistry___ 238 Atlantic, hydrology----------------------- 238 results of investigations.............. 138 Continental shelves, petroleum and natural gas_______________________________ 265 Contouring, aeromagnetic anomalies............ 153 permeability data......................... 204 Cooler-humidifier, for centrifuge moisture- equivalent test..................... 204 Copper, chemistry..........................146,171 district studies.......................3,108 geochemical anomaly......................... 77 investigations in progress............... 236 ore controls............................... 119 Copper ore minerals, inversion relations............ 161 Corals, classification and evolution.......134,135 investigations in progress............. 263,251, occurrence and age............... 83,100,104,133 use in defining the Mississippian__________ 132 Cordierite, occurrence.......................... 94 Costa Rica, geophysics......................... 247 investigations in progress................. 237 volcanology.......................... 126,260 Cratering, impact and thermal investigations. terrestrial phenomena...................... 236 Craters, lunar_____________________________142,143 terrestrial, experiments__________________ 147 occurrence...................... 143,147 Crust and upper mantle, geophysical studies, investigations in progress__________ 247 geophysical studies, results of investigations. 149 See also Index to List of Publications Page Crustal evolution, isotope studies............ A172 Crustal studies. See Geophysics, regional. Cryptoexplosion structures, occurrence.. 85,142,143 Crystal chemistry, results of investigations... 156 Crystalline rocks, water movement in........... 177 Cu-Ag-S system, phase equilibria................. 6 Cu-S system, phase equilibria.................... 5 Current meters, water, accuracy of measurements.......................................... 203 Cylic deposition, occurrence................73,103 D Dahomey, investigations in progress............ 237 Dams, effect on yield of wells................. 180 upstream effect on sedimentation.......... 186 Data collection and processing, hydrology, investigations in progress......... 251 Data processing, seismic records.............. 150 See also Computers, Geologic data. Delaware, cooperating agencies................. 222 paleontology............................... 74 quality of water.......................... 256 Delaware River basin, low-flow relations.... 175 Delrioite, crystallography..................... 159 Density currents, vertical, in lakes........... 188 Deposition studies............................. 186 Desmostybans, occurrence and age............... 136 Detergents, investigations in progress......... 236 occurrence in water supplies.............. 58 See also ABS. Deuterium, occurrence.......................... 170 Diatoms, studies_________________________ 253,251 use in correlation and paleoecology.... 137 Differentiation, basaltic lava................. 167 District of Columbia, construction and terrain problems.......................... 61 cooperating agencies...................... 222 geologic mapping......................... 11,2 geophysics............................... 21,8 geothermal studies...................... 151 urban geology............................. 260 dogsled, Project, geologic studies.............. 53 Project, investigations in progress....... 236 “Down-structure” method of tectonic analysis........................................... 106 dribble, Project, geologic and hydrologic studies...........................55,61 Drift, Glacial. See Glacial drift. Dunes, large-scale study....................... 186 E Earthquakes, Alaska............................ 69 effect on water levels.................... 178 Eastern United States, paleontology___________ 251, See also Northeastern United States, Southeastern United States, and names of individual States. Effluent collector, for gas chromatography__ 202 Elasticity, modulus of, measurement............. 63 Electrical resistivity, tektites.------------- 147 Electrode, glass, for water study........... 202,203 Electron diffraction powder studies____________ 157 Electron microprobe studies, metals in meteorites.......................................... 146 summary.................................. 199 Elements, relation to health.................. 21,9 See also Minor elements. Engineering geology. See construction and terrain problems; Urban geology. Engineering hydrology. See Land subsidence, Evaporation-suppression studies, Floods. Page Erosion, dated by tree-ring counts........... A100 rates and processes..................... 184,191 Estuaries, biological study, Maryland.......... 140 Evaporation-suppression studies, results of investigations....................... 65 Evaporite-mineral equilibria................... 238 Evaporites, district studies..................... 12 Evapotranspiration, investigations in progress.......................................... 236 results of investigations...............45,181 Extraterrestrial studies, investigations in progress.......................... 236 lunar, dust clouds........................ 149 experiments___________________________ 236 mapping and terrain studies____________ 140, 147,148,235,236 microphotometer data.................... 149 materials.................................. 144 F Fe-Zn-S system, phase equilibria.................. 5 Feldspar, new staining technique............... 200 X-ray study............................... 157 Fern bush, antimony content.................... 201 Ferris Wheel, Project, investigations in progress........................ 235,236 Ferro-alloy metals, investigations in progress. Fischer assay, use in shale study............... 156 Fish, fossil, occurrence and age................ 93 Fish eggs, effect of sediment__________________ 186 Flame photometry, oxygen-sheathed burner.. 195 Floods, areal studies, investigations in progress............................................ 137 areal studies. See also under names of Slates. characteristics, investigations in progress. 236 discharge, investigations in progress___ 237 district studies.......................... 65 effect on trees........................ 192 frequency, investigations in progress... 237 results of investigations................ 68 inundation mapping, investigations in progress........................ 237 urban area............................... 69 severe, 1963-64........................... 65 Florida, clay.................................. 231, cooperating agencies.................... 222 evaporation studies.....................181,236 flood studies........................... 236 geochemistry............................. 17 geologic mapping....................... 21,2 ground water............. 27,28,164,178,179,180 hydrology............................... 21,9 paleontology.......................... 75,261, petroleum and natural gas.................. 255 phosphate-.............................. 255 quality of water................... 28,164,239 sea-water intrusion....................... 257 surface water......................... 27,28,179 water resources......................... 262 Fluid inclusions, composition.................. 170 investigations in progress................ 238 occurrence and composition.............. 162 Flume studies, bedforms...................... 187 velocity and sediment concentration....... 184 Fluoride, occurrence in ground water.........61,164 Fluorine, content in volcanic glass.......... 163 determination in silicate rocks......... 195 Fluorspar, district studies---------------------- 10 investigations in progress................ 237 Foraminifera, as indicators of environment... 139 investigations in progress......... 253,254, Ml occurrence and age................. 74,134,135 746-002 0 - 64 - 24A360 INDEX Page Foreign nations, geologic investigations......A2S7 hydrologic investigations................- - - 123 Forests, cutting, effect on sediment load----- 185 fires, effect on stream water______________ 190 Freeze-thaw effects, ground water............... 164 Fuel resources, compilations and topical studies............................ 262 See also Coal, Oil shale, Petroleum and natural gas. Fuller’s earth, investigations in progress----234, 242 G Galena isotopic composition.................... 171 Gas, natural. See Petroleum and natural gas. Gasoline, contaminant of ground water......... 59 Gastropods, investigations in progress.......... 264 occurrence and age......................... 137 use in correlation....................... 138 Geochemical data, results of investigations... 162 Geochemical distribution of the elements, investigations in progress_______________________ 238 Geochemical exploration, investigations in progress........................... 238 results of investigations__________ 84,200,201 Geochemistry, distribution of the elements... 238 experimental, investigations in progress .. 238 results of investigations.............. 159 field studies, investigations in progress_ 239 field studies, results of investigations. 154 organic, investigations in progress...... 238 water, investigations in progress__________ 238 results of investigations_____________ 163 See also under names of States. Geochronology, investigations in progress_____ 239 list of age determinations................. 169 results of investigations................ 84,168 See also Isotope and nuclear studies, K/Ar method, Rb/Sr method, Pb/alpha method, Pb/U method, and under names of States. Geologic data, coding and retrieval.......... 238 Geologic mapping, investigations in progress.. 239 See also under names of States. Geologic thermometry, investigations in progress........................................... 238 Geologic time scale, investigations in progress. 239 Geomorphology, investigations in progress.. 244,247 results of investigations............... 191 See also Sedimentation, and under names oj States. “Geophysical Abstracts,” continued publication......................................... 153 Geophysics, regional, investigations in progress............................... 247 theoretical and experimental, investigations in progress______________________ 248 results of investigations........... 151 See also Aeromagnetic surveys, Gravity surveys, Infrared studies, Radio-metric surveys, Seismic surveys, and under names of States. Georgia, attapulgite............................. 12 clay....................................... 234 cooperating agencies....................... 222 flood studies...........................236,237 fuller’s earth______________________________ 12 geochemistry............................... 238 ground water......................._ 26,177,179 low-flow studies___________________________ 252 minor elements............................. 61 paleontology.......................... 74,134 plant ecology............................ 192 See also Index to List of Publications Georgia—Continued Page quality of water........................ A59,166 sea-water intrusion...................... 257 sedimentation............................. 258 soil-moisture studies-------------------- 183 surface water....................... 26,27,179 water resources....................-.... 262 Geothermal studies, results of investigations.. 151 Geothermometers, sphalerite...................... 5 Glacial drift, estimation of lithology----- 188 Glacial geology, investigations in progress... 249 See also under names of States. Glacier flow, Washington....................... 193 Glaciology, investigations in progress....... 249 results of investigations................. 50,193 gnome, Project, geologic and hydrologic studies........................ 54 Gold, investigations in progress........ .. 249 method of microdetermination.......... 196 Granite, isotopic variation of lead........ 172 sites for nuclear experiments............ 235 Graptolites, investigations in progress.... 264 occurrence and age......................... 83 Gravity surveys, district-------------------- 63,78, 81,88,87,91,99,109,112.117,120 investigations in progress.............. 247 reservoir rocks___________________________ 17 See also Bouguer anomalies. Great Basin, paleontology..................... 132 silica................................. 13 Great Lakes region. See Lake Superior region, Lake Erie. Great Plains, Quaternary geology----------------- 93 Great Salt Lake, mineral transport______________ 189 quality of water......................... 189 Greenland, construction and terrain problems 235 geologic mapping.......................... 242 glacial geology............................ 249 investigations in progress................. 238 Ground movement, inventory..................... 235 Ground water, analog models.................. 42,177 apparent artesian conditions by soil freezing........................................ 178 arsenic content............................ 61 chemistry............................. 164,238 contamination, investigations in progress.. 236 occurrence........................ 58,59,60 rating of sites......................... 58 controls of permeability................... 176 correlation of spring discharge and precipitation..................................... 179 correlation of water-level records......... 178 crystalline rocks.......................... 177 effect of dams on well yield............... 180 effect of earthquakes....................70,178 effect of permafrost................... 194,265 effect of sonic booms on water levels__________ 178 fluoride content. ..................... 61,164 hydraulics, investigations in progress.. 249 interbasin movement, control................ 53 investigations in progress................. 250 limestone............................... 177 movement of radionuclides in................ 54 permeability of aquifer materials__________ 177 recharge, artificial.....*.............. 46,233 natural.............................177,179 relation of spring flow to artesian pressure. 180 relation to land subsidence and compaction___________________________________ 64 relation to low flows of streams........... 179 result of surface-water fluctuations....... 180 saline, investigations in progress......... 266 specific yield............................. 177 temperature fluctuations................... 178 Ground water—-Continued Page tracer studies....................... A54 transmissibility....................... 176 See also Aquifers, Soil moisture, and under names of States. Ground water-surface water relations, investigations in progress........................... 249 Guam, cooperating agencies................... 225 mineralogy.............................. 140 paleontology.........................134,140 water resources....................... 262 Gulf coast, paleontology..................... 254 Gulf of Mexico, organic geochemical investigations.......................................... 17 Gypsum, dehydration.......................... 165 Gypsum-anhydrite equilibria.................. 161 Hafnium, in volcanic rocks....................... 155 Hawaii, bauxite................................11,233 cooperating agencies........................ 222 floods................................... 68,237 geochemistry................................ 239 geophysics.............................166,167 ground water................................. 47 petrology.............................. 166,239 springs...................................... 47 surface water............................ 47 volcanology............................ 166.230 water resources......................... 261 Hawaiian Volcano Observatory, investigations........................................... 166 Health, relation to distributions of elements, investigations in progress........ 249 Heavy-liquid mineral separations................. 200 Heavy metals, district studies..........—. 3 geochemical anomalies........................ 77 Heavy minerals, trends in the Colorado Plateau........................... 187 Helium, in ground water........................... 40 Heulandite, physical chemistry.................. 158 Hexanol, use in mineral separations.............. 199 Hydraulics, ground water, investigations in progress........................- 249 surface water, investigations in progress. 249,250 Hydrologic-data collection and processing, investigations in progress_________________________ 250 Hydrologic measurements and instrumentation, results of investigations............. 202 Hydrology, effects of urbanization............... 260 ground water, investigations in progress.. 261 isotopic.................................... 261 mining, investigations in progress.......... 261 model studies, investigations in progress.. 261 nuclear explosions, investigations in progress............................ 261 radioactive-waste disposal, investigations in progress------------------------ 261 surface water, investigations in progress. _ 261 temperature studies, investigations in progress............................ 261 See also Ground water, Surface water. 1 Ice wedges, distribution........................ 194 Idaho, cenosite................................. 15 clay.—........................-......... 11.234 cooperating agencies........................ 222 copper........................................ 4 ferro-alloy metals.......................... 236INDEX A361 Idaho—Continued Page floods.................................. A 67 geochemistry.......................... 200,239 geologic mapping......................240,242 geophysics..............-........... 109, 247 hydrology................................. 110 ilmenite________________________________ 11 lead and zinc............................. 251 mineralogy................................ 159 monazite................................... 11 oil seeps.................................. 16 paleontology............................... 90 petrology........................... 89,90,2S9 phosphate...............................6,255 quality of water........................... 61 radioactive-waste disposal................ 267 springs.................................... 45 stratigraphy............................... 89 structural geology.............. 89,90,104,109 surface water.............................. 44 thorium................................ 259 tungsten.................................... 4 uranium................................... 260 volcanology............................... 260 water resources........................... 262 water use.................................. 44 waterpower_____________________________ 267 See also Pacific Northwest. Illinois, cooperating agencies............... 222 floods................................ 236,287 fluorspar__________________________________ 11 geologic mapping.......................... 243 geophysics................................ 247 lead and zinc............................. 261 low-flow studies.......................... 262 paleobotany............................... 258 petrology............................. 170,239 structural geology......................... 87 Impact phenomena............................. 142 Impactite, electron microprobe analyses.......... 146 India Ocean, tellurium........................ 15 Indiana, cooperating agencies................ 222 geologic mapping.......................... 248 geomorphology............................. 247 ground water............................... 31 lake studies.......................... 188,252 paleontology.............................. 131 quality of water........................31,188 sedimentation............................ 261 surface water...................... 31,175,261 water resources___________________________ 262 Indochinites, spherules, chemistry........... 144 Indonesia, construction and terrain problems geologic mapping.......................... 127 investigations in progress................ 288 Industrial minerals, investigations in progress. 251 Industrial wastes, occurrence in water supplies......................................... 59 Industrial water supplies, investigations in progress.......................- 256 Infared studies, results of investigations-148,153 Instruments, hydrologic...................... 250 Iodine, occurrence in Spanish-moss........... 200 X-ray fluorescence determination.......... 198 Ion-exchange phenomena_______________________ 160 Ion-exchange separation, tin from silicates_ 196 Iowa, coal................................16,284 cooperating agencies...................... 222 flood studies........................... 287 geologic mapping.......................... 24s geomorphology............................. 247 geophysics............................. 87,248 See also Index to List of Publications Iowa—Continued Page ground water.............................. A32 low-flow studies.......................... 261 petrology............................... 170 quality of water........................... 32 surface water.............................. 32 urban geology............................. 260 water resources____________-............ 262 Iron, content in copper....................... 146 district studies.........................3,123 ferrous, determination in small samples... 145 method of determination................... 196 in meteorites............................. 146 investigations in progress................ 251 Iron and steel industry, water use.............. 1 Iron deposits, investigations in progress... 244 Iron-formation, electrical and magnetic properties_______________________________-.....- 152 Iron ore, investigations in progress.......... 289 Isotope and nuclear studies, investigations in progress.......................... 251 See also Geochronology. Isotopes, light stable, results of investigations. 170 tracer studies............................ 171 use in crustal studies.................... 172 j Jadeite, physical chemistry................... 157 Japan, geophysics............................. 247 investigations in progress................ 288 K K/Ar method, investigations in progress........... 289 Kansas, cooperating agencies.................. 223 floods.................................... 287 geologic mapping.......................... 243 ground water............................... 39 lead and zinc............................. 251 low-flow studies.......................... 252 petroleum and natural gas................. 265 quality of water....................... 39,256 sedimentation_____________________________ 257 stratigraphy.............................. 259 surface water.............................. 39 urban hydrology...........-............. 260 water resources------------------------- 262 Kelsh plotter, modified, tests................ 218 Kentucky, coal..............................16,284 cooperating agencies...................... 223 floods............................. 66,286,287 geochemistry.................-.......... 156 geologic mapping................ 74,84,24S, 247 hydrology................................. g50 mining hydrology.......................... 268 paleontology...................... 131,133,254 petrology................................. 156 quality of water....................... 59,256 sedimentation............................. 187 stratigraphy......................... 74,82,85 structural geology......................... 85 surface water...............-........... 32 water resources........................... 263 water utilization......................... 261 Korea, ground water......................... 127 L Lake Eric, quality of water................... 189 Lake Superior region, geophysics............86,247 See also Michigan, Minnesota, Wisconsin. Page Lakes, deposits, closed basins................ A165 deposits, glacial....................79,81,107 glacial, history..................... 81,93,107 levels, investigations in progress......... 251 quality of water....................... 188,189 results of investigations.................. 188 saline..................................... 189 seepage.................................... 175 volume formula............................. 175 Land subsidence, district studies.............62,63 investigations in progress................. 251 relation to ground water.................... 63 Landslides, occurrence................... 62,69,167 Laumontite, occurrence..................... 117,120 Lead, district studies........................ 4,87 geochemical anomaly......................... 77 geochemistry and origin, investigations in progress............................ 289 isotopic variation in rocks................ 172 reference sample for isotope study......... 171 use in age determinations.................. 289 Lead ore, isotopic composition................. 171 Lead and zinc, investigations in progress— 246,261 Lepidolite, occurrence.......................... 94 Leucite, physical chemistry.................... 158 Leveling, improvements in technique............ 217 Liberia, investigations in progress............ 288 Libya, geologic mapping........................ 127 investigations in progress................. 288 water resources............................ 267 Light metals, district studies................... 6 Limestone, reefs........................... 128,140 well tests................................. 177 Limeetone-terrane hydrology, investigations in progress......................... 261 Limnology, investigations in progress.......... 261 See also Lakes. Lithiophorite, formula......................... 158 Lithium, determination in tektites............. 145 district studies............................ 13 spectrometric determination________________ 197 Logger, geophysical, multifunction type............ 204 Louisiana, cooperating agencies................ 223 floods................................. 68,287 ground water____________________________ 33.164 petroleum and natural gas.................. 255 quality of water_____________________ 34,60,164 sedimentation........................... 34,268 stratigraphy................................. 258 „ surface water............................... 42 water resources............................ 268 Low flow, relation to geology.................. 175 Low flow and flow duration, investigations in progress_________________________ 262 Luminescence, results of investigations............ 153 Lunar geology. See Extraterrestrial studies, lunar. M Magnesium, method of microdetermination.. 196 X-ray fluorescence determination.......... 198 Magnetic anomalies, depth calculation......... 153 See also Aeromagnetic anomalies. Magnetic surveys, district.............. 86,99,167 See also Aeromagnetic surveys. Magnetic susceptibility, measurement.......... 154 tektites................................... 146 Magneto-acoustic studies...................... 154A362 INDEX Page Maine, cooperating agencies.................... A223 economic geology........................... 77 flood studies............................. £37 geochemical prospecting................... £38 geochemistry.......................... 200,201 geologic mapping.......................... £43 geophysics...................-........152,248 glacial geology............................ 77 paleontology............................... 76 petrology.................................. 77 stratigraphy and sedimentation............ 259 structural geology....................76,77 water resources........................... 263 Mammals, fossil, classification and evolution. 136 fossil, occurrence and age................ 133 See also Desmostylians, Oreodonts, Shrews, Whales. Manganese, concentration in water...........56,165 district studies____________________________ 5 geochemistry and geology, investigations in progress.................... 239,244 Manganese nodules, tellurium content........... 163 Mapping, flood inundation........................ 69 geologic, investigations in progress...... 239 See also under names of States. paleo tectonic........................... £57 topographic, results of Topographic Division investigations...................... 207 Mapping technique, slope measurement........ 147 Maps, geologic, Moon........................ 140 geological and geophysical, large regions... 72 isotonal, Moon............................ 148 topographic......................... 138,207 Marcasite, inversion relations—................ 161 Marine geology and hydrology, investigations in progress....................... 252 results of investigations................ 138 Marine hydrology, investigations in progress.. 252 See also Sea-water intrusion. Maryland, clay................................. 11 construction and terrain problems.......... 61 cooperating agencies...................... 223 flood studies............................. 237 geologic mapping........................ 243 geophysics............................£47,248 ground water............................... 26 lightweight aggregate...................... 11 marine biology............................ 140 marine hydrology......................... 252 paleontology............................. 73 plant ecology........................... 192 quality of water...................... 25,256 sedimentation............................. 185 stratigraphy and sedimentation......... 82,269 surface water............................ 25 urban geology............................. 260 urban hydrology........................ 260 water resources........................ 263 Mass-budget studies, glaciers.................. 193 Massachusetts, construction and terrain problems........................... 235 cooperating agencies...................... 223 flood studies............................. 237 geochemistry and petrology______________ 239 geologic mapping.......................... 243 geomorphology............................. £47 geophysics......................... 63,78.£48 glacial geology......................... 78,79 ground water............................... 21 hydrology............................... £61 low-flow studies.......................... £61 See also Index to List of Publications Massachusetts—Continued Page petrology.............................. A 78 quality of water............................... 22 sedimentation................................. 188 stratigraphy................................... 77 stratigraphy and sedimentation................ 269 structural geology............................. 78 surface water.................................. 22 urban geology................................. 260 water resources............................... 263 Mathematical model, prediction of ripple index................................. 186 Mercury, determination of small amounts_____ 200 See Quicksilver for natural occurrences of mercury. Metamorphic rocks, geochemistry and petrology........................................ 156 Meteorites, investigations in progress............. 236 occurrence, Antarctica........................ 121 See also Extraterrestrial studies; Nickel, distribution in meteorites; Tek-tites. Meteorology, measurement of storms with radar................................. 204 Methane, in ground water........................... 164 Metropolitan areas, topographic mapping_____ 207 See also Urban areas, Urban geology, Urbanization. Micas, new minerals, crystal chemistry................. 253 See also Biotite, Muscovite, Paragonite. Michigan, artificial recharge...................... 233 cooperating agencies.......................... 223 copper........................................ 236 geologic mapping....................... 86,243 geomorphology................................. 247 geophysics............................. 86,87,248 glacial geology................................ 87 ground water........................... 30,48,179 iron.........................................3,251 petrology...................................... 86 quality of water............................... 58 saline-water resources................. 48 stratigraphy........................... 86 surface water........................30,179 water resources....................... 263 See also Lake Erie. Microprobe studies. See Electron microprobe studies. Microscope, for measuring sand-grain orientation.............................. 204 Midcontinent area, geochronology................... 168 Mine bumps.................................. 62 Mine drainage, investigations in progress.... 245 Mine water, used for industrial water supply. 32 Mineral lands, classification............... 49 Mineral resources, compilations and topical studies, investigations in progress. 252 compilations and topical studies. See also specific minerals. Mineral separations, methods....................... 199 Mineralization, blood vessels................. 199 Mineralogic studies, results of investigations.. 156 Mineralogy and crystallography, experimental, investigations in progress___________ 252 See also Geochemistry, experimental. Minerals, new or unusual, analysis.......197,199 production from Federal lands_________________ 50 Mining hydrology, investigations in progress. 261 Minnesota, cooperating agencies................ 223 geochemistry......................... 170 geochronology........................ 169 geophysics.......................... 87,247 ground water.......................... 30 iron_________________________________3,251 Minnesota—Continued ^age paleontology............................. A132 water resources........................... 263 Minor elements, distribution, relation to health..............-............ 61 district studies........................... 15 in rocks________________________________ 155,162 in water................................ 190 investigations in progress................ £63 Mississippi, cooperating agencies.............. 223 floods............................. 68,236, £37 geologic mapping.......................... 243 geophysics................................ £48 ground water.............................33,55 hydrology................................. £63 low-flow studies........................ 252 nuclear test site....................... 55 paleontology.............................. £54 petroleum and natural gas................ £55 quality of water...................—....33,60 sedimentation.............................. 34 water resources........................... £68 Mississippi Embayment, hydrology............. £61 water resources............................ 34 Mississippi River basin, hydrology........... 261 Missouri, cooperating agencies................. 223 flood studies........................... £37 geologic mapping.......................... £43 geophysics..............................88,248 ground-water............................... 32 lead and zinc............................. £61 low-flow studies.......................... £62 quality of water........................ 32,261 sedimentation............................. £68 surface water______________________________ 32 water resources........................... 264 Model studies, hydrologic, investigations in progress_________________________ £53 Mollusks, evolution............................ 135 investigations in progress.............. 263, £64 occurrence and age_________________ 73,134,138 See also Pelecypods, Cephalopods, Gastropods. Molybdenum, district studies..................... 3 See also Ferro-alloy metals. Monazite, investigations in progress........... £63 Montana, artificial recharge................... £63 base metals............................... £33 chromite................................ £36 coal_______________________...__________16, £34 construction and terrain problems......... 235 cooperating agencies................... 223 flood studies............................. 237 fluorine________________________________ 6 geochemistry and petrology........... 154,238,239 geologic mapping..........................£40, £43 geomorphology............................. 247 geophysics.........................92, 21^7, £48 glacial geology........................... 93 glaciology.............................. £49 ground water....................... 35,179, £49 iron.................................... £51 manganese_______________________________ £36 paleontology_____________________________ 93 petroleum and natural gas................ 255 petrology............................ 92,93 phosphate...............................6,255 plant ecology............................. 192 quality of water........................... 35 reservoir studies....................... £49 sedimentation........................... 186,257 soil-moisture studies..................... 183INDEX A363 Montana—Continued Page stratigraphy.............................. A93 structural geology.................... 92,259 surface water..........................179,249 uranium................................... 6 urban geology............................. 260 volcanology-..........................93 ,261 water resources........................ 264 waterpower................................ 267 Moon. See Extraterrestrial studies, lunar. Mudflow studies............................... 235 Muscovite, crystallography.................... 158 N National parks, topographic mapping----------- 209 Natural gas. See Petroleum and natural gas. Nebraska, construction and terrain problems. 285 cooperating agencies...................... 223 floods............................ 67,236,937 geochemistry............................. 289 geologic mapping.....................98, £44 ground water............................... 37 hydrology................................. 268 petroleum and natural gas................. 255 quality of water........................... 37 sedimentation......................... 258,269 stratigraphy___________________________ 269 surface water..........................173,176 urban geology............................. 260 water resources........................... £64 Nepal, water resources........................ 267 Nevada, base metals........................... 288 beryllium............................. 284,288 borate.............................. 13, £54 construction and terrain problems........ 285 cooperating agencies...................... 223 copper................................... 236 evapotranspiration studies................ 182 floods................................. 67,287 geochemical prospecting................... 288 geochemistry............ 108,154,155,171,197,288 geophysics........................ 53,153, 248 geologic mapping...................... 240,244 geothermal studies....................... 151 ground water.......................... 45,53,180 hydrology................................ 258 land subsidence__________________________ 64 lead and zinc............................. 251 mineralogy................................ 199 nuclear test site.......................... 51 paleontology.................. 103,104,134, £54 petrology............... 51,52,107,108,154,155 phosphate_____________________________ 255 phreatophytes............................ 183 quicksilver............................... 5 radioactive-waste disposal................ 267 sedimentation_________________________ 258,259 stratigraphy.................. 103,104,107,259 structural geology... 52,102,104,105,107,109,259 tellurium__________________________________ 15 water resources.......................... £64 waterpower................................ 267 Nevada Test Site, geologic and hydrologic studies............................ 51 investigations in progress........ 285,244,248 New England, geologic map..................... 75 geophysics................................ £47 summary of geology......................... 75 See also names of States. New Hampshire, cooperating agencies............... 223 hydrology................................. 261 surface water............................. 260 water resources........................... 264 See also Index to List of Publications Page New Jersey, cooperating agencies.............. A223 flood studies........................... 237 geochemistry........................... 73,74 geologic mapping.......................... 244 geophysics................................ 248 ground water............................... 24 hydrolog>......................... 249,250,251 iron...................................... 251 nuclear-power plant site studies........... 57 paleontology..........................83,254 petrology................................73,74 precipitation............................. 256 quality of water................ 23,59,838,254 sedimentation............................. 268 stratigraphy............................... 73 structural geology......................... 83 surface water...................175,250,261 water resources........................... 264 New Mexico, artificial recharge................ 288 acoustical studies of rock................. 54 beryllium................................... 9 coal.................................. 16,284 construction and terrain problems......... 285 cooperating agencies...................... 223 copper.................................... 886 geochemical prospecting................... 288 geochemistry.......................... 155,289 geologic mapping................. 101,240, £44 geomorphology............................. 247 geophysics............................. 99,248 ground water.................... 40,54,177,258 hydrology............................... 249 lead and zinc............................4,261 nuclear test site.......................... 54 petroleum and natural gas............... 255 petrology............................. 155,289 potash................................ 256 quality of water................ 40,60,164,256 radioactive-waste disposal................ 267 radionuclide movement in natural water.. 54 saline minerals........................... 267 sedimentation................... 184,185,267,259 stratigraphy................. 89,96,97,100,259 surface water............................. 174 uranium............................... 14, £60 volcanology............................... 261 water resources........................... 264 water utilization......................... 256 waterpower______________________________ 267 New York, cooperating agencies................. 223 floods................................. 65,237 geochemistry.............................. 239 geologic mapping.......................... £44 geomorphology............................. 247 geophysics..............................81,248 glacial geology............................ 81 ground water............................23,178 iron____________________________________ 261 low-flow studies.......................... 252 paleontology..........................132,138 petrology...............................81,239 plant ecology............................. 193 quality of water...................... 58,256 sedimentation........................... 259 stratigraphy........................... 81,259 surface water------------------------- 22,250 water contamination------------------ 235,286 water resources_______________________—- 264 water-temperature studies............... 259 Nickel, in meteorites........................ 145,146 See also Ferro-alloy metals. Nigeria, water resources....................... 267 Page Niobium, district studies.................. a 15 investigations in progress................ 253 Nitrogen, occurience in water well............ 40 North Carolina, beryllium...................... 10 'Cooperating agencies..................... 224 floods.................................... 237 geochemical exploration................. g4 geochronology.............................. 84 geologic mapping.......................... 244 geomorphology..........................244,247 geophysics.............................84,248 paleontology............................ 134 pegmatites................................ 254 phosphate................................... 7 precipitation studies..................... 164 quality of water.................... 26,60,266 Quaternary geology......................... 84 sedimentation.......................... 184,258 surface water___________________________ 180 thorium.................................... 15 tungsten.................................... 5 uranium.................................... 15 water resources........................... 266 zeolites................................... 12 North Dakota, coal............................ 284 cooperating agencies...................... 224 evapotranspiration studies________________ 181 flood studies............................. 237 geochemistry.............................. 289 geologic mapping.......................... 245 geomorphology............................. £47 glacial geology............................ 93 ground water............................... 35 petroleum and natural gas................. 255 quality of water------------------------- 256 water resources.__________________________ 265 Northeastern United States, geophysics............ £47 See also names of individual northeastern States. Northwestern United States, paleontology— 264 See also Pacific Northwest and names of individual northwestern States. Nuclear energy, use in sediment sampler........... 203 Nuclear explosions, effects................... 235 hydrology, investigations in progress---- 268 peaceful uses.............................. 53 underground, detection..................... 55 effect on ground water.............- 53,54 Nuclear power plants, study of sites.......... 57 o Obsidian, solubility in water................. 160 viscosity................................. 161 Ohio, cooperating agencies.................... 224 floods--------------------------------- 66,237 geophysics-------------------------- 247,248 ground water________________________ 31,250,265 low-flow studies.......................... 252 paleontology.............................. 131 plant ecology............................. 103 quality of water....................... 59,256 surface water_____________________________ 175 water resources------------------------- 265 See also Lake Erie. Ohio River basin, hydrology................... 261 Ohio River valley, floods...................... 67 geomorphology............................. £47 Oil shale, district studies................17,116 effect of weathering.................... 156 investigations in progress.........240,246,868 Oil wells, effect of land subsidence on...... 64 Okinawa, water resources........-.......... 267A364 INDEX Page Oklahoma, coal............................... A.284 cooperating agencies........................ 224 floods.................................. m geologic mapping.......................— 245 ground water...........................4l, 179 lead and zinc.............................. 261 mineralogy............................. 171 petroleum and natural gas.................. 255 quality of water......................41,266 stratigraphy and sedimentation......... 259 surface water.................... 41,173,175,250 water resources ........................... 265 waterpower................................. 267 Omphacite, crystallography.................... 158 Optical spectroscopy, results of investigations. 197 Ore deposition, environment................ 288 Oregon, artificial recharge................ 238 borates.................................... 284 coal........................................ 284 cooperating agencies................... 224 ferro-alloy metals..................... 286 geologic mapping.................Ill, 240,245 geomorphology.......................... 247 geophysics.............................112,248 glacial geology........................ 249 hydrology................................... 260 lake studies........................... 189.251 nickel.................................... 286 paleontology........................... 134,254 petrology.............................. Ill quality of water................. 61,165,189,256 quicksilver............................ 257 radioactive-waste disposal............. 267 saline lakes.............................. 189 sedimentation.......................... 268 stratigraphy.............................108,111 structural geology ......................... ill surface water.................... 44,175,189 volcanism.________________________________ 111 water resources............................. 265 water-temperature studies______________ 269 waterpower.................................. 267 See also Pacific Northwest. Oreodonts, occurrence and age.................. 135 Organic fuels, district studies_________________ 15 See also Coal, Petroleum and natural gas. Ostracodes, investigations in progress_____ 264 occurrence and age.............. 76,132,134,138 Oxygen sheath, for flame photometry........ 195 Oysters, occurrence and age. ................. 137 p Pacific coast, paleontology................ 254 volcanology............................. 261 See also names of States. Pacific islands, geologic mapping.......... 245 paleontology...........................137,258 vegetation............................. 260 Pacific Northwest, geophysics.................. 247 ground water................................. 44 quality of water___________________________ 61 springs.................................. 44 See also Idaho, Oregon, Washington. Pacific Ocean, geophysics.................. 247 organic geochemical investigations...... 17 submarine landslides................... 167 Tellurium............................... 15 Pacific Southwest, geophysics.............. 247 Pakistan, chromite......................... 128 coal...................................... 128 geologic mapping......................... 127 ground water........................... 128 See also Index to List of Publications Pakistan—Continued Page investigations in progress................. A288 stratigraphy and paleontology............... 128 structural geology.......................... 128 water resources.........._.............. 267 Paleobotany, occurrence and age of fossils.. 136,137 systemic, investigations in progress............ 258 Paleomagnetism, results of investigations........... 151 Paleontology, invertebrate, systematic, investigations in progress........................ 258 invertebrate, systematic. See also classes of invertebrates. stratigraphic, investigations in progress.._ 254 vertebrate, systematic, investigations in progress........................... 254 systematic, occurrence and age of fossils.........................114,133 See also under names of States. Paleotectonic maps............................. 267 Palladium, magnetic susceptibility............. 154 method of microdetermination_______________ 196 Panama, paleontology....................... 135,264 Paragonite, crystallography____________________ 158 Pb/alpha method, investigations in progress.. 289 Pb/U method, investigations in progress............ 239 Pegmatites, investigations in progress. ....... 264 Pelecypods, evolution.......................135,136 investigations in progress. ............... 254 occurrence and age. .....................75,137 See also Oysters. Pennsylvania, coal______________________ 15,234,245 cooperating agencies....................... 224 geologic mapping........................... 245 geomorphology............................... 83 geophysics..........................83,247,248 glacial geology............................. 84 ground water.............................25,178 low-flow studies.......................... 252 paleomagnetism_____________________________ 152 phosphate.................................... 7 quality of water..................... 24,25,266 sea-water intrusion....................... 257 sedimentation............................ 259 silica...................................... 13 stratigraphy............................ 84,269 structural history.......................... 83 surface water.............................24,25 uranium.................................... 14 water resources............................ 265 Periscope, for borebole inspection............. 204 Permafrost, effect on ground water............. 255 investigations in progress................. 255 results of investigations.................. 194 Permeability, aquifer, effect on ground water. 33 data, contouring........................... 204 distribution in sedimentary basins............. 176 laboratory research....................... 184 values according to drillers’ descriptions.. 176 Peru, proposed geological survey............... 129 Pesticides, determination in water........ 201,286 occurrence in water supplies............... 58 Petrographic techniques, results of investigations........................................ 199 Petroleum and natural gas, district studies. 16,116,118 investigations in progress............. 241,256 production from Federal lands............... 50 use of gravity studies to estimate oil and gas content......................... 17 Petrology, field studies, investigations in progress........................................... 289 field studies, results of investigations_ 154 See also under names of States. Phase studies, pyrrhotite—sphalerite........... 199 Philippine Islands, investigations in progress. 288 Page Philippinites, spherules, chemistry....... A144 Phosphate, district studies.................... 6 influence of latitude on distribution..... 8 investigations in progress..............242,255 Phosphate minerals, crystal chemistry....... 262 Photogrammetry, research and development. 217 Photography, aerial, use in topographic mapping........................................215,218 Photometry, flame, new oxygen sheath........ 195 Phreatophytes, accumulation of boron by_____ 183 water loss by______________________________ 181 Pierre Shale, stratigraphy and sedimentation. 268 Plankton, removal of skeletal material........ 139 Plant analysis, laboratory................ 288 Plant ecology, investigations in progress... 256 results of investigations............. 191 Plant fossils, occurrence and age........... 76,88 Plants, relation to soil-moisture storage... 192 Platinum, method of microdetermination...... 196 plowshare, Program, geologic and hydrologic studies........................... 53 Plutonic rocks, geochemistry and petrology... 131 Pollen, investigations in progress........ 253 Pollen and spores............................. £64 Potash, investigations in progress........ £66 Potassium, shape of Fermi surface......... 154 Prairie potholes, water loss from..------- 181 Precipitation, chemical composition.—-...... 164 effect on tree form....................... 191 investigations in progress................. £66 See also Rainfall. Probe, drag-wire, use in hydraulic study.... 205 electron, studies of metals............... 146 studies of minerals................... 179 freezing, use in sediment sampling.... 203 Programs, Atomic Energy Commission. See VELA UNIFORM, PLOWSHARE. Projects, Atomic Energy Commission. See BILBY, CHARIOT, DOOSLED, DRIBBLE, FERRIS WHEEL, GNOME, SCHOONER. Prospecting. See Geochemical exploration. Public domain, water resources................ £61 Public water supplies, investigations in progress........................... £66 Publications, fiscal year 1964—.............. 277 Puerto Rico, cooperating agencies.............. 225 floods............................. 66,286, £27 geologic mapping.------------------------ 120,246 geomorphology.--........................... 120 geophysics.........................120,247,248 geothermal studies....................... 151 ground water.......................-.... 29 mineralogy-.............................- 120 quality of water............................ 28 structural geology......................... 120 surface water..................-........ 28 water resources................-........ £66 Pyrite, inversion relations-------------------- 161 Pyrrhotite-sphalerite phase studies............ 199 Q Quality of water, chemical, public supplies... 20 intrumentation for measurement............. 202 investigations in progress................ 266 processing of data....................... 205 temperature recorder...----------------- 202,204 Quicksilver, district studies.................. 5 investigations in progress..............-. 257 occurrence.........................-.... 108 See also under names of States.INDEX A365 R Page Radar, use in measuring storms--------------- A204 Radioactive disequilibrium, natural........... 170 Radioactive materials, transport in water, investigations in progress......- 257 Radioactive minerals, district studies......... 13 Radioactive-waste disposal, in streams......... 55 investigations in progress........-.... 957 laboratory and theoretical studies........ 56 underground............................... 57 Radioactivity, distribution.................. 938 Radioactivity surveys, district............. 98,114 Radiolaria, investigations in progress...... 264 Radiometric surveys, district.................. 84 Radionuclides, adsorption equilibria with rock. 54 movement in natural water.............. 54,56 Radon, migration of isotopes in ground...... 152 Rainfall, relation to runoff.................. 68 Rare-earth elements, geochemistry and resources..................................... 239 investigations in progress............... 253 spectrographic determination............. 197 Rare-earth metals, investigations in progress. Set Minor elements. Rare earths, district studies.................. 15 Rb./Sr method, investigations in progress... 239 Recharge, ground-water. See Ground water, recharge. Recorder, water temperature, continuous..... 204 Records, digital punch, use in recording rainfall and stream data.......................... 202 Reefs, limestone.......................... 127,140 Refractory minerals, acid decomposition, equipment........................ 196 Regional studies and compilations, large areas of the United States.............. 267 Relief model, Antarctica...................... 216 Reservoirs, effect on water yield............. 175 evapotranspiration losses............... 183 oscillations in water surface........... 174 sedimentation studies, investigations in progress.......................... 258 seepage.................................. 180 Rhenium, investigations in progress. See Minor elements and Ferro-alloy metals. Rhode Island, cooperating agencies........... 224 geologic mapping.......................79,246 glacial geology.......................... 80 ground water............................ 22 petrology.............................. 79,80 quality of water.......................... 22 water resources.......................... 265 Rhodium, method of microdetermination....... 196 Ripple index, mathematical prediction........ 186 Ripple marks, wave-tank study................. 186 Rivers. See Surface water. Rock chemical analysis, investigations in progress.......................333,238 Rock deformation, research................... 236 results of investigations................ 152 Rubidium, determination in tektites........... 145 Runoff, magnitude and frequency................ 68 procedure for comparison of departures... 174 relation to meteorological factors_____68,174 Ryukyu Islands, paleoecology.................. 253 s Saline minerals, investigations in progress_ 257 Saline water, in aquifers..................... 23, 2a 29,37,38,44, 47,48, 59,60,166 in lakes............................. 189 See also Index to List of Publications Saline water—Continued Page in oil fields, origin................... A156 in streams.............................. 59,60,61 map of resources in United States.......... 48 See also Brine. Salmon spawning, optimum stream discharge. 176 Salt, in surface water, effect on vegetation_ 61 Salt deposits, use in nuclear testing________ 54, 55 Salt dome, aquifer overlying................... 33 Samoa. See American Samoa. Sample preparation, disaggregation method... 204 Sampling, sediment, new equipment............. 203 Sampling methods, computer study............... 163 Sand, beach and eolian, indistinguishable.... 186 Sandstone, sites for nuclear experiments_____ 235 uranium deposits........................... 13 Saudi Arabia, geologic mapping................. 129 investigations in progress............... 238 mineral resources......................... 129 Schist, age. New Jersey...............-...... 74 schooner, Project, geologic studies............. 53 Project, investigations in progress..... 236 Sea-water intrusion, investigations in progress. 257 See also under names of States. Sediment, new sampling equipment............... 203 Sediments, deposition....................... 186 erosion__________________________________ 184 transport...............................- 184 Sedimentary rocks, geochemistry and petrology.......................... 156 minor elements............................ 238 Sedimentation, investigations in progress... 257,268 results of investigations................. 183 See also under names of States. Seismic recorders, portable, new............... 151 Seismic records, data processing............... 150 Seismic sea waves, in Alaska earthquake...... 69 Seismic surveys, district.................... 62,63, 78 Seismology, cooperative experiments.......... 150 Hawaii.................................... 167 Selenium, district studies...................... 15 in hot-springs and volcanic sulfurs........ 15 investigations in progress.............. 239,253 See also Minor elements. Shale, chemical analyses....................... 196 Shape factor, for gravel fragments............. 188 Shrews, classification and evolution........... 136 Silica, district studies........................ 13 investigations in progress................ 268 stability studies.................... 142 Silicate rocks, determination of fluorine in_ 195 manual for systematic analysis............ 195 separation of tin from.................... 196 Silicates, solubility in water............... 159 Silver, occurrence............................. 108 Sino-Soviet terrain, atlas..................... 235 Skeletal material, removal from plankton..... 139 Slope development, mathematical study........ 191 Snails. See Gastropods. Snake River Plain, aquifer analog.............. 253 Snowmelt, effect on sediment load in rivers... 185 Soil moisture, investigations in progress.... 258 mathematical and analog analysis.......... 181 rates of percolation and evaporation.... 183 relation to overbank flooding............. 183 storage effect on plants.................. 192 Soils, change in composition, dated by tree rings.............................. 201 lateritic, relation to bedrock............ 140 uranium fractionation pattern............. 170 Solid-state studies............................ 153 Sonic booms, effect on water levels............ 178 Sonic profiling, use in structure studies.... 139 Page South Carolina, cooperating agencies......... A224 flood studies............................. 237 geochemistry.............................. 239 ground water............................... 57 hydrology................................. 260 low-flow studies.......................... 252 petrology...............................83,239 radioactive-waste disposal.............. 57,257 water resources........................... 265 South Dakota, coal............................ 234 construction and terrain problem__________ *$5 cooperating agencies...................... 224 flood studies............................. 237 geochemistry.............................. 239 geochronology............................. 168 geologic mapping.......................... 246 geophysics................................ 248 glacial geology............................ 93 ground water............................36,177 molybdenum.................................. 3 pegmatites............................... 256 petroleum and natural gas................. 265 quality of water________________________ 37, 238 resource compilation........................ 1 springs.....-........................... 37 uranium................................ 37,260 urban geology............................. 260 water resources___________________________ 265 Southeastern United States, asbestos.......... 233 bauxite................................... 233 ferro-alloy metals...................... 236 hydrology................................. 251 geochemistry.............................. 239 monazite.................................. 253 phosphate................................. 265 talc............................—....... 259 See also names of individual southeastern States. Southwestern United States, copper............ 236 paleontology.......................... 253,254 See also names of individual southwestern States. Space-flight studies.......................... 147 Spanish-moss, iodine content................ 21* Specific yield, laboratory research........... 184 Spectrographic analysis, determination of metal in stream sediment.......... 200 methods, extraterrestrial material—....... 145 sandstone............................... 163 Spectrometer, use in lithium determination... 197 Spectrophotometry, new methods and reagents.................................... 195.196 Spectroscopy, atomic absorption, in mercury determination..................... 200 investigations in progress................ 268 Sphalerite, as a geothermometer................. 5 S podumene, physical chemistry................ 157 Spores, occurrence and age--------------------- 73 See also Pollen and spores. Springs, correlation of discharge and precipitation...................................... 179 investigations in progress.-------------- 268 occurrence........................ 37,44,45,47 thermal................................ 164 Statistical methods, in rating of analysts.. 195 Statistical studies, vegetation mapping..... 192 Stishovite, physical chemistry________________ 142 Stratification, streambed deposits........... 187 Stratigraphy, investigations in progress.... 258 See also Paleontology, stratigraphic; specific areas under Geologic mapping; and under names of States.A366 INDEX Page Stream channels, morphology___________________ A191 Stream controls, artificial, evaluation________ 203 Streamflow, differentiating sources of base flow.....—.......................— 180 effect of swamps.......................... 175 effect of water use on channel width..... 176 ground-water contributions................. 180 relation to aquifers....................... 180 relation to drainage area. ..............- 175 relation to geology and topography------- 179 relation to ground-water storage........... 179 use of recorders and computers in processing data--------------------------------- 202 See also Floods, Surface water. Streams. See Streamflow, Surface water. Strontium, isotopic variation in volcanic rocks.............................. 172 Strontium/rubidium ratios, determination_____ 198 Structural geology and tectonics, investigations in progress______________________________ 269 See also under names of States; specific areas under Geologic mapping. Sudan, water resources....................... 267 Sulfide deposits, investigations in progress_ 2S6 Sulfur, content in granite and diabase......... 196 effect on inversion temperature of chalco- cite............................... 5 Surface water, base-flow computations.......... 179 channel underflow......................... 173 chemistry. _____________________________ 163 contamination, occurrence___________________ 58 dispersion of solutes.____________________ 173 dissolved and suspended load, amount_____ 185 diurnal fluctuation produced by hydraulic changes____________________________ 173 effect of seepage........................ 180 effect of snowmelt on sediment load------ 185 effect of urbanization on sediment load... 185 effect on ground-water fluctuations...... 180 flow in alluvial channels.................. 174 flow in open channels...................... 174 flow through contractions.................. 173 hydraulics, investigations in progress... 260 low-flow relations......................... 175 prediction of sediment load_______________ 184 radioactive*waste disposal.................. 55 regression estimates....................... 175 relation of bed material to open-channel flow............................... 174 relation of discharge and precipitation-- 174 relation of flow and drainage area......... 175 relation to aquifers....................... 179 runoff..................................... 174 sources of base flow____________________ 180 storage-draft relations by probability routing___________________________ 175 vertical*velocity profiles................ 173 See also Floods, Streamflow, and under names of States. Switzerland, lake studies____________________ 188 Systems, chemical. See Cu-Ag-S, Cu-S, Fe-Zn-S. T Talc, investigations in progress............... 269 Tantalum, investigations in progress------------- 263 investigations in progress. See also Minor elements. Tektites, geochemistry and petrography_________ 144 investigations in progress.................. 236 magnetic and electrical properties----------- 146 See also Index to List of Publications Page Tellurium, district studies................A15,108 in hot-springs and volcanic sulfurs___________ 15 in manganese nodules. .................... 163 new method for quantitative determination...................................... 15 Temperature studies, water, investigations in progress........................ 269 Tennessee, coal............................16,234 cooperating agencies..................... 224 copper................................. 236 cryptoexplosion structures............... 143 floods........................... 66,236,237 geochemistry......................... 156 geologic mapping......................... 246 geophysics............................ 248 geothermal studies........................ 151 ground water............................32,178 hydrology..............-............... 249 iron................................... 251 lead and zinc---------------------------- 261 low-flow studies......................... 262 petrology................................ 156 quality of water------------------------- 32 radioactive-waste disposal............... 267 stratigraphy.............................. 82 surface water___________________________ 174 urban hydrology.......................... 260 water resources_____________-............. 266 zinc_________________________________ 245,253 Tennessee River, radioactive-waste disposal.. 55 Texas, clay mineralogy........................ 75 cooperating agencies.*.------------------- 224 cryptoexplosion structure................. 142 evapotranspiration--------------------- 181,236 floods.................-.........-..... 67,237 "geochemistry and petrology............... 239 geochronology--------------------------- 168 geologic mapping.......-............... 246 geomorphology............................ 88 geophysics........................... 247,248 ground water------------------------------- 42 hydrology........................... 250,261 land subsidence............................ 65 low-flow studies------------------------- 252 model studies---------------------------- 253 paleontology................----------- 88,254 petroleum and natural gas_________________ 255 quality of water....................... 42,60,256 sedimentation-------------------- 34,187,258,259 stratigraphy__________________________ 258,259 structural geology------------------- 106,142 surface water...........................42,176 uranium................................14,260 urban geology............................. 260 urban hydrology.......................... 260 water resources-------------------------- 266 Thailand, geologic mapping-.................. 129 investigations in progress---------------- 238 mineral resources_________________________ 129 stratigraphy--------------------------- 129 Thermal springs, occurrence------------------- 164 Thermal water, occurrence and origin_______156,164 Thermal waters and deposits, investigations in progress...................... 239 Thermoluminescence, results of investigations. 153 Thorium, content in igneous rocks_____________ 162 determination, new reagent---------------- 195 district studies.......................... 15 investigations in progress________________ 259 Tiltmeter surveys, Hawaii--------------------- 166 Tin, district studies--------------------------- 4 investigations in progress________________ 269 method of separation from silicates___________ 196 Page Topographic mapping. See Mapping, topographic. Tracer studies, isotope------------------------- A171 Transmissibility, determination------------------ 176 Transport, sediments---------------------------- 184 Trees, form, relation to rainfall interception. _ 191 growth rates, relation to hydrology and climate............................. 193 measurement of water flowthrough-------- 181 relation to flooding......................... 192 relation to geology and hydrology------------ 192 Tree leaves, effect on water quality............ 190 Tree rings, composition, indicator of soil change..........................- 201 Trilobites, investigations in progress......... 254 occurrence and age......................... 90,133 Tritium, fractionation in porous media------ 166 in precipitation and stream water............ 164 Tunellite, crystal structure.................... 158 Tungsten, district studies...................... 5 investigations in progress................... 241 investigations in progress. See also Ferroalloy metals. Tunisia, water resources_________________________ 267 Turkey, water resources-------------------------- 267 u United Arab Republic, water resources------- 267 Uranium, content in igneous rocks---------------- 162 district studies............................ 13 fractionation of isotopes___________________ 170 in sandstone................................. 13 in stream water.............................. 164 investigations in progress........... 239,262,269 Uranium deposits, effect on blueberries....... 201 Uranium minerals, crystal chemistry-------------- 252 Uranyl tricarbonate, synthetic, new.......... 159 Urban areas, flood map............................ 69 topographic mapping..------------------------ 207 Urban geology, investigations in progress--- 260 investigations in progress. See also Construction and terrain problems. Urbanization, effect on floods-------------------- 68 effect on runoff----------------------------- 46 effect on sediment load--------------------- 185 hydrologic effects, investigations in progress...................................- 260 Utah, base metals................................ 233 beryllium............................... 8,234 coal___________________________________ 235,245 coal-mine bumps.............................. 62 construction and terrain problems----.... 235 cooperating agencies....................... 224 copper....................................... 236 evaporites............................... 13 ferro-alloy metals......................... 236 floods..............................— - 237 fluorspar. ................................ 237 geochemical prospecting..................... 238 geochemistry________________________________ 170 geologic history.......................... 107 geologic mapping....................... 240,245 geophysics.............................. 62,248 ground water............................38,48 lake studies. .........................189, £5/ lead and zinc............................... 251 lithium................................... 13 mineral resources......................... 262 oil shale........................... 18,246,263 paleontology................................. 104 petroleum and natural gas.................... 265 petrology.................................. 106INDEX A367 Utah—Continued Fage phosphate______________________________ AQ,£66 potash.................................... £56 quality of water................... 38,189, £66 resource compilation........................ 1 saline minerals_________________________ £67 saline-water resources..................... 48 sedimentation______________________186 ,£68, £69 stiatigraphy................... 100,101,104,250 structural geology................. 104,105,108 surface water.............................. 38 uranium___________________________________ £60 urban geology............................. £60 vanadium.................................. £60 water resources__________________________ £66 waterpower.............................. £67 v Valleriite, crystal structure.................. 157 Vanadium, bibliography......................... 284 investigations in progress................ £60 Vegetation, changes in local distribution___ 192 determination of mercury in............... 200 effect on water quality................... 190 investigations in progress............... £60 mapping, statistical studies.............. 192 tolerance of salt.......................... 61 See also Plant ecology. vela uniform, Program, geologic and hydro- logic studies....................... 55 Vermont, asbestos.............................. £88 cooperating agencies...................... 224 floods.................................... £87 geologic mapping.......................... £46 geophysics................................. 81 hydrology................................. £61 talc...................................... £69 Vertebrate fossils. See Paleontology, vertebrate. Virgin Islands, cooperating agencies........... 225 ground water............................... 29 quality of water.......................... 29 water resources........................... £66 Virginia, coal................................. £86 construction and terrain problems......... £86 cooperating agencies---------------------- 224 floods.................................65, £87 geochemistry.............................. 156 geologic mapping.......................... £\6 geomorphology........................... £47 geophysics............................. 153, £48 lead and zinc............................ £61 paleontology............................ 82,83 petroleum and natural gas................ £55 petrology................................ 156 plant ecology........................... 192 precipitation studies..................... 164 quality of water.......................... 190 silica..................................... 13 stratigraphy-------------------------- 81,82 surface water..........................175, £50 tungsten................................... 5 urban geology............................. £60 water resources........................... £66 zinc.----------------------------------- £6£ Volcanic rocks, beryllium content.............. 10 geochemistry and petrology............... 155 isotopic variation of lead and strontium.. 172 minor elements........................... £88 Volcanic-terrane hydrology, investigations in progress........................... £60 Volcanoes, Hawaii............................ 166 Volcanology, investigations in progress_____ £60 results of investigations............... 166 See also Index to List of Publications W Page Wabash River basin, ground water.............. A34 Wallrock alteration, lead-zinc deposits........... 4 Washington, clay........................ 11, £84 coal...................................... £85 construction and terrain problems........ 61 cooperating agencies...................... 225 copper...................................... 4 flood studies............................. £37 geologic mapping......................£40, £46 geomorphology............................. £47 geophysics................................ £48 glacial geology....................89, III, £49 glaciology............................193, £49 ground water...........................44,178 hydraulics................................ £50 hydrology................................. £49 ilmenite................................... 11 lead and zinc............................. £61 marine hydrology.......................... £5£ monazite___________________________________ 11 petroleum and natural gas................. £55 petrology..........-...........-....... 110 quality of water...........................61, £66 radioactive-waste disposal............£6£, £68 resource compilation........................ 2 sea-water intrusion...................... 44 sedimentation.................. 184,185, £58, £69 springs................................. 44 stratigraphy................... 89,108,110, £69 structural geology........................ 110 surface water.............................. 44 uranium................................... £60 urban geology............................. £60 volcanism............................... 110 water resources_________________________ £66 waterpower------------------------------- £67 See also Pacific Northwest. Water, activity in salt lake.................. 161 analysis, flow-through system............. 204 analysis, results of investigations. __... 201 quality. See Quality of water. Water-budget studies, Florida.................. 28 Water management, Colorado..................... 39 Water supplies, public, chemical quality___ 20 Water use, effect on stream-channel width___ 176 iron and steel industry.................... 20 Rocky Mountain States.......... 36,38,39,41, 42 United States.............................. 19 Waterpower classification, investigations in progress.......................... £67 Waterpower resources, Alaska___________________ 43 Waterpower sites, classification............... 49 Wave-tank studies, ripple marks............... 186 Weathering, chemical, Monongahela River basin.............................. 59 effect on oil content of shale____________ 156 Wells, technique for anticipating clogging. 178 West Virginia, cooperating agencies.......... 225 floods____________________________________ 66 geologic mapping......................... £46 geomorphology_____________________________ £47 geophysics............................ £48 ground water_______________________________ 26 phosphate................................... 7 quality of water....................... 58,59,169 silica____________________________________ 13 surface water__________________________26,180 water resources.......................... £66 Western United States, beryllium.............. £34 hydrology............................... £61 paleobotany............................. £58 Western United States—Continued paleontology...........................A £64 radioactive-waste disposal................. £57 thorium_________________________________ £59 Western United States. See also names of individual States. Whales, fossil, as indicator of Miocene..... 139 Wisconsin, cooperating agencies............. 225 flood studies.............................. £87 geochemistry........................ 201 ,£88, £89 geologic mapping....................... £46 geophysics................................. £48 ground water_______________________ 30,176,179 hydrology.............................. 2 49 iron_______________________________________ £51 lead and zinc...................4,87, £46, £51 low-flow studies........................... £6£ mineral resources..._______________________ £5£ petrology................................. 170. £39 quality of water............................ 30 sedimentation.............................. £58 surface water............................ 179 water resources............................ £66 World’s Fair exhibit_____________________________ 1 Wyoming, coal___________________________________ £86 construction and terrain problems........... 63 cooperating agencies____-................ 225 floods................................ 69, £86 geochemistry________________________ 155, £89 geologic mapping_______________________ £46 geomorphology.............................. £47 geophysics......................63, 91, £47, £48 glacial geology............................. 91 glaciology................................. 193 gold....................................... £49 ground water...........................36,176 iron...................................... £61 mineralogy................................. 159 oil and gas fields.......................... 16 oil seeps................................... 16 oil shale.............................. 17,£68 paleobotany------------------------------ 137 paleoecology............................... £68 paleontology................................ 91 permeability studies, sandstone............ 204 petroleum and natural gas.................. £56 petrology................................. 155, £89 phosphate--------------------------------7, £66 quality of water............................ 36 saline minerals............................ £67 sedimentation...................91,184 ,£59,£61 stratigraphy.......................91,96 ,£59 structural geology........................91,98 uranium................................7,14, £60 water resources............................ £67 x, y, z X-ray analysis, tektites........................ 145 X-ray fluorescence, analysis, results of investigations...................................... 198 X-ray powder diffraction studies, use of computers in...................................... 156 Yellowstone National Park, oil seeps............. 16 Zeolites, district studies....................... 12 investigations in progress................. £67 Zinc, district studies......................... 4,87 geochemical anomaly........................ 77 See also lead and zinc. Zinc deposits, investigations in progress___£45,£6£ Zircon, hafnium-zirconium ratios................ 155 Zirconium, in volcanic rocks.................... 155 Zircon, luminescence............................ 153 magnetic susceptibility_________________ 154 U. S. GOVERNMENT PRINTING OFFICE : 1964 O - 746-002 £>&75 /-U/e&jc Pa x 50/-'3 GEOLOGICAL SURVEY RESEARCH 1964 Chapter B lU T*--------------—--- GEOLOGICAL SURVEY _____________________f_ ______________________ PROFESSIONAL PAPER 501GEOLOGICAL SURVEY RESEARCH 1964 Chapter B GEOLOGICAL SURVEY PROFESSIONAL PAPER 501 Scientific notes and summaries of investigations prepared by members of the Geologic and Heater Resources Divisions in the fields of geology, hydrology, and related sciences UNITED STATES GOVERNMENT PRINTING OFFICE, WASHINGTON: 1964UNITED STATES DEPARTMENT OF THE INTERIOR STEWART L. UDALL, Secretary GEOLOGICAL SURVEY Thomas B. Nolan, Director For sale by the Superintendent of Documents, U.S. Government Printing Office, Washington, D. C., 20402FOREWORD This collection of 46 short papers is one of a series to be released as chapters of Geological Survey Research 1964. The papers report on scientific and economic results of current work by members of the Geologic and Water Resources Divisions of the TJ.S. Geological Survey. Some of the papers present results of completed parts of continuing investigations; others announce new discoveries or preliminary results of investigations that will be discussed in greater detail in reports to be published in the future. Still others are scientific notes of limited scope, and short papers on techniques and instrumentation. Chapter A of this series will be published later in the year, and will present a summary of results of work done during the present fiscal year. Thomas B. Nolan, Director. mCONTENTS Page Foreword-------------------------------------------------------------------------------------------------------------------------- 111 GEOLOGIC STUDIES Structural geology Interpretation of the Garden Springs area, Texas, by the “down-structure” method of tectonic analysis, by P. B. King---------- B1 Cryptoexplosive structure near Versailles, Ky., by D. F. B. Black-------------------------------------------------------------- 9 A late Tertiary low-angle fault in western Juab County, Utah, by D. R. Shawe------------------------------------------------ 13 Structure of part of the Timber Mountain dome and caldera, Nye County, Nev., by W. J. Carr____________________________________ 16 Diverse recurrent movement along segments of a major thrust fault in the Schell Creek Range near Ely, Nev., by Harald Drewes---------------------------------------------------------------------------------------------------------------------- 20 Stratigraphy and paleontology Facies relations of exposed Rome Formation and Conasauga Group of northeastern Tennessee with equivalent rocks in the subsurface of Kentucky and Virginia, by L. D. Harris____________________________________________________________________ 25 Stratigraphy of the Lee Formation in the Cumberland Mountains of southeastern Kentucky, by K. J. Englund---------------------- 30 The Little Stone Gap Member of the Hinton Formation (Mississippian) in southwest Virginia, by R. L. Miller-------------------- 39 The Chattanooga Shale (Devonian and Mississippian) in the vicinity of Big Stone Gap, Va., by J. B. Roen, R. L. Miller, and J. W. Huddle____________________________________________________________________________________________________________ 43 The Wildcat Valley Sandstone (Devonian) of southwest Virginia, by R. L. Miller, L. D. Harris, and J. B. Roen--- 49 The Goose Egg Formation in the Laramie Range and adjacent parts of southeastern Wyoming, by E. K. Maughan- 53 Foraminifera from the Exogyra ponderosa zone of the Marshalltown Formation at Auburn, N. J., by J. F. Mello, J. P. Mihard, and J. P. Owens..........------------------------------------------------------------------------------------------- 61 Mineralogy and petrology Rare-earth silicatian apatite from the Adirondack Mountains, N.Y., by M. L. Lindberg and Blanche Ingram....................... 64 Ferroan northupite in the Green River Formation of Wyoming, by Charles Milton and Robert Meyrowitz.--------------------------- 66 Walsen composite dike near Walsenburg, Colo., by R. B. Johnson._______________________________________________________________ 69 Zonal features of an ash-flow sheet in the Piapi Canyon Formation, southern Nevada, by P. W. Lipman and R. L. Christiansen________________________________________________________________________________________________________ 74 A welded-tuff dike in southern Nevada, by P. W. Lipman________________________________________________________________________ 79 A new uranyl tricarbonate, K2Ca3(UO2)2(CO3)6-9-10H2O, by Robert Meyrowitz, D. R. Ross, and Malcolm Ross....................... 82 Geochemistry Fractionation of uranium isotopes and daughter products in weathered granite and uranium-bearing sandstone, Wind River basin region, Wyoming, by J. N. Rosholt, E. L. Garner, and W. R. Shields______________________________________________ 84 Hafnium content and Hf/Zr ratio in zircon from the southern California batholith, by David Gottfried and C. L. Waring. 88 Geochemical anomalies in the lower plate of the Roberts thrust near Cortez, Nev., by R. L. Erickson, Harold Masursky, A. P. Marranzino, Uteana Oda, and W. W. Janes_______________________________________________________________________________ 92 Cesium and strontium sorption studies on glauconite, by M. M. Schnepfe, Irving May, and C. R. Naeser__________ 95 Distribution of beryllium in igneous rocks, by D. R. Shawe and Stanley Bernold_______________________________________________ 105 Geophysics T-phase of May 11, 1962, recorded in Hawaii, by H. L. Krivoy and R. A. Eppley_________________________________________________ 105 Effects of the gnome nuclear explosion upon rock salt as measured by acoustical methods, by D. D. Dickey---------------------- 108 Economic geology Habit of the Rocky Valley thrust fault in the West New Market area, Mascot-Jefferson City zinc district, Tennessee, by J. G. Bumgarner, P. K. Houston, J. E. Ricketts, and Helmuth Wedow, Jr__________________________________________________________ 112 Relation of economic deposits of attapulgite and fuller’s earth to geologic structure in southwestern Georgia, by C. W. Sever_______________________________________________________________________________________________________________________ 116 vVI CONTENTS Geomorphology and glacial geology Page Profiles of rivers of uniform discharge, by W. B. Langbein---------------------------------------------------- B119 Large retrogressive landslides in north-central Puerto Rico, by W. H. Monroe__________________________________ 123 The zanj6n, a solution feature of karst topography in Puerto Rico, by W. H. Monroe............................ 126 The Charleston, Mo., alluvial fan, by L. L. Ray_______________________________________________________________ 130 Pleistocene glaciations of the southwestern Olympic Peninsula, Wash., by D. R. Crandell...........—......— 135 Sedimentation Preliminary report on bed forms and flow phenomena in the Rio Grande near El Paso, Tex., by R. K. Fahnestock and Thomas Maddock, Jr------------------------------------------------------------------------------------------ 140 Rapid method of estimating lithology of glacial drift of the Adirondack Mountains, New York, by C. S. Denny and A. W. Postel........................................................................................... 143 Analytical techniques Determination of hafnium content and Hf/Zr ratios in zircon with the direct-reading emission spectrometer, by C. L. Waring_______________________________________________________________________________________________________ 146 A spectrographic method for the determination of cesium, rubidium, and lithium in tektites, by Charles Annell_ 148 Staining of plagioclase feldspar and other minerals with F. D. and C. Red No. 2, by R. V. Laniz, R. E. Stevens, and M. B. Norman_______________________________________________________________________________________________ 152 Successful separation of silt-size minerals in heavy liquids, by Robert Schoen and D. E. Lee__________________ 154 HYDROLOGIC STUDIES Surface water Effect of seiches and setup on the elevation of Elephant Butte Reservoir, N. Mex., by G. L. Haynes, Jr________ 158 Flood inundation mapping, San Diego County, Calif., by L. E. Young and H. A. Ray.............................. 163 The relation of discharge to drainage area in the Rappahannock River basin, Virginia, by H. C. Riggs__________ 165 Ground water The artesian aquifer of the Tierra del Fuego area, Chile, by W. W. Doyel and Octavio Castillo U.._____________ 169 Quality of water A method for evaluating oil-field-brine pollution of the Walnut River in Kansas, by R. B. Leonard_____________ 173 Theoretical hydrology Computing stream-induced ground-water fluctuation, by M. S. Bedinger and J. E. Reed___________________________ 177 Use of water-level recession curves to determine the hydraulic properties of glacial outwash in Portage County, Wis., by E. P. Weeks_________________________________________________________________________________________________ 181 Tree growth proves nonsensitive indicator of precipitation in central New York, by W. J. Schneider and W. J. Conover.. 185 INDEXES Subject------------------------------------------------------------------------------------------------------------ 189 Author_____________________________________________________________________________________________________________ 191GEOLOGICAL SURVEY RESEARCH 1964 INTERPRETATION OF THE GARDEN SPRINGS AREA, TEXAS, BY THE “DOWN-STRUCTURE” METHOD OF TECTONIC ANALYSIS By PHILIP B. KING, Menlo Pork, Calif. Abstract.—Complex structures in Paleozoic rocks of the Garden Springs area, west Texas, plunge to the southwest and are capable of interpretation by the “down-structure” method of tectonic analysis. When the map is oriented so that the geologist views it in the direction of plunge, the outcrop pattern becomes a structure section, but in a near-horizontal plane rather than the vertical plane of conventional structure sections. This analysis demonstrates that the Garden Springs area contains what was originally a low-angle thrust fault that was subsequently steeply folded. In 1937 Bailey and Mackin (1937, p. 189) called attention to several “self-evident propositions in geologic map reading, some of which are not found in ordinary text books,” including: If two boundaries of a formation, under the influence of pitch, follow one another with rough parallelism across the regional strike of fold axes, then the one boundary is (structurally) at the top, and the other is (structurally) at the bottom of the formation. . . . If the observer orients the map so as to look along it in the direction of pitch, he will see the formations disposed on the flat surface of the map in much the same attitude as they would present in a vertical cross-section, though, of course, with different proportions. Mackin (1950) later termed the use of these propositions in tectonic analysis “the down-structure method of viewing geologic maps.” Knopf (1962, p. 42-A5) and Christensen (1963, p. 97-102) recently summarized the use which has been made of this method in the analysis of structures in metamorphic terranes in the Alps (where Lugeon applied it as early as 1901), the Scottish Highlands, and elsewhere,1 and they themselves used it to interpret relations of the metamorphic rocks of the Stissing Mountain area, New York, and the Hoosac Mountain area, Massachusetts. 1 The reference list by Christensen (1963, p. 107) provides the best summary of previous uses of the “down-structure” method. U.S. GEOL. SURVEY PROF. The Garden Springs area in western Texas provides an excellent example of the application of the “down-structure” method to tectonic analysis. The area was described about 25 years ago (King, 1937, p. 124-128, pi. 19B), but in a report that dealt so extensively with other matters that the example has largely escaped the notice of tectonic geologists. The features of the Garden Springs area are here illustrated by a geologic map (fig. 1), which is based on field surveys made in 1929 and 1930 and wrhich presents more data than were included in the small-scale map of the original report, and by an aerial photograph of the area taken in 1954 (fig. 2). Use of the “down-structure” method to interpret the relations shown on the map is demonstrated by structure sections (fig. 1) and by the tectonic diagrams (% 4). The Garden Springs area lies in the Marathon Basin about 10 miles south of the town of Marathon, Brewster County. The Marathon Basin exposes a sequence of Paleozoic rocks of Cambrian to Pennsylvanian age, which were deformed during late Pennsylvanian and early Permian orogenies that produced structures of the Appalachian type. The Paleozoic rocks are virtually unmetamorphosed, but their structural complexity equals that of many metamorphic terranes. General features of the Marathon Basin have been described by King (1937), and the results of later investigations have been summarized by Flawn (1961, p. 49-61). The Garden Springs area lies on the northwest flank of the Dagger Flat anticlinorium, which is one of the large uplifts of the Marathon Basin where older rocks come to the surface. The anticlinorium as a whole has many complex structures; the particular significance of the Garden Springs area is that it contains a representative sample of these structures within a relatively PAPER 501-B, PAGES B1-B8 B1B2 STRUCTURAL GEOLOGY Marathon Marathon Basin 'Area of report \w\Ga rile n\Spring st '*■ • ; V:.. . /'■ 103° 15' 2 MILES 30 30 \os 30° 00 TEXAS Area of report / oKING B3 EXPLANATION Alluvium Intrusive igneous rocks Tesnus Formation Caballos Novaculite Lower novaculite member separately mapped Maravillas Chert CO l I < in z > <^Q_ LJ Q *\ Woods Hollow Shale Fort Pena Formation Alsate Shale < o r> o Q cc O Marathon Limestone Dagger Flat Sandstone o Contact Dotted where concealed Fault Arrow shows relative direction of movement. Dotted where concealed —1— -R- ~+” Strike and dip of beds Right-side-up, inverted, and vertical ----3800---- Elevation of land surface In feet above mean sea level. Contour interval 100 feet 1 2 MILES _l Figure 1.—Geologic map and structure sections of the Garden Springs area. Geology mapped by P. B. King in 1929 and 1930; geologic mapping has not been adjusted to agree with the aerial photograph taken later (fig. 2). Inset maps show location of area in the Marathon Basin, and in the State of Texas. Rectangle ABCD outlines the area shown in the structure sections on the opposite page, and projected in the tectonic diagrams of figure 4 as rectangles ARC'D' and ARC" D". Sections are drawn at half-mile intervals and are oriented as though the geologist were looking south westward down the plunge of the folds. Consequently, sections are seen in an order opposite to that indicated on the map. Alluvial cover is thin in the area and is omitted in sections.B4 STRUCTURAL GEOLOGY Figure 2.—Vertical aerial photograph of the area shown on figure 1, at approximately the same scale. Enlarged from part of a photograph by U.S. Army Map Service taken in 1954 (photograph 2854, lot AM, western U.S. project 138; original scale 1:63,000). small compass. As elsewhere in the Marathon Basin, the sequence in the Garden Springs area consists of alternating “hard” and “soft” units, each a few hundred to more than a thousand feet thick; the “hard” and “soft” units show contrasting competency under deformation, and contrasting resistance to erosion. Within the area, the most conspicuous “hard” unit is formed by the Caballos Xovaculite (Devonian and Mississippian) and the Mara villas Chert (Upper Ordovician), which together produced prominent ridges and outcrops; a lesser “hard” unit lower in the sequence is the Fort Pena Formation (Middle Ordovician), which forms lower narrower ridges. The map and photograph of the area (figs. 1 and 2) indicate anomalous features. The ridge-making Caballos Xovaculite and Maravillas Chert form two belts of outcrop which end in hooks that face in opposite directions, one at Ridge Spring on the north, the other west of Garden Springs on the south. The hook on the south defines an anticline, but the Caballos extendsKING B5 only a little past its crest, where it is bent back on itself. The anticline is bordered on the southeast by a fault, termed the Garden Springs overthrust in the original report, which brings older Ordovician formations against the Maravillas Chert on the anticlinal flank. The northwestern flank of the anticline is also bordered by a fault, which likewise brings older Ordovician formations against the rocks of the anticline. Although the connection between the two faults is partly concealed by alluvium, they evidently join, as the older Ordovician formations outside the two faults are continuous southwestward around the nose of the anticline. These relations are especially baffling because, whereas the component formations are distinctive and easily recognizable, lie in a known stratigraphic sequence, and have a well-defined structure at any individual exposure, these local structures cannot be rationalized into any larger structure made up of the usual kinds of folds and faults. The essential clue to interpretation of the Garden Springs area is the plunge of its structures. The outcrop pattern of the anticline west of Garden Springs suggests a plunge to the southwest, which is confirmed by the dips of its component beds. The pattern of the hook-shaped outcrop at Ridge Spring suggests an anticline that plunges to the northeast, but the dip of its component beds indicates that it, too, plunges to the southwest—hence, that it is a synform, rather than an anticline in the usual sense. More specific data as to the plunge of the structures can be obtained by plotting the poles of the 111 observed strikes and dips on the lower hemisphere of an equal-area projection (figs. 3 A, B, and C). This plotting indicates a well-defined girdle that closely follows a great circle whose plane dips 60° northeast (fig. 2>D). A line normal to this plane, with a dip of 30° southwest, is approximately parallel to the plunge of the folds.2 Tectonic analysis can now proceed by means of the “down-structure” method. If the geologist turns the map so that he faces southwestward down the plunge of the folds, he will see that the map itself provides a sort of structure section. In the present example, as the topographic relief is slight, this section is in a nearly horizontal plane, rather than in the vertical plane of conventional structure sections, and hence is 2 Mackin (1950, p. 62-65) and other authors have shown that in asymmetrical plunging folds it is geometrically necessary that the direction of the plunge of the folds should diverge down the plunge from the surface traces of the folds. A disconcerting result of the present analysis is that the direction of the plunge obtained from it is nearly the same as the direction of the surface traces on the geologic map (fig. 1). However, the margin of error in determining the strike of the plane of the great circle is probably somewhat greater than 10°, and the divergence must lie within these limits. much distorted in one dimension. The gross structure thus perceived can be verified by preparation of sections showing the structure of the near-surface rocks along closely spaced, parallel lines. No single section affords much of an idea of the gross structure, yet if the sections are arranged in geographic order, with those down the plunge above those up the plunge, a blurred picture is produced that closely resembles the map pattern (fig. 1). Even more illuminating than the structure sections is a tectonic diagram, in which the map pattern is projected down the plunge into a vertical plane, the plane conventionally used in structure sections (fig. 4A). This projection can be made easily,3 by compressing the map pattern by the desired amount in a northeast-southwest direction. If all the structures exposed at the surface were cylindrically persistent throughout the area, such a diagram would perfectly express the gross structure, which, at localities up the plunge is now largely removed by erosion, and at localities down the plunge lies beneath the surface. But complete persistence of structures is unlikely in nature; therefore, the tectonic diagram merely provides the geologist with a picture of the style of the gross structure with which he is dealing. Although a tectonic diagram projected into a vertical plane provides a picture of the gross structure as it would appear in a conventional structure section, it is nevertheless not a true representation of the deformation. A true representation in an area of plunging folds is in a plane normal to the plunge, and this will differ more or less from representation in a vertical plane, depending on the steepness of the plunge. In the present example, where the folds plunge 30° southwest, true representation of the deformation is in a plane dipping 60° northeast (fig. 4B); even in this example where the plunge is low, note that representation is perceptibly less distorted in a plane normal to the folds than in a vertical plane. Interpretation of the features which are revealed by the “down-structure” method in the Garden Springs area, and elsewhere in the Dagger Flat anticlinorium, have been set forth elsewhere (King, 1937, p. 124-128). Suffice it to say that the Garden Springs area must contain what was originally a low-angle thrust fault, the 3 To prepare a tectonic diagram in the desired plane: Trace the generalized map pattern onto a rectangle made up of a grid of squares; the rectangle is so oriented that one dimension is parallel to, and the other dimension at right angles to, the plunge of the folds. By means of a grid of rectangular coordinates, transfer the pattern points onto a second rectangle oriented similarly to the first. The sides of this second rectangle and of the smaller rectangles subdividing it that lie at right angles to the plunge have the same lengths as the similar elements in the first rectangle. However, the sides parallel to the plunge have the lengths to which the similar elements in the first rectangle would be reduced if projected onto the desired plane.B6 STRUCTURAL GEOLOGY C D Figure 3.—Diagrams prepared to calculate plunge of folds in Garden Springs area, showing poles of observed strikes and dips of bedding, plotted and contoured on lower hemisphere of an equal-area projection. A. Right-side-up beds and vertical beds; poles of 69 observations, including 6 observations on inverted beds in synform at Ridge Spring; contour interval 9 percent of 1 percent of area. B. Inverted beds; poles of 42 observations; contour interval 20 percent of 1 percent of area. C. All observations on bedding; poles of 111 observations; contour interval 10 percent of 1 percent of area. D. Summary diagram : a, outer contour on right-side-up beds; 6, outer contour on inverted beds. I, maximum of poles of right-side-up beds on southeast flanks of folds; II, maxima of poles of right-side-up beds on northwest flanks of folds; III, maximum of poles of vertical beds; IV, maxima of poles of inverted beds on northwest flanks of folds. x-x’, great circle which approximates the girdle shown by the contours, whose plane dips 60° northeast. A line normal to this plane dips 30° southwest, and is approximately parallel to the plunge of the folds.A Northwest B Figure 4.—Tectonic diagrams that summarize the structure of the Garden Springs area. A, surface outcrop pattern of area ABCD of figure 1 projected into a vertical plane, ABC'D', the plane used in conventional structure sections; vertical transverse faults are omitted from outcrop pattern used. B, a similar projection into a plane normal to the plunge of the folds, ABC'D", or with a dip of 60° northeast (fig. 3D) ; note the lesser vertical distortion than in A. Diagrams are oriented in the same manner as the structure sections of figure 1. WB8 STRUCTURAL GEOLOGY Garden Springs overthrust, which was subsequently folded. The synform at Ridge Spring was produced by drag of the Caballos Novaculite and Maravillas Chert on the leading edge of the upper plate of the thrust. Comparable drag on the lower plate of the thrust occurs where the Caballos is bent back on itself near the anticlinal crest west of Garden Springs. The anticline near Garden Springs in the Caballos, Maravillas, and older formations of the lower plate is evidently a younger feature, formed during folding of the thrust. Perhaps at about the time of this folding, the whole structure acquired its plunge to the southwest. One other significant structural item in the Garden Springs area has not so far been mentioned—the host of minor transverse faults. These were not considered in the preceding analysis because they are probably younger than the folding and thrust faulting, and because they merely blur, but do not obliterate the map pattern of the earlier structures. Many transverse faults were located during the field survey (fig. 1), and more are evident on the aerial photograph (fig. 2). As mapped, all of them are of short length, and all lie in the “hard,” competent units, especially the Caballos Novaculite and Maravillas Chert. Although it is impossible to trace the transverse faults into the ad- jacent “soft,” incompetent units, the presumption is great that they die out there. Gently dipping slicken-sides on the surfaces of many of the transverse faults indicate that they have a large component of strike-slip displacement; in the Garden Springs area this displacement is mainly left-lateral. Probably the transverse faults originated during a late phase of the Paleozoic deformation, and they may have resulted from a greater northwestward surge of the central part of the Dagger Flat anticlinorium than of its northeastern and southwestern ends. REFERENCES Bailey, E. B., and Maekin, J. H., 1937, Recumbent folding in the Pennsylvania Piedmont; a preliminary statement: Am. Jour. Sci., 5th ser., v. 33, no. 195, p. 187-190. Christensen, M. N., 1963, Structural analysis of Hoosac nappe of northwestern Massachusetts: Am. Jour. Sci., v. 261, no. 2, p. 97-107. Flawn, P. T., 1961, The Marathon area, in Flawn, P. T., Goldstein, August, Jr., King, P. B., and Weaver, C. E., The Ouachita system: Texas Univ. Pub. 6120, p. 49-58. King, P. B., 1937, Geology of the Marathon region, Texas: U.S. Geol. Survey Prof. Paper 187,148 p. Knopf, E. B., 1962, Stratigraphy and structure of the Stissing Mountain area, Dutchess County, New York : Stanford Univ. Pubs. Geol. Sci., v. 7, no. 1, p. 1-55. Maekin, J. H., 1950, The down-structure-method of viewing geologic maps: Jour. Geology, v. 58, no. 1, p. 55-72.GEOLOGICAL SURVEY RESEARCH 1964 CRYPTOEXPLOSIVE STRUCTURE NEAR VERSAILLES, KENTUCKY By DOUGLAS F. B. BLACK, Lexington, Ky. Work done in cooperation with the Kentucky Geological Survey Abstract.—A circular structure nearly a mile in diameter was mapped 3% miles northeast of Versailles, Ky. This structure, of undetermined origin, consists of a brecciated central dome, a marginal structural depression partly bounded by normal faults, and, on the east, an outer semicircular anticline of low amplitude. A previously unreported cryptoexplosive structure approximately 5,000 feet in diameter was discovered by E. R. Cressman and the author 3i/2 miles northeast of Versailles, Woodford County, Ky. (fig. 1), in October 1962 and has since been mapped by the author at a scale of 1: 24,000. A. M. Miller (1924) mapped an elongate graben that in part coincides with the arcuate graben on the north side of the cryptoexplosive structure, though his map does not show the circular nature of this structure or its extent. The term “cryptoexplosive” (Dietz, 1946) is used because it has little-genetic implication. Versailles is in the central Blue Grass region of Kentucky. Topographic relief is gentle, soils are deep, and outcrops generally sparse. The geologic map (fig. 2) is based on about 100 outcrops within and adjacent to the structure. The nearly circular feature is expressed physiographically by an almost continuous ring of small sinkholes. Rocks exposed in the structure are Middle and Upper Ordovician carbonates with some beds of shale and comprise the upper part of the Lexington Limestone, the Cynthiana Formation, and the basal part of the Million Shale of Nickles (1905). The cryptoexplosive structure consists of a central uplift, a nearly circular marginal structural depression bounded by arcuate normal faults, and on the east an outer rim of gentle anticlinal folds which flank the marginal depression. Figure 1.—Location of the Versailles cryptoexplosive structure and similar structures in Kentucky and the surrounding States. The central uplift of the structure is shown as an asymmetrical dome. This interpretation is borne out by all observed outcrops, though much of the central area is concealed. Numerous outcrops of coarsely brecciated limestone containing large blocks derived from beds of the Lexington Limestone and the lower part of the Cynthiana Formation are exposed near the center of the central uplift. This area, shown on the map as undifferentiated Cynthiana Formation and Lexington Limestone, may be intricately crosscut by faults or possibly underlain by a lens of limestone breccia. The crest of the dome is uplifted relative to the marginal depression, but the rocks in the central uplift have little stratigraphic throw compared with undisturbed beds surrounding the structure. U.S. GEOL. SURVEY PROF. PAPER 501-B, PAGES B9-B12 B9BIO STRUCTURAL GEOLOGY 84°41'00" 38° 05' 00" Figure 2.—Geologic map of the cryptoexplosive structure near Versailles, Ky.BLACK Bll The marginal structural depression is bounded, at least in part, by normal faults, many of which are readily defined by well-developed zones of breccia and in some cases by moderate to steeply dipping beds adjacent to the faults. The faults are presumed to be high-angle ones, but no accurate dip measurements were obtained because of poor exposure and very low topographic relief. The maximum downward displacement of strata in the depression is slightly more than 100 feet relative to undisturbed rocks surrounding the structure. An asymmetrical synclinal fold in the marginal depression, having a steeper limb on the northeast, can be seen in upper Cynthiana and basal Million rocks exposed above the stock pond 1,000 feet northeast of the junction of the Heddon and Big Sink Roads. This folding may be the result of settling and readjustment of faulted blocks subsequent to initial faulting. The curved anticlinal folds outside the marginal depression are apparently restricted to the eastern margins of the structure. These folds are generally of low amplitude and are located in the field only by small altitude differences on key beds. Folded strata with measurable dip occur locally along the southern edge of the structure. The limestone breccias of this structure are believed to be finer grained than those described by Eggleton and Shoemaker (1961) from the Sierra Madera structure in Texas, but they seem otherwise very similar. The Versailles breccias consist of angular limestone blocks, some of which are several feet across, enclosed in a matrix of smaller fragments of more than one rock type. The youngest rocks known to have been involved in this cryptoexplosive structure belong to the basal part of the Million Shale of Nickles (1905), thus, the structure is of Late Ordovician or younger age. The similarity of the Versailles structure to structures of known and supposed meteorite-impact origin, and the high degree of brecciation, otherwise rare in this region, may indicate a similar origin for the Versailles structure. The possibility of volcanic origin as postulated by Bucher (1933,1936) for some structures of this type cannot yet be abandoned here, although no evidence of volcanism has been found. Previously described structures which seem especially similar to this include the Crooked Creek structure, Missouri (Hendricks, 1954); Jeptha Knob, Kentucky (Bucher, 1925); Middlesboro Basin, Kentucky (Englund and Roen, 1963); the Flynn Creek disturbance, Tennessee (Wilson and Born, 1936; Conant and Swanson, 1961, p. 9-12); the Wells Creek Basin, Tennessee (Bucher, 1936, p. 1066-1070); the Howell structure, Tennessee (Born and Wilson, 1939); the Serpent Mound structure, Ohio (Bucher, 1936, p. 1061-1064; Heyl and Brock, 1962); and the Sierra Madera structure, Texas (King, 1930). Because of the small diameter of the Versailles structure, further detailed study to determine its nature and origin might prove to be less costly than similar studies of larger cryptoexplosive structures. Such a study might include a closer search for shatter cones such as those described by Dietz (1959), a coring program designed to determine the subsurface structure, tests for shock-induced thermoluminescence, both at the surface and at depth (Angino, 1959; Roach and others, 1961, 1962), and tests for high-pressure minerals (Chao and others, 1960, 1962). REFERENCES Angino, E. E., 1959, Pressure effects on thermoluminescence of limestone relative to geologic age: Jour. Geophys. Research, v. 64, no. 5, p. 569-573. Bom, K. E., and Wilson, C. W., Jr., 1939, The Howell structure, Lincoln County, Tennessee: Jour. Geology, v. 47, p. 371-388. Bucher, W. H., 1925, Geology of the Jeptha Knob: Kentucky Geol. Survey, ser. 6, v. 21, p. 193-237. --------1933, Volcanic explosions and overthrusts: Am. Geophys. Union Trans., 14th ann. mtg., p. 238-242. ------ 1936, Cryptovolcanic structures in the United States [with discussion] : Internat. Geol. Congress, 16th, v. 2, p. 1055-1084. Chao, E. C. T., Shoemaker, E. M., and Madsen, B. M.„ I960, First natural occurrence of coesite: Science, v. 132, no. 3421, p. 220-222. Chao, E. C. T., Fahey, J. J., Littler, Janet, and Milton, D. J., 1962, Stishovite, SiC>2, a very high pressure new mineral from Meteor Crater, Arizona: Jour. Geophys. Research, v. 67, no. 1, p. 419^421. Conant, L. C., and Swanson, V. E., 1961, Chattanooga shale and related rocks of central Tennessee and nearby areas: U.S. Geol. Survey Prof. Paper 357, 91 p. Dietz, R. S., 1946, Geological structures possibly related to lunar craters : Pop. Astronomy, v. 54, p. 465-467. ------ 1959, Shatter cones in cryptoexplosion structures (meteorite impact?) : Jour. Geology, v. 67, p. 496-505. Eggleton, R. E., and Shoemaker, E. M., 1961, Breccia at Sierra Madera, Texas: Art. 342 in U.S. Geol. Survey Prof. Paper 424-D, p. D151-D153. Englund, K. J., and Roen, J. B., 1963, Origin of the Middlesboro Basin, Kentucky: Art. 184 in U.S. Geol. Survey Prof. Paper 450-E, p. E20-E22. Hendricks, H. E., 1954, The geology of the Steelville quadrangle, Missouri: Missouri Geol. and Water Resources Survey, v. 36, ser. 2, p. 52-70. Heyl, A. V., and Brock, M. R., 1962, Zinc occurrence in the Serpent Mound structure of southern Ohio: Art. 148 in U.S. Geol. Survey Prof. Paper 450-D, p. D95-D97. King, P. B., 1930, The geology of the Glass Mountains, Texas; pt. 1, Descriptive geology: Texas Univ. Bull. 3038, p. 123-125. [1931] -2 725-328 O—64-B12 STRUCTURAL GEOLOGY Miller, A. M., 1924, Geologic map of Woodford County, Kentucky : Kentucky Geol. Survey, ser. 6, 1950 reprint. Nickles, J. M., 1905, The Upper Ordovician rocks of Kentucky and their Bryozoa: Kentucky Geol. Survey Bull. 5, 64 p. Roach, C. H., Johnson, G. R., McGrath, J. G., and Spence, F. H., 1961, Effects of impact on thermoluminescence of Yule Marble: Art. 272 in U.S. Geol. Survey Prof. Paper 424-0, p. C342-C346. Roach, C. H., Johnson, G. R., McGrath, J. G., and Sterrett, T. S., 1962, Thermoluminescence investigations at Meteor Crater, Arizona: Art. 149 in U.S. Geol. Survey Prof. Paper 450-D, p. D98-D103. Wilson, C. W., Jr., and Born, K. E., 1936, The Flynn Creek disturbance, Jackson County, Tennessee: Jour. Geology, v. 44, p. 815-835.GEOLOGICAL SURVEY RESEARCH 1964 A LATE TERTIARY LOW-ANGLE FAULT IN WESTERN JUAB COUNTY, UTAH By DANIEL R. SHAWE, Denver, Colo. Abstract.—A low-angle fault in western Juab County, Utah, has moved Cambrian carbonate rocks at least 1 mile over late Tertiary volcanic rocks. Tuff beneath the fault is probably correlative with tuff that contains large beryllium deposits at Spor Mountain; this or similar faults therefore may conceal additional deposits. A low-angle fault about 10 miles southeast of the Spor Mountain beryllium deposits, in western Juab County, Utah (fig. 1), has moved Cambrian carbonate rocks at least 1 mile over volcanic rocks that are prob- 113°15' 113°00' Figure 1.—Map showing location of low-angle fault and beryllium deposits. U.S. GEOL. SURVEY PROF. ably Miocene and Pliocene in age. It is thus the youngest low-angle fault of this magnitude now known in the region. A tuff unit underlying the fault may be correlative with tuff that contains large beryllium deposits at Spor Mountain, and therefore this fault or others like it may in places conceal additional beryllium deposits. The fault, which is exposed on three sides of a group of hills (fig. 2) about 2 miles east of the north end of the Drum Mountains, was mapped in August 1963 by the author and Stanley Bernold during a study of Tertiary volcanic rocks related to the beryllium deposits at Spor Mountain. The upper plate of the low-angle fault consists of at least several hundred feet of carbonate rocks, mostly dolomite, that are folded and brecciated. The carbonate rocks are recrystallized and apparently unfossilif-erous. They are dominantly thin- to thick-bedded gray dolomite, but locally they contain layers of light-pinkish-brown dolomite as much as several tens of feet thick. Probably the upper plate consists of more than one formation (M. H. Staatz, oral communication, 1963). On the State map of Utah the carbonate rocks in this area are termed the Notch Peak Limestone of Late Cambrian age (Stokes and Hintze, 1963). The rocks beneath the low-angle fault consist of two units of gently tilted rhyolitic welded tuff and one of water-laid vitric-lithic tuff. The tuffs contain moderate to abundant amounts of quartz, sanidine, and biotite crystals, and lithic fragments. The oldest unit is light-brown rhyolitic welded tuff a few hundred feet thick. It is lithologically similar to, and in the same stratigraphic position as, rhyolitic welded tuff of probable Miocene age in the Thomas Range about 10 miles to the northwest. The tuff in the Thomas Range is probably nearly the same age as quartz-sanidine crystal tuff which M. H. Staatz (1963, p. M12) reported as 20 million years old on the basis of a Larsen-method age determination on zircon (Jaffe and others, 1959, p. 71). PAPER 501—B, PAGES B13-B15 B13B14 STRUCTURAL GEOLOGY EXPLANATION 'T' 5 Topaz-bearing rhyolite UNCONFORMITY i____ L Water-laid tuff » < I Black to gray glassy welded tuff > o; a. UJ t- Light-brown ^ welded tuff Carbonate rocks Contact Dashed where approximately located High-angle fault Dotted where concealed -»—*—»—w~ Low-angle fault Sawteeth on upper plate 0 12 MILES 1 __I__I___I___I___I_________________I Figure 2.—Geologic map of area of low-angle fault. Location of area shown on figure 1. Overlying the light-brown welded tuff is a sheet of black to gray glassy welded tuff 50 to 100 feet thick. The base of this unit is black vitrophyre that contains moderate amounts of crystals and fragments of carbonate rocks and volcanic rocks. The welded tuff above the basal vitrophyre contains abundant flattened perlitic lapilli of black pumiceous vitrophyre, as well as other fragments and crystals, all in a gray matrix. This unit is correlated here with a welded tuff that overlies the rhyolite of probable Miocene age 4 miles to the north in the Thomas Range. Above the black to gray welded tuff is a unit of light-yellowish-brown and light-pinkish-brown water-laid bedded tuff, 50 to 200 feet thick, which contains numerous fragments of pumice, other volcanic rocks, carbonate rocks, and other sedimentary rocks, and crystals. This unit is correlated here with vitric tuff in the Thomas Range considered by Staatz (1963, pi. 1) to be Pliocene(?). Locally, near high-angle faults (fig. 2) the water-laid tuff unit has been hydro-thermally altered to a soft rock that contains abundant montmorillonite showing ghostlike relics of original texture. Such rock looks lithologically very similar to the altered and mineralized tuff at Spor Mountain. Southeast of the low-angle fault, topaz-bearing rhyolite flows aggregating as much as several hundred feet in thickness overlie these three tuff units unconform-ably; elsewhere the flows mostly lie conformably on the water-laid tuff. The topaz-bearing rhyolite is light gray, flow layered, and contains sparse phenocrysts of quartz and sanidine in an aphanitic groundmass. Locally abundant lithophysae and vugs contain small crystals of topaz and quartz. This rhyolite unit is also assigned to the Pliocene (?) by Staatz (1963, pi. 1). The low-angle fault is nearly horizontal at the north end of the hills shown in figure 3 and dips about 15° southwest at the south end of the hills. Locally the dip of the fault surface may vary as much as 5°. Beneath the fault, water-laid tuff is virtually undisturbed except in a zone of pulverized material within a few inches of the fault surface (fig. 4). Bedding in the tuff is virtually parallel to the fault. Decrease in thickness of the water-laid tuff from north to south (fig. 2) could be the result of slight truncation by the Figure 3.—View of low-angle fault at northeast side of mapped area. Black outcrop at foot of hills is part of basal vitrophyre of black to gray glassy welded tuff. White layer is water-laid tuff; upper contact of tuff is low-angle fault. Above the fault are Cambrian carbonate rocks.SHAWE B15 Figure 4.—Closeup view of low-angle fault at northwest side of mapped area. Brecciated carbonate rock overlies water-laid tuff along contact, near end of pick handle. Tuff is undisturbed except where pulverized within 2 inches of fault. fault, although it also could be attributed to difference in original thickness. Above the low-angle fault, carbonate rocks are considerably deformed. Strikes are variable, and beds dip as much as 30° into the underlying fault plane. Breccia cemented by carbonate and by dark-brown silica (jasperoid) is common in many places close to the fault and appears in some places 100 feet or more above the fault. Breccia consisting of pieces of carbonate rock separated by thin gouge layers is widespread within a few feet of the fault (fig. 4). Locally the gouge and breccia are irregularly sheeted subparallel to the low-angle fault. Folds with amplitudes of at least 100 feet are evident locally. The upper plate contains several high-angle and low-angle faults that do not extend into underlying rocks. The low-angle fault cuts rocks as young as the water-laid tuff of Pliocene (?) age, and as it is offset by a normal fault older than the topaz-bearing rhyolite flows also of Pliocene(?) age (fig. 2), it is dated as Pliocene(?). The high-angle faults that have displaced the low-angle fault (fig. 2) are probably of basin-range type. They bound a horst whose uplift accounts for a large part of the relief shown by the hills in which the low-angle fault is exposed. The low-angle fault may mark the base of a regional plate or a local plate. This distinction would become important if beryllium deposits in water-laid tuff prove to be widespread in the vicinity of Spor Mountain. In other words, if the fault is local, the Cambrian rocks of the upper plate may conceal tuff only within the area of figure 2, but if regional, Cambrian rocks may conceal beryllium-bearing volcanic rocks in other places, making other carbonate-rock areas of potential interest for beryllium exploration. REFERENCES Jaffee, H. W., Gottfried, David, Waring, C. L., and Worthing, H. W., 1959, Lead-alpha age determinations of accessory minerals of igneous rocks (1953-1957) : U.S. Geol. Survey Bull. 1097-B, p. 65-148. Staatz, M. H., 1963, Geology of the beryllium deposits in the Thomas Range, Juab County, Utah: U.S. Geol. Survey Bull. 1142-M, p. M1-M36. Stokes, W. L., and Hintze, L. F., 1963, Geologic map of northwestern Utah: Utah Geol. and Mineralog. Survey.GEOLOGICAL SURVEY RESEARCH 1964 STRUCTURE OF PART OF THE TIMBER MOUNTAIN DOME AND CALDERA, NYE COUNTY, NEVADA By W. J. CARR, Denver, Colo. Work done in cooperation with the U.S. Atomic Energy Commission Abstract.—The center of the Timber Mountain caldera northeast of Beatty is a structural dome in a thick sequence of ash-flow tuffs. Doming resulted in two episodes of faulting: an arcuate system of faults that were intruded by possible ring dikes, and graben faults that resulted in irregular collapsed segments in the middle of the dome. Timber Mountain, on the western edge of the Nevada Test Site, is a domal uplift in the center of the Timber Mountain caldera (fig. 1). The uplift is dissected by a radial drainage system and culminates in 2 high points more than 7,000 feet in altitude. A central topographic trough trending roughly east-west between the high points contains Cat Canyon and its subordinate valleys (fig. 2). The dome is elliptical in plan, measuring about 10 by 8 miles; the long dimension trends northwest. An arcuate, relatively low lying area about 5 miles wide surrounds the dome on all but the west side. This moatlike depression is drained by Fortymile Canyon on the east and by Beatty Wash on the south. In general the rocks on Timber Mountain dip outward toward the moat. The southeastern part of the dome, where erosion has cut into the flanks of the uplift and has exposed the underlying structure, is described in this preliminary article. Also, a brief history of the center of the caldera as interpreted from structural evidence in and around Timber Mountain is presented. STRATIGRAPHY More than 3,000 feet of tuff is exposed within the Timber Mountain dome. The tuffs of Timber Mountain (fig. 2) are more than 2,500 feet thick and occupy most of the area discussed here. They are probably a composite ash-flow sheet as defined by Smith (1960, B16 116'30' Figure 1.—Index map of the Timber Mountain caldera, showing topographic outlines and area of figure 2 (shaded outline). p. 158). No air-fall tuffs are present between ash flows in this sheet, and in some areas virtually the entire section of tuff is welded. In many places, individual ash flows can be distinguished only with difficulty, if at all. Devitrification of originally glassy pyroclastic material is complete nearly everywhere. In the following discussion the tuffs of Timber Mountain have been divided into units 1, 2, and 3, from oldest to U.S. GEOL. SURVEY PROF. PAPER 50X-B, PAGES B16-B19CARR B17 youngest (fig. 2). The base of the tuffs is not exposed, but the top is well exposed at the eastern end of Cat Canyon where the tuffs of Timber Mountain are un-conformably overlain by bedded tuffs, tuffaceous sandstones, and ash-flow tuffs. These younger ash-flow tuffs lap out onto the dome in this area. In the same area, at the mouth of Cat Canyon, but stratigraphically higher, are local silicic lava flows, basalt of Fortymile Canyon, poorly welded tuff of the Thirsty Canyon Tuff, basalt of Buckboard Mesa, and much interbedded, locally tuffaceous conglomerate, sandstone, and colluvium. These rocks fill the moat and lap out onto the dome. No outcrops of the Piapi Canyon Formation, a thick sequence of ash-flow tuffs that is older than the tuffs of Timber Mountain, have been identified on the Timber Mountain dome. The Piapi Canyon is extensive elsewhere on the test site, but is exposed mainly outside the caldera. STRUCTURE Part of the structural history of the Timber Mountain uplift can be interpreted from the structural relations of the rocks exposed in the southeastern part of the dome (figs. 1 and 2). Large faults of the dome affect all rocks up to and including the tuffs and sandstones immediately overlying the tuffs of Timber Mountain, but displacements in the younger rocks locally are somewhat smaller than in the older rocks. Minor faulting began in the Timber Mountain area before deposition of the tuffs of Timber Mountain was completed, but the oldest major structure of the southeastern part of the dome is an arcuate zone of faulting, here called the inner ring fracture, that cuts the tuffs of Timber Mountain near the edge of the moat fill (fig. 2). The zone, which is about a mile wide, is exposed for about 3 miles, and may extend farther in areas covered by younger rocks. In general the inner ring-fracture zone parallels the strike of the tuffs and consists of branching normal faults which individually have small displacements, but which together have considerable displacement. The main fault of the zone can be traced for several miles. It probably dips toward the moat at about 45° to 65° in places, and is thus nearly parallel to the dip of the tuffs on the down thrown side (fig. 2, section). In most places it occurs at about the same stratigraphic position and results in the omission of several hundred feet of unit 2 of the tuffs of Timber Mountain. Many strike faults on the moat side of this main fault dip more steeply and cause numerous repetitions of unit 3. These faults are less persistent and some may dip inward and end against the main fault. Along the main fault in the ring-fracture system is a chain of small rhyolitic intrusions. These dikes, together with stratigraphic position, aid in tracing this fault. Many of the intrusions are brecciated, but the wallrocks are relatively undisturbed, indicating either possible movement on the fault during emplacement of the dike, or autobrecciation of the dike. Along the south side of the dome, tuffs inside the main fault of the inner ring-fracture zone generally dip away from the dome at angles of less than 35°. In the outer part of the zone, outside the main fault, the same tuffs commonly dip outward at more than 35°, and local dips as high as 65° are observed along the south edges of the dome. A second large structural feature of the map area is a group of granite porphyry intrusions (fig. 2) containing alkali feldspar, zoned plagioclase, and biotite phenocrysts in a fine-grained matrix of quartz and alkali feldspar. The largest exposure of this rock is about 4,500 feet long and 1,500 feet wide. Although the intrusions are irregular in shape they tend to be elongated in a northeasterly direction, and they form a group that trends about N. 45° E., which closely parallels the ring-fracture zone. The mapped intrusions join at depth, as indicated by the downward widening of individual bodies, and by the presence of a roof pendant in one place. They are restricted to the stratigraphically lowest part of unit 1, and contacts with unit 2 are probably faults. In at least one place the line of intrusions is displaced by a system of northwestward-trending graben faults. Horsts and grabens, which control the topography of the central trough area of the Timber Mountain dome, trend from nearly due west to about N. 50° W., and intersect the inner ring-fracture zone at fairly large angles in the southeastern part of the dome. Most of the northwest-trending faults clearly offset the inner ring-fracture system, and the faults bounding one graben displace the granite porphyry intrusions. The grabens appear to be the result of relative subsidence of elongate irregular blocks on fairly steep normal faults, perhaps as illustrated by Smith (1961, p. D148). In the center of the graben zone of eastern Cat Canyon are several small, shallow rhyolitic intrusions (fig. 2) that tend to enlarge upward and probably reached the surface in places. They cut the youngest ash flows of unit 3, and in a few places overlie these tuffs, separated from them by a thin tuff breccia. The age of these intrusions with respect to faulting is uncertain, but their distribution suggests that they are related to the formation of the grabens. Postgraben structural movement is not well recorded within the area shown on figure 2. Some small faults of northwesterly trend, parallel to the graben system,B18 STRUCTURAL GEOLOGYCARR B19 EXPLANATION Qac Alluvium and colluvium QTg * Gravel, tuffs, and colluvium of the caldera fill Tt Thirsty Canyon Tuff Tb Basalt of Fortymile Canyon and interbedded sediments Trt Rhyolitic flows and tuffs Includes some Tts. Queried where identification uncertain UNCONFORMITY Tts Tuffs and tuffaceous sediments Includes some tuffs of younger age UNCONFORMITY > x < z x UJ H < D O >■ X X UJ I- -x r > < A v Tr <£- > Rhyolite flows and shallow intrusions \" l-Td / i ' , Granite porphyry Rhyolitic dikes and small plugs Tuffs of Timber Mountain Stippled, unit S Shaded, unit 2 Hachured, unit 1 Contact Fault Dotted where concealed Main fault or fracture system Dotted where concealed Strike and dip of beds 25 Strike and dip of flow layering Figure 2.—Generalized geologic map and section of the southeastern corner of the Timber Mountain quadrangle, Nye County, Nev., by W. J. Carr and W. D. Quinlivan, 1962. may be later than the grabens. A few minor faults, mostly of northerly trend, cut the younger rocks of the moat area, including the ash-flow tuffs of the Thirsty Canyon. Gravels (fig. 2, section) in the Cat Canyon area probably were not displaced significantly by movement on the graben faults, but the Thirsty Canyon Tuff exposures on the flanks of the dome in the Cat Canyon area (fig. 2) are about 500 feet structurally higher than in the moat to the east. Some post-Thirsty Canyon Tuff uplift seems necessary to account for this difference in altitude. STRUCTURAL HISTORY The foregoing evidence leads to a tentative interpretation of the history of the Timber Mountain dome and inner moat area. Faulting began before deposition of the tuffs of Timber Mountain was completed, as some faults do not cut the youngest of these tuffs. Shortly after deposition of the tuffs, the Timber Mountain area was domed, probably by upward magma pressure. The central part of this “blister” failed along an inner ring-fracture zone that may have been controlled by fractures developed during caldera collapse. This zone consisted of a persistent outward-dipping fault with associated, possibly antithetic, faults. Blocks were rotated and dips steepened on the downthrown side of the main fault. The relatively consistent stratigraphic position of the main fault in the ring-fracture zone indicates that the zone predates most of the other faults in the area. Small silicic intrusions occurred along the main fault of the ring fracture, and granite porphyry was intruded into the lower part of the tuffs, coming nearest the surface in the general area of the inner ring-fracture zone to form a possible ring dike. Tuffs and sandstones were deposited on the rising dome with minor angular unconformity. In the later stages of doming, grabens were formed. This faulting was followed or accompanied by extrusion of rhyolite in the moat and intrusion of shallow rhyolite plugs in the Cat Canyon area. The moat rhyolites are cut by only a few very small faults. The moat was partially filled with sedimentary and volcanic rocks, including the ash-flow tuffs of the Thirsty Canyon. Structural relief of these tuffs on the dome indicates that minor uplift of Timber Mountain recurred subsequent to their deposition. REFERENCES Smith, R. L., 1960, Zones and zonal variations in welded ash flows: TJ.S. Geol. Survey Prof. Paper 354—F. ----- 1961, Structural evolution of the Valles caldera, New Mexico, and its bearing on the emplacement of ring dikes: Art. 340 in U.S. Geol. Survey Prof. Paper 424-D, p. D145-D149.GEOLOGICAL SURVEY RESEARCH 1964 DIVERSE RECURRENT MOVEMENT ALONG SEGMENTS OF A MAJOR THRUST FAULT IN THE SCHELL CREEK RANGE NEAR ELY, NEVADA By HARALD DREWES, Denver, Colo. Abstract.—Normal faulting, then low-angle gravity sliding, and finally renewed normal faulting occurred along a segment of an earlier thrust fault. Along this segment the later faults appear to have followed virtually the same fault plane, but the relative direction of movement was reversed. The Schell Creek Range extends north-south 100 miles in central-eastern Nevada. The part of the range shown in figure 1 is underlain by Paleozoic sedimentary rocks and Tertiary sedimentary and volcanic rocks. Some large structural features of this part of the range have been described briefly by Spurr (1903, p. 44-47), Misch and Easton (1954), and Drewes (1960). Part of the northern end of the range has been mapped by Young1 (1960). Current work in the central part of the range indicates that there were at least four episodes of deformation: (1) Mesozoic or early Tertiary low-angle faulting, thought to be chiefly thrust faulting during which faults were formed and gently folded during or after faulting; (2) middle Tertiary normal faulting; (3) middle or late Tertiary low-angle faulting, thought to be glide faulting in which faults were formed solely by gravity and not pushed laterally; and (4) late Tertiary or Quaternary normal faulting. Complicated relations between structures account for some of the difficulties in dating the faults and explaining their origin. Normal faults locally follow the plane of weakness of older structures and are deflected along parts of thrust faults, so that their strikes are changed slightly and their dips are decreased. Glide plates have moved on, or close to, stripped parts of earlier thrust faults. Parts of thrust plates that moved eastward or northeastward were later shifted westward along deflected normal faults, so that some blocks across the thrust faults apparently moved in different directions. The relations between these structures are generalized on figure 1. On the map the fault symbols overlap where recurrent movement is inferred; in the structure section the sequence of fault movements is indicated by numbers. Low-angle, near-bedding-plane faults that cut the Paleozoic rocks have reduced the normal stratigraphic sequence from a thickness of about 5 miles to about 3% miles. The Paleozoic rocks consist of marine limestone, dolomite, quartzite, and interbedded shale. The low-angle faults commonly lie along, or close to, the contacts between units of markedly different competence. In many places the faults parallel the bedding, although in other places, beds above or on both sides of such faults are inclined toward the faults at angles of more than 30°; thus the low-angle faults are not strictly bedding-plane faults. The structures in the Paleozoic rocks differ from those in the Tertiary rocks, suggesting that the older structures were formed in a structural environment different from that of the younger ones. In the Paleozoic rocks, beds along the faults are generally missing rather than repeated, but locally some slices of rock are shingled. The plates between adjacent low-angle faults are broken into numerous large blocks that have been rotated along horizontal axes, with respect to adjacent blocks, mainly by normal faults but also by reverse faults and subsidiary low-angle faults. Some small low-angle faults die out along their strike, merge at low angles with adjacent faults, or separate disharmonic plates; some larger faults are truncated by others higher in the section or end against tear faults. SCHELL CREEK RANGE THRUST FAULT The Schell Creek Range thrust fault has been mapped for 18 miles along the range and may extend 1 J. C. Young, 1960, Structure and stratigraphy in the north-central Schell Creek Range, eastern Nevada : Princeton Univ., Ph. D. thesis. B20 U.S. GEOL. SURVEY PROF. PAPER 501-B, PAGES B20-B24DREWES B21 114° 39° 15' N A Figure 1.—Generalized geologic map of part of the Schell Creek Range, Nev., showing segments of a thrust fault, normal faults, and a glide fault. Where they merge they are shown by separate symbols only for clarity; actually they are superposed or very nearly parallel. Numbers in structure section indicate sequence of development. A 12,000' 8000' 6000' ■12.000' 10.000’ 8000' 6000' EXPLANATION i ^ * . Alluvium Sedimentary and volcanic rocks Sedimentary rocks of upper thrust plate O O N >■2 _J < 0. Sedimentary rocks of lower thrust plate Contact Marker bed -A___a___A. Schell Creek Range thrust fault Barbs on upper plate 111 II Normal fault Hachures on downthrown side A__________ft A Glide fault Barbs on glide plate; arrow shows direction of movement Major anticlinal axis Showing direction of plunge Strike and dip of bedsB22 STRUCTURAL GEOLOGY 30 miles farther. It is the only thrust fault shown on figure 1. Where structural relations are simple along the main trace, the fault dips 25° westward, but east of the main trace and over the crest of the range the fault is nearly horizontal. On the east flank of the range, near Cleve Creek, it dips eastward beneath a klippe. As much as 15,000 feet of beds is missing along the fault where Permian rocks have moved over Upper Cambrian rocks. The other low-angle faults in the area can be traced only a few miles, and along them only a few hundred to a thousand feet of beds is missing. The Schell Creek Range thrust fault described here is not the decollement fault (not shown on fig. 1) described by Misch and Hazzard (1962, p. 319) east of Connors Pass. The inclination of minor drag folds with respect to the fault planes, and the offset of steeply inclined beds along subsidiary low-angle faults in the area of figure 1 indicate that the upper plates of the Schell Creek Range thrust fault and the subsidiary thrust faults moved eastward relative to the lower ones. Locally the faults can be dated no closer than Mesozoic or early Tertiary; the fault cuts rocks of Permian age but not those of Eocene (?) or Oligocene (?) age. However, the thrust faults probably are the same age as similar faults in neighboring ranges, some of which are probably Late Jurassic or Early Cretaceous (Misch, 1960, p.33). Local evidence for the origin of the low-angle faults in the Paleozoic rocks is indirect. Neither a satisfactory root area for thrust faults nor a suitable high area from which glide plates might have moved has been identified. However, at least as late as Early Jurassic time the base of the Paleozoic section evidently was covered by 6y2 to 7 miles of sedimentary rocks, including Mesozoic rocks no longer present in the Schell Creek Range. Beneath such a column of rock the pore pressure may well have equaled the lithostatic pressure. If such a pressure balance existed, it would give the underlying Precambrian rocks great strength against further load deformation and may help account for their lack of deformation beneath much-faulted Paleozoic rocks. It seems easier to picture the development of thrust faults or squeezed-out plates in such a deep structural environment and to picture the development of glide faults in a shallower structural environment. In the absence of a clear decollement surface beneath widespread imbricate plates formed comparatively near the surface, I provisionally favor a thrust-fault origin for most of the low-angle faults in the Schell Creek Range. The genesis of the low-angle faults is, however, less critical to the present thesis than establishing the age of the low-angle faults, described above as thrust faults, as older than certain normal faults, and indicating that such low-angle faults were probably formed in a much deeper structural environment than other, younger low-angle faults described below as glide faults. During or after thrusting, the Paleozoic rocks and the thrust faults were gently warped into broad southward-plunging anticlines that follow the crest of the Schell Creek Range and the crest of the topographically lower Duck Creek Range, northwest of Steptoe Creek. One of these folds, along whose western flank the beds and thrust fault were inclined moderately steeply, played an important part in localizing younger structures. MIDDLE TERTIARY NORMAL FAULTS Normal faults of probable middle Tertiary age cut the Schell Creek Range thrust fault, subsidiary thrust faults, and some rocks that lap across the older structures. The largest of these normal faults form a graben that extends from the upper reach of Steptoe Creek (fig. 1) 25 miles northward along Duck Creek Valley to the vicinity of North Creek (Young,2 and Young, 1960, pi. 1). The west border fault of the graben dips steeply to the east, and the east border fault, actually a fault zone, dips about 45° W. Along the border faults, rocks as young as the Ely Limestone of Pennsylvanian age and limestone of Permian age in the upper plate of the Schell Creek Range thrust fault are displaced against rocks as old as the Pole Canyon Limestone of Middle Cambrian age in the lower plate, giving a false impression of the displacement along the normal faults. Southeast of Steptoe Creek, the east bounding fault of the graben bends eastward and follows the zone of weakness along the Schell Creek Range thrust fault. At the present level of exposure the normal fault has been deflected by the older structure, but presumably these faults diverge at depth. Similarly, 3 to 4 miles northeast of Connors Pass a normal fault follows a moderately steeply inclined segment of the Schell Creek Range thrust fault. Two units of Tertiary conglomerate, which are separated from each other by an angular unconformity at the base of marker bed d (fig. 1), are tilted eastward at different angles along this normal fault. As the younger conglomerate dips less than the older, this segment of the normal fault appears to have moved twice. The normal faults are younger than some of the Tertiary rocks shown in figure 1, believed to be of Eocene (?) age, but as some volcanic vents of about this age are alined along the faults, the faults are prob- 2 Op. cit.DREWES B23 ably not much younger. Provisionally they are assigned a middle Tertiary age. The later of the two episodes of normal faulting northeast of Connors Pass is considerably younger and probably is of late Tertiary or Quaternary age, for the younger faults cut rocks of Pliocene (?) age. MIDDLE OR LATE TERTIARY GLIDE FAULTS Low-angle faults believed to be glide faults underlie two plates of rocks of Eocene (?) or 01igocene( ?) age. One plate is between Cooper Canyon and Cave Creek, and the other is north of Cave Creek (fig. 1). Rocks in these glide plates consist of a sequence, in ascending order, of conglomerate, a rhyolite vitrophyre lava flow, slightly welded rhyolite tuff, much unwelded tuff, and dacite vitrophyre lava flows and tuff. In the larger glide plate the sequence is about 1 mile thick, but in the other it is much thinner. The Tertiary rocks in these plates have been warped into open synclines that plunge gently eastward, and the larger plate is broken by several normal faults. The beds of the smaller plate and of the eastern half of the larger plate dip 20° to 45° into clay-rich, slightly gypsiferous Chain-man Shale of Mississippian age and locally also into Ely Limestone (Pennsylvanian), both in the upper plate of the Schell Creek Range thrust fault. Where the eastern edge of the larger plate lies along or crosses the thrust fault, the beds of the glide plate dip into rocks of Cambrian or Ordovician age of the lower plate of the thrust fault. The surface beneath the larger plate ranges from saucer shaped to flat. Along the north and east sides, the basal contact dips about 40° southward and westward; along the south side of the block it is nearly horizontal; and along the west side it dips gently eastward. In the northern part of the Schell Creek Range, Young3 reports that there, too, the Tertiary rocks are structurally discordant on Paleozoic rocks along low-angle faults. The displaced Tertiary rocks in the glide plates are thought to have slid westward along glide faults from the flank of a highland, formed by uplift of the rocks east of the normal fault that farther north forms the east border of the graben near Steptoe Creek, and into a large valley underlain by Chainman Shale. A glide-fault interpretation is favored here because the fault surfaces are exposed all around the plates, because there is a slope down which the plates could have moved, and because the plates were formed under little cover. The leading, western half of the larger glide plate moved westward a minimum of 3,500 feet to accommodate the rotation of about 40° of the trailing, eastern half of the plate. As the plate moved, drag along the s Op. clt., p. 123-125. flanks exceeding that beneath the center gently warped the beds within the plate. Locally, blocks of Ely Limestone that had been resting on the Chainman Shale were dragged along the base of the Tertiary rocks. A most significant point in this interpretation of the origin of the glide plate of tilted Tertiary rocks is that parts of the plate followed a part of the surface, stripped along or close to the older Schell Creek Range thrust fault and the normal fault of middle Tertiary age, thereby acquiring a structural position of rocks truly part of the upper plate of the thrust fault. Movement of the glide plates postdates the deposition of rocks of Eocene(?) or 01igocene( ?) age in the plates, and presumably it postdates the normal fault along which the source area of the plates was raised. The glide faulting, therefore, is dated as middle or late Tertiary. LATE TERTIARY OR QUATERNARY NORMAL FAULTS Several normal faults cut the larger glide plate of Tertiary rocks and the underlying glide fault. Near Cave Creek the fault cutting across the center of the plate has a stratigraphic displacement of several thousand feet, for the marker beds a and b (fig. 1) east of the fault lie topographically and structurally far above the same beds to the west of the fault. Because it has large displacement near the north edge of the glide plate, the normal fault probably extends northward beyond the glide block. The only surface available for the extension of this fault is the surface already utilized by the Schell Creek Range thrust fault, by the normal fault of middle Tertiary age bounding the east side of the graben along Steptoe Creek, and possibly also by the glide fault beneath the smaller of the glide plates. Where the normal fault of middle Tertiary age diverges from the thrust fault, the later normal fault probably follows the plane of the older normal fault. Some movement along this younger fault may also have been contemporaneous with gliding, as beds a and b are offset more than the glide-fault plane. This late normal fault is dated as late Tertiary or Quaternary, because northeast of Connors Pass it cuts the unit above marker bed d which is as young as Pliocene(?) (fig. 1), and similar faults elsewhere in the area cut gravel of Pleistocene age. Apparently, glide faulting occurred at a time of active normal faulting and volcanism, during which the source area was uplifted. The tectonic activity of middle Tertiary age probably set the stage for glide faulting, and the activity continued after the gliding. SUMMARY In much of the central part of the Schell Creek Range, normal faults, thrust faults, and glide faults areB24 STRUCTURAL GEOLOGY abundant and form plainly decipherable map patterns. Complexity of map pattern arises along segments of the major thrust fault where younger faults have been deflected, and the complexity increases where the direction of movement along later normal faults was different from that along the thrust fault. As a result of postthrust normal faulting, in several places Tertiary rocks younger than the thrust faults are faulted down into the rocks of the upper plate of the major thrust fault and against rocks of the lower plate. As a result, the map pattern formed by these bodies of Tertiary rocks mimics that formed by rocks that are actually part of the upper plate of the thrust fault, although the direction of movement of the hanging block of the normal faults that were deflected along segments of the thrust fault was opposite to that of the upper plate of the thrust fault. Under such circumstances of recurrent and diverse movement along some thrust faults, however local, detailed mapping of relatively large areas around the faults is essential to understanding the timing and dynamics of the thrust faults. REFERENCES Drewes, Harald, 1960, Bedding-plane thrust faults east of Connors Pass, Schell Creek Range, eastern Nevada: Art. 122 in U.S. Geol. Survey Prof. Paper 400-B, p. B270-B272. Misch, Peter, 1960, Regional structural reconnaissance in central-northeast Nevada and some adjacent areas; observations and interpretations, in Intermountain Association of Petroleum Geologists, Guidebook, East central Nevada: p. 17-42. Misch, Peter, and Easton, W. H., 1954, Large overthrust near Connors Pass in the southern Schell Creek Range, White Pine County, eastern Nevada [abs.] : Geol. Soc. America Bull., v. 65, no. 12, pt. 2, p. 1347. Misch, Peter, and Hazzard, J. C., 1962, Stratigraphy and metamorphism of late Precambrian rocks in central northeastern Nevada and adjacent Utah: Am. Assoc. Petroleum Geologists Bull., v. 46, p. 289-343. Spurr, J. E., 1903, Descriptive geology of Nevada south of the fortieth parallel and adjacent portions of California: U.S. Geol. Survey Bull. 208, 229 p. Young, J. C., 1960, Structure and stratigraphy in north-central Schell Creek Range, in Intermountain Association of Petroleum Geologists, Guidebook, East central Nevada: p. 158-172.GEOLOGICAL SURVEY RESEARCH 1964 FACIES RELATIONS OF EXPOSED ROME FORMATION AND CONASAUGA GROUP OF NORTHEASTERN TENNESSEE WITH EQUIVALENT ROCKS IN THE SUBSURFACE OF KENTUCKY AND VIRGINIA By LEONARD D. HARRIS, Knoxville, Tenn. Abstract.—The Rome Formation, Conasauga Shale, and Cona-sauga Group were deposited in a northwest transgressive phase of the Early, Middle, and Late Cambrian seas. Sandstone of the Rome in central Kentucky is by lateral gradation a facies equivalent of approximately the lower half of the Conasauga Group of northeastern Tennessee. The Rome probably ranges in age from Early Cambrian in eastern Tennessee to Middle Cambrian in central Kentucky. In the Valley and Ridge province of extreme southwest Virginia and the adjacent part of Tennessee the oldest Cambrian formations exposed are the Rome Formation of Early Cambrian age and the Conasauga Shale or Group of Middle and Late Cambrian age. These formations plunge into the subsurface of Kentucky and are not exposed in that State. In recent years a series of deep test wells drilled to or near basement rocks in central and eastern Kentucky has provided the link necessary to show facies relations between the subsurface rocks of Kentucky and the surface exposure of the Rome and Conasauga in Virginia and Tennessee (fig. 1). Early workers in Virginia and Tennessee (Campbell, 1894; and Keith, 1896) recognized that a facies relation exists between the Conasauga Shale and the unit now called the Conasauga Group (Rodgers, 1953, p. 47). They found that the thick limestone units of the group wedge out northward into a shale section. The name Conasauga Shale was used for the shale facies on the northwest, and to the east and south the equivalent sequence was divided in ascending order into four formations—the Rutledge Limestone, Rogersville Shale, Maryville Limestone, and Nolichucky Shale. Later stratigraphic studies in eastern Tennessee have not altered the basic facies concept of the earlier workers; however, some of the terminology has been modified by restriction of the Rome Formation and recognition of additional formations considered to be equivalent to the Conasauga Shale (Rodgers and Kent, 1948). These later nomenclatural developments were summarized by Rodgers (1953, p. 43-53). In a diagram he (1953, p. 46) illustrated how the Conasauga Shale on the northwest side of the Valley and Ridge province is gradually supplanted to the southeast by six alternating units of shale and limestone, which he included in his Conasauga Group. These formations from oldest to youngest are the Pumpkin Valley Shale, Rutledge Limestone, Rogersville Shale, Maryville Limestone, Nolichucky Shale, and Maynardville Limestone. These later studies have done much to standardize and clarify the terminology and have established a firm base for regional stratigraphic work in northeast Tennessee. Consequently, I have used Rodgers’ terminology as the basis for developing the subsurface nomenclature for eastern Kentucky and extreme southwest Virginia. This use of Tennessee surface nomenclature in the subsurface of southwest Virginia and central and eastern Kentucky is not without precedent. Tennessee terms have been used in most recent subsurface studies in southwest Virginia (Miller and Fuller, 1954) and eastern Kentucky (Thomas, 1960; Woodward, 1961; and Calvert, 1962), as shown on figure 2. One exception to this was Freeman (1953) who used midcontinent terms. The rocks of the Valley and Ridge province in northeast Tennessee and southwest Virginia are cut by a series of northeast-trending thrust faults (fig. 1). Northwestward movement along many of these faults is probably measured in miles. This movement tends to obscure regional facies changes by bringing rocks deposited in different parts of the original basin of deposition in close proximity. Within particular fault belts the lithology of individual formations re- B25 U.S. GEOL. SURVEY PROF. PAPER 501-B, PAGES B25-B29B26 STRATIGRAPHY AND PALEONTOLOGY 84” Figure 1.—Location of wells and measured sections referred to in text. mains relatively constant, but across fault belts, facies are markedly different. In order to remove the effect of shortening of the depositional basin by thrusting, I have attempted to restore the sections and wells in figure 3 to their relative position before thrusting. At present, only the amount of movement on the northernmost fault—the Pine Mountain thrust—can be calculated accurately. Miller and Fuller (1954, p. 260) have shown that the displacement within the area discussed in this article along the Pine Mountain fault is about 6 miles. In the present study, 6 miles was used as a minimum displacement on the faults to the southeast and was added to the present geographic distance between sections in an attempt to restore them roughly to near their original position. Thus, the distance between sections 5 and 6 (fig. 3) was increased by 6 miles, and that between 4 and 5 by 12 miles. The distance between wells 3 and 4 was increased by 6 miles, as shown by the fact that well 4 was drilled through the Rome Formation and Conasauga Shale above the Pine Mountain thrust fault, whereas well 3 penetrated the same section below the fault. ROME FORMATION Stratigraphic studies of the exposed Rome Formation in northeast Tennessee are complicated because everywhere the “base” of the Rome is marked by a major thrust fault. Therefore, until key beds or zones were established in the formation, an estimate could not be made of how much or what part of the Rome was represented in any given section. Rodgers and Kent (1948) simplified the problem by pointing out a distinctive dolomite unit and a sandstone unit at the top of their restricted Rome Formation. Detailed mapping and measurement of sections have established that both these units can be used as key beds in regional stratigraphic studies. On the outcrop in Tennessee the Rome Formation is a sequence of sandstone, siltstone, and shale containing a few beds and one thick zone of dolomite (fig. 3). Unweathered clastic rocks of the Rome are micaceous and abundantly glauconitic. The proportion of sandstone to shale and siltstone gradually increases toward the northwest. This relation holds true in the sub-HARRIS B27 Freeman (1953) Lincoln County, Kentucky Calvert (1962) Leslie County, Kentucky Woodward (1961) Leslie County, Kentucky Thomas (1960) Leslie County, Kentucky Miller and Fuller (1954) Lee County, Virginia Rodgers and Kent (1948) Hawkins County, Tennessee This report Central Kentucky Tennessee Series Maynardville Middle Knox Group (lower part) Maynardville limestone Maynardville limestone Maynardville Dolomite Member Maynardville ^v^^^Formation Limestone member Bonneterre dolomite (lower part) Conasauga Shale Conasauga Shale Conasauga Shale Conasauga shale Nolichucky shale per Cambrian (/> a D o O Maryville limestone Maryville Limestone “Spears sand” / w \ / 00 > L—-, > / U) (0 00 3 ro «/> (0 c ro a £ Rome Formation Rome Formation Rome Formation Rome formation Rogersville shale c o Rogersville Rome / Shale o O ro o Rutledge limestone [ jc^frutledge / Sandstone Sandstone Dark Ridge 0) QJ and shale member B and shale member B Member White Rocks White Rocks^^ White^Roc^ Sandstone Sandstone y Sandstone Member Member^/ Member^/ Sandstone Sandstone Chadwell member A member A Member / / Lower / Overlook \ \ \ \ \ tongue Member Figure 3.—Stratigraphic nomenclature of the Lee Formation in the Cumberland Mountain outcrop belt of southeastern Kentucky. tion is marked by a linear depression or notch between massive Lee sandstones, or by mines and prospects in the Cumberland Gap coal bed. An argillaceous very fine to fine-grained partly ripple bedded sandstone in the upper part of the member thickens northeastward to about 100 feet in the vicinity of White Rocks, where it overlies 40 feet of medium-dark-gray shale in the lower part of the member. There the basal contact of the Dark Ridge Member is gradational with the underlying White Rocks Sandstone Member, and where the White Rocks wedges out the base is gradational with the Chadwell Member. Middlesboro Member A thick sequence of massive conglomeratic sandstone, previously included in sandstone member C (fig. 3), is herein designated the Middlesboro Member. It is named after the city of Middlesboro, which is situated at the northwest approach to Cumberland Gap. The type section is exposed on Skyland Road on the north side of the gap as follows: Type section of the Middlesboro Member at Cumberland Gap Lee Formation: Thickness Hensley Member (in part): Ft in Shale, medium-gray, silty, poorly bedded; base sharp__________________________________________ 6 6 Middlesboro Member (469 ft 10 in.) Sandstone, white to very light gray, massive, quartzose, crossbedded, sparsely conglomeratic________________________________________ 12 6 Sandstone, very light gray, very fine grained, ripple-bedded, argillaceous_________________________ 10 Sandstone, very light gray, fine-grained, quartzose; base sharp__________________________ 1 6 Shale, medium-light-gray, clayey; base sharp. 6 Sandstone, white to very light gray, finegrained, massive, quartzose, crossbedded; base sharp____________________________________ 16 0 Shale, light-gray, clayey; base sharp___________________ 7 Sandstone, very light gray, fine-grained; base sharp_________________________________________________ 2 Shale, medium-gray, evenly bedded; base sharp_________________________________________________ 8 Sandstone, light-gray, weathers reddish brown, fine-grained; base sharp_______________________ 3 Shale, medium-light-gray...........-......... 6B36 STRATIGRAPHY AND PALEONTOLOGY Type section of the Middlesboro Member at Cumberland Gap— Continued Lee Formation—Continued Thickness Middlesboro Member—Continued Ft In Sandstone, very light gray, fine- to coarsegrained, massive, quartzose; very conglomeratic in basal 20 ft, sparsely conglomeratic in upper part; base sharp________________ 70 0 Shale, medium-dark-gray, evenly bedded; base sharp_________________________________________ 3 0 Sandstone, medium-light-gray, very fine grained, lenticular; beds range from 1 to 3 in. in thickness______________________________ 1 10 Shale, medium-gray, evenly bedded, clayey; base sharp____________________________________ 5 5 Sandstone, very light gray, very fine to finegrained, moderately quartzose; in beds up to 1 ft 4 in. in thickness with a few ripple- bedded surfaces; base sharp__________________ 10 2 Siltstone, weathers reddish brown, evenly bedded; very fine grained sandstone occurs in some laminae; base sharp___________________ 1 1 Sandstone, very light gray, fine-grained, quartzose; in beds as much as 1 ft in thickness; base sharp_______________________________ 13 2 Shale, medium-dark-gray, evenly bedded; base sharp____________________________________ 2 2 Sandstone, very light gray, fine-grained, quartzose; bedding ranges from 6 in. to 1 ft in thickness with some ripple-bedded surfaces. 6 6 Sandstone, light-gray, very fine grained, micaceous; ripple-bedded; some argillaceous laminae; base sharp........................... 9 0 Sandstone, white to very light gray, mediumgrained, subrounded, massive, quartzose, crossbedded, conglomeratic; quartz pebbles are well rounded and average J4 in. in di- ameter; base sharp________________________ 35 0 Shale, medium-dark-gray, evenly bedded; abundant fossil plant fragments_____________ 4 0 Sandstone, white to very light gray, mediumgrained, quartzose, massive; base sharp___ 5 0 Shale, medium-gray, highly weathered__________ 5 0 Sandstone, white to very light gray, mediumgrained, quartzose, subrounded, massive, conglomeratic, crossbedded; base sharp__ 265 0 Dark Ridge Member (in part): Coal bloom (Cumberland Gap coal bed)______ 2+ 0 The Middlesboro Member ranges from 400 to 500 feet in thickness and because of this great thickness of conglomeratic sandstone, it is the principal ridge- and clitf-forming unit along Cumberland Mountain and along Pine Mountain on the northwest limb of the Middlesboro syncline. The member also caps Rocky Face Mountain, which is formed by a large up warp in the Middlesboro syncline about 5 miles north of Cumberland Gap. The member consists predominantly of fine- to coarse-grained white to very light gray quartzose sandstone with a abundance of well-rounded quartz pebbles that commonly range from ^ to 1 inch in diameter. Conglomeratic sandstone generally occurs in four beds that are locally separated by thin beds of shale, coal, underclay, and thin-bedded very fine to fine-grained sandstone. Where these intervening non-resistant beds are absent the member also tends to crop out in a series of four ledges or hogbacks. The basal contact is sharp and locally undulates several feet into the underlying beds. Hensley Member The nonresistant beds of the Lee Formation that lie between the top of the Middlesboro Member and the base of the Bee Rock Sandstone Member have been referred to informally as sandstone and shale member D (fig. 3). These beds are here designated the Hensley Member from Hensley Flats, an upland area between the crests of Brush and Cumberland Mountains, which is underlain by the member. The type section is exposed along Skyland Road and U.S. Highway 25E on the northwest side of Cumberland Gap as follows: Type section of the Hensley Member at Cumberland Gap Thickness Lee Formation: pt in Bee Rock Sandstone Member (in part): Sandstone, very light gray, fine- to mediumgrained. thick-bedded to massive; base sharp.. 12 0 Hensley Member (319 ft 6 in.): Shale, very dark gray to black, evenly bedded; few ironstone nodules________________________ 21 0 Coal (Tunnel coal bed)___________________________ 2 0 Underclay, medium-light-gray; abundant fossil rootlets; base gradational_____________________ 4 6 Sandstone, light-gray, very fine grained, poorly bedded, silty___________________________!____ 2 0 Coal__________________________________________________ 2 Underclay, medium-light-gray; rootlets; base gradational____________________________________ 1 6 Sandstone, light-gray, very fine grained, poorly bedded, silty________________________________ 6 6 Sandstone, very light gray, fine- to mediumgrained, moderately quartzose, thick-bedded to massive; base sharp________________________ 33 0 Shale, medium-gray, silty, evenly bedded_________ 30 0 Shale, dark-gray, evenly bedded; ironstone nodules and beds as much as 1 in. thick______ 25 0 Ironstone, sideritic, nodular_________________________ 4 Shale, medium-gray, evenly bedded________________ 4 0 Shale, medium-gray, very silty___________________ 15 0 Shale, medium-gray, evenly bedded________________ 4 6 Coal; few shale laminae________________________________ 10 Underclay, medium-light-gray; rootlets; base gradational___________________________________ 2 0 Shale, medium-gray, silty, poorly bedded_________ 8 0 Shale, medium-gray, evenly bedded; few very fine grained sandstone lenses as much as 3 in. thick; base sharp______________________________ 5 0 Sandstone, light-gray, very fine to fine-grained, unevenly bedded________________________________ 1 8 Shale, medium-gray, poorly exposed; base sharp. 4 0ENGLUND B37 Type section of the Hensley Member at Cumberland Cap—Con. Lee Formation—Continued Thickness Hensley Member—Continued Ft in Sandstone, very light gray, very fine to finegrained, partly orossbedded; bedding ranges from 2 in. to 3 ft in thickness; base sharp_ 28 0 Sandstone, very light gray, very fine grained; bedding ranges from 1 to 6 in. in thickness; interbedded with medium-gray silty shale; base sharp---------------------------------- 12 10 Sandstone, very light gray, very fine grained, moderately quartzose; bedding is parallel and ranges mostly from 6 in. to 1 ft in thickness; partly orossbedded; base sharp______________ 60 0 Shale, medium-gray, silty; fine mica flakes on bedding planes; evenly bedded............... 8 6 Shale, dark-gray, evenly bedded________________ 7 0 Coal........................................... 1 3 Shale, black, abundant coal laminae___________ 8 Underclay, medium-gray, rootlets_______________ 1 10 Shale, medium-dark-gray, poorly bedded; abundant fossil plant fragments____________________ 6 0 Coal, few shale laminae_______________________ 5 Underclay, medium-gray, silty, rootlets; base gradational__________________________________ 1 6 Shale, medium-gray, silty, poorly bedded_______ 7 0 Sandstone, light-gray, very fine grained, silty; in beds as much as 18 in. thick; base sharp_ 7 0 Shale, medium-gray, silty, poorly bedded; base sharp____________________________________ 6 6 Middlesboro Member (in part): Sandstone, white to very light gray, massive, quartzose, orossbedded, sparsely conglomeratic. 12 6 The Hensley Member ranges from about 320 to 400 feet in thickness and consists mostly of shale in the lower, middle, and upper parts with two very fine to medium-grained thin- to thick-bedded sandstones in between. In contrast to the excellent exposures of adjacent beds of conglomeratic sandstone, the outcrop belt of the Hensley Member is commonly a concealed interval with scattered outcrops of sandstone. The sandstones are persistent and resistant enough to form low ridges in the outcrop belt. In addition to several thin coal beds, the member contains near its top the Tunnel coal (Ashley and Glenn, 1906, p. 115), which ranges from 24 to about 50 inches in thickness and has been mined at several localities. The basal contact is conformable and is placed where the conglomeratic quartzose sandstone of the underlying Middlesboro Member is succeeded by shale and thin-bedded nonconglomer-atic sandstone. Bee Rock Sandstone Member The Bee Rock Sandstone Member (Campbell, 1893, p. 17) is the uppermost conglomeratic sandstone in the Lee Formation along Cumberland Mountain. The name is well established in the Pennington Gap area of the outcrop belt (Giles, 1925, p. 21; Wanless, 1946, p. 136), and it has been extended south westward to the Cumberland Gap area by tracing the member on aerial photographs and by field mapping. The best development and exposure of the Bee Rock Sandstone Member, as mapped in the Cumberland Gap area, is at the northeast end of Brush Mountain where the following reference section crops out in a cliff overlooking Martins Fork: Reference section of the Bee Rock Sandstone Member at the northeast end of Brush Mountain Thickness Ft In Hance Formation (in part): Sandstone, light-gray, very fine to fine-grained, argillaceous, partly ripple bedded; base grada- tional................................... 5+ 0 Lee Formation: Bee Rock Sandstone Member (258 ft 6 in.): Sandstone, white to very light gray, fine- to medium-grained, quartzose, sparsely conglomeratic; base sharp_____________________ 125 0 Shale, medium-gray, evenly bedded; base gradational._______________________________ 3 6 Sandstone, white to very light gray, fine- to medium-grained, quartzose, conglomeratic, orossbedded; base sharp__________________ 130 0 Hensley Member (in part): Shale, dark-gray, evenly bedded__________ 6+ 0 The Bee Rock Sandstone Member ranges generally from 200 to 250 feet in thickness and consists of two massive sparsely conglomeratic quartzose sandstone beds of about equal thickness, separated by a thin shale bed. Quartz pebbles decrease in size and number south-westward along the outcrop belt and are absent southwest of Cumberland Gap. In the section at Cumberland Gap (fig. 1) most of the sandstone in the upper part of the member is very fine to fine-grained and occurs as sedimentary breccia in several beds. The base of the member is sharp and undulatory, and the top is gradational with overlying beds. UPPER BOUNDARY OF THE LEE FORMATION In the Cumberland Mountain outcrop belt the upper boundary of the Lee Formation was placed by Campbell (1893, p. 36) at the top of the Bee Rock Sandstone Member. The overlying rocks consist of relatively non-resistant beds of shale, siltstone, sandstone, coal, and underclay that make up the Hance Formation of the Breathitt Group. In contrast to the sandstones of the Lee Formation, those of the Hance Formation are non-conglomeratic and are typically more micaceous and less quartzose. In the nearby Pine Mountain outcrop belt the top of the Lee Formation was placed by Ashley and Glenn (1906, p. 35) at the top of the NaeseB38 STRATIGRAPHY AND PALEONTOLOGY Sandstone Member, which is lithologically similar to the Lee sandstones but stratigraphically above the Bee Rock Sandstone Member. Recent geologic mapping and stratigraphic studies have shown that the Naese Sandstone Member is a southeastward protruding lobe of partly conglomeratic and quartzose sandstone, as much as 250 feet in thickness, that overlies a regional disconformity and tongues out southeastward in the lower part of the Hance Formation. The southeastern edge of the Naese Sandstone Member grades gradually into sandstone that is lithologically typical of sandstones in the Hance Formation. Below the disconformity the sandstones in the Lee Formation tongue out to the northwest, whereas the Naese and other sandstones above the disconformity tongue out to the east or southeast. This reversal in the deposi-tional trend is interpreted as a change from an eastern or southeastern source to a local northwestern source which may have originated from the uplift and reworking along the erosional surface of previously deposited Lee sediments. Such a reworking hypothesis would account for the deposition of lithologically similar sediments above the disconformity. In view of its diverse depositional trend and higher stratigraphic position, the Naese Sandstone Member could be excluded from the Lee Formation. Its lithologic similarity to the Lee Formation rather than to the Hance Formation, however, favors the previously established practice of recognizing the Naese Sandstone Member as a tongue of the Lee Formation in the Pine Mountain outcrop belt. Only the extremity of the Naese Sandstone Member is present locally in the Cumberland Mountain outcrop belt, where it is a thick-bedded to massive moderately quartzose nonconglomeratic sandstone. Except for this local occurrence of the Naese, which is mapped as a tongue of the Lee that wedges out in the Hance Formation, the top of the Lee is placed as originally desig- nated by Campbell at the top of the Bee Rock Sandstone Member in the Cumberland Mountain outcrop belt. REFERENCES Ashley, G. H., and Glenn, L. C., 1906, Geology and mineral resources of part of the Cumberland Gap coal field, Kentucky : U.S. Geol. Survey Prof. Paper 49, 239 p. Campbell, M. R., 1893, Geology of the Big Stone Gap coal field ol Virginia and Kentucky: U.S. Geol. Survey Bull. Ill, 106 p. ------1898, Description of the London quadrangle: U.S. Geol. Survey Geol. Atlas, Folio 47, 3 p. Eby, J. B., 1923, The geology and mineral resources of Wise County and the coal-bearing portion of Scott County, Virginia : Virginia Geol. Survey Bull. 24, 617 p. Englund, K. J., and Smith, H. L., 1960, Intertonguing and lateral gradation between the Pennington and Lee Formations in the tri-state area of Kentucky, Tennessee, and Virginia [abs.] : Geol. Soc. America Bull., v. 71, no. 12, pt. 2, p. 2015. Englund, K. J., and Harris, L. D., 1961, Itinerary—geologic features of the Cumberland Gap area, Kentucky, Tennessee, and Virginia: Geol. Soc. Kentucky Field Trip, April 1961, Guidebook, 30 p. Englund, K. J., Landis, E. R., and Smith, H. L., 1963, Geology of the Varilla quadrangle, Kentucky and Virginia: U.S. Geol. Survey Geol. Quad. Map GQ-190. Englund, K. J., Smith, H. L., Harris, L. D., and Stephens J. G., 1963, Geology of the Ewing quadrangle, Kentucky and Virginia : U.S. Geol. Survey Bull. 1142-B, 23 p. Giles, A. W., 1925, The geology and coal resources of the coalbearing portion of Lee County, Va.: Virginia Geol. Survey Bull. 26,177 p. McFarlan, A. C., 1943, Geology of Kentucky: Kentucky Univ., 531 p. Wanless, H. R., 1939, Pennsylvanian correlations in the Eastern Interior and Appalachian coal fields: Geol. Soc. America Spec. Paper 17,130 p. ------ 1946, Pennsylvania geology of a part of the southern Appalachian coal field: Geol. Soc. America Mem. 13, 162 P- Wood, G. H., Jr., Trexler, J. P., and Arndt, H. H., 1962, Pennsylvanian rocks of the southern part of the Anthracite region of eastern Pennsylvania: Art. 74 in U.S. Geol. Survey Prof. Paper 450-C, p. C39-C42.GEOLOGICAL SURVEY RESEARCH 1964 THE LITTLE STONE GAP MEMBER OF THE HINTON FORMATION (MISSISSIPPIAN) IN SOUTHWEST VIRGINIA By RALPH L. MILLER, Washington, D.C. Abstract.—A limestone member of the Hinton Formation has been mapped at the surface and recognized in the subsurface in southwest Virginia. Eeger applied the name Avis to this unit, but the name was preoccupied. The member is here rename the Little Stone Gap Member. Various writers have described a limestone or calcareous shale 35 to 55 feet thick in the Hinton Formation of the Pennington Group of southwest Virginia and in the Hinton Group, as used by the West Virginia Geological Survey, in southern West Virginia. These beds of late Chester (Mississippian) age, are persistent at the surface and in the subsurface. They form a highly fossiliferous unit in a relatively unfossiliferous sequence. Until recently no attempt has been made to map this unit as a separate entity, but with the publication of topographic maps on the scale of 1:24,000 for parts of this region, it is now feasible to map these calcareous strata separately on detailed geologic maps. The writer, in mapping this calcareous shale unit in Scott, Wise, and Lee Counties, Va. (fig. 1), has been faced with the necessity of designating it only as an informally named unit or else applying a new name. Because these calcareous strata comprise such a distinctive and areally extensive unit, a formal name seems more appropriate. Hence, the name Little Stone Gap Member is here proposed. It is the uppermost of three mapped members of the Hinton Formation in this part of Virginia, of which the basal member is named the Stony Gap Sandstone Member and the middle member is called the middle red member (Wilpolt and Marden, 1959). Campbell and Mendenhall (1896, p. 487-489) first applied the name Hinton Formation to a series of predominantly clastic sedimentary rocks about 1,100 feet thick along the New River Gorge near Hinton, W. Va. (fig. 1). They noted the presence of several fossiliferous limestone zones within the Hinton. Although 82* l— 81° —|— / v 03 Q 3 03 o rt Si GO o3 bo o o 3 d +* +3 d ,3 o Big Stone Gap member Olinger member Cumberland Gap member TJ 3 03 co bC 3 fi 03 .2 3 fcfi+3 65? 6 -3 O £ 0<1h£ VWWW\A J13 13 -3 33 03 Fh « g 03 - a S.9« • 2 CO a to o '55 > CO Q§ 3 .2 d > 03 Q 03 O 03 _Q GO 03 o a 03 O © a a a o 5” 00-2 MCO S co r! CO 3 'go .2 .2 & Devonian or Mississippian 3 .2 *3 03 Q 08 -3 02 03 bO O O 3 o3 -4-3 -4-3 o3 -3 o a oj O ». 03 03 X2 O S 4-3 03 02^! W) s 2 © bC 3 © 03 T3 g 03 -G co < f-< ^0 03 ©^Q ^ a 42 © * O I-? because of few and poor outcrops in the black shale belts in the structurally complex region, but it is also due in part to difficulty in recognizing Swartz’ divisions by lithologic criteria alone, a difficulty which Swartz himself also met in his studies. In a report on an area southwest of Big Stone Gap, Bates (1939) followed Swartz’ usage of the name Chattanooga. To the lower and middle parts of the black-shale sequence, he applied Stose’s names Genesee and Portage. A year later, Butts (1940) extended the name Brallier Shale from its type region in south-central Pennsylvania to southwest Virginia, applying it to the beds that Stose referred to as Portage and Big Stone Gap Shales. At Big Stone Gap, Butts (1940, p. 312, pi. 45) designated the beds underlying his Brallier Shale as Genesee(?). He also suggested that these beds may be equivalent to his Millboro Shale (Butts, 1940, p. 308-312) in Bath County, Va., the fossils of which he believed to range from as old as Marcellus age to as young as Naples age. Butts’ introduction of the name Brallier into the Big Stone Gap region and his reference to Millboro seem to us only to confuse an already complex picture, and his usage does not conform to subdivisions of the black shale that we have been able to map. Harris (Harris and Miller, 1958) mapped a threefold division of the black-shale sequence in the Duffield quadrangle, Virginia (fig. 1). These were the same three major lithologic units originally recognized by Campbell and subsequently termed Genesee, Portage, and Big Stone Gap Shales by Stose (see table). Hass (Harris and Miller, 1958), who studied the conodont faunas from this area, has indicated that Stose’s lower unit (Genesee) is of Genesee (of early New York usage) and younger age (lower and middle Late Devonian), and that Stose’s middle unit (Portage) is of Late Devonian age, but younger than Portage of early New York usage.1 Hass assigned a Late Devonian and Early Mississippian age to the Big Stone Gap Shale (of Stose) in the Duffield quadrangle. Harris therefore did not use the names Genesee and Portage, but called the lower unit shale (unnamed), the middle unit siltstone (unnamed), and the upper unit Big Stone Gap Siltstone. In mapping and measuring sections, the writers have recognized and found it practicable to use the lithologic divisions that correspond to those of Campbell (1893), 1 Current nomenclature for the Upper Devonian of central New York, compared with early nomenclature, is given in a recent paper by de Witt and Colton (1959)\.B46 STRATIGRAPHY AND PALEONTOLOGY Stose (1923), and Harris and Miller (1958) in all of the Big Stone Gap quadrangle and most of the Keokee quadrangle. These lithologic divisions are: a lower black-shale unit, a middle unit of gray siltstone with interbedded black shale, and an upper unit of black shale and silty shale. Accurate measurements of thickness of these units are exceedingly rare because of few exposures, intertonguing of the black and gray facies, and the possibility of folds and faults in covered intervals. The lower black-shale unit appears to be from 300 to 400 feet thick, the middle gray-siltstone unit from 140 to 400 feet thick, and the upper black-shale unit from 200 to 325 feet thick. In the Keokee quadrangle (fig. 1), mapping of these three units became uncertain because the scarcity of good outcrops did not permit accurate mapping of the apparently thinning middle gray siltstone which divides the otherwise continuous blaclc-shale sequence. In the Pennington Gap quadrangle, which adjoins the Keokee quadrangle on the west, the middle gray siltstone unit could not be recognized, and the whole black-shale sequence was mapped as an undivided unit. In logging deep wells a few miles north of the Big Stone Gap area, Roen and Miller also were unable to recognize the middle gray siltstone unit. It thus appears that the threefold lithologic division is confined to a relatively small area in southwest Virginia. Where the subdivision into thinner mapped units fails, the most appropriate name for the undivided sequence is Chattanooga Shale. It seems better to treat the Chattanooga Shale in southwest Virginia as a formation locally divisible into three members that can be mapped separately, rather than as three formations. We therefore propose that the Big Stone Gap Shale be reduced in rank to the Big Stone Gap Member of the Chattanooga Shale. The two underlying mapped units, because of their limited areal extent, do not merit new formal member names. Rather, we propose that they be called the lower black-shale member and the middle gray-siltstone member of the Chattanooga Shale. In the Big Stone Gap area the Chattanooga Shale is overlain by the Price Siltstone of Early Mississippian age. The contact is conformable. Locally the gray siltstone of the Price and the black shale of the Chattanooga are interbedded in a zone that may be as much as 12 feet thick. In the vicinity of Big Stone Gap, the Chattanooga disconformably overlies the Wildcat Valley Sandstone of Early and Middle Devonian age [Miller and others, 1964, p. B51 (this chap.)]. To the northwest, west, and south of the Big Stone Gap area, the Wildcat Valley Sandstone thins to extinction in a few miles, and the Chattanooga lies on the next older Hancock Dolomite (Limestone) of Late Silurian age. Stose (1923, p. 46, 47) gives two reconnaissance sections of his Big Stone Gap Shale in the Big Stone Gap area, one on the Powell River just north of the town of Big Stone Gap, and the other at Little Stone Gap, 7 miles northeast of the town. He does not indicate, however, which of these he intended for the type section of the Big Stone Gap Shale. We have remeasured both of these sections. The Powell River section, given below, is the better of the two for the upper part of the shale sequence, and is here designated the type section of our Big Stone Gap Member of the Chattanooga Shale. Type section of the Big Stone Gap Member of the Chattanooga Shale. Section is located along the southwest hank of the Powell River at Big Stone Gap, Va., 0.6 mile north-northwest of the center of the town of Big Stone Gap. Measured by R. L. Miller and J. B. Roen, November 28,1962. Thickness Price Siltstone (+25 feet) : (feet) 20. Siltstone, medium-gray; even beds average 1 foot in thickness; concretionary structures present; sandstone very fine grained at top, slightly wavy bedded________________________________ 25. 4 Chattanooga Shale: Big Stone Gap Member (242.6 feet) : 19. Shale, grayish-black, silty; with conspicuous beds of medium-dark-gray siltstone as much as 2 inches thick; contact with Price appears conformable; siltstone of this unit indistinguishable from Price, indicating apparent transi- tional sedimentation__________________________ 1. 3 18. Siltstone, grayish-black, thin- to shaly-bedded; few grayish-black silty shale beds------------ 4. 8 17. Shale, grayish-black, silty; %-inch bed of medium- dark-gray siltstone in middle of unit_________ 4. 5 16. Covered ________________________________________ 15.4 15. Shale, dark-gray, silty; slightly more resistant siltstone laminae----------------------------- 10.1 14. Shale, dark-gray ; no siltstone; top drawn at first siltstone laminae----------------------------- 10.1 13. Shale, grayish-black, silty; similar to unit 12; 1-inch ironstone bed at top and 2-inch ironstone bed 1 foot below top; pronounced gully in middle of unit___________________________________ 10. 7 12. Shale, grayish-black ; thin bedded but bedding not as conspicuous as in units 7 and 8; top of unit is conspicuous 3-inch medium-gray ironstone bed___________________________________________ 12.9 11. Shale, grayish-black, silty; a few siltstone beds; appears similar to units 10 and 12--------- 41. 2 10. Shale, grayish-black ; thin, even bedded________ 40. 4 9. Clay shale, medium-dark-gray ; bedding contorted and indistinct; unit contains lenses and concretions of light-olive-gray siltstone and gray- ish-black well-bedded shale; small brachiopods and pelecypods collected 3 feet above base----- 24. 5 8. Shale, grayish-black ; fault repeats 9.7 feet of beds including contact between unit 9 and this unit— 4. 9 7. Shale, grayish-black; three grayish-black silty shale beds 3 to 6 inches thick; irregular pits on weathered surface--------------------,------------- 3. 2ROEN, MILLER, AND HUDDLE B47 Type section of the Big Stone Gap Member of the Chattanooga Shale—Continued Chattanooga Shale—Continued Thickness Big Stone Gap Member—Continued (feet) 6. Shale and siltstone; shale, grayish-black, silty; siltstone, grayish-black; irregular pits as much as % inch in diameter scattered on weathered surface, which has a slaglike luster-------------- 3. 5 5. Shale, grayish-black, very thin bedded------------- 32. 8 4. Covered ----------------------------------------- 14.3 3. Shale, grayish-black, even-bedded; weathers to plates less than Vi6 inch thick; conformable contact with unit 2 placed at highest prominent siltstone ________________________________________ 8. 0 Middle gray siltstone member (+23 feet) : 2. Shale, grayish-black, silty, with occasional laminae of medium-dark-gray siltstone____________ 13. 6 1. Clay shale, olive-gray, with resistant medium-dark-gray siltstone and shale interbedded in a zone 6 inches to 2 feet thick_______________________ 9. 3 The Chattanooga Shale in the Big Stone Gap area ranges in age from earliest Late Devonian, or possibly late Middle Devonian to Early Mississippian. These age determinations were made by W. H. Hass (written communications, 1953,1954) and Huddle, and are based on conodont collections made by Hass in 1944, Harris and Hass in 1952-53, and the writers in 1962-63. Cono-donts found in the basal beds of the lower black-shale member of the Chattanooga Shale in the Duffield quadrangle, Virginia, include Polygnathus linguiformis Hinde and Icriodus latericrescens Branson and Mehl. These species are common in the Middle Devonian rocks of Newr York but are also found in the Upper Devonian part of the Genesee Formation of New York. The age of the basal beds is therefore not definitely determined. Most of the lower black shale member has a Late Devonian conodont fauna including several species of Palma-tolepis. Palmatolepis glabra Ulrich and Bassler, Palmatolepis perlobata Ulrich and Bassler, and Ancyrognathus bifuroata (Ulrich and Bassler) occur in the upper part of the lower member and represent the conodont assemblage found in the Upper Devonian Perrysburg Formation in New York (middle Late Devonian). The middle gray-siltstone member of the Chattanooga Shale has yielded few conodonts. Two collections from this unit in the Duffield quadrange contain Spathog-nathodus inomatus (Branson and Mehl) and Palmatolepis perlobata Ulrich and Bassler. These species suggest a correlation of the middle gray member in the Big Stone Gap area with part of the Gassaway Member of the Chattanooga in central Tennessee and the upper part of the Ohio Shale in Ohio. The Big Stone Gap Member of the Chattanooga Shale contains both Early Mississippian and Late Devonian conodont faunas. The lower part of this member, up to and including unit 5 in the Powell River section at Big Stone Gap (see stratigraphic section), contains Spathognathodus inomatus (Branson and Mehl), S. strigosus (Branson and Mehl), and S. aculeatus (Branson and Mehl), and several species of bar-type conodonts. This part of the member is considered Late Devonian in age. Units 7 and 8 in the Powell River section contain Spathognathodus inor-. natus (Branson and Mehl), S. anteposicornis Scott, S. strigilis (Huddle), and several species of Hindeodella. S. anteposicornis occurs with S. inomatus in the Louisiana Limestone in the Mississippi Valley, the Bedford Shale of Ohio, and in the Knapp Formation of northwestern Pennsylvania. These formations have been classified as Early Mississippian by some authors and as Late Devonian by others. No identifiable conodonts have been found in the medium-dark-gray clay shale, unit 9, of the Powell River section of the Big Stone Gap Member. Units 7, 8, and 9 of the Powell River section are here regarded as being Mississippian or Devonian in age. The lowest definitely Mississippian conodont fauna occurs in the basal 0.3 feet of unit 10 in the Powell River section. This is the base of the Big Stone Gap Member of Swartz (1929a). The fauna is characterized by Siphonodella and occurs throughout the upper part of our Big Stone Gap Member at Big Stone Gap and Little Stone Gap, Va. The following species have been found: Elictognathus lacerata (Branson and Mehl) Polygnathus communis (Branson and Mehl) Polygnathus inomatus (E. R. Branson) Pseudopolygnathus sp. Siphonodella duplicata (Branson and Mehl) Siphonodella quadruplicata (Branson and Mehl) Spathognathodus aciedentatus (E. R. Branson) This fauna is clearly Early Mississippian Kinder-hookian in age, and hence units 10-19 in the Powell River section are considered Kinderhookian in age. This fauna also occurs in the Maury Formation of Tennessee and the Sunbury Shale of Ohio, but has not been found in New York. REFERENCES Bates, R. L., 1939, Geology of Powell Valley in northeastern Lee County, Virginia: Virginia Geol. Survey Bull. 51, pt. 2, p. 31-94. Butts, Charles, 1940, Geology of the Appalachian Valley in Virginia: Virginia Geol. Survey Bull. 52, pt. 1, 568 p. Campbell, M. R., 1893, Geology of the Big Stone Gap coal field of Virginia and Kentucky: U.S. Geol. Survey Bull. Ill, 106 p. -----1894, Description of the Estillville quadrangle (Ky-Tenn- Va) : U.S. Geol. Survey Geol. Atlas, Folio 12.B48 STRATIGRAPHY AND PALEONTOLOGY Conant, L. C., and Swanson, V. E., 1961, Chattanooga shale and related rocks of central Tennessee and nearby areas: U.S. Geol. Survey Prof. Paper 357, 91 p. de Witt, Wallace and Colton, G. W., 1959, Revised correlations of lower Upper Devonian rocks in western and central New York: Am. Assoc. Petroleum Geologists Bull., v. 43, no. 12, p. 2810-2828. Harris, L. D., and Miller R. L., 1958, Geology of the Duffield quadrangle, Virginia: U.S. Geol. Survey Geol. Quad. Map GQ-111. Hass, W. H., 1956, Age and correlation of the Chattanooga Shale and the Maury Formation: U.S. Geol. Survey Prof. Paper 286, 47 p. Miller, R. L., Harris, L. D., and Roen, J. B., 1964, The Wildcat Valley Sandstone (Devonian) of southwest Virginia, in Geological Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B49-B52. Stose, G. W., 1923, Pre-Pennsylvanian rocks, in Eby, J. B., The geology and mineral resources of Wise County and the coal-bearing portion of Scott County, Virginia: Virginia Geol. Survey Bull. 24, 617 p. ------1924, The black shale of southwestern Virginia: Jour. Geology v. 32, no. 4, p. 311-315. Swartz, J. H., 1926a, The Big Stone Gap shale of southwestern Virginia : Science, new ser., v. 64, p. 226. ------1926b, The age of the Big Stone Gap shale of southwestern Virginia: Am. Jour. Sci., 5th ser., v. 12, p. 522-531. ------1927, The Chattanooga age of the Big Stone Gap shale: Am. Jour. Sci., 5th ser., v. 14, p. 485-499. ------1929a, The age and stratigraphy of the Chattanooga shale in northeastern Tennessee and Virginia: Am. Jour. Sci., 5th ser., v. 17, p. 431-448. ------1929b, The Devono-Mississippian boundary in the southeastern United States: Science, new ser., v. 70, p. 609.GEOLOGICAL SURVEY RESEARCH 1964 THE WILDCAT VALLEY SANDSTONE (DEVONIAN) OF SOUTHWEST VIRGINIA By RALPH L. MILLER,1 LEONARD D. HARRIS,2 and JOHN B. ROEN,1 1 Washington, D.C.,2Knoxville, Tenn. Abstract.—A conspicuous formation in Wise, Scott, and Lee Counties, Va., has previously been called Helderberg Limestone or Helderberg Limestone of Stose. Helderberg is not a formation in its type region but a stage of Devonian time. The formation in southwest Virginia is renamed the Wildcat Valley Sandstone. In Scott, Wise, and Lee Counties of southwest Virginia, the Devonian System is represented by a calcareous sandstone about 45 feet thick, overlain by a black shale sequence hundreds of feet thick. The black shale is the Chattanooga Shale, largely of Late Devonian age. The underlying calcareous sandstone has in the past been called Helderberg Limestone (Stose, 1923). Because Helderberg has been used as a time stratigraphic term in this area, that is, for a stage of Devonian time (Cooper, G. A., and others, 1942), and also because in places the topmost beds of the sandstone contain post-Helderberg fossils, the new name Wildcat Valley Sandstone is here introduced for this rock stratigraphic unit. In the Estillville folio covering this region (Campbell, 1894), the Wildcat Valley Sandstone was included with underlying limestones of Late Silurian age in the Hancock Limestone (or Dolomite). Stose (1923) later mapped the calcareous sandstone as a separate formation in his section of the Virginia Geological Survey report on Wise County, calling it the Helderberg Limestone because of faunal similarities to the Helderberg of New York. Butts (1940) calls the unit “Helderberg undivided” in his classic report on the Appalachian Valley of Virginia. The new formation name is derived from Wildcat Valley in southwestern Wise County, Va. (Big Stone Gap topographic quadrangle map, scale 1: 24,000,1957). Wildcat Valley lies about 2 miles south of the town of Big Stone Gap between Wallen Kidge on the northwest and Powell Mountain on the southeast (fig. 1). It is drained northeastward by Wildcat Creek, which flows into the South Fork of the Powell Kiver. Along the U.S. GEOL. SURVEY PROF. 36" 82°45' Figure 1.—Sketch map showing type locality of the Wildcat Valley Sandstone in the northeast part of the Big Stone Gap quadrangle, Virginia. lower course of the creek, southeast-dipping beds of Hancock Limestone form a line of low knobby hills on the southeast side of the valley. The crests of the knobs are in most places capped by the Wildcat Valley Sandstone. On most of the hills the basal beds of the Chattanooga Shale lie on the back slopes of the knobs, and the remainder of the formation underlies the lowest slopes of Powell Mountain. The type section of the Wildcat Valley Sandstone was measured at the southwest end of the peninsula-shaped knob 0.15 mile south of Irondale Church, which is in the small community of Irondale on U.S. Highway 23. The section of the upper part of the Hancock Limestone and of the Wildcat Valley Sandstone exposed at this locality follows. APER 501-B, PAGES B49-B52 B49B50 STRATIGRAPHY AND PALEONTOLOGY Type section of the Wildcat Valley Sandstone, and upper part of the Hancock Limestone. Section is located 2 miles south-southeast of Big Stone Gap, Wise County, Va., on a spur overlooking Wildcat Creek, 0.15 mile south of Irondale Church on U.S. Highway 23. Section begins with lowest beds exposed on southwest slope of spur and ends uAth black-shale exposures on highest point of spur. Measured by Ralph L. Miller, August 26, 1963. Thickness (feet) Chattanooga Shale: 16. Black shale, almost in place on crest of spur. Wildcat Valley Sandstone (41 feet) : 15. Covered; float from upper part is fine-grained, porous, fossiliferous, sandstone that weathers pale yellowish brown and is partly replaced by granular white chert; abundant fossils, principally brachiopods; float from lower part is similar sandstone, but more dense, and without fossils __________________________________________13+ 14. Sandstone, fine-grained, porous, friable; in irregular beds________________________________________13. 5 13. Sandstone, fine-grained, pale-yellowish-brown, little-weathered, laminated; interstitial calcium carbonate. Contains Leptaena sp. and other brachiopods. Before weathering, unit 14 prob- ably had similar lithology______________________ 3. 7 12. Sandstone, fine-grained, calcareous; abundant brachiopods; tiny patches of white chert. Might be called sandy limestone, but after dissolving of carbonate, coherent sandstone remains________ 2.1 11. Covered _________________________________________ 4.3 10. Sandstone, very fine grained, calcareous, pale-yel- lowish-brown; numerous fragmented fossils— 1. 3 9. Sandstone, fine-grained, light-brownish-gray, calcareous ; in uneven thin beds with indistinct fossils_________________________________________ 3.4 Hancock Limestone (66+ feet) : 8. Limestone, very fine crystalline, olive-gray, faintly laminated ; petroliferous odor after fracturing; beds somewhat slumped_____________________________ 8± 7. Limestone, fine and very fine crystalline, brownish-gray ; in beds 2 to 6 inches thick; petroliferous odor after fracturing________________________________12. 6 6. Limestone, dolomitic, dense, olive-gray, faintly laminated. Not as dolomitic as units 2 and 4_____11. 7 5. Limestone like unit 3; weathers thin bedded in upper part; petroliferous odor after fracturing__10. 2 4. Dolomite, very fine crystalline, dense, olive-gray with steely luster; even beds as much as 3 feet thick _________________________.____________________10. 5± 3. Limestone, very fine crystalline, olive-black; in even beds 1 inch to 2 feet thick; silty laminae show faintly on weathered surfaces; petroliferous odor after fracturing_______________________________ 9. 7 2. Dolomite, very fine crystalline, olive-gray, irregularly bedded and faintly laminated________________________ 1. 6 1. Limestone, fine crystalline, light-olive-gray; in irregular beds; conspicuous vertical joints; weathers very dark gray with white blotches_______________ 1. 8 Miller and Roen have mapped the Wildcat Valley Sandstone throughout its outcrop belt in the Big Stone Gap and Keokee quadrangles (maps in preparation). Harris and Miller have also mapped this unit under the name “Sandstone (Helderberg as used by Stose)” in the Duffield quadrangle (Harris and Miller, 1958), which lies just south of the Big Stone Gap quadrangle (fig. 2). In all three quadrangles, sandstone is the predominant rock type at the outcrop. Before weathering, probably all the sandstone beds were calcareous. Northeast of the Big Stone Gap quadrangle, at the extreme east end of the Powell Valley, sandy and argillaceous limestone is dominant according to Stose (1923), which is w hy he referred to this unit as the Helderberg Limestone. Even here, however, sandstone seems to predominate over limestone in roadside exposures we have seen. A facies change to still more calcareous beds appears to take place northeast of the Big Stone Gap area (Butts, 1940, p. 264-291). The Wildcat Valley Sandstone in most surface (that is, weathered) exposures consists of fine-, medium-, and coarse-grained porous and friable sandstone normally stained light shades of yellow or very light brown. In places, particularly near faults, the sandstone is stained or recemented with limonite or hematite and appears red, brown, or nearly black. In some places, the weathered sandstone is no longer coherent, and the outcrop consists of a sand pile which may still preserve traces of original bedding. Elsewhere, however, the sandstone is moderately resistant in spite of its porous character. It caps small hills, causes changes of slope, and may form a sparse blocky float. Fossils, predominantly large brachiopods, are abundant and where not replaced by chert consist principally of external and internal molds. The fossiliferous nature of the rock may be deduced from the fact that we used the field term “Devonian fossil sand” for the unit in mapping it in the Duffield quadrangle. White chert is a variable constituent of the formation and occurs principally as replacements of fossils or fillings of cracks, but in some beds it fills interstices between sand grains or replaces sand grains. Calcium carbonate generally forms the cement between sand grains, where the rock is little weathered, but in most outcrops the carbonate is completely dissolved. Nodular chert is scarce, and fragments of chert in the soil derived from weathering of the rock are mostly small and thin. In the type section, chert is abundant in the uppermost beds. Locally, a few feet of very cherty sandstone is present at the top. These beds contain corals in abundance in some places. Where we have mapped the formation in the Duffield and Big Stone Gap quadrangles it is consistently about 40 to 45 feet thick. It thins southwestward, in the Keokee and Stickleyville quadrangles, and is absent in the Pennington Gap quadrangle and the western part of the Stickleyville quadrangle (fig. 2). NorthwardMILLER, HARRIS, AND ROEN B51 83°7'30" 83° 00' 52'30" 82“45' Figure 2.—Map of part of southwest Virginia, showing belts of outcrop and the type locality of the Wildcat Valley Sandstone. and northwestward, within a few miles of Big Stone Gap, it also feathers out beneath the younger strata of the Cumberland Plateau, as shown by deep wells in western Wise County. The Wildcat Valley Sandstone, disconformably over-lies the Hancock Limestone (or Dolomite) of Late Silurian age. The contact is sharp but with little apparent erosion of the Hancock. Disconformably overlying the Wildcat Valley Sandstone is the black Chattanooga Shale, without apparent significant erosion of the beds beneath the contact. Although the Wildcat Valley Sandstone is relatively thin and is virtually a lithologic unit, it is not a paleon- tologic entity. Various geologists have collected from the formation in sections near Big Stone Gap. Campbell (1894) mapped the Big Stone Gap region but included all the Wildcat Valley Sandstone with the under lying Hancock Limestone (Silurian). H. S. Williams, whose fieldwork postdated that of Campbell, mentions the sandstone underlying the black shale at Big Stone Gap from the top beds of which he collected “corals of Corniferous (Onondaga) age” (Williams, 1897, p. 398-399). His reference to the Helderberg Limestone beneath the sandstone appears to mean the Hancock Limestone, now considered Late Silurian. Kindle (1905, p. 27-29) lists faunas collected from fourB52 STRATIGRAPHY AND PALEONTOLOGY localities near Big Stone Gap, two of which he dates as “Oriskany” (quotes are Kindle’s). The other two faunules are not dated. Later, Kindle (1912, p. 50-53) collected again, this time from the topmost beds beneath the black shales at two localities near Big Stone Gap. He dated these coral-rich faunules as Onondaga, but noted correctly that the coral-rich beds were not everywhere present overlying the more sandy and less cherty beds that he had previously called “Oriskany”. Stose (1923) called the unit that he mapped in Wise County the Helderberg Limestone, apparently basing this designation on sections measured and paleontologic studies made in the area by E. O. Ulrich. The main body of the formation was correlated by Ulrich and Stose with the New Scotland and Becraft Limestones of the Helderberg Group of New York. The coral-rich faunules noted by Kindle were also recognized by Ulrich as having Onondaga affinities, but he “found that the coral fauna occurs in several bands in the upper 50 feet or more of the formation and that the intervening beds contain an unquestionable Becraft fauna. He therefore regards these corals as representing an earlier invasion of species that are elsewhere known only in limestones of Onondaga age” (Stose, 1923, p. 42). Stose therefore assigned these coral-bearing beds as well as the underlying rocks to the Helderberg. We believe that the recurrence in several bands of the coral faunas noted by Ulrich was probably due to repetition of beds by faulting, although this cannot be verified because Ulrich’s localities are not specified. Bates (1939) followed Stose in assigning a New Scotland and Becraft age to the Helderberg Formation in northeastern Lee County, Ya. Harris (Harris and Miller, 1958) in collaboration with A. J. Boucot collected fossils from the formation, here named the Wildcat Valley Sandstone, in the Duffield quadrangle and also in the Big Stone Gap area. Boucot (written communications, 1954), who studied the brachiopods from these new collections as well as the earlier collections made by other paleontologists in the Big Stone Gap area, has indicated that the lowest part of the Wildcat Valley Sandstone contains fossils of probable Helderberg age, whereas the middle and most of the upper parts of the formation are of New Scotland or Becraft age. As with others before them, Harris and Boucot at some localities found post-Helderberg fossils in the top few feet of the formation. These seemed to Boucot to be of Schoharie or Onondaga age, and at one locality Boucot identified brachiopods of Oriskany age between the beds of Helderberg age and those of Schoharie or Onondaga age. W. A. Oliver, Jr. (oral communication, 1963) has recently examined the corals from these faunules designated by Boucot as Schoharie or Onondaga and believes that they are of Schoharie age. In spite of the fact that beds of diverse ages are apparently present in the Wildcat Valley Sandstone, it is virtually one geologic unit for mapping purposes. At some localities in the Big Stone Gap area, it seems to be entirely of Helderberg age, but at other places in the same region, as much as 8 feet of beds of probable Schoharie age is included at the top, and a few localities have yielded fossils of apparent Oriskany age between the two. These thin zones of post-Helderberg age are probably remnants of a more extensive but thin layer of late Lower Devonian and possibly early Middle Devonian sedimentary rocks that has only locally been preserved from pre-Chattanooga erosion. The erosion of only a few feet of beds in Onondaga and Hamilton time would account for the spotty occurrences of the post-Helderberg beds. Thus, the Wildcat Valley Sandstone is largely of Early Devonian age, but in places lower Middle (?) Devonian beds are present at the top of the formation. REFERENCES Bates, R. L., 1939, Geology of Powell Valley in northeastern Lee County, Va.: Virginia Geol. Survey Bull. 51-B, p. 31-94. Butts, Charles, 1940, Geology of the Appalachian Valley of Virginia: Virginia Geol. Survey Bull. 52, p. 264-291. Campbell, M. R., 1894, Description of the Estillville quadrangle (Ky.-Tenn.-Va.) : U.S. Geol. Survey Geol. Atlas, Folio 12. Cooper, G. A., and others, 1942, Correlation of the Devonian sedimentary formations of North America: Geol. Soc. America Bull. v. 53, p. 1729-1794. Harris, L. D., and Miller, R. L., 1958, Geology of the Duffield quadrangle, Virginia: U.S. Geol. Survey Geol. Quad. Map GQ-111. Kindle, E. M., 1905, Sections in Virginia and West Virginia, in Williams, H. S., and Kindle, E. M., Fossil faunas of the Devonian and Mississippian (“Lower Carboniferous”) of Virginia, West Virginia, and Kentucky: U.S. Geol. Survey Bull. 244, p. 144. ------ 1912, The Onondaga fauna of the Allegheny region: U.S. Geol. Survey Bull. 508, p. 144. Stose, G. W., 1923, Pre-Pennsylvanian rocks, in Eby, J. B., The geology and mineral resources of Wise County and the coal-bearing portion of Scott County, Virginia: Virginia Geol. Survey Bull. 24, p. 40-43. Williams, H. S., 1893, On the southern Devonian Formations: Am. Jour. Sci., 4th ser., v. 3, p. 393-403.GEOLOGICAL SURVEY RESEARCH 1964 THE GOOSE EGG FORMATION IN THE LARAMIE RANGE AND ADJACENT PARTS OF SOUTHEASTERN WYOMING By EDWIN K. MAUGHAN, Denver, Colo. Abstract.—The name Goose Egg Formation is applied in southeastern Wyoming to that part of the Permian and Triassic red-bed sequence that contains interstratified carbonate and sulfate rocks. These strata compare with those of the type section near Casper, Wyo., composed of Opeche Shale, Minnekahta Limestone, Glendo Shale, Forelle Limestone, Difficulty Shale, Ervay, Freezeout Shale, and Little Medicine Members. Discussion of red beds of Permian and Triassic age in southeastern Wyoming has been difficult heretofore owing to inadequate nomenclature for these rocks. The Goose Egg Formation was named by Burk and Thomas (1956) for exposures near the Goose Egg Post Office, NW14 sec. 12, T. 32 N., R. 81 W. (fig. 1), in central Wyoming, for that part of this red-bed sequence that is interstratified with carbonate and sulfate rocks. Units that compose the Goose Egg Formation at the type section near Casper (table 1) can be identified in surface and subsurface sections throughout most of southeastern Wyoming. For this reason, and to establish a consistent nomenclatural system for the red beds and other rocks, the name Goose Egg Formation is extended into the southeastern part of the State. The stratigraphic relations of the members that make up the formation in southeastern Wyoming are discussed in this article. All the red beds in southeastern Wyoming now known to be of Permian and Triassic age were included originally in the Chugwater Formation by Darton (1904, p. 397-398). Strata equivalent to the Minnekahta Limestone and Opeche Shale, which Darton (1901, p. 513-514) had previously named in the Black Hills, were not differentiated in his definition of the Chugwater. Subsequently, strata in the lower part of the original Chugwater were excluded in the Laramie Basin and named there the Satanka Shale and overlying Forelle Limestone (Darton, 1908). 106” 104” Figure 1.—Index map showing location of places referred to in text. Numbers indicate geologic sections illustrated on figure 2. Triangle, outcrop section; dot, subsurface section. Thomas (1934) established the age for the part of the red-bed sequence that is interstratified with carbonate and sulfate rocks by tracing these strata westward into rocks of known Permian and Triassic age. The Ervay tongue in central Wyoming he correlated with the uppermost part of the Park City Formation (then known as the Phosphoria Formation) in the Wind River Range of western Wyoming and established it B53 U.S. GEOL. SURVEY PROF. PAPER 501-B, PAGES B53-B60B54 STRATIGRAPHY AND PALEONTOLOGY Table 1.—Nomenclature of Permian and Lower Triassic rocks in southeastern Wyoming. as the uppermost unit of Permian age. Red beds enclosing the Ervay he named the Freezeout Tongue of the Chugwater Formation. The part of the Freezeout that overlies the Ervay was correlated westward by Thomas with the lower part of the Din woody Formation of Early Triassic age and is overlain by a bed of limestone that Thomas named the Little Medicine Tongue of the Din woody Formation. The Little Medicine is found in most of eastern Wyoming. Condra and others (1940) introduced additional names for red beds of Permian age in southeastern Wyoming. The Owl Canyon Formation and a thin sandstone locally found at its top, which they provisionally correlated with the Lyons Sandstone, were recognized beneath the Opeche Shale. These strata are the equivalent of the lower part of the Satanka Shale (Darton, 1908). The Opeche Shale and Minnekahta Limestone, names extended from the Black Hills, and the Glendo Shale, a name which Condra and others introduced for the red-bed unit between the Minnekahta and the Forelle, were applied along the east flank of the Laramie Range for strata equivalent to the upper part of the Satanka Shale. The Freezeout Shale was applied to the red beds above the Forelle and below their Dinwoody sandstone (Little Medicine Tongue). The Freezeout as used by Condra and others includes thin limestone and gypsum beds of the Ervay. The Goose Egg Formation of Burk and Thomas (1956) included in ascending order: Opeche Shale, Minnekahta Limestone, Glendo Shale, Forelle Limestone, lower part of the Freezeout, Ervay, upper part of the Freezeout, and Little Medicine Members. This nomenclature has been extended throughout the Powder River Basin in northeastern Wyoming by Privrasky and others (1958) with the exception that the two parts of the Freezeout were left unnamed.MATJGHAN B55 Units that comprise the Goose Egg Formation at its type section can be traced into southeastern Wyoming and differentiated in most places from other Permian and Triassic red beds (fig. 2 and table 2). They are distinct in exposures in the Laramie Range, except in the southern part, and in the Hartville uplift. Electric logs of the formation throughout southeast Wyoming differ only slightly from the electric log of the formation in the Mississippi River Fuel Co. 1 Government-Goose Egg well, which Burk and Thomas (1956, fig. 1, p. 6) compare with the surface type section. The base of the Goose Egg Formation is the base of the lowest gypsum beds in the Opeche Shale Member; the underlying red beds lack bedded gypsum. The top of the formation is the top of the highest dolomite or gypsum in the Little Medicine Member; these kinds of rocks are absent in the overlying red beds. It is a distinctive sequence in most of southeastern Wyoming where exposures are moderately good; however, in the southern Laramie Basin and along the eastern front of the southern part of the Laramie Range, identification of the Goose Egg is difficult. Near Laramie, the equivalents of the members of the Goose Egg are present and can be identified at the few places where these rocks are well exposed, although some of the units are much thinner than correlative strata farther north. However, because all units except the Forelle are poorly exposed at most places in the Laramie area, the Goose Egg cannot be readily subdivided nor differentiated, and the nomenclature of Darton (1908) should be retained. ROCKS BELOW THE GOOSE EGG FORMATION Underlying the Goose Egg Formation throughout southwestern Wyoming is the Owl Canyon Formation of Condra and others (1940) or equivalent strata. The formation is composed dominantly of reddish siltstone and very fine grained sandstone. Southward in Colorado the Owl Canyon Formation grades into the Lyons Sandstone, and southwestward in the Laramie Basin it similarly grades into sandstone (Maughan and Wilson, 1960) that probably is a remnant of the Lyons in that area. The Owl Canyon thins northward in the Laramie Range and also grades into sandstone in the northern part of the range where it forms part of the Casper Formation. Consequently, strata equivalent to the Owl Canyon probably underlie the Goose Egg in the Casper area. Strata similar and perhaps equivalent to the Owl Canyon Formation are included as a lower part of the Opeche Shale at some places in the southern Black Hills. Where these strata grade into sandstone they are included as a part of the Minnelusa Formation. Throughout southeastern Wyoming the Opeche has been restricted to the overlying dominantly claystone unit described below. ROCK UNITS IN THE GOOSE EGG FORMATION Opeche Shale Member The Opeche Shale Member is a thin but very widespread unit which extends throughout most of eastern Wyoming at the base of the Goose Egg Formation (Burk and Thomas, 1956, p. 9). At the type section of the Goose Egg the Opeche Member is 70 feet thick. In the Hartville uplift area and as far south as Horse Creek in the Laramie Range the Opeche ranges between 20 and 70 feet in thickness. At Horse Creek the Opeche is about 70 feet thick, but it thins markedly southward and probably is very thin or absent at Lodgepole Creek and farther south, in Colorado. A similar abrupt thinning of the Opeche occurs in the subsurface in the northern part of the Laramie Basin and in exposures in the Freezeout Hills northwest of the basin. At a few places on the margins of the southern part of the Laramie Basin and south of Boxelder Creek in Colorado, red and purplish-red claystone directly above strata equivalent to the Owl Canyon probably are a wedge edge of the Opeche equivalent. The Opeche is composed mostly of moderate-reddish-orange claystone. The upper part is purplish in most places where it grades upward into the overlying Min-nekahta. The claystone generally is composed of strata ranging from parallel thin laminae to thin beds and is moderately fissile. At many places the lowermost strata are silty or sandy, but more commonly they include beds of dolomite or gypsum, which in the Laramie Basin are moderately thick. The Opeche is believed to be of late Leonard age. Southeastward it seems to correlate and probably is contemporaneous with the Flowerpot Shale of that age in Kansas. Westward it intertongues in central Wyoming with the Park City Formation at about the stratigraphic position of the Meade Peak Phosphatic Shale Member of the Phosphoria Formation, also of Leonard age. Minnekahta Limestone Member The Minnekahta Limestone is about 50 feet thick in the Black Hills and gradually thins southwestward to about 30 feet in the Hartville uplift, and to between 10 to 30 feet at most places in the northern parts of the Laramie Range and the Laramie Basin where it is a member of the Goose Egg. The Minnekahta and Opeche are thin in the same areas. In the south half of the Laramie Basin the Minnekahta is less than 10 feet thick, and at some places it is missing (fig. 2). Onw Ox N, neutron EXPLANATION Shale Sandstone U--1- i Limestone Dolomite Gypsum Missing sample or covered section Argillaceous Sandv G0 £3 > H t-H O M > ►a W K* > a ►a > E* M O 2 H O c o a «! Calcareous Dolomitic Gypsiferous Figure 1. Cross sections of the Goose Egg Formation in southeastern Wyoming, the top line 0f sections is from the Goose Egg type area near Casper, Wyo., to the east side of the Laramie Range near Iron Mountain, by way of Sand Canyon in the Hartville uplift. The bottom line is from the Goose Egg type section source^rf* secthms are gfven^n Cibbf 2 Y ° 1'•eezeout Hills and Laramie Basin. Lines of sections are shown on figure 1 and description of location andMAUGHAN B57 Table 2.—Location and source of sections shown on figure 8 No. on figure 2 Well or geologic section Location Source Section Town- ship (north) Range (west) 1 2 3 4 5 6 7 8 9 10 11 12 13 Mississippi River Fuel 1 Government-Goose Egg- Goose Egg Formation type section.............. Socony Vacuum 32X-21G_________________________ Mobil Producing F-14-19-G_____________________ Section in Sand Canyon________________________ Seaboard Oil 1 Wilson_________________________ Section at Iron Mountain______________________ Section in vicinity of Laramie________________ Section at Red Mountain_______________________ Pacific Western 1 Strom_______________________ California Co. 3 Seven Mile Unit______________ British-American 2 State-Horn Bros____________ Section at Difficulty_________________________ 14 Tidewater-Associated 81-22 Lawn Creek 9 32 12 32 21 35 19 32 29 29 29 25 29 19 2 23 16 18 12 32 15 9 17 17 21 10 24 22 29 81 Burk and Thomas (1956). 81 Do. 77 («). 70 (>). 67 Denson and Botinelly (1949). 65 ('). 70 This article. 73 Do. 76 Do. 76 (>). 77 «. 78 (>). 80 Modified from Thomas (1934, p. 1680). 80 (>). 1 Sample Information from log by American Stratigraphic Co. 2 Approximate. the east side of the Laramie Range the Minnekahta is about 25 feet thick at Horse Creek, but it is generally less than 5 feet thick at Lodgepole Creek and farther south. At places in the Boxelder Creek area, where strata equivalent to the Minnekahta are 4 feet thick, this unit rests directly upon Lyons Sandstone and is itself moderately sandy. The Minnekahta generally is composed of thin even parallel beds and laminae of finely crystalline pinkish-and purplish-gray dolomitic limestone. Commonly, the Minnekahta contains interstratified thin beds of purplish-red claystone, especially in the lower part; geodes incrusted with gypsum, and lenses of gypsum, are common in the upper part. Southeastward from the Laramie Range and Hartville area, the Minnekahta is increasingly gypsiferous. At Owl Canyon, gypsum quarried from a few feet above the Lyons may be a facies of the Minnekahta. However, it is more likely that a dolomite bed half a foot thick and 8 feet above the top of the gypsum is the Minnekahta, and that the gypsum is the bed included in the Opeche Shale Member at Red Mountain (fig. 2, section 9) and elsewhere in the Laramie Basin. In central Wyoming the Minnekahta Member intertongues with the Franson Member of the Park City Formation. In Nebraska and Kansas it correlates with the Blaine Formation (M. R. Mudge, oral communication, 1959), which is stratigraphically above the Blaine Gypsum of the type section in Oklahoma. At Boxelder Creek in northern Colorado the Minnekahta and Opeche may intertongue with the upper part of the Lyons Sandstone; but these units seem to thin and lap onto the previously deposited sandstone which locally is reworked into overlying and younger Minnekahta. Glendo Shale Member The Glendo Shale Member is between 50 and 60 feet thick at most places, but is as much as 80 feet thick at some places. The type locality of the Glendo designated by Condra and others (1940, p. 5) is “in Spring Creek Valley 1 mile south and 2 miles west of Glendo, Wyoming; land] comprises the interval between the Forelle and Minnekahta limestones . . .” This member, also, is widespread throughout most of eastern Wyoming and because of the characteristic lithologic features described below can be identified in the Laramie Basin where Minnekahta and Opeche are absent and the Glendo rests upon somewhat similar strata of the Owl Canyon Formation. The Glendo is composed dominantly of moderate reddish-orange mudstone and siltstone. The rock is mottled by abundant yellowish-gray to light-greenish-gray spots as much as % inch in diameter, which are a characteristic feature and aid identification of this member throughout southeastern Wyoming. This member probably was originally formed in parallel thin beds and laminae and tabular sets of low-angle small-scale cross laminae; however, at most places the bedding is now complexly contorted, perhaps because of slumping or flowage penecontemporaneous with deposition or during very early stages of compaction of the sediments. Locally, in the Laramie Basin, the Cheyenne area, and farther south along the Laramie Range in north-central Colorado, the Glendo or equivalent strata include anhydrite and gypsum lenses about 20 to 30 feet below the top of the member. These lenses grade into dolomite or limestone still farther south along the Front Range. In central Wyoming the Glendo intertongues with the Franson Member of the Park City Formation. It cor-B58 STRATIGRAPHY AND PALEONTOLOGY relates southeastward in Kansas, northeastern Colorado, and Nebraska with rocks equivalent to the Permian Whitehorse Sandstone of Oklahoma. Equivalent rocks in the Golden, Colo., area are the Harriman Shale, Falcon Limestone, and Bergen Shale Members of the Lykins Formation of LeRoy (1946). The Falcon previously has been correlated with the Minnekahta j1 however, in parts of the Laramie Basin and on the east side of the Laramie Range both Falcon and Minnekahta are present and are separated by about 45 feet of typical Glendo Shale Member. Forelle Limestone Member The Forelle Limestone Member, although only about 30 feet thick, is very widespread and extends throughout most of eastern Wyoming. The Forelle is generally a threefold unit consisting of finely crystalline dolomitic limestone in the upper and lower parts and an argillaceous limestone in the middle. Crenulated laminae and thin beds, probably algal, are characteristic of the Forelle, and at some places the upper part is formed of closely spaced domes 2 to 4 feet in diameter that are probably algal heads. The Forelle changes into anhydrite and gypsum east of the Laramie Range in eastern Wyoming. In the southern Black Hills, equivalent strata, included in the lower part of the Spearfish Formation, locally are partly composed of dolomite that retains the characteristic “crinkly” lamination of the Forelle (D. E. Wolcott, oral communication, 1959). The Forelle connects westward through the Big Horn Basin in north-central Wyoming with the middle or upper part of the Franson Member of the Park City Formation. A westward connection was illustrated by Thomas (1934, fig. 3, p. 1664), who showed the Forelle in central Wyoming as an eastward-extending tongue of the Park City Formation. The Forelle crops out discontinuously along the east side of the Laramie and Front Ranges in southern Wyoming and northern Colorado and is equivalent to the “Crinkly Sandstone” of Fenneman (1905, p. 25) or Glennon Limestone Member of the Lykins Formation of LeRoy (1946, p. 44) near Golden, Colo. The correlation of the Forelle with the “Crinkly” or Glennon is based on similarities of lithologic detail, especially the supposed algal structures, stratigraphic position above mudstone characteristic of the Glendo Shale Member, as well as correlations (M. R. Mudge, oral communication, 1957) of both the Forelle and “Crinkly” into the Day Creek Dolomite of Kansas and Nebraska. 1 T. L. Broin, 1957, Stratigraphy of the Lykins Formation of eastern Colorado : Colorado Univ., Ph. D. dissert. Difficulty Shale Member The Freezeout Tongue of the Chugwater Formation of Thomas (1934) is divided into an upper and a lower part by the eastward extension of the Ervay Member of the Park City Formation. Because of this division of the Freezout by the Ervay the concept of the Freezeout as a tongue is untenable, and consequently Thomas (oral communication, 1960) has recommended revision of the Freezeout. The lower part of the Freezeout, like other units of Upper Permian rocks in eastern Wyoming, is widespread and nearly uniform in thickness, generally about 50 feet thick. This unit, bounded by the Forelle and the Ervay Members is herein named the Difficulty Shale Member of the Goose Egg Formation. The type section for this unit is in the Freezeout Hills, in the SW1^ sec. 10, T. 24 N., R. 80 W., about % mile northeast of the location of the old Difficulty Post Office, and seems to be in the same location as the section described near Difficulty by Thomas (1934, p. 1680). Strata composing the Difficulty Shale Member are mostly moderate-reddish-orange parallel-laminated and thinly bedded mudstone and siltstone. The unit grades upward within a few feet into dolomite or gypsum of the overlying member. Westward the Difficulty Member grades laterally into carbonate rock of the upper part of the Franson Member of the Park City Formation in central Wyoming. In Colorado, equivalent strata are included in the Lykins Formation, probably in the lower part of the Strain Shale Member of LeRoy (1946). In Kansas the Difficulty seems to correlate with the Taloga Formation (Cragin, 1897).. Ervay Member The Ervay Member at the Goose Egg type section is 6 feet thick according to Burk and Thomas (1956). However, the underlying 98 feet of interbedded gypsum, carbonate rcok, and shale seems to be a facies of a thicker limestone section included in the Ervay farther west. In this article this gypsum is included in the Ervay. Strata equivalent to the Ervay extend throughout eastern Wyoming and are moderately well exposed in the Black Hills, Hartville area, and the northern part of the Laramie Range. The Ervay in southern Wyoming and its equivalent in northern Colorado is mostly gypsum ranging from 5 to 10 feet in thickness and is generally poorly exposed. The Ervay is mostly limestone and dolomitic limestone in western Wyoming but grades eastward to dolomite in central Wyoming and to gypsum in most of the eastern half of the State. The gypsum facies is com-MATJGHAN B59 posed of beds of gypsum or anhydrite interstratified with thin beds of reddish claystone or mudstone. The Ervay and equivalent strata are the youngest Permian rocks in Wyoming and are overlain with seeming conformity at most places by correlatives of the Dinwoody Formation of Early Triassic age. Southward thinning of the Ervay in the Laramie Basin as illustrated on figure 2 seems most likely due to truncation of the member prior to deposition of the overlying strata, although a slower rate of deposition in this area may account for the thinning. The truncation or depositional thinning suggests a minor tectonic movement of the nearby ancestral Front Range highland during or closely following the time of deposition of the Ervay. Freezeout Shale Member (restricted) The upper part of the Freezeout Tongue of the Chug-water Formation of Thomas (1934) lies above the Ervay Member and is overlain by the Little Medicine Member. The name Freezeout is restricted to this unit designated herein as the Freezeout Shale Member of the Goose Egg Formation. The type section of the restricted Freezeout is in the NE(4 sec. 2, T. 24 N., R. 80 W., and 1(4 miles northeast of Difficulty in the Freezeout Hills and is near the section described by Thomas (1934, p. 1680). It is 35 feet thick at the type section and ranges between 10 and 50 feet in thickness in southeastern Wyoming. The Freezeout, like the Difficulty Member, is mostly moderate-reddish-orange, parallel-laminated and thinly bedded mudstone and siltstone. It is gradational with the overlying member and commonly contains gypsiferous siltstone and thin beds of gypsum in its upper part. The Freezeout Shale Member grades westward into yellowish calcareous siltstone in the lower part of the Dinwoody Formation of Early Triassic age. On the basis of the blanketlike distribution of this member and of the strata which enclose it, the Freezeout is of the same age as the equivalent strata in the Dinwoody. Little Medicine Member The Little Medicine Member, although thin, is widespread and forms the top of the Goose Egg Formation. At the Goose Egg type section this member is 20 feet thick but ranges between 5 and 25 feet in thickness in southeastern Wyoming. It correlates westward into a part of the Dinwoody Formation of Early Triassic age in western Wyoming. The Little Medicine Member is gypsiferous and argillaceous dolomite or limestone in the northern Laramie Range, the Shirley Basin, and the Freezeout Hills. Southeastward of these areas this member is mostly 725-328 0—64---5 gypsum or anhydrite. At most places it includes thin beds of reddish siltstone and claystone interbedded with the sulfate and carbonate rocks. Similarities such as gradation of reddish mudstone of the Freezeout Member upward into the sulphate and carbonate of the Little Medicine, much like the gradation of the Difficulty into the Ervay Member, indicate that the pattern of sedimentation in Early Triassic time repeated that of Late Permian time. ROCKS ABOVE THE GOOSE EGG FORMATION The Goose Egg Formation is conformably overlain by a thick sequence of moderate-reddish-orange siltstone and very fine grained sandstone very similar to the older Owl Canyon Formation. These rocks are equivalent to the Red Peak Member of the Chugwater Formation of Love (1939). SEDIMENTATION AND ENVIRONMENT Sediments that formed the red beds within the Goose Egg Formation probably were the initial deposits in a sea that overspread a nearly level plain in most of eastern Wyoming and parts of adjacent States. This area probably was a vast shallow lagoon or tidal flat that extended from the edge of the deeper Phosphoria sea in central Wyoming eastward to the north end of, and far to the south along the east side of, the nearly buried ancestral Front Range highland. The hematitic claystone and associated evaporitic rocks, dolomite, and limestone, indicate a probable marginal marine environment with relatively high salinity and suggest a warm arid climate. The chemically deposited rocks suggest submergence of the detrital source areas or an increased rate of evaporation. Differences of salinity are indicated by deposition of dominantly carbonate rock of the Minne-kahta and Forelle Members and of gypsum of the lower part of the Opeehe, the Ervay, and the Little Medicine Members. These differences probably reflect variations in the strength and direction of currents within the lagoon and in variations in the inflow of water from the open ocean, but climatic variations may have affected the rate of evaporation also and accounted for the differences of salinity. REFERENCES Burk, C. A., and Thomas, H. D., 1936, The Goose Egg Formation (Permo-Triassie) of eastern Wyoming: Wyoming Geol. Survey Rept. Inv. 6, 11 p. Condra, G. E., Reed, E. C., and Scherer, O. J., 1940, Correlation of the formations of the Laramie Range, Hartville uplift, Black Hills, and western Nebraska : Nebraska Geol. Survey Bull. 13A (revised ed., 1950]. Cragin, F. W., 1897, Observations on the Cimarron series: Am. Geologist, v. 10, p. 703-737.B60 STRATIGRAPHY AND PALEONTOLOGY Darton, N. H., 1901, Geology and water resources of the southern half of the Black Hills and adjoining regions in South Dakota and Wyoming, in U.S. Geol. Survey Ann. Rept* 21, pt. 4; p. 489-599. ----—1904, Comparison of the stratigraphy of the Black Hills, Bighorn Mountains, and Rocky Mountain Front Range: Geol. Soc. America Bull., v. 15, p. 379-448. ----—1908, Paleozoic and Mesozoic of central Wyoming: Geol. Soc. America Bull., v. 19, p. 403-470. Denson, N. M., and Botinelly, Theodore, 1949, Geology of the Hartville uplift, eastern Wyoming: U.S. Geol. Survey Oil and Gas Inv. Prelim. Map 102, Sheet 2. Fenneman, N. M., 1905, Geology of the Boulder district, Colorado : U.S. Geol. Survey Bull. 265. LeRoy, L. W., 1946, Stratigraphy of the Golden-Morrison area, Jefferson County, Colorado: Colorado School Mines Quart., v. 41, no. 2. Love, J. D., 1939, Geology along the southern margin of the Absaroka Range, Wyoming: Geol. Soc. America Spec. Paper 20. Maughan, E. K., and Wilson, R. F., 1960, Pennsylvanian and Permian strata in southern Wyoming and northern Colorado, in Guide to the Geology of Colorado: Denver, Colo., Geol. Soc. America, Rocky Mountain Assoc. Geologists, and Colorado Sci. Soc., p. 34-42. Privrasky, N. C., and others, 1958, Preliminary report on the Goose Egg and Chugwater Formations in the Powder River Basin, Wyoming, in Wyoming Geol. Assoc. Guidebook 13th Ann. Field Conf.: p. 48-55. Thomas, H. D., 1934, Phosphoria and Dinwoody tongues in the lower Chugwater of central and southeastern Wyoming: Am. Assoc. Petroleum Geologists Bull., v. 18, p. 1655-1697.GEOLOGICAL SURVEY RESEARCH 1964 FORAMINIFERA FROM THE EXOGYRA PONDEROSA ZONE OF THE MARSHALLTOWN FORMATION AT AUBURN, NEW JERSEY By J. F. MELLO, J. P. MINARD, and J. P. OWENS, Washington, D.C. Abstract.—The Upper Cretaceous Marshalltown Formation, near the top of the Matawan Group, is exposed at Auburn, N.J., where it contains abundant specimens of Exogyra ponderosa (Roemer) and Ostrea species. A rock sample from this locality yielded an abundant foraminiferal fauna consisting of 30 identified species, 8 of which are planktonic. Comparison of these Foraminifera, listed but not described here, with the age ranges of the same species on the Gulf Coastal Plain suggests that the sample is of late Taylor age. A sample collected from an outcrop of the Upper Cretaceous Marshalltown Formation near Auburn in southwest New Jersey (fig. 1) has yielded an abundant microfauna. The microfossils occur in association with numerous megafossils, the most conspicuous of which are the thick shelled Exogyra, ponderosa (Roemer) and thin-shelled Ostrea species. The outcrop is at the head of the small gully in the south bank of Oldmans Creek at Camp Kimble. As defined by Stuart Weller (1907, p. 17), the Marshalltown is near the top of the Matawan Group of New Jersey (table 1), and below the Exogyra costata zone of the overlying Monmouth Group. A report on the microfauna from the base and middle of the Monmouth Group was published earlier (Minard and others, 1961). Table 1.—Marine Upper Cretaceous formations of New Jersey [Adapted from Richards and others, 1957] Group Subdivision Exogyra zone Red Bank Sand 1 Exogyra Icostata Monmouth Navesink Formation Mount Laurel Sand Wenonah Formation Marshalltown Formation Exogyra ponderosa Matawan Englishtown Formation Woodbury Clay Merchantville Formation Figure 1.—Index map showing localities discussed in text. Throughout much of its outcrop to the northeast, the Marshalltown is unfossiliferous. Foraminifera have been reported by Joyce Mumby (1961, p. 38) from Fellowship, N.J., and by Harold Gill1 from Mantua and Swedesboro, N.J., but no faunal lists accompanied either article. The Swedesboro locality may be the 1 Harold Gill, 1956, A stratigraphic analysis of the Matawan Group: Rutgers Univ., unpub. Ph. D. thesis. U.S. GEOL. SURVEY PROF. PAPER 501-B, PAGES B61-B63 B61B62 STRATIGRAPHY AND PALEONTOLOGY same as either locality 177 or 180 of Weller (1907, p. 82-84), both of which are only a short distance from the locality cited in this article. The Marshalltown outcrop at Auburn appears relatively unweathered. The rock is an unconsolidated olive-gray (5 Y 4/1) to olive-black (5 Y 2/1) clayey medium-grained feldspathic quartz-glauconite sand. Small clusters of pyrite are abundant. A high percentage of the glauconite grains are accordion forms (Galliher, 1935), a characteristic of glauconite from the Marshalltown Formation (Owens and Minard, 1960, p. B430). Heavy minerals include abundant apatite and some staurolite, sillimanite, kyanite, anda-lusite, biotite, chlorite, chloritoid, and homdblende. At Auburn, the Marshalltown is approximately 18 feet thick and is underlain by the very micaceous and clayey deposits of the Englishtown Formation (fig. 2). A similar relation has been observed along the strike from north of Fellowship to as far south as Auburn. This article lists the Foraminifera recovered from the Marshalltown sample and also indicates the time-stratigraphic position of this part of the Marshalltown with respect to the Upper Cretaceous sequence of the Gulf Coastal Plain. The Marshalltown sample contains a large foraminif-eral fauna both in terms of number of specimens and number of species. Because the aim of this study was to determine the age of this part of the Marshalltown, no attempt was made to identify all the species present. More intensive analysis probably would add to the number of species. The identified species indicate that this assemblage is of Taylor age. Two additional samples from the Marshalltown Formation near Auburn, previously ex- EXPLAN ATION I-!-'.--I h^l l-rs-l la al |<» w| Gravel Sand Clay Glauconite Mica Fossils Figuee 2.—Outcrop section at fossil locality, Camp Kimble, Auburn, N.J. amined by Ruth Todd (written communication, 1963), also contained Foraminifera of Taylor age, although fewer species were listed. The accompanying list of species (table 2) does not include data on the samples examined by Miss Todd. The ranges given for the identified species illustrate their known age ranges in the Cretaceous deposits of the Gulf coast. If a species has not been reported from the Gulf coast, or if its range is increased by an occurrence elsewhere, a notation is added. The correlation of L. W. Stephenson and others (1942, chart 9) between the standard European stages and the Gulf coast stratigraphic sequence is followed. The terms Austin age, Taylor age, and Navarro age are adopted from J. A. Cushman (1946), with time-stratigraphic boundaries between these units as defined by Stephenson and others (1942, p. 448, explanation of chart 9). Of the 30 identified species, 27 occur in the Gulf coast Cretaceous deposits and all but 3 of this number have ranges that include a Taylor age. All three Gulf coast species that have not been reported from the Taylor have been reported from the Navarro. One of these species, Fissurina marginata, is probably nondiagnostic. Another, Globigerina (Rugoglobigerina) rugosa, has been reported from older beds elsewhere than on the Gulf coast. The third species, Biglobigerinella bifora-minata, has been seen by the senior author in samples from the upper part of the Taylor Marl (Cushman Colin. 64875, 64877) and Pecan Gap Chalk Member of the Taylor Marl (Cushman Colin. 64876). Six of the eight planktonic species are reported from beds of Austin, Taylor, and Navarro ages on the Gulf coast, or from their age equivalents elsewhere. The two species with more restricted ranges are Globotruncana wilsoni (Santonian) and Hedbergella planispira (Albian, Cenomanian, and Turonian). The age restriction presently ascribed to G. Wilsoni can be discounted because this species has been reported only once before. Careful comparison of the Marshalltown specimens included under Hedbergella planispira with the type specimens of Globorotalia? youngi Fox, a junior synonym of H. planispira, leaves no doubt that they belong in the same species. It can only be concluded that H. planispira is longer ranging than was previously supposed. Pseudogaudryinella capitosa, Nonionella austinana, and Bolivinitella eleyi do not occur in beds younger than Taylor age in the Gulf coast deposits and have not been reported from younger beds elsewhere. Typical Taylor species, found in the Marshalltown sample, but which are not restricted to beds of this age, are: Bulimina reussi, Dentalina basitorta, Eouvigerina americana, and Pla/nulina taylorensis. We conclude that the foramini-MELLO, MUSTARD, AND OWENS Table 2.—Foraminifera from the Marshalltown Formation near Auburn, N.J. B63 Recorded ranges Species Gulf coast Austin Taylor Anomalina rubiginosa Cushman Biglobigerinella biforaminata (Hofker)__ Bolivina incrassata Reuss_______________ Bolivinitella eleyi (Cushman)___________ Bulimina prolixa Cushman and Parker.. Bulimina reussi Morrow__________________ Bulimina kickapooensis Cole_____________ Caucasina vitrea (Cushman and Parker). Dentalina basitorta Cushman_____________ Eouvigerina americana Cushman___________ Fissurina marginata (Walker and Jacob) x x X X X X X X X X Globigerina (Rugoglobigerina) rugosa Plummer? Globotruncana cretacea Cushman________________ Globotruncana lapparenti bulloides Vogler----- Globotruncana wilsoni Bolli___________________ Gyroidina depressa (Alth)_____________________ Hedbergella planispira (Tappan)--------------- Heterohelix globulosa (Ehrenberg)_____________ x x X X X Heterohelix pulchra (Brotzen)___________ Hoeglundina supracretacea (ten Dam)? x x X Lagena cf. acuticosta Reuss______________________ Marginulina cf. taylorana Cushman________________ Neobulimina canadensis Cushman and Wickenden Neobulimina spinosa Cushman and Parker----------- Nonionella austinana Cushman_____________________ Planulina taylorensis (Carsey)___________________ Pseudogaudryinella capitosa (Cushman)...........■ Pseudoglandulina cf. lagenoides (Olszewski)------ Pyrulina cylindroides (Roemer) ------------------ Textularia ripleyensis Berry_____________________ x x x X X X X X X X X X X X X Navarro Elsewhere Lower Cretaceous of Australia; Tertiary of Trinidad. x X X X X X X X X X One possible occurrence in beds of Navarro age. Especially common in beds of Taylor age. Early Campanian of California; Tertiary of Trinidad. Turonian to Maestrichtian of Trinidad. Turonian to Maestrichtian in several areas. Santonian of Trinidad. Eagle Ford Shale of Texas; Tertiary of Trinidad. Albian, Cenomanian. Santonian and Coniacian of western interior United States. Maestrichtian of New Jersey. Hauterivian of the Netherlands; Turonian of California. Hauterivian of the Netherlands. Eagle Ford Shale of Texas. Cenomanian of Egypt. x x x Albian of the Netherlands; Tertiary of Trinidad. feral evidence indicates a Taylor age for the Marshalltown sample, and that the large number of species which range into the Navarro suggest that the sample is probably of late rather than early Taylor age. REFERENCES Cushman, J. A., 1946, Upper Cretaceous Foraminifera of the Gulf coastal region of the United States and adjacent areas : U.S. Geol. Survey Prof. Paper 206, 241 p. Galliher, E. W., 1935, Geology of glauconite: Am. Assoc. Petroleum Geologists Bull., v. 19, no. 11, p. 1569-1601. Mlnard, J. P., Owens, J. P., and Todd, Ruth, 1961 Redefinition of the Mount Laurel Sand (Upper Cretaceous) in New Jersey: Art. 173 in U.S. Geol. Survey Prof. Paper 424-C, p. C64-C67. Mumby, Joyce, 1961, Second annual field conference: Atlantic Coastal Plain Geol. Assoc. Guidebook, p. 38. Owens, J. P., and Minard, J. P., 1960, Some characteristics of glauconite from the coastal plain formations of New Jersey: Art. 196 in U.S. Geol. Survey Prof. Paper 400-B, p. B430-B432. Richards, H. G., Groot, J. J., and Germeroth, R. M., 1957, Cretaceous and Tertiary geology of New Jersey, Delaware, and Maryland: Geol. Soc. America, Guidebook for field trips, Atlantic City mtgs. 1957, p. 183-230. Stephenson, L. W., King, P. B., Monroe, W. H., and Xmlay, R. W., 1942, Correlation of the outcropping Cretaceous formations of the Atlantic and Gulf Coastal Plain and Trans-Pecos Texas: Geol. Soc. America Bull., v. 53, p. 435-448. Weller, Stuart, 1907, A report on the Cretaceous paleontology of New Jersey: New Jersey Geol. Survey Paleontology Ser., v. 4, 871 p.GEOLOGICAL SURVEY RESEARCH 1964 RARE-EARTH SILICATIAN APATITE FROM THE ADIRONDACK MOUNTAINS, NEW YORK By MARIE LOUISE LINDBERG and BLANCHE INGRAM, Washin3ton, D.C. Abstract.—An apatite unusually rich in rare-earth oxides and silica, RA.i(Ca.Mn)7 (Si04) 2.s(P04)8.2F1.9(Oil)0.«, from the Adirondack Mountains, N.Y., contains 36.7 percent rare-earth oxides and 12.9 percent Si02. Unit-cell dimensions are: o=9.43±0.02, c=6.93±0.015 A; hexagonal; spaces group P6s/m; uniaxial negative; w=1.703±0.002, e=1.699±0.002. An apatite unusually rich in rare earths and silica, R+33.i(Ca,Mn)7(Si04)2.8(P04)3.2F1.9(OH)o.6, was submitted as a public sample from the Adirondack Mountains of New York. The exact locality is unknown, but the ratio of the rare-earth elements present is similar to that reported in apatite from the Mineville district, Essex County, N.Y. (McKeown and Klemic, 1956). The rare-earth apatite here described occurs as coarse (average size 1.0 mm) anhedral grains embedded in a black glassy matrix. It is yellow to pale reddish brown. Its unusual chemical composition was first indicated by the indices of refraction, very high for an apatite mineral, of w=1.703±0.002, e=1.699±0.002 (uniaxial negative). The specific gravity is 3.83±0.05, measured with a specific gravity bottle and toluene. The unit-cell size is: a=9.43±0.02, c=6.93±0.015 A. The apatite is partially metamict; the sharpness of the reflections and resolution of the 211-112 doublet is increased by heating. The X-ray diffraction data, given in table 1, are not unlike data of other apatite. The chemical analysis and molecular ratios are given in table 2. The analyzed sample of apatite contained no separate grains of impurity, no visible inclusions, and was significantly free of titanium, one of the principal constituents of the matrix. The ratio of titanium in the mineral to that in the matrix is 1: 500, calculated from 0.015 percent Ti in the purified apatite sample and 7 percent Ti in the matrix (Helen Worthing, written communication). Approximately three atoms of rare-earth elements, valence +3, substitute for calcium Table 1.—X-ray diffraction data on rare-earth apatite [Symmetry: hexagonal; space group: P6s/m (No. 176)] Calculated 1 Measured * Cu/Ni, X=1.5418 A Unheated Heated hkl tfAftl(A) I dhki (A) I dhhi (A) 100 8. 17 001 6. 93 101 5. 285 110 4. 717 200 4. 085 6 4. 095 15 4. 073 111 3. 900 3 3. 909 12 3. 880 201 3. 519 3. 465 002 50 3. 466 50 3. 435 102 3. 190 28 3. 193 35 3. 173 210 3. 088 14 3. 085 2. 811 30 3. 087 211 2. 820 } 100 / 100 2. 817 112 __ ... _ 2. 793 \ 50 2. 775 300 2. 723 23 2. 724 50 2. 721 202- 2. 642 16 2. 647 18 2. 629 301 2. 535 2. 358 220 003 2. 310 212 2. 306 310 2. 266 8 2. 265 20 2. 263 221 2. 233 103 2. 223 311 2. 154 4 2. 152 302 2. 141 113 2. 075 10 2. 080 18 2. 069 400 2. 043 203 2. Oil 15 1. 949 40 1. 946 4 1. 900 15 1. 895 25 1. 850 60 1. 845 4 1. 812 15 1. 828 4 1. 780 12 1. 784 4 1. 758 20 1. 759 22 1. 735 35 1. 724 4 1. 514 15 1. 507 4 1. 464 12 1. 479 20 1. 458 4 1. 439 12 1. 436 1 dhki calculated from a=9.43±0.02 A, e=6.93±0.015 A, the cell dimensions derived by precession camera techniques from unheated apatite crystals. 2114.59-mm camera. Film measurements corrected for shrinkage. Lower limit of 20 measureable approximately 7°. Intensities of reflections given for the unheated apatite are a percentage of the combined (unresolved) 211 and 112 reflections; intensities for the heated sample are in percentage of the resolved 211 reflection. Heating the apatite, which is partially metamict, increases the crystallinity; the cell size is decreased, the reflections are sharpened, and the absorption of radiation with increasing 6 is decreased. U.S. GEOL. SURVEY PROF. PAPER 501-B, PAGES B64-B65 B64LINDBERG AND INGRAM B65 atoms, with a concomitant substitution of three Si04"4 for three POT3 anionic groups. The black glassy matrix in which the apatite is embedded is radioactive and metamict; the unheated sam- the radioactive-radiation background; the 10 Mg, Fe________________________________________________ 10 Ca, K_________________________________________________ 0.3 Si, Mn________________________________________________ 0.1 Al, Ti, Ba____________________________________________ 0. 03 Table 2.—Microchemical analysis of ferroan northupite, Na3 (Mg, Fe)Cl(CC>3)2, with Mg:Fe 69:31, from Sweetwater County, Wyo. [Analyst: Robert Meyrowitz; analyses In weight percent] Na20 K20 Ferroan northupite 35. 6 <0. 2 10. 5 7. 6 0. 6 <0. 2 33. 6 13. 9 2. 2 NasFeCl (COa)! (theoretical) 33. 2 NasMgCl (COa)j (theoretical) 37. 37 MgO.. . . 16. 21 FeO 25. 6 CaO I C02 Cl Insoluble residue in (1 + 1) HC1 31. 4 12. 7 35. 38 14. 25 Subtotal 104. 0 102. 9 103. 21 1 1 1 1 1 1 1 1 1 1 1 1 1 1 5 II o -3. 1 -2. 9 -3. 21 Total 100. 9 100. 0 100. 00 Specific gravity.- .. 2. 52 1 2. 407 Index of refraction 1. 550 ± 0. 002 1 1. 514 1 Fahey (1962). tions of (1+1) HC1 insoluble residue, MgO, Na20, CaO, and K20. The first portion of the sample was decomposed by ignition at 900°C in a stream of oxygen. V205 was added to the sample to insure complete decomposition of all carbonates present. Total carbon dioxide was determined by use of a modified microcombustion train of the type used for the determination of carbon and hydrogen in organic compounds. The second portion of the sample was dissolved in nitric acid and filtered. An aliquot of the filtrate was used for the gravimetric determination of the chlorine as AgCl. An Emich microbeaker and sintered glass filterstick were used. The third portion of the sample was dissolved in 2.4A HC1. Aliquots of this solution were used for the spec-trophotometric determination of FeO and total iron using o-phenanthroline. The determinations of FeO and total iron were identical except that the addition of hydroxylamine hydrochloride was omitted for the determination of FeO. The concentration of FeaCh in the sample was calculated using the values for total iron and FeO. The fourth portion of the sample was boiled with (1 + 1) HC1 to determine the insoluble residue. AnB68 MINERALOGY AND PETROLOGY Emich microbeaker and sintered glass filterstick were used for the separation of the insoluble residue, which was dried to constant weight at 110°±5°C. The residue was washed with water before drying to constant weight. Aliquots of the filtrate from the acid-insoluble determination were used for the MgO, Xa20, CaO, and K20 determinations. MgO was determined by photometric microtitration with approximately 0.001 M standard disodium ethylenediamine tetra-acetate (Versene) using Erio-chrome Black T as the indicator. Na20 was determined by flame photometry (wavelength=589 m/u). The solution was compared to standard sodium solutions containing approximately the same concentrations of HC1, iron, and magnesium present in the solution analyzed. CaO was determined by flame photometry (wavelength = 554 rri/t). The solution was compared to standard calcium solutions containing approximately the same concentrations of HC1, iron, magnesium, and sodium present in the solution analyzed. K20 was determined by flame photometry (wavelength=768 mil). The solution was compared to standard potassium solutions containing approximately the same concentrations of HC1, iron, magnesium, and sodium present in the solution analyzed. Total iron (as Fe203) was determined by X-ray fluorescence (table 3) in almost colorless massive and yellow-green massive northupite, and also in the associated clear-green prismatic northupite. This last has a somewhat higher iron content than the sample analyzed in table 2 (total iron as FeO, 8.7 percent compared with 8.1 percent ). Table 3.—X-ray fluorescence determination of total iron in ferroan northupite [Analyst: Robena Brown] Type of ferroan northupite Total iron as FeaCh (weight percent) Total iron as FeO (weight percent) Almost colorless, massive 5.8 5. 2 Yellow green, massive Clear green, prismatic 8.4 7. 6 9.7 8. 7 The iron content of the deepest colored specimens, 8.7 percent FeO, is equivalent to about y3 molar ferroan northupite, and therefore is not enough to class the mineral as a species, its marked dissimilarity to ordinary northupite notwithstanding. The varietal name, ferroan northupite, however, does seem well justified. Why this variety should form where it does, in limited zones as compared with the far more abundant and widespread virtually iron-free northupite, is not known. The necessary iron is present almost throughout the formation as pyrite and (or) pyrrhotite. Siderite, though, is extremely rare, if not absent, in much of the Wyoming trona series of the Green River Formation. W. H. Bradley (personal communication) has observed siderite associated with pyrrhotite in relative abundance in upper beds of the Tipton Shale Member of the Green River Formation below the Wilkins Peak Member in which the trona series with ferroan northupite occurs. Various ionic modifications of the ordinary northupite structure are known, but ferroan northupite appears to be the first recognized with significant substitution of other ions for magnesium. The chlorine ion is replaced by S04 in the mineral tychite, and artificially, by Br"1 and Cr04"2 (Watanabe, 1933a, b). Also, Pen-field and Jamieson (1905) prepared octahedral crystals of composition 2MgC03 -2Na2C03 -MgC03, presumably carbonate tychite. The recognition of ferroan northupite in the trona series may have some economic or technologic interest in soda-ash refining, as it presents a possible source of soluble iron, which discolors the soda-ash product unless removed (W. E. Bauer, personal communication). REFERENCES Fahey, J. J., 1962, Saline minerals of the Green River Formation, with a section on X-ray powder data for saline minerals of the Green River Formation, by M. E. Mrose: U.S. Geol. Survey Prof. Paper 405, 50 p. Penfield, S. L., and Jamieson, G. S., 1905, On tychite, a new mineral from Borax Lake, California, and on its artificial production and its relations to northupite: Am. Jour. Sci., 4th. ser., v. 22, p. 217-224. Waring, O. L., 1962, The microspectrochemical analysis of minerals, II: Am. Mineralogist, v. 47, p. 741-743. Waring, C. L., and Worthing, H. W., 1961, Microspectrochemical analysis of minerals, with an accompanying mineralogical note by Alice D. Weeks: Am. Mineralogist, v. 46, p. 1177-1186. Watanabe, TokonosukS, 1933a, Synthese de la northupite, de la tychite et de nouveaux mineraux de meme groupe: Tokyo, Inst. Phys. and Chem. Research, Scientific Papers, v. 21 p. 1-29. ------ 1933b, Les structures crystalline de la northupite 2MgC03-2NaaC03 Na2S04: Tokyo, Inst. Phys. Chem. Research, Scientific Papers, v. 21, p. 40-62.GEOLOGICAL SURVEY RESEARCH 1964 WALSEN COMPOSITE DIKE NEAR WALSENBURG, COLORADO By ROSS B. JOHNSON, Denver, Colo. Abstract.—The Walsen composite lamprophyre dike of Eocene or early Oligocene age was intruded in three distinct stages into a tension joint trending normal to the northerly strike of the sedimentary wallrocks. The earliest dike was a soda-minette containing scattered xenoliths. The second dike, a minette, was emplaced along the north contact of the soda-minette. Finally, another minette was injected into shrinkage cracks in the earlier dikes. The Walsen dike (Knopf, 1936, p. 1764), an easterlytrending composite dike of late Eocene or early Oligocene age (Johnson, 1961, p. 580) made up of three separate lamprophyric intrusives, extends for 6y2 miles near Walsenburg, in south-central Colorado (fig. 1). The Walsen dike does not form a high vertical wall as do many of the nearby more silicic porphyry dikes of the Spanish Peaks radial dike system; however, the dike and the indurated sedimentary rocks adjacent to the dike form a conspicuous serrate ridge that stands 50 to 100 feet above the surrounding country. At the surface the sedimentary rocks cut by the Walsen dike (fig. 1) include Pierre Shale, Trinidad Sandstone, Vermejo Formation, Eaton Formation, and Poison Canyon Formation (Johnson, 1958, p. 563-565). The Trinidad Sandstone and Poison Canyon Formation are mainly sandstone and conglomerate; the other formations are predominantly shale. Coal occurs in the Vermejo and Eaton Formations. The Walsen dike is one of a large system of subparallel dikes that transect the radial dikes associated with the Spanish Peaks (Johnson, 1961, p. 581-586) southwest of Walsenburg. The dikes of this system extend for 36 miles from the Purgatoire Eiver on the south to the Huerfano Eiver on the north (Johnson and others, 1958), and they trend normal to the general strike of the folded sedimentary rocks. The strike of these dikes ranges from N. 60° E. in the southern part to N. 86° E. in the northern part of their outcrop area. It is believed that the dikes were intruded along tension fractures formed during folding of the structural Eaton basin in southern Colorado and northern New Mexico (Johnson,1961, p. 588). Most of the dikes are lamprophyres, and many are composite or multiple. They are easily eroded and generally not well exposed. However, the Walsen dike is transected by several roadcuts, a railroad cut, and an arroyo, and thus it can be more completely studied petrographically and structurally than other composite dikes in the Spanish Peaks region. The width of the dike is fairly uniform throughout most of its extent, varying between 20 and 30 feet. The dike is vertical, although its contacts with the enclosing rocks are locally irregular. Small high-angle reverse faults with several inches of displacement cut wallrock along the northern margin of the dike (fig. 2). The faults strike parallel to the dike, dip 60° to 70° toward the dike, and are separated vertically by as little as 10 feet. As a result of several inches of reverse dip-slip displacement along each fault, the preexisting tension fracture tends to widen upward. Otherwise, there is no apparent differential vertical displacement of the wallrock. Visible baking of the invaded sedimentary rocks extends as far as 10 feet on both sides of the dike and extends farther from the dike in shale than in sandstone and conglomerate. PETROGRAPHY The Walsen dike comprises three intrusives; a composite dike of soda-minette and minette, and a later minette intruded into shrinkage cracks and locally along both margins of the earlier dike (fig. 2). The composite nature of the dike was recognized by Knopf (1936, p. 1764-1765), who distinguished two intrusives, a biotite-augite vogesite, and a biotite lamprophyre. Hills (1900, B69 U.S. GEOL. SURVEY PROF. PAPER 501-B, PAGES B69-B73B70 MINERALOGY AND PETROLOGY EXPLANATION Dikes and sills .Tpc Poison Canyon Formation Raton Formation 7Z77 Vermejo Formation Trinidad Sandstone 37° 37' 30" Pierre Shale Contact Strike and dip of beds 104°52'30l COLORADO W alsenburg# 3 MILES Figure 1.—Geologic map of the area adjacent to the Walsen dike near Walsenburg, south-central Colorado. igneous geology sheet) apparently recognized only one intrusive and classed it as basalt. The earliest intrusive, a greenish-gray weathered soda-minette, makes up the southeastern part of the composite dike, and ranges from 10 to 13 feet in width. It was sampled at three places (Iocs. 1, 2, and 5, fig. 1). Phenocrysts are mainly biotite with augite as much as 2 mm across, and olivine as much as 4 mm across. The groundmass is microcrystalline and in thin section consists of analcitized sanidine, analcitized andesine (An35), red and brown biotite, diopsidic augite, apatite, ilmenite, and magnetite, and locally hematite, chloro-phaeite, bowlingite, iddingsite, clay, and an unidentified zeolite. The mineralogic composition (table 1) of the soda-minette varies slightly throughout the dike, but local variation is probably due to deuteric alteration. The only xenoliths found in the composite dike occur in this intrusive. At locality 1 a spherical 6-inch cobble of Precambrian gneiss is enclosed in the soda-minette. At locality 5 a highly baked angular block of Pierre Shale in almost its original orientation is separated from the south wall of the dike by 10 inches of soda-minette.JOHNSON B71 Figure 2.—Exposure of the Walsen dike at a highway cut on U.S. Highway 85, 87 (loc. 3) at the north limits of Walsenburg, Colo. Kp, Pierre Shale; Kpm, baked Pierre Shale; 8-M, soda-minette intrusive; Mi, first minette intrusive; M-Z, mixed zone; and Mi, second minette intrusive. View is toward the southwest. The second intrusive, a fairly hard durable light-gray minette, makes up the northwestern part of the composite dike. It ranges from 12 to 16 feet in width, but locally it is more than 20 feet wide. The minette was sampled at three places (Iocs, 4, 2, and fig. 1). Phenocrysts are mainly red biotite as much as 2 mm across with some olivine crystals as much as 4 mm across, a few augite crystals as much as 1 mm across, and local crystals of sanidine as much as 3 mm across. Under the microscope the groundmass consists of anal-citized sanidine, analcitized andesine (An35), red biotite, augite, apatite, ilmenite and magnetite, hematite, and locally serpentine, clay, and an unidentified zeolite. The soda-minette (first intrusive) and the minette (second intrusive) are separated by 2 to 3 feet of finegrained very hard and durable medium-gray micro-minette. This rock was sampled at three places (Iocs. 1, 2, and 4i fig- 1). The microscopic phenocrysts are mainly biotite, augite, and olivine. Serpentine and zeolite replace olivine, and a few crystals of olivine are rimmed with minute augite crystals and replaced by zeolite. Some of the biotite phenocrysts show resorbed ends. The modal composition is intermediate between that of the soda-minette and the minette (table 1), but is closer to that of the minette. The third intrusive, a minette that fills shrinkage fractures in the earlier rocks, was sampled at three localities (Iocs. 2, 4, and 5, fig. 1). This intrusive rangesB72 MINERALOGY AND PETROLOGY Table 1.—Average modal composition, in volume percent, of rocks of the Walsen dike [Compositions based on three samples from each zone) First intrusive (soda-minette) Mixed zone (micro-minette) Second intrusive (minette) Third intrusive (minette) Sanidine 17 26 28 24 01igoclase(An25)_ 18 Andesine (Ams). 24 22 19 Biotite 24 20 21 27 Augite.. 8 10 9 ■4 Olivine 2 4 5 Apatite . 4 3 4 4 Magnetite and ilmenite.. 17 15 13 11 Serpentine Tr. Tr. 2 Chlorophaeite. . Tr. Bowlin gite Tr. Iddingsite.. . Tr. Hematite and limonite 3 Tr. 1 7 Clay Tr. Tr. Calcite Tr. 1 Zeolite Tr. Tr. Tr. 2 from 3 inches to 3 feet in width. It is a friable rock, but on fresh exposures displays conspicuous flow banding (fig. 3). Although its structure gives the rock an appearance resembling some types of spheroidal weathering, the effect is quite distinct from the small amount of spheroidal weathering noted along some of the joint surfaces in the earlier dike rocks. It is medium light gray where fresh and medium reddish brown where highly weathered. In the weathered rock, sanidine and oligoclase (An25) are highly analcitized, and the rock breaks up into small pea-sized pebbles. Figure 3.—Closeup view of the Walsen dike, showing flowbanding in a minette, M2, here intruding an earlier minette, Mi. View is toward the north. Red biotite occurs in serial sizes up to phenocrysts as large as 3 mm across, olivine is absent, and augite occurs as clustered small crystals in the groundmass. In all samples, small vesicles make up 1 to 6 percent of the volume of the rock and are filled by calcite and an unidentified zeolite. Table 2.—Chemical analyses, in weight percent, of rocks of the Walsen dike [Rocks from loc. 2 (flg. 1); rapid rock analyses by P. Elmore, S. Botts, G. Chloe, L. Artis, and H. Smith, analysts] First intrusive (soda-minette) Mixed zone (microminette) Second intrusive (minette) Third intrusive (minette) Si02 45.3 47.1 47.1 46. 7 AI2O3 n. 2 11.5 11. 6 10. 9 Fe203 — 8. 2 6. 0 6. 4 9. 5 FeO 3. 6 3. 9 3. 4 1. 8 MgO 7. 0 8. 0 8. 3 6. 8 CaO. 9. 6 9. 5 9. 4 8. 6 Na20 2. 6 2. 6 2. 3 2. 1 K20 4. 0 4. 3 4 5 4. 6 H20- . 90 . 71 1. 3 2. 0 h2o+ 2. 5 2. 2 2. 2 2. 8 Ti02 2. 3 2. 2 2. 1 2. 0 P2O5 2. 3 1. 3 1. 4 1. 8 MnO . 15 . 14 . 16 . 16 C02 <. 05 <. 05 <. 05 <. 05 Total 100 100 100 100 Table 3.—Spectrographic analyses (semiquantitative) of rocks of the Walsen dike [J .C. Hamilton, analyst. Results reported in percent to nearest number in the series J, 0.7, 0.5, 0.3, 0.2, 0.15, and 0.1, etc., which represents approximate midpoints of group data on a geometric scale. The assigned group for semiquantitative results includes the quantitative value about 30 percent of the time. Symbols: M, major constituent (greater than 10 percent); 0, looked for but not detected; ...not looked for] First intrusive (soda-minette) Mixed zone (microminette) Second intrusive (minette) Third intrusive (minette) Si M M M M A1 7. 0 M 7. 0 7. 0 Fe.. 7. 0 7. 0 7. 0 7. 0 Mg 3. 0 5. 0 5. 0 5. 0 Ca M M M 5. 0 Na 3. 0 3. 0 3. 0 3. 0 K_ 5. 0 5. 0 5. 0 7. 0 Ti 1. 5 2. 0 1. 5 1. 5 P-. . 7 . 5 . 5 . 5 Mn . 07 . 07 . 07 . 05 Ba . 5 . 7 . 7 . 5 Be . 0002 . 0002 0 . 00015 Ce <. 05 <. 05 <. 05 0 Co . 005 . 005 . 005 . 003 Cr . 03 . 05 . 05 . 03 Cu . 01 . 01 . 01 . 015 Ga _ . 003 . 003 . 003 . 007 La . 015 . 015 . 015 . 007 Nb . 005 . 005 . 005 . 007 Ni . 02 . 02 . 02 . 03 Pb . 0015 . 0015 . 0015 . 0015 Sc . 002 . 003 . 003 . 003 Sr . 5 . 7 . 7 . 3 V . 05 . 05 . 05 . 03 Y Yb . 003 . 003 . 003 . 003 Zr . 03 . 03 . 03 . 02 Nd . 03 . 03 . 03 . 015JOHNSON B73 Petrographically, the minettes are typical biotite-syenite lamprophyres, and the soda-minette is a typical biotite-syenodiorite lamprophyre; the two types differ mainly in the ratio of the plagioclase feldspars to sani-dine (table 1). CHEMISTRY The soda-minette and minette of the [Walsen dike are chemically (table 2) classified as basic and unsaturated, metaluminous, and alkalic. In comparison with other syenites and syenodiorites in the Spanish Peaks region, they are high in Fe203, MgO, CaO, K20, H20, Ti02, and P205 content (table 2); the lamprophyres of the Walsen dike also have a relatively high content of Ba, Ce, Cr, Cu, Ni, Sc, Sr, V, Zr, and Nd (table 3). The chemical analyses (table 2) indicate that the lamprophyric intrusives of the Walsen dike were derived from a low-viscosity high-volatile olivine-nepheline-basalt parent magma (table 4). Table 4.—Normative composition, in weight percent, of rocks of the Walsen dike First intrusive (soda-minette) Mixed zone (microminette) Second intrusive (minette) Third intrusive (minette) or 23. 63 25. 41 26. 59 27. 18 ab 18. 38 13. 93 13. 61 17. 76 an__ 7. 08 7. 02 8. 04 6. 73 ne __ 1. 95 4. 36 3. 16 mt 5. 43 6. 65 5. 39 . 53 hm __ 4. 46 1. 41 2. 68 9. 14 il 4. 37 4. 18 3. 99 3. 80 ap 5. 45 3. 08 3. 32 4. 26 di 19. 86 24. 61 22. 91 18. 81 hy 3. 66 oL _ 5. 76 5. 96 7. 04 3. 19 Total 96. 37 96. 61 96. 73 95. 06 SEQUENCE AND MECHANICS OF EMPLACEMENT The soda-minette magma (S-M, fig. 2) appears to have been the first to be intruded. During its emplacement, blocks were torn from the wallrock to form xeno-liths; some were brought up from great depths, whereas others were merely separated from the wall and remained close to their original position and orientation. There does not appear to have been much melting or assimilation of the wallrock. The second magma, a minette {M,, fig. 2), was intruded along the north wall of the soda-minette, apparently before the soda-minette had cooled and completely solidified. The magma of the minette may have worked its way between the soda-minette and the wallrock, and then forced its way upward by separating the north wall from the soda-minette by creating a series of small reverse faults (fig. 2) which widened the fracture upward. The amount of assimilation of the invaded rock seems to have been of the same order as that for the soda-minette (table 2). The microminette (M-Z, fig. 2) between the soda-minette and minette intrusives appears to be a mixture of the two rocks. Reaction rims of minute augite crystals on some of the olivine phenocrysts, partial resorption of some of the biotite phenocrysts, and a chemical composition (table 2) intermediate between the compositions of the soda-minette and minette intrusives confirm the mixed origin of this rock. It resembles a chilled margin of minette against soda-minette; however, there is no corresponding chilled margin against the sedimentary wallrock, which certainly must have been as cool or cooler than the soda-minette at the time of the invasion of the minette magma. The third magma, a minette (M2, fig. 2), was injected after the first two intrusives had cooled and shrunk away from the wallrock. Cracks had formed across both of the early intrusives as well as the intervening mixed zone. A magma was forced upward through these shrinkage cracks along narrow tortuous channels. At the levels now exposed the magma appears to have been more viscous than the previous two magmas. This may be demonstrated by the flow banding observed in this intrusive. However, from the chemical analyses (table 2) and from the presence of vesicles, the magma appears to have remained fairly volatile until solidified. REFERENCES Hills, R. C., 1900, Description of the Walsenburg quadrangle, Colorado: U.S. Geol. Survey Geol. Atlas, Folio 68. Johnson, R. B., 1958, Geology and coal resources of the Walsenburg area, Huerfano County, Colorado : U.S. Geol. Survey Bull. 1042-0, p. 557-583. ------ 1961, Patterns and origin of radial dike swarms associated with West Spanish Peak and Dike Mountain, south-central Colorado: Geol. Soc. America Bull., v. 72, p. 579-590. Johnson, R. B., Wood, G. H., Jr., and Harbour, R. L., 1958, Preliminary geologic map of the northern part of the Raton Mesa region and Huerfano Park in parts of Las Animas, Huerfano, and Custer Counties, Colorado: U.S. Geol. Survey Oil and Gas Inv. Map OM-183. Knopf, Adolph, 1936, Igneous geology of the Spanish Peaks region, Colorado : Geol. Soc. America Bull., v. 47, p. 1727-1784.GEOLOGICAL SURVEY RESEARCH 1964 ZONAL FEATURES OF AN ASH-FLOW SHEET IN THE PIAPI CANYON FORMATION, SOUTHERN NEVADA By P. W. LIPMAN and R. L. CHRISTIANSEN, Denver, Colo. Work done in cooperation with the V.8. Atomic Energy Commission Abstract.—Chemical analyses from devitrified, lithophysal, and vapor-phase zones of an ash-flow sheet in southern Nevada, newly named the Yucca Mountain Member, indicate limited compositional variation. Nonwelded vitric tuff at the edges of the ash-flow sheet differs appreciably in composition from crystallized tuff because of incipient secondary alteration of metastable glass shards. In the vicinity of the southwestern part of the Nevada Test Site (fig. 1) a previously undescribed sheet of nonwelded to densely welded ash-flow tuff wedges into the Piapi Canyon Formation. The Piapi Canyon Formation has been dated by the potassium-argon method as about 13 million years old, near the Miocene-Pliocene boundary (R. Kistler, written communication, 1963). As originally described the Piapi Canyon Formation comprises 5 members, of which 4 are ash-flow sheets— in ascending order, the Stockade Wash, Topopah Spring, Tiva Canyon, and Rainier Mesa Members (Poole and McKeown, 1962). The fifth member, the Survey Butte, consists of lithologically distinctive ash-fall tuffs into which the three lower ash-flow sheets wedge out. The newly recognized sheet occurs immediately below the Tiva Canyon Member and conformably overlies a thick sequence of bedded tuffs correlative with the Survey Butte Member. In accordance with previous designation of major ash-flow sheets of the Piapi Canyon Formation as members, the newly described sheet is here named the Yucca Mountain Member. The northwest end of the mesalike part of Yucca Mountain in the Topopah Spring 15-minute quadrangle is designated the type locality because the member is best exposed there and because all its zones are represented. B74 116-30' Figure 1.—Map of the southwestern part of the Nevada Test Site and vicinity, showing areal extent (stippled), thickness, and type locality of the Yucca Mountain Member of the Piapi Canyon Formation. Isopachs show approximate thickness; contour interval is 100 feet. X, outcrop at which Yucca Mountain Member is absent. A, B, C, D, locations of measured sections that are shown on figure 2. U.S. GEOL. SURVEY PROF. PAPER 501-B, PAGES B74-B78LIPMAN AND CHRISTIANSEN B75 Outcrops of the Yucca Mountain Member are confined to about 20 square miles near the type locality and 5 square miles near Pah Canyon; the unit appears to have a more limited areal extent than other members of the Piapi Canyon Formation. From a maximum thickness of 250 feet near the type locality the sheet thins to the east and south. It underlies the entire west-central part of the Topopah Spring 15-minute quadrangle, and its depositional edge can be located almost continuously around the east and south sides of Yucca Mountain (fig. 1). The original distribution of the sheet has not been satisfactorily reconstructed to the north or west because of erosion, faulting, and cover by younger rocks. About 100 feet of the unit is present east of Fortymile Canyon, at Pah Canyon, and the depositional edge of the sheet has been mapped 2y2 miles south of that locality. Adequate exposures demonstrate that the sheet was not deposited between Yucca Mountain and Pah Canyon, and that the two outcrop areas apparently represent the southeastern ends of separate lobes of an ash-flow sheet which originated to the north and northwest. PETROLOGIC DESCRIPTION The Yucca Mountain Member before welding and crystallization was a distinctively uniform shard tuff containing only very small amounts of pumice, pheno-crysts, and lithic inclusions. The original character of the tuff can be determined by examination of the non-welded glassy margins of the ash-flow sheet. Refractive indices of unaltered glass shards average about 1.50. The phenocryst content of the tuff, mainly alkali feldspar and some oligoclase, is constant at about 1 per- cent. Quartz and mafic minerals are scarce. Pumice typically makes up 3 to 4 percent of the tuff but increases in abundance toward the edges of the ash-flow sheet, where it locally makes up as much as 10 percent. A few small grayish-red aphanitic lithic inclusions are present. The abundance of these constituents does not vary significantly in vertical sections of the sheet. This uniformity contrasts with other major ash-flow sheets of the Piapi Canyon Formation, especially the Topopah Spring and Tiva Canyon Members, in which pumice and phenocrysts increase in abundance upward in vertical sections. Tuffs of the Yucca Mountain Member closely resemble crystal-poor pumice-poor lower parts of the Topopah Spring and Tiva Canyon Members. Although relict shard textures and the proportions of pumice, phenocrysts, and lithic inclusions demonstrate initial vertical and lateral uniformity of the Yucca Mountain Member, differential welding and crystallization during cooling produced a variety of rocks that differ in color, density, crystallinity, and other physical properties. These variations are zonal in character and show a consistent pattern throughout the exposed part of the ash-flow sheet. Such zonal variations in welded ash flows have been discussed recently by Smith (1960). Smith’s concepts of welding and crystallization zones, although based on extensive field observations, were presented as hypothetical models. The Yucca Mountain Member provides a particularly fine example to illustrate Smith’s concepts because of its uniform simple composition, its uncomplicated cooling history, and because the distal end of the sheet, rarely preserved in prehistoric ash flows (Smith, 1960, p. 150), is well exposed in several places. FEET 250-i 200- 150- 100- 50- o-J EXPLANATION Figure 2.—Diagrammatic longitudinal cross section showing measured sections of the Yucca Mountain Member and schematic zonal variations of the ash-flow sheet. Numbers in section C indicate positions of analyzed samples (tables 1 and 2). Locations of sections shown on figure 1. The sections are plotted in order of decreasing distance from the distal edge of the sheet in such a manner as to emphasize the wedgelike character of the separate zones. 725-328 O—64——6B76 MINERALOGY AND PETROLOGY In Smith’s terminology, the Yucca Mountain Member is a simple cooling unit. The sheet is wedge shaped in cross section (fig. 2) and on a large scale can be divided into a nonwelded to welded glassy envelope enclosing a welded devitrified core. Where the de-vitrified core is thickest and most densely welded, it contains an inner zone characterized by lithophysal cavities (see Smith, 1960, pi. 21L). Most of the glassy part of the Yucca Mountain Member is nonwelded. Where the sheet is less than about 50 feet thick, the outermost part of the nonwelded zone is white to pink tuff that grades inward into gray tuff with the inception of welding. The gray tuff owes its color to magnetite crystallites, and the pink color of the peripheral tuff probably resulted from oxidation of magnetite to hematite where the outer part of the ash-flow sheet was in contact with air during cooling. Where the sheet is thicker, either nonwelded or incip-iently welded gray tuff extends to the base of the sheet, and underlying ash-fall and reworked tuffs are reddened to a depth of 6 to 10 inches indicating baking by the overlying ash-flow sheet. The nonwelded vitric shard tuffs of the Yucca Mountain Member appear unaltered in hand specimen, and the shards are transparent in thin section. Fine-grained dusty material is present around the edges of the shards, however, and X-ray analysis indicates that this material is a calcic montmorillonitic clay constituting 5 to 10 percent of the glassy tuffs. The transition from nonwelded to partly welded tuff, marked by the first recognizable deformation of shards or compaction of pumice (Smith, 1960, p. 151), is approximately coincident with a change in color from gray to orange brown or red brown. The partly welded rock commonly forms bluffs and has imperfect columnar jointing. In the area studied, devitrification extended into the zone of partial welding, and no vitro-phyre zone was formed. In most places the boundary between glassy and devitrified tuff is abrupt and can be located within a few inches. The boundary between zones of partial and dense welding, being within the zone of devitrification, cannot be precisely located because the primary porosity has been obscured by crystallization. The devitrified zone typically is composed of dense purple-brown welded tuff with closely spaced platy or semiconchoidal fractures subparallel to the eutaxitic foliation. X-ray examination shows that the devitrified rock consists mainly of alkali feldspar and cristobalite. Where the Yucca Mountain Member is thickest, the devitrified zone contains in its center a distinctive subzone characterized by lithophysal crystallization in roughly spherical to lenticular gas cavities. These cavities are as much as 5 cm in diameter and may produce as much as 25 percent bulk porosity. The lithophysal minerals are mainly alkali feldspar and tri-dymite. The zone of partial welding near the top of the sheet is thin and shows evidence of vapor-phase crystallization. This vapor-phase zone is inconspicuous, mainly because drusy crystallization of alkali feldspar and tridymite in the cavities of pumice fragments, the most distinctive feature of the zone (Smith, 1960, p. 156), was limited by the scarcity of pumice in the Yucca Mountain Member. Tuff of the vapor-phase zone is pale gray, in contrast to the brownish colors of welded tuff from the main part of the devitrified zone. CHEMICAL AND SPECTROGRAPHIC ANALYSES Some writers (for example, Smith, 1960, p. 156) have suggested that different crystallization zones which have developed in an initially homogeneous tuff might have chemical variations as a result of volatile transfer during crystallization. The possibility of such chemical variation in the Yucca Mountain Member resulting from devitrification, formation of lithophysae, or vapor-phase crystallization was tested by a series of chemical and semiquantitative spectrographic analyses. The Yucca Mountain ash-flow sheet is in certain respects a nearly ideal unit for such a study; it is quite homogeneous in composition and has a very low content of crystals and lithic inclusions throughout. A bulk analysis approximates the composition of the glass shards. Analyses were made of samples of four lithologic zones collected from a single vertical section of the Yucca Mountain Member, as follows: (1) the basal nonwelded glassy gray shard zone, (2) the densely welded devitrified zone, (3) the lithophysal zone, and (4) the vapor-phase zone. Positions of the analyzed samples are shown in figure 2. Chemical and semiquantitative spectrographic analyses are given in table 1. For direct comparison of the cationic constituents of the four zones, the chemical analyses have been recalculated free of water and calcite and are presented in table 2 as cation percentages. The cation percentages of the four zones sampled indicate, for the most part, strikingly little variation. Silicon averages 71.4 percent of the cations with a max-LIPMAN AND CHRISTIANSEN B77 Table 1.—Chemical and spectrographic analyses of ash-flow tuffs of the Yucca Mountain Member [Analyses given in weight percent; numbers in boxheads refer to locations shown on fig. 2; sample numbers in parentheses] Component 1 Nonwelded vitric zone (62L-50O)1 2 Densely welded devitrified zone (62L-50q) 3 Lithophysal zone (62L-50qq) 4 Vapor-phase zone (62L-50y) Chemical analyses: 2 Si02 .. 71. 5 76. 0 75.4 76. 4 Ti02 . 14 . 13 . 14 . 15 AI2O3 12. 6 13. 0 12. 3 12. 7 Fe203-- . 80 . 81 . 82 . 94 FeO . 14 . 17 . 16 . 03 MnO . 10 . 12 . 12 . 10 MgO . 86 . 20 . 30 . 07 CaO . 41 . 12 . 32 . 18 Na20 2. 8 4. 3 4. 0 4. 2 k2o 4. 8 4. 7 4. 6 4. 6 5. 6 . 68 . 93 . 40 C02 . 10 <. 05 . 19 <. 05 P205 . 02 . 02 . 02 . 03 Total. 99. 9 100. 3 99. 3 99. 9 Spectrographic analyses: 3 4 Ba __ 0. 01 0. 01 0. 01 0. 01 Be . 0005 . 0007 . 0007 . 0005 Cu . 0003 . 0003 . 0003 . 0005 Ga . 003 . 003 . 003 . 003 La . 003 . 003 . 003 . 003 Mo . 001 . 001 . 001 . 001 Nb . 002 . 003 . 003 . 002 Pb . 005 . 005 . 003 . 005 Sr . 005 . 003 . 003 . 002 V . 001 . 001 . 002 0 Y . 003 . 003 . 003 . 003 Yb . 0003 . 0003 . 0003 . 0003 Zr . 02 . 02 . 02 . 02 Powder density- 2. 39 2. 45 2. 54 2. 51 1 Refractive index of glass from the nonwelded vitric zone=1.498±0.001. 2 By rapid methods (Shapiro and Brannock, 1962) by P. Elmore, S. Botts, G. Chloe, L. Artis, and H. Smith. 3 By J. C. Hamilton. Results reported to the nearest number in the series 0.02, 0.015, 0.01, 0.007, 0.005, 0.003, 0.002, 0.0015, 0.001, 0.0007, 0.0005, 0.0003, which represent approximate midpoints of group data on a geometric scale. Assigned group for semiquantitative results will include the quantitative value about 30 percent of the time. < Other elements looked for but not found in any specimen: Ag, As, Au, B, Bi, Cd, Ce, Co, Cr, Eu, Ge, Hf, Hg, In, Li, Ni, Pd, Pr, Pt, Re, Sb, Sc, Sm, Sn, Ta, Te, Th, Tl, U, W, Zn. imum deviation of only 0.6 percent of that value. Total iron is virtually constant within a range of 2.5 percent of the mean value of 0.70 cation percent. The minor constituents titanium, manganese, and phosphorus are practically constant for all four zones, and the trace constituents have no major variations. The Fe+2/ Fe,„tai ratio is almost constant in all except the sample from the vapor-phase zone, a relation which indicates considerable oxidation in that zone. Of the remaining cations, all except possibly magnesium are constant within the limits of determinative error for the three crystallized zones, but they vary significantly between the glassy and crystalline rocks. It is notable that crystallization from a vapor phase, either in primary pore spaces of partly welded tuff or Table 2.—Cation weight-percentage compositions of ash-flow tuffs of the Yucca Mountain Member [Numbers in boxheads refer to locations shown on fig. 2; sample numbers in parentheses] Cation 1 Nonwelded vitric zone (62L-50O) 2 Densely welded devitrified zone (62L-50q) 3 Lithophysal zone (62L-50qq) 4 Vapor-phase zone (62L-50y) Si 71. 2 71. 0 71. 8 71. 7 Ti . 10 . 09 . 10 . 10 A1 14. 8 14. 3 13. 8 14. 0 Fe+3 . 60 . 57 . 58 . 66 Fe+2 . 11 . 13 . 12 . 02 Mn . 08 . 09 . 09 . 08 Mg 1. 27 . 25 . 42 . 10 Ca . 33 . 12 . 13 . 18 Na 5. 4 7. 8 7. 4 7. 6 K 6. 0 5. 6 5. 6 5. 5 P . 01 . 01 . 01 . 02 Total 100. 0 100. 0 100. 0 100. 0 . 71 . 70 . 70 . 68 Fe+2/Fet„,ai . 16 . 18 . 17 . 03 in the formation of lithophysae, has no measureable effect on the bulk composition of the rocks; only the local redistribution of major elements and the oxidation of iron in the vapor-phase zone appear to have been involved. The glassy tuff is higher in aluminum, magnesium, calcium, and potassium content and is much lower in sodium content than the crystallized rocks. Similar variations in several other paired analyses of glassy and devitrified ash-flow tuffs from the Piapi Canyon Formation indicate that these differences are not fortuitous (analyses 5 and 6 of Cornwall, 1962, table 2, are from the Tiva Canyon Member; other such analyses made by the U.S. Geological Survey and still unpublished have a similar pattern). The higher aluminum, magnesium, and calcium content of glassy tuff of the Yucca Mountain Member is explained by the presence of 5 to 10 percent calcic montmorillonitic clay coating glass shards as indicated by X-ray determination and optical estimates. The significance of the excess potassium in the glass is not entirely clear; possibly potassium has been added by base exchange within the glass. Although low sodium and high calcium content might indicate some base exchange between the clay mineral or the glass and ground water, only a small part of the sodium deficiency can be explained in this way. Considerable additional sodium would appear to have been leached from the metastable glass by percolating fluids. The noted presence of similar chemical patterns for other paired analyses indicates that leaching of sodium and formation of montmorillonitic clays may be common alteration features of rhyolitic glasses. AnalysesB78 MINERALOGY AND PETROLOGY of even apparently fresh glasses should be regarded with some caution as representatives of an original magma. REFERENCES Cornwall, H. R., 1962, Calderas and associated volcanic rocks near Beatty, Nye County, Nevada, in Engel, A. E. J., and others, eds., Petrologic studies (Buddington volume) : New York, Geol. Soc. America, p. 357-371. Poole, F. G., and McKeown, F. A., 1962, Oak Spring Group of the Nevada Test Site and vicinity, Nevada : Art. 10 in U.S. Geol. Survey Prof. Paper 450-C, p. C60-C62. Smith, R. L., 1960, Zones and zonal variations in welded ash flows: U.S. Geol. Survey Prof. Paper 354-F, p. 149-159. [1961] Shapiro, Leonard, and Brannock, W. W., 1962, Rapid analysis of silicate, carbonate, and phosphate rocks: U.S. Geol. Survey Bull. 1144-A, p. A1-A56.GEOLOGICAL SURVEY RESEARCH 1964 A WELDED-TUFF DIKE IN SOUTHERN NEVADA By P. W. LIPMAN, Denver, Colo. Work done in cooperation with the V.8. Atomic Energy Commission Abstract.—A small welded-tuff dike In an ash-flow sheet Is thought to represent an underlying nonwelded tuff that was remobilized and intruded into a dilatant tensional fracture in the still-hot sheet. During mapping of the 7%-minute Thirsty Canyon SE quadrangle in southern Nevada, a small tuff dike with welded pyroclastic textures was observed in intrusive contact with ash-flow tuff wallrock. Although a relatively minor feature, this dike is significant because pyroclastic intrusives, despite relatively widespread occurrence, rarely show compaction or welding features and are not known to occur within ash-flow sheets as feeders (Smith, 1960a, p. 817-818). A welded-tuff dike might readily be interpreted as a fissure vent, but in the present occurrence, substantial evidence favors an alternative interpretation—that the dike is part of a stratigraphically lower ash-flow tuff that was emplaced upward into hot dilatantly fractured volcanic country rock. Such an origin would be analogous to formation of clastic sandstone dikes. The dike occurs at lat 37°02'15" N., long 116°35'12" W. (about 15 miles northeast of Beatty, Nev., at the Nevada Test Site), in a talus block near the contact between two petrologically distinct cooling units1 of ash-flow tuff of the Rainier Mesa Member of the Piapi Canyon Formation (Pliocene or younger) (Poole and McKeown, 1962). The lower cooling unit of the Rainer Mesa Member is nonwelded to partly welded near the dike locality and contains 20 to 30 percent phenocrysts (varying mainly with degree of welding). The dominant phenocrysts are alkali feldspar and quartz, with minor plagioclase. Biotite forms 1 percent or less of the phenocrysts, and clinopyroxene is very scarce (absent in most thin sections). The upper cooling unit, eroded at its top, is densely welded to its base at the dike SW NE Figure 1.—Sketched cross section, showing relations between lower cooling unit and upper cooling unit of the Rainier Mesa Member, and location of talus block containing the dike. Patterning of upper cooling unit indicates approximate orientation of eutaxitic foliation. locality and averages about 35 percent phenocrysts. Its phenocryst proportions contrast strikingly with those of the lower cooling unit—plagioclase is almost twice as abundant as quartz, biotite averages 4 to 5 percent of the phenocrysts, and augite is fairly abundant. The upper cooling unit overlies the lower cooling unit unconformably, but the surface of uncomfority is barely discordant in most places. In a few places, including the dike locality, the upper cooling unit was deposited on an irregular surface of several hundred feet of relief eroded on the lower cooling unit. Zones of welding in the lower cooling unit are truncated, and the compaction foliation of the upper unit dips at high angles, locally approaching vertical. The structural relations between the two cooling units at the dike locality are shown in figure 1. 1 Terminology of ash-flow tuffs as used by Smith (1960a, 1960b). B79 U.S. GEOL. SURVEY PROF. PAPER 501-B, PAGES B79-B81B80 MINERALOGY AND PETROLOGY The dike is nowhere exposed in place. The talus block in which it occurs is about 5 feet across and lies about 20 feet below the base of the upper cooling unit (fig. 1). Despite the detrital nature of this block, the original position of the dike can be closely determined because of certain zonal welding and crystallization changes in the upper cooling unit. Both the wallrock of the dike and the lithologically similar basal part of the upper cooling unit are dark gray because of the presence of abundant microlites of magnetite. Since the upper cooling unit changes color and becomes red brown about 10 feet above its base because of oxidation of the magnetite microlites to hematite, the block containing the dike must have come from within a few feet of the contact between the upper and lower cooling units. The dike is red brown, in contrast to the dark-gray wallrock; it has generally planar parallel contacts and averages about 16 inches in width (fig. 2). Its exposed length is about 4 feet. It truncates the well-developed eutaxitic foliation of its country rock at about 65° and contains a lenticular inclusion of the country rock oriented parallel to the walls of the dike. The eutaxitic foliation of the inclusion is at an angle of about 25° to foliation in the wallrock, indicating rotation of the inclusion during emplacement of the dike. This inclusion shows that the dike was emplaced after welding of the upper cooling unit. The pyroclastic texture of the dike is obscure in outcrop, but is evident in thin section (fig. 3). Pumice lapilli are thoroughly compacted and are parallel to sides of the dike at a large angle to foliation in the wallrock. Petrographically the dike closely resembles tuff of the lower cooling unit of the Rainier Mesa Member, except that it shows a greater degree of welding. The proportions of major and minor phenocrysts are strik- Figure 2.—Welded-tuff dike cutting upper cooling unit of the Rainier Mesa Member. Dark inclusions in center of dike are recognizable wallrock. Pencil on wallrock shows scale. Contact I DIKE „ I . WALLROCK l____5 mm_____, Figure 3.—Photomicrograph showing truncation of wallrock foliation by eutaxitic foliation of dike. ingly similar. As in the lower cooling unit, the phenocrysts in the dike are mainly alkali feldspar and quartz, with little plagioclase; only about 1 percent of biotite is present, and clinopyroxene is absent. Figure 4, Quartz Figure 4.—Triangular diagram showing variations in proportions of quartz and feldspar phenocrysts in the dike (open circle), the lower cooling unit (dots), and the upper cooling unit (crosses) of the Rainier Mesa Member. Dashed lines are tie lines connecting samples from the same vertical section.LIPMAN B81 based on modal counts of 1,400 to 2,000 points in single thin sections, shows proportions of feldspar and quartz, which together account for most of the phenocrysts in both ash-flow and dike rocks. All samples of the Rainier Mesa Member were collected within 1 mile of the dike locality and either within a few feet above the base of the upper cooling unit or within a few feet below the uppermost exposures of the lower cooling unit. Samples A and B are from an outcrop immediately above the dike locality. The compositional range of the lower cooling unit is greater than that of the upper, probably because irregular erosion of its top has led to sampling of different despositional levels within the cooling unit. In contrast, all samples of the upper cooling unit should be from the same depositional level, and the spread of points for these samples in figure 4 probably represents the expectable degree of scatter from sampling and counting inaccuracies. The petrologic similarity of the dike to the lower cooling unit and the structural position of the dike only a few feet above the contact between cooling units strongly suggest that the dike was formed by secondary mobilization of tuff from the lower cooling unit and that it is not a primary igneous feature. By this hy- pothesis the heat for welding (“fusion”) of the dike would have come from the wallrock, and intrusion of the dike would have immediately followed emplacement and welding of the upper cooling unit. Perhaps a tensional fracture developed in the upper cooling unit as a result of small-scale flowage during welding and compaction on a slope and provided structural control for intrusion of the dike. The nonwelded tuff of the lower cooling unit then would have been mobilized by the pressure potential arising from dilatant fracturing, perhaps assisted by expansion and volatilization of interstitial water heated by the overlying ash-flow sheet. A similar mechanism of emplacement has been deduced by Walton and O’Sullivan (1950) for a clastic sandstone dike that was injected into a hot dolerite sill. REFERENCES Poole, P. G., and McKeown, F. A., 1962, Oak Spring Group of the Nevada Test Site and vicinity, Nevada: Art. 80 in U.S. Geol. Survey Prof. Paper 450-C, p. C60-C62. Smith, R. L., 1960a, Ash flows. A review: Geol. Soe. America Bull., v. 71, p. 795-842. Smith, R. L., 1960b, Zones and zonal variations in welded ash flows: U.S. Geol. Survey Prof. Paper 354-F, p. 149-159. [1961] Walton, M. S., Jr., and O’Sullivan, R. B., 1950, The intrusive mechanics of a clastic dike: Am. Jour. Sci., v. 248, p. 1-22.GEOLOGICAL SURVEY RESEARCH 1964 A NEW URANYL TRICARBONATE, K2Ca3(UO2)2(CO3)6*9-10H2O By ROBERT MEYROWITZ, DAPHNE R. ROSS, and MALCOLM ROSS, Washington, D.C. Abstract.—A new uranyl tricarbonate, K20a.i CL702) 2 (COn) a • 9-IOIIlO has been synthesized using U02(N03)2-6H20, K2C03, and Ca (N03)2-4H20. The green-yellow crystals show parallel extinction. They are biaxial positive, 2V=20°-30°; a= 1.544±0.003, /3=1.549±0.003, and y=1.563±0.003 (white light). The measured and calculated specific gravities are 2.93 and 3.01 g/cm3 respectively. The compound is orthohombic, space group Pnmn (No. 58) or Pn2n (No. 34), with a=17.98 A, 5=18.29 A, c=16.95 A, V=5,574 A3, and Z=8. Two quantitative chemical analyses and X-ray powder data are given. A new uranyl tricarbonate, KijCasCUOa^COs^^-10TI.O, has been synthesized. This green-yellow crystalline compound was obtained either alone or with liebigite, Ca2U02(C03)3-10H20, using K2C03 as a source of the carbonate (Meyrowitz and others 1963). Its powder X-ray diffraction pattern is identical to that of a crystalline substance obtained by M. E. Thompson (oral communication, 1953) while attempting to synthesize liebigite by a procedure similar to that used by Axelrod and others (1951) in the synthesis of bayleyite. The initial crop of crystals obtained by M. E. Thompson by allowing the solution containing the proper salts to evaporate at room temperature contained potassium. At that time (1953) the compound was considered to be an unknown substance because its powder X-ray diffraction pattern could not be identified. Because this compound formed in so many experiments performed by Meyrowitz in 1958, we decided it was a stable compound worth further investigation. The following reproducible procedure for the synthesis of this compound was developed. Twenty milliliters of an aqueous solution containing 5.02 grams U02(N03)2-6H20 equivalent to 0.01 mole TJ03 is added dropwise with constant stirring to 200 ml of an aqueous solution containing 4.15 g anhydrous K2COs equivalent to 0.03 mole C02. The mixed solution is allowed to stand until the small amount of yellow amorphous precipitate that forms coagulates and set- B82 U.S. GEOL. SURVEY PROF. ties to the bottom of the beaker. The mixture is filtered through a fine filter paper. Twenty ml of an aqueous solution containing 3.54 g Ca(N03)2-4H20 equivalent to 0.015 mole CaO is added slowly with constant stirring to the filtered solution. The pH of the solution is then adjusted to 8.5 by the dropwise addition of a dilute solution of K2CO3. The beaker is sealed with a plastic film to retard evaporation and is allowed to stand for approximately 4 weeks. The crystals are then detached from the sides and bottom of the beaker and washed a few times by decantation with water. Most of the excess water is removed by rolling the crystals on absorbent paper. The crystals (some as large as 1X4 mm) are finally air dried. Two preparations of the compound were analyzed (table 1) by semimicrochemical procedures. Carbon dioxide was determined on one portion of each sample by decomposing with HC1 and absorbing the C02 in a microabsorption train. Water was determined on a second portion with a modified microcombustion train of the type used for carbon and hydrogen determinations in organic compounds. The samples were decomposed by ignition at 900°C in a stream of oxygen. The third portion of each sample was dissolved in dilute nitric acid, and aliquots of this solution were used for determining U03, CaO, and K20. U03 was determined spectrophotometrically with ammonium thiocy- Table 1.—Chemical composition of a new uranyl tricarbonate 1 [Analyst: Robert Meyrowitz; analyses in weight percent] KjCaatUOjU KjCa3(UOs)i Sample Sample (COsJe-OHaO (CO3)e40H2O Constituent SRM-S SRM-10 {theoretical) (theoretical) K20_______________ 7. 6 7. 4 7. 4 7. 4 CaO______________ 14. 0 14. 4 13. 3 13. 2 U03______________ 44. 3 44. 8 45. 4 44. 7 C02_______________ 20. 7 20. 7 21. 0 20. 6 H20_______________ 13. 7 12. 9 12. 9 14. 1 Total_________ 100. 3 100. 2 100. 0 100. 0 1 Specific gravity, 2.93 PAPER 501-B, PAGES B82-B83MEYROWITZ, ROSS, AND ROSS B83 Table 2.—X-ray powder data for K2Ca3(U02)2 (CO3)«*9-10 H20 1 [Sample SRM-10] d( A) d (A) 4(A) /(A)> (meas.) (calc.)3 hkl KA)1 (meas.) 12. 82 110 6 3. 40 12. 43 Oil 2 3. 34 12. 33 101 5 3. 28 10. 23 111 6 3. 22 9. 15 020 6b 3. 17 8. 99 200 6 3. 15 100 8. 7 8. 48 002 9b 3. 13 7. 94 201 14 3. 10 7. 67 102 9b 3. 07 7. 35 121 6 3. 05 7. 28 211 4 3. 02 7. 07 112 4 2. 96 36 6. 40 6. 41 220 4 2. 93 4 6. 25 6. 22 022 7 2. 91 6. 17 202 11 2. 86 7 6. 03 6. 00 221 4 2. 83 13 5. 95 5. 87 122 18 2. 75 5. 84 212 7 2. 72 5. 77 130 2 2. 70 4 5. 73 5. 74 031 4 2. 63 5. 70 310 4 2. 60 5. 65 301 4 2. 59 11 5. 50 5. 47 131 6 2. 57 5. 40 311 4 2. 52 4 5. 43 5. 40 013 9 2. 50 5. 39 103 4 2. 478 46 5. 17 5. 17 113 4 2. 445 5. 11 222 6 2. 428 6 4. 94 4. 89 302 6 2. 421 4. 84 231 7 2. 412 4. 81 32] 4 2. 406 4. 78 203 7 2. 371 4. 77 132 7 2. 366 4. 73 312 7 2. 358 4. 64 123 6 2. 352 31 4. 60 4. 63 213 6 2. 313 4. 57 040 4 2. 225 11 4. 51 4. 50 400 6 2. 203 11 4. 37 4. 34 401 7 2. 148 4. 34 232 4 2. 143 20 4. 32 4. 31 322 6 2. Ill 4. 29 141 16 2. 105 4. 27 330 11 2. 100 4. 24 223. 7 2. 092 4. 24 004 7 2. 087 14 4. 21 4. 23 411 4 2. 069 4 4. 17 4. 14 331 4 2. 064 4. 14 033 6 2. 052 4. 12 104 7 2. 040 4. 11 303 6 2. 036 24 4. 06 4. 08 240 7 2. 018 4. 04 133 6 2. 014 4. 03 420 4 1. 995 4. 02 042 4 1. 924 11 4. 00 4. 02 114 11 1. 913 4. 01 313 11 1. 908 9 3. 96 4 1. 826 7 3. 92 11 1. 766 11 3. 82 7 1. 761 24 3. 59 4 1. 708 9 3. 55 9 1. 701 14 3. 51 7 1. 696 1 CuKa radiation, Ni filter (X=1.5418 A) Camera diameter: 114.59 mm. Lower limit d measurable: approximately 11.0 A. 2 Intensities were measured with a calibrated intensity strip. 3d-spacings were calculated from the following unit-cell data: orthorhombic, Pnmn, a = 17.98 A, 6 = 18.29 A, c = 16.95 A. All calculated spacings > 4.00 permitted by the space group are listed. anate in an acetone-water medium. CaO was determined by flame photometry (wave length=554 mg). The solution was compared with standard calcium solutions containing approximately the same concentration of uranium and potassium present in the solution analyzed. K20 was determined by flame photometry (wave length=768 mg). The solution was compared with standard potassium solutions containing approximately the same concentration of uranium and calcium present in the solution analyzed. The specific gravity (sample SRM-10) was determined by the hydrostatic weighing method. A 5-ml Erlenmeyer flask and toluene were used. The sample size for the specific-gravity determination was approximately 600 milligrams. Single-crystal studies of K2Ca3(U()2)2(C03)6-9-10H2O (sample SRM-10) were made with the Buerger precession camera using molybdenum (X=0.7107 A) and copper (A=1.5418 A) radiation. Patterns were taken of the hk0, 0kl, hkl, 1 kl, and 2kl reciprocal lattice nets. The compound is orthorhombic, space group Pnmn (No. 58) or Pn2n (No. 34), with a= 17.98 A, 6 = 18.29 A, u=16.95 A, V=5,574 A3, and Z=8. The calculated (for K2Ca3(lI02)2(C03)6,9H20) and observed specific gravities are 3.01 and 2.93 g/cm3, respectively. The indexed X-ray powder data for this compound are given in table 2. The optical properties of sample SRM-10 as determined by Thomas L. Wright, U.S. Geological Survey, using white light are: biaxial positive, a=1.544±0.003, p=1.549±0.003, o=1.563±0.003, and 2V=20°-30°. The crystals show parallel extinction. The synthetic compound described in this article belongs to a group of compounds in which the uranyl tricarbonate complex is the only anion. However, the new substance is the only member of this group in which the ratio of monovalent to divalent cations is 2:3. The other members of the group have either all monovalent cations, all divalent cations, or a ratio of monovalent to divalent cations of 2:1. REFERENCES Axelrod, J. M. Grimaldi, F. S., Milton, Charles, and Murata, K. J., 1951, The uranium minerals from the Hillside mine, Yavapai County, Arizona: Am. Mineralogist, v. 36, p. 1-22. Meyrowitz, Robert, Ross, D. R., and Weeks, A. D., 1963, Synthesis of liebigite: Art. 43 in U.S. Geol. Survey Prof. Paper 475-B, p. B162-B163.GEOLOGICAL SURVEY RESEARCH 1964 FRACTIONATION OF URANIUM ISOTOPES AND DAUGHTER PRODUCTS IN WEATHERED GRANITE AND URANIUM-BEARING SANDSTONE, WIND RIVER BASIN REGION, WYOMING By J. N. ROSHOLT; E. L. GARNER,1 and W. R. SHIELDS,1 Denver, Colo.,- Washington, D.C, Abstract.—Isotopic ratios of U235/!'234 for three samples representing different stages of weathering of granite show 7 to 23 percent deficient U234. The slightly weathered rock is most deficient, suggesting major U234 leaching at an early stage in the decomposition. Isotopic ratios in samples from a uranium deposit in sandstone showed slight excess U234 in unoxidized sandstone and up to 72 percent excess U234 in parts of the adjoining oxidized sandstone characterized by relatively high uranium content. Th230/!?234 ratios indicate relatively recent deposition of redistributed uranium in parts of the oxidized sandstone where the XJ234/!!235 ratio is high. The low U234/ U235 ratios prevailing in uranium-poor parts of the oxidized sandstone are believed to have resulted from preferential leaching of U234 in these places and over a considerable time. The use of abundance of uranium isotopes in geochronology of the Pleistocene, as suggested by Thurber (1962, 1963), in Pa231/Th230 chronology (Rosholt and others, 1961), and in Th230/Th232 chronology (Goldberg and Koide, 1962), depends on an extensive knowledge of the fundamental physico-chemical behavior of U234 daughter product in relation to parent U23S in hydro-logic environments. It has been shown that significant fractionation exists between U234, with a 250,000-year half life, and the longer lived isotopes, U238 and U235, in sandstone-type uranium deposits (Rosholt and others, 1963). Most phases of the hydrologic environment should be investigated, including the environmental effect on uranium in its ultimate source, igneous rocks. Preferential leaching of U234 from a variety of rock types has been demonstrated by measurements of U234/ U238 ratios in waters draining uranium-bearing host rocks (Ancarani and Bettinali, 1960; Koshelev and Syromyatnikov, 1961). Ratios of U234/U238 and Th230/ 1 National Bureau of Standards. Th234 in natural waters, fossil bones, soils, and shells of fresh-water mollusks have been investigated by Cherdyntsev and others (1963). More detailed study of the mechanism of fractionation, starting from the ultimate source of uranium and progressing through the hydrologic cycle of uranium, is needed to throw light on the specific controls involved. This article compares the U235/U234 fractionation pattern observed in 3 samples of granite from the Owl Creek Mountains, Wyo., with that noted in 11 samples of ore and barren rock taken across the contact of a typical roll-type sandstone deposit of uranium in the adjoining Gas Hills area of the Wind River basin, Wyo. In addition, the study of the variation of the radioactive-equilibrium ratios of Th230 to U234 and of Pa231 to U235 or U238 within the part of the deposit sampled provides a further useful tool in working out the mechanism of uranium-isotope fractionation. Investigation of uranium-bearing sandstones that have been saturated with ground water provide a desirable area for preliminary study because of the abundant supply of uranium and extensive geological and geochemical knowledge of this type of deposit. PROCEDURE Isotopic ratios of uranium were measured on a 12-inch, 60°-sector mass spectrometer (Rosholt and others, 1963). Uranyl nitrate was prepared from the rock samples by extraction with ethyl acetate after dissolution of uranium from rock or ore with concentrated nitric acid. Sufficient sample was used to yield from 1 to 5 milligrams of uranium. Approximately 50-microgram uranium aliquots of the uranyl nitrate solution B84 U.S. GEOL. SURVEY PROF. PAPER 501-B, PAGES B84-B87ROSHOLT, GARNER, AND SHIELDS B85 were used for each mass-spectrometric measurement. Variations of the ratios were determined by comparison of the ratios of U235/234 and U235/238 in the National Bureau of Standards reference sample with ratios in the sample. The reference sample is Republic of Congo pitchblende ore. No significant variations in the U235/ U238 ratio were found at the ^-percent confidence level in the samples. Direct comparison of isotopic ratios in reference standards and in samples is shown in tables 1 and 2. Illustration of the roll feature shows the relation of each sample to its percentage isotopic variation, 8, where 8 (percent) = 100 £ U235/U234 (reference) >} U235/U234 (sample) as shown in figure 2. The isotope-ratio term in the above equation is shown in tables 1 and 2. The numerical result is the same as the U234/U235 (sample) ratio, expressed in radioactive equivalent units; and the ratio is stated in this form in much of the subsequent discussion. Since no significant variation in the IT235/!?38 ratio occurs, U234 daughter is frequently compared to U238 parent rather than to U235. Radiochemical methods (Rosholt, 1957; Rosholt and Dooley, 1960) were used for the determination of the radioactive daughter products in the decay series below uranium. The results for these daughter products and for U234 in table 3 are expressed as equivalents to the parent nuclides in terms of percent equivalent. GRANITE Samples of weathered granite, weighing approximately 5 pounds each, were collected from Copper Mountain in the Owl Creek Mountains which flank the north side of the Wind River basin, as shown by Woodmansee (1958, fig. 1). It is not known whether this particular granite contributed to the detritus making up a large part of the upper coarse-grained facies of the Wind River Formation in the Gas Hills area (Zeller, 1957, p. 157); however, in general, it may be similar to granite which contributed uranium and sediments to a typical intermontane basin. Fresh rock could not be obtained from the outcrops at Copper Mountain. The fresh granite sample (256179) was taken from a drill core at a 50-foot depth in granite on the south side of Heath’s Peak, sec. 14, T. 27 N., R. 84 W., in the Pedro Mountains, Carbon County, Wyo. (Bell and Harshman, report in preparation). Ura-ninite is known to occur in granite in this area, and the rock sampled is apparently mineralized, as indicated by its uranium content. The results in table 1 show a correlation between the U234/IT235 ratio and the degree of weathering. The slightly decomposed granite has the lowest U234/U235 ratio, indicating that U234 is preferentially leached with respect to U238 and U235 at an early stage in the decomposition of the rock. Enrichment by uranium with a higher U234/U235 ratio may have occurred in the very weathered rock, as indicated by the anomalously high uranium content. URANIUM-BEARING SANDSTONE Uranium-ore samples from sandstone were collected by D. H. Norton, U.S. Atomic Energy Commission, in 1958 from the south pit wall of Lucky Me Project 4A mine, sec. 26, T. 33 N., R. 90 W., Gas Hills area, Fremont County, Wyo. The deposit is in the Wind River Formation of the Wind River basin and has been described by Zeller (1957, fig. 1), together with the stratigraphy and structure of the Gas Hills area. The lithologic features shown in figure 1 indicate a contact between oxidized and unoxidized sandstone in the wall of the mine, several feet below the water table. Normally, in this area, sandstone is oxidized above the water table and unoxidized below; thus, oxidized sandstone on the concave side of the contact may be the result of a geochemical process different from the surface oxidation above the water table. Somewhat similar contacts between altered and unaltered sandstone have been reported in deposits below the water table in the Shirley basin (Harshman, 1962, fig. 122.1). Results of analyses of 18-inch vertical channel samples taken at approximately 6-inch intervals across the contact are shown in tables 2 and 3. Table 1.—Isotopic ratios of uranium in granite samples from Fremont and Carbon Counties, Wyo. USOS sample number Degree of weathering 256179 2_____ Very fresh________ 256175 _____ Slightly weathered. 256176 _____ Weathered_________ 256177 2____ Very weathered____ U2M/UKM (reference) U»VU«* (reference) Uranium 1 —----------------------- ------------------------ (percent) vm/V®' (sample) U*«/U»> (sample) 0. 040 0. 9907 1. 0027 . 002 . 7677 1. 0041 . 002 . 8852 1. 0014 . 013 . 9251 1. 0045 1 Uranium analyses by fluorimetric method by E. J. Fennelly, U.S. Geological Survey. 2 Relatively high uranium content; may be mineralized.B86 GEOCHEMISTRY Figure 1.—Geologic section showing lithology and location of channel samples taken across oxidized-unoxidized sandstone contact in the wall of the Lucky Me Project 4A mine, Gas Hills area, Fremont County, Wyo. Redrawn from photograph taken by D. H. Norton, U.S. Atomic Energy Commission. Table 2.—Isotopic ratios of uranium in sandstone samples from Gas Hills roll, Fremont County, Wyo. Field No. U23i/lj23< Qreference) jjmjjjm (reference) USGS sample No. (figs. 1 and 2) XJ238/U234 (sample) XJ238/XJ238 (sample) 273084 15 0. 8464 1. 0016 273085 14 1. 718 1. 0019 273086 13 1. 630 1. 0027 273087 12 . 9283 1. 0009 273088 11 1. 604 1. 0033 273089 10 1. 369 . 9985 273090 9 1. 292 1. 0012 273091 8 1. 014 1. 0014 273092 7 1. 096 1. 0027 273093 6 . 9930 1. 0019 273094 5 . 9688 1. 0015 Comparison of the percentage isotopic variation, 8, of U234/U235 ratios for each sample, together with the uranium content indicated at the location of each channel sample, is shown in figure 2. The peak concentration of uranium occurs in a 1%-foot interval in the unoxidized sandstone near the oxidized contact, and slight enrichment in uranium occurs at a few places in the oxidized sandstone. TJ234/U23S ratios show a large excess of U234 in the more uraniferous samples of oxi- Table 3.—Radioactive disequilibrium analyses of sandstone samples from Gas Hills roll, Fremont County, Wyo. [Isotopes given as percent equivalent of parent nuclide, except as noted] Field No. USOS (figs. I U388 sample No. and 2) (percent) Fa231 U884 Th880 Ra88a Rn888 Pb310 273084 . 15 0.004 0.01 0.003 0.004 0.010 0.01 0.010 273085 ........ 14 . 018 . 02 . 031 .004 . 010 . 01 .009 273086 13 . 030 . 03 . 049 . 006 . 012 . 01 .010 273087 ________ 12 . 004 . 01 .004 . 004 . 013 . 01 .011 273088 ________ 11 .018 . 02 . 029 . 005 . 019 . 02 . 017 273089 . . 10 . 062 . 07 . 085 . 011 .10 .10 . 092 273090 _ 9 .11 (>) 14 .04 .05 .04 .052 273091 ........ 8 . 50 . 54 . 51 .52 .14 .10 .12 273092 ......... 7 . 52 . 52 . 57 . 58 .14 .12 .12 273093 ......... 6 . 091 .08 . 090 .11 .032 . 03 . 023 273094 5 . 010 . 02 010 . 014 . 016 . 02 . 014 i Pa884 could not be determined because of exceptionally high content of Ac887. Analyses for additional isotopes In this sample: Th888, 0.01 percent; Ac887, 0.86 percent equivalent. Figure 2.—Variations of percentage total uranium (numbers) and percentage U235/ 234 ratio, 8, (solid blocks) across the oxidized-unoxidized sandstone contact in the Lucky Me Project 4A mine. Locations of midpoints of individual channel samples are denoted by X. Italic numbers are field numbers referred to in tables 2 and 3. dized sandstone and a slight excess to a slight deficiency of U234 in the unoxidized sandstone. Two samples (12 and 15) with low uranium content are deficient in U234. At the peak concentration of uranium, as shown by the data in table 3, Pa231 and Th230 are present in radioactive-equilibrium amounts with uranium-isotope parents, U235 and U234, respectively. This indicates that the process of uranium accumulation began at leastROSHOLT, GARNER, AND SHIELDS B87 100,000 years ago. Th230 is deficient at the places of slight uranium enrichment in the oxidized sandstone, suggesting that the excess U234 accumulation was a relatively recent event. The relation of low Th230 content to high U234 content in the oxidized sandstone suggests deposition of uranium from ground water containing a high concentration of uranium enriched in U234. This probably represents redistribution of uranium with a high U234/U335 ratio derived by preferential leaching of U234 from nearby deposits undergoing slight oxidation. The two samples with low uranium content may be from part of the sampled mine wall with a small amount of uranium which has been in place for a considerable length of time; some of the U234 has been preferentially leached from these two samples. A similar low uranium content with deficient U234 may have existed throughout the oxidized sandstone; this effect may be masked by redistributed uranium that was deposited erratically at a later time. CONCLUSIONS To describe the mechanism of uranium-isotope fractionation, it has been suggested (Rosholt and others, 1964) that total U234 is contributed in two ways to the environment in which it is found: (1) those atoms that have been mixed and transported with U238 and U235 remain with these two isotopes and are not subject to removal by preferential leaching, and (2) atoms generated in place from the radioactive disintegration of U238 are subject to differential migration with respect to the U238. One result of the latter process is a deficiency of U234 caused by its being preferentially leached from a uranium source in the solid phase; on the other hand, small amounts of excess U234 can result from accumulation, on particulate matter, of its parent isotopes, Th234 and Pa234, generated from soluble U238 in pore water. The weathered granites are primarily examples of the second type that show a deficiency of U234 from preferential leaching. Samples of uranium-enriched areas in oxidized sandstone in the Gas Hills suite are examples of the first type. These oxidized sandstones give the following clue that may be useful in many occurrences of excess U234. The presence of excess U234, together with considerably less than equilibrium amounts of Th230, indicates relatively recent accumulation of transported uranium. REFERENCES Ancarani, L., and Bettinali, C., 1960, Analisi isotopica dell’Uranio e dello Zolfo nello studio delle mineralizzazioni di Canale Monterano: Studi e Ricerehe della Dlvlsione Geomineraria, v. III. Comitato Nazionale per le Ricerehe Nuclearl, Roma, p. 1-22. Cherdyntsev, V. V., Kazachevski, I. V., and Kuzmina, E. A., 1963, Istotopic composition of uranium and thorium in the zone of hypergenesis. Investigation of fossil bones, soil and shells of mollusks: Geokhimiya, no. 3, p. 254—266. Goldberg, E. D., and Koide, M., 1962, Geochronological studies of deep sea sediments by the ionium/thorium method: Geochim. et Cosmochim. Acta, v. 26, p. 417—435. Harshman, E. N., 1962, Alteration as a guide to uranium ore, Shirley Basin, Wyoming: Art. 122 in U.S. Geol. Survey Prof. Paper 450-D, p. D8-D10. Koshelev, I. P., and Syromyatnikov, N. G., 1961, Some regularities in the migration of uranium-234 and uranium-238 isotopes : Fzvest. Akad. Nauk Kazakh. SSR, Ser. Geol., no. 3, p. 73-82. Rosholt, J. N., Jr., 1957, Quantitative radiochemical methods for the determination of the sources of natural radioactivity: Anal. Chem., v. 29, p. 1398-1408. Rosholt, J. N., Jr., and Dooley, J. R., Jr., 1960, Automatic measurements and computations for radiochemical analyses : Anal. Chem., v. 32, p. 1093-1098. Rosholt, J. N., Jr., Emiliani, C., Geiss, J., Koczy, F. F., and Wangersky, P. J., 1961, Absolute dating of deep-sea cores by the Pa^'/Th230 method: Jour: Geology, v. 69, p. 162-195. Rosholt, J. N., Jr., Harshman, E. N., Shields, W. R., and Garner, E. L., 1964, Isotopic fractionation of uranium related to roll features in sandstone, Shirley Basin, Wyoming: Econ. Geology. I In press] Rosholt, J. N., Jr., Shields, W. R., and Garner, E. L., 1963, Isotopic fractionation of uranium in sandstone: Science, v. 139, p. 224-226. Thurber, D. L., 1962, Anomalous U231/U2W iu nature: Jour. Geophys. Res., v. 67, p. 4518-4520. ------ 1963, Natural variation in the ratio u^/u238 and an investigation of the potential of U234 for Pleistocene chronology : Columbia Univ. Ph. D. thesis, 153 p. Woodmansee, W. C., 1958, Ground water in sandstone-type uranium deposits: United Nations Internat. Conf. on Peaceful Uses of Atomic Energy, 2d, Geneva, 1958, v. 2, p. 351-357. Zeller, H. D., 1957, The Gas Hills uranium district and some probable controls for ore deposition: Wyo. Geol. Assoc. Guidebook, 12th Ann. Field Conf., p. 156-160.GEOLOGICAL SURVEY RESEARCH 1964 HAFNIUM CONTENT AND Hf/Zr RATIO IN ZIRCON FROM THE SOUTHERN CALIFORNIA BATHOLITH By DAVID GOTTFRIED and CLAUDE L. WARING, Washin3ton, D.C. Abstract.—The hafnium content and the Hf/Zr ratio in zircon indicate a progressive enrichment of hafnium in relation to zirconium from the malic to the more siliceous rocks. Zircon from the gabbro studied contains 1.0 percent hafnium and has a Hf/Zr ratio of 0.020. Zircon from the granite has a hafnium content ranging from 1.3 to 2 percent and Hf/Zr ratios ranging from 0.027 to 0.040. Within the rocks of a single stock of Woodson Mountain granodiorite, hafnium and the Hf/Zr ratio are highest in the zircon of finest mesh sizes. Zircon is one of the most common accessory minerals in the igneous rocks of the southern California batho-lith and occurs in variable amounts in rocks ranging in composition from gabbro to granite. Because hafnium and zirconium are one of the best known pairs of geochemically coherent elements, a study of the hafnium content and Hf/Zr ratio in zircon was undertaken to determine the behavior of hafnium during magmatic differentiation and perhaps to shed some light on the paragenesis of zircon. Earlier data for zircon from rocks of this batholith were summarized and briefly discussed (Gottfried and others, 1959) with regard to the much debated problem of the crystallization history of zircon. This article presents the results obtained on additional samples of zircon from a wide range of chemically analyzed rocks to show (1) the relation of hafnium and the Hf/Zr ratio in zircon to the bulk composition of the host rock, (2) the variation of Hf and the Hf/Zr ratio in zircon from rocks from a single stock, and (3) the variation of Hf and the Hf/Zr ratio in zircon fractions of different mesh size from the same rock. The hafnium content and the Hf/Zr ratio were determined with a direct-reading spectrometer using a 1-milligram sample of zircon mixed with 5 mg of graphite and arced for 3 minutes in a controlled atmosphere [Waring, 1964, p. B146 (this chap.)]. The method B88 yields results reproducible to better than ±5 percent as determined by replicate analyses. Cross checks with data obtained by X-ray fluorescence show satisfactory agreement. SOUTHERN CALIFORNIA BATHOLITH Forty analyses for hafnium and the Hf/Zr ratio of zircon concentrates separated from 32 rocks ranging in composition from gabbro to granite are listed in table 1. Nearly all these rocks are similar to those studied by Larsen (1948) and Everhart (1951). Chemical analyses are available for 27 of the rocks; figure 1 shows how the hafnium content and Hf/Zr ratio in zircon vary with the chemical composition of the rocks. The position of each rock in figure 1 is calculated, from its chemical analysis, by the method described by Larsen (1938). The lowest hafnium content (1.00 percent) and Hf/Zr ratio (0.020) are found in zircon from the gabbroic rocks. In the 8 tonalites studied the zircon averages 1.10 percent hafnium and has a Hf/Zr ratio of 0.022. The data in table 1 show a wide variation in the hafnium content and Hf/Zr ratio in zircon from the different types of granodiorite. Those variations that exceed the experimental error appear to be related to significant differences in the chemical composition and relative age of the rocks. Another factor that helps account for the observed variation in hafnium content and Hf/Zr ratio is related to variations in grain size of the zircon. Figure 2 summarizes data on zircon from 10 rocks from a single stock of Woodson Mountain Granodiorite located a few miles below Temecula, Calif. Particularly striking are the variations between 100-200- and 200-325-mesh zircon separated from the same rock. In each instance the finer mesh zircons have a higher U.S. GEOL. SURVEY PROF. PAPER 501-B, PAGES B88-B91GOTTFRIED AND WARING B89 Table 1.—Hafnium content and Hf/Zr ratio in zircon from igneous rocks of the southern California batholith Sample No. SM....... BL 60-5____ BL 60-6.... Ct—S BL 60-1BB BL 60-1 B_. Z-19_______ LTS-3 1____ BL 60-1.... S-l________ BL 60-2 G-13____ BL 60-7 BL 60-8 S-17____ S-9_____ S-8_____ S-13____ S-2_____ LTS-4 i S-ll... S-12___ S-l 5__ S-14___ S-10... S-6____ G-12..... Z-17_____ El 38-167 LTS-2___ El 38-265 BL 60-4.. Mesh size Rock type Position H SiOs+ KzO-CaO-FeO-MgO Hafnium content (percent) Hf/Zr ratio 100-200 San Marcos Gabbro . 1. 00 0. 020 100-200 San Marcos Gabbro (quartz-biotite-norite) + 1. 9 + 1. 5 1. 00 . 020 100-200 Green Valley Tonalite __ _ 1. 05 . 021 100-200 Tonalite 1. 01 . 021 100-200 Bonsall Tonalite . 1. 10 . 022 100-200 Inclusion in BL 60-1BB -6. 2 1. 10 . 022 100-200 Bonsall Tonalite 1. 15 . 023 100-200 do _ _ _ _ _ ___ + 9. 4 + 9. 5 + 8. 7 + 8. 6 + 15. 6 + 22. 0 + 16. 9 1. 05 . 021 100-200 do 1. 10 . 022 100-200 Lakeview Mountain Tonalite . _ . 1. 20 . 024 100-200 do.. _ _ - 1. 10 . 022 100-200 Granodiorite. .. 1. 12 . 024 100-200 100-200 Indian Mountain Leucogranodiorite (granodiorite) Stonewall Formation (granodiorite).. 1. 24 1. 25 . 025 . 025 100-200 Woodson Mountain Granodiorite. 1. 28 . 027 100-200 100-200 100-200 200-235 100-200 200-325 100-200 1 do . + 20. 6 21. 2 / 1. 28 l 1. 30 / 1. 32 l 1. 48 / 1. 32 1 1. 35 1. 37 . 026 . 026 . 027 . 030 . 027 . 028 . 028 1 do J \ do + 22. 2 + 23. 2 + 23. 9 + 22. 9 + 26. 4 + 24. 3 + 25. 7 + 28. 8 + 20. 9 + 26. 5 + 22. 4 + 25. 5 + 26. 1 + 27. 7 + 27. 4 _ do. 100-200 do. _ 1. 40 . 029 100-200 __do_ . . - _ _ __ 1. 35 . 027 100-200 200-325 100-200 200-325 100-200 200-325 100-200 200-325 100-200 \ do / 1. 50 1 1. 60 / 1. 35 l 1. 60 J 1. 28 l 1. 37 / 1. 37 \ 1. 65 1. 60 . 030 . 032 . 027 . 032 . 026 . 028 . 028 . 033 . 033 1 do. \ do . J } do J do _ 100-200 do 1. 48 . 030 100-200 200-325 100-200 100-325 | Mount Hole Granodiorite / 1. 75 l 1. 80 1. 32 1. 60 . 035 . 036 . 026 . 032 Quartz monzonite of Rubidoux Mountain, coarse phase. do 100-200 100-200 Quartz monzonite of Rubidoux Mountain fine phase Roblar Leucogranite (granite) . .. .. 1. 73 1. 32 . 036 . 026 1 Provided by Dr. L. T. Silver, Dept, of Geology, California Institute of Technology. hafnium content and Hf/Zr ratio. Moreover, it was found that there is a strong tendency for the zircon in the more siliceous rocks of this stock to be concentrated in the finer mesh sizes. Hence it is clear that an analysis on a particular fraction of zircon is not necessarily representative of all the zircon in the rock. Taking into consideration the relative amounts of zircon in the different size fractions, the data show a progressive increase in the hafnium content and Hf/Zr ratio in zircon from the relatively mafic to the more siliceous granodiorite. Zircon from rocks most typical of this stock average about 1.35 percent hafnium and have a Hf/Zr ratio of about 0.028. Zircon of the porphyritic Mount Hole Granodiorite, which is younger than the Woodson Mountain Granodiorite (Larsen, 1948), has a minimum hafnium content (1.75 percent) and a minimum Hf/Zr ratio (0.035) greater than zircon from any other granodiorite in this study. Zircon from the quartz monzonite of Rubidoux Mountain and granite contains from about 1.32 to 1.73 percent hafnium and has a Hf/Zr ratio ranging from 0.026 to 0.036, thus overlapping the range shown by zircon of the granodiorite. MOJAVE DESERT AREA The hafnium content and Hf/Zr ratio of zircon from a granodiorite, quartz monzonite, and five samples of granite from satellitic instrusions exposed in the desert ranges east of the batholith are listed in table 2. Zircon from one of these granites (G-24) has a greater hafnium content (2.02 percent) and Hf/Zr ratio (0.042) than any of the zircon from the batholithic rocks listed in table 1. These few data also show the enrichment of hafnium in zircon in the more siliceous rocks.HF/ZR HAFNIUM, IN PERCENT B90 GEOCHEMISTRY Figure 1.-—Hafnium content and Hf/Zr ratio in zircon plotted against composition of the rocks. Dots, 100-200-mesh-size zircon ; circles, 200-325-mesh-size zircon. Table 2.—Hafnium content and Hf/Zr ratio in zircon from igneous rocks of the Mojave Desert Sample No. Mesh size Rock type Hafnium content (percent) Hf/Zr ratio RCE-28 A 100-200 Granodiorite -. 1. 15 0. 023 RCE-14 C__. do Quartz monzonite_. 1. 40 . 028 RCE-18 A do Granite 1. 35 . 027 RCE-27 C... do do 1. 45 . 029 RCE-14 B do do 1. 60 . 032 RCE-28 B do do 1. 60 . 032 G-24 _ _do_ _ do _ _ _ 2. 02 . 042 ratio on the average show a progressive increase from the early formed gabbroic rocks to the late siliceous differentiates. The general trend shown by the data on samples from separate plutons of different composition is also shown on a more detailed scale by samples from a single differentiated stock. Much of the scatter of the data on the variation diagram (fig. 1) is probably caused by separate subparallel trends that may be present in individual plutonic units. Considerable scatter of the data may also be observed on a finer scale (fig. 2) where wide differences are found between zircon crystals differing in grain size from the same rock. If these uncertainties are taken into account, the hafnium and Hf/Zr data appear to vary in a systematic manner and to clearly show an enrichment of hafniumGOTTFRIED AND WARING B91 relative to zirconium as differentiation of the magma progresses. From this hafnium enrichment it appears that within a given rock the finer sized crystals of zircon are formed later than the coarser ones in the normal course of crystallization. With regard to the time of crystallization of zircon, the data lend further support to the belief (Gottfried and others, 1959) that in plutonic rocks, zircon crystallizes continuously throughout most of the interval of magmatic differentiation. The wide variations in its composition clearly show that zircon crystallizes in a continuously changing physico-chemical environment, its composition being approximately fixed for any stage in the differentiation of the magma. Lyakhovich and Shevaleyevskii (1962) have reached similar conclusions from a study of the Hf/Zr ratios in some plutonic rocks from the Soviet Union. Based on the estimates of the abundance of the various rock types of the batholith published by Larsen (1948), the weighted average hafnium content and Hf/Zr ratio for zircon of the batholith are about 1.12 percent and 0.023, respectively. This ratio agrees with the estimate given by Fleischer (1955) for the Hf/Zr ratio in the earth’s crust based on previously published data. REFERENCES Everhart, D. L., 1951, Geology of the Cuyumaca Peak quadrangle, San Diego County, California: Calif. Dept. Nat. Res., Div. Mines Bull. 159, p. 51-115. Fleischer, Michael, 1955, Hafnium content and hafnium-zirconium ratio in minerals and rocks: U.S. Geol. Survey Bull. 1021-A, 13 p. Gottfried, David, Jaffe, H. W., and Senftle, F. E., 1959, Evaluation of the lead-alpha (Larsen) method for determining ages of igneous rocks: U.S. Geol. Survey Bull. 1097-A, 63 p. Larsen, E. S., Jr., 1938, Some new variation diagrams for groups of igneous rocks: Jour. Geology, v. 46, p. 505-520. ------ 1948, Batholith and associated rocks of Corona, Elsinore, and San Luis Rey quadrangles, southern California: Geol. Soc. America Mem. 29,182 p. Lyakhovich, V. V., and Shevaleyevskii, I. D., 1962, Zr: Hf ratio in the accessory zircon of granitoids: Geochemistry, no. 5, p. 508-524. Waring, C. L., 1964, Determination of hafnium content and Hf/Zr ratios in zircon with the direct-reading emission spectrometer, in Geological Survey Research 1964: U.S. Geol. Survey Prof. Paper 501-B, p. B146-B147. 7 725-328 0—64-GEOLOGICAL SURVEY RESEARCH 1964 GEOCHEMICAL ANOMALIES IN THE LOWER PLATE OF THE ROBERTS THRUST NEAR CORTEZ, NEVADA By R.L. ERICKSON, HAROLD MASURSKY, A. P. MARRANZINO, UTEANA ODA, and W. W. JANES, Denver, Colo. Abstract.—Arsenlc-antimony-tungsten anomalies have been discovered in jasperoid and fracture fillings in limestone in the lower-plate rocks of the Roberts thrust about 4 miles north of Cortez, Nev. Skarn pods and abundant quartz-bearing dike rocks in the limestone suggest the presence of a shallow buried intrusive mass. Anomalous amounts of arsenic, antimony, and tungsten have been discovered in fracture fillings and jasperoid in limestone of Silurian and Devonian age in the lower-plate rocks of the Roberts thrust (Cortez window) near the Crescent fault about 4 miles north of Cortez, Nev. (fig. 1). Geochemical anomalies (copper, lead-zinc-silver, arsenic, and bismuth) in the siliceous clastic rocks of the upper plate of the Roberts thrust were reported by Erickson and others (1961); the reader is referred to their article for geographical orientation and a more complete geological and geochemical discussion of the general area of the investigation reported here. Discontinuous alined masses of skarn and abundant fine-grained quartz-bearing dike rocks in the limestone of the lower plate (fig. 1) suggest that a shallow-buried intrusive mass underlies at least a part of the area of investigation. The skarn consists of calcite marble with porphyroblasts of idocrase, grossularite, and scapolite (meionite) in crystals as much as 2 inches across. This is the most intense contact metamorphic aureole in the Cortez area and it is suggested that the metal anomalies may be leakage halos emanating from concealed ore deposits in shear zones and fractures near the contact with the postulated buried intrusive. The samples collected and analyzed in this study are not representative of rock units but are grab samples of the most favorable looking host material for introduced metals (fracture fillings, jasperoid masses, and intensely altered rocks). Thus, the density of sample sites shown on figure 1 is a crude index to the abundance of “favorable-looking material.” Most of the traverses were made along drainages where bedrock exposure is best. Arsenic was determined chemically; all other metals wyere determined by semiquantitative spectro-graphic methods. The largest arsenic-antimony-tungsten anomaly extends about 1 mile in a northeasterly direction roughly parallel to the Crescent fault (fig. 1). Maximum metal values detected in a few samples from the most intensely mineralized area are: arsenic, 6,000 parts per million; antimony, 3,000 ppm; tungsten, 1,500 ppm; zinc, 2,000 ppm; lead, 200 ppm; molybdenum, 200 ppm; beryllium, 100 ppm; and silver, 30 ppm. The smaller anomalies to the south are chiefly arsenic-antimony anomalies of lesser intensity. All the metals occur in highest concentration in the most iron-rich fracture fillings or jasperiod (> 10 percent iron). In the light of the previously described zoned metal anomalies in the upper plate of the Roberts thrust (Erickson and others, 1961), the discoveries reported here in the lower-plate rocks enhance the overall favor-ability of the Cortez district as a promising area for discovery of concealed ore deposits. Location, description, and semiquantitative spectro-graphic and chemical analyses of the rocks collected in this investigation are described more fully by Erickson and others (1964).1 1 Report obtainable at cost from the U.S. Geological Survey, Federal Center, Denver, Colo. B92 U.S. GEOL. SURVEY PROF. PAPER 501-B, PAGES B92-B94ERICKSON, MASURSKY, MARRANZINO, ODA, AND JANES B93 116°37'30" Figure 1.—Preliminary geochemical and geologic map of an area in the north-central part of the Cortez quadrangle, Nevada. Geology modified from work of James Gilluly and Harold Masursky, 1957-59. Density of pattern shows intensity of geochemical metal anomaly.B94 GEOCHEMISTRY REFERENCES Erickson, R. L., Masursky, Harold, Marranzino, A. P., and Oda, Uteana, 1961, Geochemical anomalies in the upper plate of the Roberts thrust near Cortez, Nevada : Art. 401 in U.S. Geol. Survey Prof. Paper 424-D, p. D316-D320. Erickson, R. L., Masursky, Harold, Marranzino, A. P., Oda, Uteana, and Janes, W. W., 1964, Semiquantitative spec-trographic and chemical analyses of rocks from the lower plate of the Roberts thrust, north-central part of the Cortez quadrangle, Nevada: U.S. Geol. Survey open-file report.GEOLOGICAL SURVEY RESEARCH 1964 CESIUM AND STRONTIUM SORPTION STUDIES ON GLAUCONITE By MARIAN M. SCHNEPFE, IRVING MAY, and CHARLES R. NAESER, Washington, D.C. Work done in cooperation with the V.8. Atomic Energy Commission Abstract.—Studies of the ion-exchange behavior of cesium and strontium with glauconite in column experiments at pH 3, 6, and 10 indicate that increasing the pH increases the uptake of these ions. The strontium uptake averages 95 percent of capacity values at pH 10, while the cesium uptake is approximately 50 percent. Initial acid-treatment of glauconite increases the exchange with cesium to near capacity levels at pH 10, but reduces the strontium uptake by about 30 percent. The interaction of three New Jersey glauconite mineral samples with cesium- and strontium-bearing solutions was studied to evaluate glauconite as a possible scavenging agent for cesium-137 and strontium-90 in nuclear-waste solutions. Glauconite is a term used with dual connotation (Burst 1958a, 1958b). It is the name of a micaceous hydrous silicate mineral of iron, aluminum, and potassium, and it is also a general morphological term for rocks consisting of small spherical green pellets. The mineral, glauconite, has a dioctahedral illite structure with a charge deficiency in both tetrahedral and octahedral layers. These charge deficiencies are balanced by interlayer cations which are generally K+1, but may be Ca+2, or Na+1. There is a considerable replacement of AH by Fe+3, Fe+2, and Mg+2. Glauconite occurs typically in sand-size lobate aggre- gates of generally spherical shape. It is well known as “greensand” or “greensand marl”. It is of marine origin and is abundant in the Cretaceous and early Tertiary marls and sands of the east coast of the United States. It has been mined for use as a fertilizer and as a natural “zeolite”. Glauconite is now mined in New Jersey but is available in many other areas as well. The ion-exchange properties of glauconite are well established. A completely reversible exchange reaction between potassium, sodium, and calcium is the basis for its use as a water softener. Glauconite is stable in neutral or slightly alkaline solutions but is appreciably soluble in 24 percent HC1 (Hutton and Seelye, 1941) and somewhat soluble in weaker acid. Because of the reversible nature of its exchange reactions, glauconite might be expected to serve as a concentrating agent in the removal of radionuclides from nuclear-waste solutions. Although glauconite has a lower exchange capacity than other clays such as montmorillonite, its granular nature makes it particularly desirable as an ion exchanger. It is not ordinarily subject to the undesirable swelling and consequent impedance to solution flow so often present in other clays in ion-exchange reactions. Hendricks and Boss (1941) give the following formula as characteristic of many glauconites: [K, Cao.5, Na]0.84[A1o.47Fe^?9Feo^97Mg0. J [Si3.65A1o.350io](OH)2 2 = 0.84 2=2.03 2=4-00 U.S. GEOL. SURVEY PROF. PAPER 501-B, PAGES B95-B99 B95B96 GEOCHEMISTRY Owens and Minard (1960) computed structural formu- plain. Their formulas for glauconites with the same las from chemical analyses of glauconite concentrates origin as those used in this study are: from various formations of the New Jersey coastal Bed Bank Sand (Upper Cretaceous), [Bo. 63eNao. oof)Ca0. oil [Mg0.35Feo^8Fe^oAlo. 4sTio. 004] [Si3. bsAIq. 320io](OH)2 X) = 0.655 2=2.014 2=4.00 Hornerstown Sand (Paleocene), [K0. 764Nao. 00{>Ca0. 007] [Mgo. 384Feo^204Fei(o8Alo. 33^0,003] [Sl3. 68^10. 32O10] (OH)2 2 =0-780 2=2.031 2=4.00 ManasquanFormation (Eocene), [K0.722Na0.0i8Ca0.10] [Mgo. 40F?6Fof 925 Alo. 42Tio. 003] [S13.69AI0.31O10] (OH )2 2=0.84 2 = 1-968 2=4.00 The glauconite concentrates used in these exchange studies were washed and sieved; the — 35- to +60-mesh (sieve openings 0.50 and 0.25 mm) portions were then magnetically fractionated on the Franz Isodynamic Separator, the more magnetic fraction being taken for the exchange studies. Cesium was determined spectro-graphically to be<0.003 percent and strontium 5=0.007 percent by H. W. Worthing, U.S. Geological Survey. The chemical analyses of these fractionated samples are shown in table 1. These analyses correspond reasonably well with those of Owens and Minard (1960). X-ray studies of the glauconites described in the present article (Owens, personal communication, 1963) show them to be the disordered type of glauconite as classified by Burst (1958b). Table 1.— Chemical analyses of glauconites [Analyses by Rapid Rock Analysis Laboratory, U.S. Geological Survey. Analyses in percent] No. 1 (New No. 2 (New No. 6 (Pember-Egypt, N.J.) Egypt, N.J.) ton, N.J.) Si02______________________ 49. 0 48. 5 48. 4 AI203.................... 8. 4 6. 6 7. 6 Fe203_____________________ 17. 7 19. 9 17. 1 FeO________________________ 3. 3 3. 9 2. 6 MgO________________________ 3. 2 3. 3 3. 7 CaO____________________ .53 .62 2. 1 Na20_________________________ .04 .03 .05 K20________________________ 6. 9 7. 4 7. 0 H20_______________________ 10. 7 9. 2 9. 6 Ti02________________________ .10 .10 .08 P205___________________ .28 .28 1. 2 MnO__________________________ .02 .02 .01 C02____________________ <. 05 . 61 <. 05 Total_____________________ 100.2 100.5 99.4 No. 1, glauconite from Red Bank Sand, Upper Cretaceous in age. No. 2, glauconite from Hornerstown Sand, Paleocene in age. No. 6, glauconite from Manasquan Formation, Eocene in age. The glauconite samples were provided by James P. Owens and Dorothy Carroll, U.S. Geological Survey. We also wish to acknowledge their assistance and advice regarding the purification and characterization of these samples. TECHNIQUE Because of the obvious partial acid-decomposition of glauconite sample 2 during a column experiment, portions of the various glauconites were pretreated with acid. Samples were treated at room temperature with 2.5M HC1 for a total of 6 hours and then washed with distilled water until the washings had a pH of 4. The samples were air dried. The acid leachings from each sample were evaporated and then ignited over a burner yielding residues weighing approximately 4 percent of the original sample. Spectrographic analyses showed that the residues were largely iron, aluminum, and silicon. The total exchange capacities of both the acid-treated and the natural glauconites were determined by a batch method in which the samples were treated first with 2.5N ammonium acetate, and then the exchanged ammonium ions were removed by a Kjeldahl procedure employing barium hydroxide. Table 2 lists these exchange capacities. Table 2.—Total exchange capacity of glauconites (meqjlOO g) No. 1 No. tt No. 6 (New Egypt, (.New Egypt, (Pemberton, N.J.) N.J.) N.J.) Untreated__________________ 26. 0 19. 6 22. 3 Acid treated_______________ 27. 2 21. 2 2. 3 All column studies were made with 12-mm-diameter glass columns immersed in a constant-temperature water bath. Column charges of 1 gram of glauconite were used, and the eluates were collected in 10-milliliter fractions. Feed solutions prepared from the chlorides were 50 parts per million in either cesium or strontium with theSCHNEPFE, MAY, AND NAESER B97 pH adjusted to 3, 6, or 10 by the addition of hydrochloric acid or sodium hydroxide. In the experiments at pH 10 the sodium hydroxide contributed a sodium-ion concentration of 2.3 ppm. Because the cesium and strontium concentrations were more than 20 times greater than that of sodium and because both cesium and strontium generally have greater replacing power than sodium it was felt that the competing effect of the sodium ions could be ignored. The strontium feed solutions were spiked with strontium-89 to give counts approximately 500 times the background level of 20 counts per minute. The concentration of strontium in the glauconite-treated solutions was determined with a beta counter. The beta activity was determined on 1-ml aliquots of eluate fractions evaporated in aluminum planchets. The cesium feed solutions were spiked with cesium-137 to give gamma activity approximately 700 times the background level. The activity of the glauconite-treated solutions was measured -with a sodium iodide crystal scintillation counter. Flow rates of approximately 10 ml per 15 minutes (0.6 ml cm-2 min-1) were maintained when possible. Despite the granular nature of the glauconite, very slow flow rates were found for one of the glauconites (sample 2) at pH ranges from 3 through 10 for both the cesium and strontium solutions. An analysis of the eluate from this sample showed the presence of both aluminum and silicon, indicating partial decomposition of the sample. Typical break-through curves1 were obtained for both the acid-treated and natural glauconites. Figures 1 through 4 are the break-through curves for cesium and for strontium from the acid-treated and the natural glauconite (sample 1). The other glauconites give similar break-through curves. The C/C„ values represent the ratios of the concentration of cesium or strontium in the eluate to their concentration in the feed solution. The experimental data are summarized in table 3. The uptake values in this table apply only to the extent to which the experiments were carried to completion, this being controlled largely by convenience. In table 4 the exchange capacities have been calculated from uptake values when C/C0 equals 0.5. If V is the volume of the eluate collected up to the point when C/C0 equals 0.5, then the exchange capacity equals the product, VxC0 (Samuelson, 1953, p. 48). Many of the elution curves are not completely symmetrical and therefore the calculated capacities may differ somewhat from the true values. 1 The point at which the exchanging ion is first detected in the eluate is called the break-through point. In figure 1, at pH 3 the breakthrough of cesium occurs at 50 ml and at pH 10 at 400 ml. Table 3.—Experimental uptake of cesium and strontium Glauconite (sample No.) Feed solution (50 ppm) pH of feed solution Eluate volume (ml) Flow rate (ml cm-2 min-1) Uptake (meq/100 g) Untreated form Acid- treated form Cs Sr 1 3 670 0.3 6.7 1 6 800 .5 12.0 1 10 800 . 5 16.7 1 3 500 .3 7.5 1 6 850 .4 16.7 1 do 10 700 .3 23.6 1.. 3 700 .8 13.5 1. 6 800 .5 20.1 1 10 850 .5 28.4 1 3 600 .3 16.1 1 6 900 .5 21.2 1 do 10 600 .3 23.0 2__ . 3 455 .3 3.9 2. . 6 <10 <.005 2 . 10 180 .02 6.3 2 do 3 500 .4 6.2 2 do 6 800 .5 13.0 2 do 10 400 .06 14.9 2 3 455 .05 8.6 2 6 490 .1 16.0 2 10 340 .03 21.6 2 3 600 .4 14.2 2 6 800 .5 16.3 2 10 650 «.l 22.7 6 3 400 .5 4.3 6 6 565 .1 9.5 6 10 800 .5 13.4 6 do 3 500 .4 6.6 6 do 6 800 .5 12.5 6 do 10 400 .05 15.0 6 3 650 .4 12.1 6 . 6 695 .2 19.5 6 10 700 .5 24.2 6 3 600 .4 13.1 6 6 800 .5 17.7 6 do 10 650 .5 20.8 Table 4.—Calculated exchange capacities of glauconites [Exchange capacity (meq/100 g) calculated from uptake when C/Co=0.5] Glauconite (sample No.) pH of feed solution Untreated form Acid-treated form Cs Sr Cs Sr i 3 4. 7 10. 6 6. 0 14. 9 6 8. 8 18. 8 12. 6 17. 3 10 13. 9 23. 9 25. 2 19. 0 2 3 3. 5 8. 1 5. 8 6. 2 6 0) 13. 6 9. 8 9. 8 10 2 >6 20. 0 2 >13 15. 2 6 3 3. 0 6. 0 5. 8 8. 4 6 10. 8 17. 3 9. 2 11. 4 10 11. 5 20. 2 22. 4 14. 0 1 Run discontinued early because of excessively slow flow rate. 2 Discontinued before C/C0=0.5. DISCUSSION The total ion-exchange capacities of the New Jersey glauconites as determined by their saturation with ammonium ions range from 20 to 27 meq/100 g. The exchange capacities given in table 4 show that, as would be expected, the uptake of both cesium and strontium increase with pH. At the pH levels of 3, 6, and 10 the cesium uptake of the natural glauconites is approximately 16, 41, and 52 percent, respectively of the total capacity. The strontium uptake under similar conditions is appreciably higher than the uptake of cesium, amounting to 36,73, and 94 percent. Initial acid treatment of the glauconites causes an increase in the cesium uptake at all pH values studied,B98 GEOCHEMISTRY Figure 1.—Break-through curves for cesium from acid-treated glauconite of sample 1. C, concentration of cesium in the eluate; C0, concentration of cesium in the feed solution. and at pH 10 the uptake approaches the capacity value. In contrast to the uptake of cesium, the change in strontium uptake after acid treatment is less predictable. Table 4 shows that strontium uptake is reduced as Figure 2.—Break-through curves for cesium from the untreated form of glauconite of sample 1. C, concentration of cesium in the eluate; Co, concentration of cesium in the feed solution. much as 30 percent at pH 6 and pH 10 after acid treatment. At pH 3, strontium uptake increased in 2 out of 3 samples and decreased in the third after acid treatment.Vc SCHNEPFE, MAY, AND NAESER B99 Figure 3.—Break-through curves for strontium from acid-treated glauconite of sample 1. C, concentration of strontium in the eluate; C0, concentration of strontium in the feed solution. REFERENCES Burst, John F., 1958a, “Glauconite” pellets; their mineral nature and applications to stratigraphic interpretations: Am. Assoc. Petroleum Geologists Bull., v. 42, p. 310-327. ------ 1958b, Mineral heterogeneity in “glauconite” pellets: Am. Mineralogist, v. 43, p. 481—197. Hendricks, S. B., and Ross, C. W., 1941, Chemical composition and genesis of glauconite and celadonite: Am. Mineralogist, v. 26, p. 683-708. Figure 4.—Break-through curves for strontium from untreated form of glauconite of sample 1. C, concentration of strontium in the elu '.te; C0, concentration of strontium in the feed solution. Hutton, C. O., and Seelye, F. T., 1941, Composition and properties of some New Zealand glauconites: Am. Mineralogist, v. 26, p. 595. Owens, James P., and Minard, James P., 1960, Some characteristics of glauconite from the coastal plain formations of New Jersey: Art. 196 in U.S. Geol. Survey Prof. Paper 400-B, p. B430-B432. Samuelson, Olof, 1953, Ion exchange in analytical chemistry : New York, John Wiley and Sons, 291 p.GEOLOGICAL SURVEY RESEARCH 1964 DISTRIBUTION OF BERYLLIUM IN IGNEOUS ROCKS By DANIEL R. SHAWE and STANLEY BERNOLD, Denver, Colo. Abstract.—Beryllium concentration in igneous rocks tends to increase with increase in silica content, but reaches a maximum in rocks containing less-than-maximum amounts of silica. Among rocks having alkalic and silicic compositions, plutonic types normally contain the greatest average -amount of beryllium, hypabyssal types an intermediate amount, and volcanic types the smallest amount. The abundance and general distribution of beryllium in igneous rocks have been summarized by a number of authors (Goldschmidt and Peters, 1932; Sandell, 1952; Beus, 1956; Norton and others, 1958; Warner and others, 1959; and Turekian and Wedepohl, 1961). A study of the detailed relation between the beryllium content and other chemical components of these rocks, however, was not a major part of these studies. Some of these workers recognized that beryllium is most abundant in alkalic rocks, less abundant in silicic rocks, and still less abundant in mafic rocks. This distribution led several authors to the conclusion that beryllium is concentrated by processes of magmatic ditferentiation and that it is more abundant, along with silica and alkali oxides, in late-stage differentiates (Norton and others, 1958, p. 25; Warner and others, 1959, p. 18, 24; Griffitts and others, 1962, p. 1). In addition, a provincial variation in beryllium abundance is indicated by data which show that beryllium is characteristically more abundant in rhyolite and dacite in some areas than it is in others (Coats and others, 1962). This article shows in tabular form the average beryllium content and chemical composition of several groups of igneous rocks. It also presents a detailed comparison of the beryllium content with the silica content of B100 igneous rocks. In addition, attention is called to the apparent relation between the depth at which igneous rocks crystallized and the amount of beryllium in the rocks. In the light of the data presented, magmatic ditferentiation seems to be only one of several controls involved in the production of rocks relatively enriched in beryllium. he analyses evaluated in this summary were collected largely by Verne C. Fryklund as part of another study of igneous rocks by the U.S. Geological Survey. The analyzed rocks were distinguished as “alkalic” or “normal” according to classifications assigned by the original authors. Among the normal igneous rocks, plutonic rocks with >60 percent silica and hypabyssal and volcanic rocks with >61 percent silica were classified arbitrarily as “silicic,” and those below as “mafic”. The abundances of beryllium are based mostly on spectrographic analyses, and the accuracy of such analyses is not easily appraised. Ahrens and Fleischer (1960, p. 87) made a similar collection of analyses of granite G-l; the beryllium content commonly accepted as correct for this rock is 3.3 parts per million, but the reported values ranged from <1 to 4 ppm. This analytical uncertainty is smaller than most of the differences regarded as significant in this discussion, but it accounts for much of the scatter of the points in figure 1. Table 1 gives the range and average beryllium content of 422 igneous rocks compiled in the present study. Mafic rocks contain an average of < 1 ppm beryllium; silicic rocks, 6.5 ppm; and alkalic rocks, 11.4 ppm. The only mafic rocks that contain detectable beryllium are 6 volcanic and 4 plutonic rocks ranging in silica content from 48.6 to 60.6 percent; these 10 rocks are U.S. GEOL. SURVEY PROF. PAPER 501-B, PAGES B100-BX04SHAWE AND BERNOLD B101 Table 1.—Range and average beryllium content of igneous rocks Rock type Number of samples Silica range (weight percent) Beryllium content (parts per million) Range Average All mafic rocks 152 33. 2-60. 7 0-8 3 6.2 3.1 3.4 2.1 0.1 3.3 3.9 1.0 5.6 1.8 3.0 4.3 4 5 FeO 2.6 5.3 3.1 2.6 0.8 7.9 5.0 0.6 6.0 8.4 2.6 0.1 5 6 MgO 4.3 9.5 2.0 2.0 0.4 7.2 7.2 0.3 10.8 2.8 2.8 0.4 6 7 CaO 14.2 7.0 4.2 4.1 0.9 8.4 7.9 1.2 12.2 8.9 5.0 0.9 7 8 NaaO 6.8 2.1 4.5 4.4 6.5 4.2 2.6 3.2 2.9 5.6 5.3 7.0 8 9 KaO 3.3 7.9 7.2 5.8 3.6 1.8 6.9 10.0 5.9 5.4 6.3 5.0 9 10 TiOa 2.1 1.2 1.0 0.8 0.1 2.1 1.2 0.4 4.9 2.3 0.6 0.3 10 11 PaOs 0.6 1.0 0.4 0.5 0.4 0.3 1.0 0.1 0.9 0.6 0.3 0.2 11 12 MnO 0.3 0.1 0.2 0.1 0.0 0.1 0.2 0.0 0.2 0.2 0.2 0.2 12 13 Be (ppm) 27 18 10 2.5 5 0 17 1.5 0.8 5.2 8.0 8.0 13 1 Silica range based on silica reported in chemical analyses; analyses reported water free. SHAWE AND BERNOLD B103B104 GEOCHEMISTRY Table 4.—Comparison of beryllium content of silicic rocks crystallized at different depths but having similar ranges of silica content [Constituents given in weight percent except as noted] Pegmatite Plutonic rocks Hypabys-sal rocks Volcanic rocks Silica range 1 . 72.0- 72. 1- 71. 9- 70. 7- 75. 4 76. 0 74. 3 74. 0 No. of samples _ Constituents: 12 25 24 23 Si02 74. 9 74. 8 74. 6 75. 3 A1203 15. 3 13. 3 13. 4 13. 3 Fe203 0. 3 0. 7 1. 2 1. 0 FeO 0. 4 1. 2 1. 1 0. 5 MgO 0. 1 0. 4 0. 4 0. 2 CaO 0. 3 1. 1 1. 2 1. 0 Na20 4. 8 3. 2 3. 5 3. 5 K20 3. 5 5. 0 4. 4 5. 0 Ti02 0. 0 0. 2 0. 1 0. 2 p2o5 0. 3 0. 1 0. 1 0. 0 MnO 0. 1 0. 0 0. 0 0. 0 Be (ppm) 49 6. 8 17. 5 2. 9 1 Silica range based on silica reported in chemical analyses; analyses reported water free. 2 Includes two granophyres that appreciably raise average beryllium content. REFERENCES Ahrens, L. H., and Fleischer, Michael, 1960, Report on trace constituents in granite G-l and diabase W-l, in Stevens, R. E., and others, Second report on a cooperative investigation of the composition of two silicate rocks: U.S. Geol. Survey Bull. 1113, p. 83-111. Beus, A. A., 1956, Geochemistry of beryllium: Geochemistry (a translation of Geokhimiya), no. 5, p. 511-531 [I960]. Coats, R. R., Barnett, P. R., and Conklin, N. M., 1962, Distribution of beryllium in unaltered silicic volcanic rocks of the western conterminous United States: Econ. Geology, v. 57, p. 963-968. Goldschmidt, V. M., and Peters, C. L., 1932, Zur geochemie des berylliums: Gesell. Wiss. Gottingen Math.-phys. Kl., Nachr., Heft 4, p. 360-376. Griffitts, W. R., Larrabee, D. M., and Norton, J. J., 1962, Beryllium in the United States: U.S. Geol. Survey Min. Inv. Map MR-35. Norton, J. J., Griffitts, W. R., and Wilmarth, V. R„ 1958, Geology and resources of beryllium in the United States, in United Nations, Survey of raw material resources: Internat. Conf. Peaceful Uses Atomic Energy, 2d, Geneva, Sept. 1958, Proc., v. 2, p. 21-34. Sandell, E. B., 1952, The beryllium content of igneous rocks: Geochim. et Cosmochim. Acta, v. 2, p. 211-216. Turekian, K. K., and Wedepohl, K. H., 1961, Distribution of the elements in some major units of the Earth’s crust: Geol. Soc. America Bull., v. 72, p. 175-192. Warner, L. A., Holser, W. T., Wilmarth, V. R., and Cameron, E. N., 1959, Occurrence of nonpegmatite beryllium in the United States: U.S. Geol. Survey Prof. Paper 318, 198 p.GEOLOGICAL SURVEY RESEARCH 1964 T-PHASE OF MAY 11, 1962, RECORDED IN HAWAII By HAROLD L. KRIVOY and ROBERT A. EPPLEY, 1 Hawaiian Volcano Observatory, Hawaii, Honolulu Observatory, Hawaii Abstract.—An underwater nuclear explosion on May 11, 1962, generated a T-phase which was felt by coastal residents of Hawaii. It was also recorded throughout the State by 12 short-period seismometers. From the times of the T-phase maxima at seismographs on Hawaii, Maui, and Oahu the azimuth from the Hawaiian Islands to the source of the T-phase could be roughly calculated. A portion of the energy released in a large and (or) shallow submarine seismic event is propagated through the overlying water as sonic waves (the T-phase) with a velocity of about 1.5 kilometers per second. Hydrophones have proved effective in the detection of these water-borne sound waves and have also shown that this phase is propagated to great distances with only slight attenuation through the deep ocean “low-velocity channel.” This phenomenon is discussed by Northrup (1962) and Milne (1959). To seismologists in Hawaii, T-phases are of considerable interest because they are most effectively generated by earthquakes of submarine or near-shore origin, which include those most likely to send destructive tsunamis out across the Pacific. T-phases are quite common on records of the short-period seismometers in use in Hawaii since 1957, which have magnifications between 10,000 and 40,000 in the period range of recorded T-phases (0.2 to 0.6 sec). Indeed, T-phases are produced by many small circum-Pacific earthquakes that yield no other phases on our records. The relative ground amplitude produced by a T-phase at different stations in the Hawaii network appears to depend on many factors including direction of approach and period of the waves, distance of the recording station from the submarine slopes where the water-borne sonic waves are converted to their rock-borne equivalent, and configuration of the submarine slopes where the conversion occurs. Mere proximity of a station to D Figure 1.—Copies of portions of the short-period smoked-paper recordings made at the, Hawaiian Volcano Observatory by instruments at sites Mauna Loa (M), Ahua (A), and Desert (D). The recordings show the sharp arrival of phases of a local quake followed in about 1 minute by the large spindle-shaped arrival of a T-phase. Drum speed is 60 mm/minute. B105 1 Seismologist, U.S. Coast and Geodetic Survey. U.S. GEOL. SURVEY PROF. PAPER 501-B, PAGES B105-B107B106 GEOPHYSICS the water’s edge does not insure that it will record large-amplitude T-phases. On the other hand, the three T-phases felt in Hawaii (May 14, 1955, from a submarine nuclear explosion;2 July 10, 1958, from the Lituya Bay, Alaska, earthquake;2 and the one here reported) were felt only by people near the shore on the side of the island facing the source of the T-phase. At about 10:40 (Hawaiian standard time) on the morning of May 11, 1962, we observed that unusual records were being written by the four telemetered seismographs in the library of the Hawaiian Volcano Observatory. Three of these records are shown on figure 1. Almost at once two reports were received that residents along Hawaii Island’s northeast coast at Hilo and Ookala had felt a quake. Later, another report of a quake was received from Hilo. As can be seen on figure 1, a local quake began to be recorded about 1 minute prior to the recording of the T-phase. In order to decide which of these two events had been felt by the residents it was necessary to compare these and other records. Optical records from other Hawaii stations are represented on figure 3. The optical record made in the vault of the Hawaiian Volcano Observatory (fig. 2, 7), together with the data from the processed records shown on figure 1, indicated that the local quake that occurred just prior to the T-phase originated in the region just south of point A in figure 2. Moreover, the local quake was only of magnitude 2.2 and was not felt in populated areas near the epicenter; thus it could not have been felt in the northeastern part of the island. Data of May 11 from the Hawaiian Volcano Observatory were compared with those of the Honolulu Observatory on Oahu (fig. 2, 1, %). These data for the time of arrival of the maximum part of the T-phase led to the conclusion that the T-phase approached the Hawaiian Islands from the northeast, as shown on figure 2. This solution was arrived at by graphical means on the assumptions that (1) a distant source was involved and the wave front would be linear as it passed through the Hawaiian chain, (2) the average T-phase velocity was 1.5 km/sec in water, and (3) travel time across the terminal “land” portion of each path was negligible. The three graphical solutions agree within 1°. On figure 1 it can be seen that records from Mauna Loa, Ahua, and Desert (fig. 2, M, A, and D) are sufficiently similar in character to permit relative timing 2 Based on unpublished data furnished by J. P. Eaton, U.S. Geological Survey. of the T-phase maxima with an error no larger than 1 or 2 seconds. On figure 3, however, it is seen that while records from the Hawaiian Volcano Observatory and Maui retain this character, those from Naalehu ((?), Pahoa (5), Hilo (^), and the Honolulu Observatory (£) do not have such quality and character as to permit more than a rough estimate of the arrival time of T-maxima. The calculated azimuth of approach of the waves may be in error by several degrees. This T-phase was detected in the absence of P, S, R, or other features of a distant earthquake. Furthermore, no earthquake was reported near southern California, the only active seismic near-shore area in the direction of the source. It was therefore assumed to be of artificial origin. Hawaiian newspapers of May 12 carried a short story indicating that a nuclear device had been fired beneath the Pacific. The eventual listing of U.S. Atomic Energy Com-mision press releases from the Project Dominic series (U.S. Atomic Energy Commision, 1962) indicated a shot on “May 11th at 4:P.M., EDT, Eastern Pacific Ocean several hundred miles from the closest land area, low yield.” With the above origin time, a 40-minute T-wave travel time is indicated. 158° 157' 156° 155' 154' Figure 2.—-Wave fronts and azimuth of the T-phase of May 11, 1962, computed from the time of arrival of the T-phase maximum at various seismograph stations in the Hawaiian Islands. Short-period seismographs are at Mauna Loa (M), Ahua (A), and Desert (D). Others are at Honolulu Observatory (1, 2) Maui (3), Hilo (4), Pahoa (5), Naalehu (6), and Hawaiian Volcano Observatory (7).KRIVOY AND EPPLEY B107 Hawaiian Volcano ( 7) Observatory Hilo (4) Naalehu (6) Maui (3) Honolulu Observatory ( /( 2 ) Figure 3.—T-phase envelopes traced from the optical records of five short-period vertical seismometers, Numbers in parentheses refer to locations shown on figure 2. Minor tsunamis have originated from earthquakes smaller than magnitude 7.0 for which no T-phase was recorded. On the other hand, we have observed T-phases from large earthquakes which sent no tsunami to Hawaii, as for example, the Lituya Bay, Alaska, earthquake of 1958 that was felt by residents along the northeast coasts of Hawaii and Kauai. It does not seem likely that study of the T-phase will supply a simple technique for predicting tsunamis, because tsunami-producing quakes do not necessarily produce T-phase on seismograms in Hawaii. It is to be expected, however, that the growing knowledge of these phenomena will improve our assessment of other parameters of a seismic event, such as focal depth, magnitude, fault motion, and ocean-floor displacement. REFERENCES Eaton, J. P., Richter, D. H., and Ault, W. U., 1961, The tsunami of May 23, 1960, on the Island of Hawaii: Seismol. Soc. American Bull., v. 51, no. 2, p. 135-157. Milne, A. R., 1959, Comparison of spectra of an earthquake T-phase with similar signals from nuclear explosions: Seismol. Soc. America Bull., v. 49, no. 4, p. 317-329. Northrup, John, 1962, Evidence of dispersion in earthquake T-phases: Jour. Geophys. Research, v. 67, no. 7, p. 2823-2830. U.S. Atomic Energy Commission, 1962, AEC press releases, in Seismological notes: Seismol. Soc. America Bull., v. 52, no. 4, p. 974. 725-328 O—84——8GEOLOGICAL SURVEY RESEARCH 1964 EFFECTS OF THE GNOME NUCLEAR EXPLOSION UPON ROCK SALT AS MEASURED BY ACOUSTICAL METHODS By D. D. DICKEY, Denver, Colo. Work done in cooperation with the V.S. Atomic Energy Commission Abstract.—An attempt was made to measure, by acoustical methods, changes in physical properties of rock salt at the gnome site, New Mexico, which were caused by the detonation of a nuclear device. Longitudinal and shear velocities of rock in place were measured before and after the explosion. Postexplosion velocities were slower, owing to fracturing of the rock, for a distance of more than 200 feet from the shot point. Various elastic constants were calculated for the rock salt before and after the blast, using the measured velocities. A nuclear device of about 3 kilotons equivalent TNT used in project gnome was detonated December 10,1961, in rock salt of the Salado Formation of Late Permian age. The device was 1,200 feet below the surface of the earth at a location about 25 miles southeast of Carlsbad, N. Mex. The preexplosion dynamic elastic properties of the rock salt were calculated from measurements of the compressional and shear velocities of acoustic waves made in the tunnel that was excavated preparatory to emplacement of the device (line Y-Z, fig. 1). Postexplosion measurements were made on June 15 and 16, 1962, in the reentry tunnel. Figure 1 shows the spatial relationships of the shot point, the preexplosion and postexplosion tunnels, and the lines along which the velocities were measured. The accompanying table lists the results obtained from these measurements. All measurements were made in the same manner and with the same equipment. The rock salt is not pure; some units contain as much as 30 percent clay. Polyhalite beds are present in the salt sequence, one of which is less than 10 feet above the explosion center and another of which is less than 10 feet below it. Further details of the geology are given by Gard (1963). Figure 1.—Map of gnome underground workings and cavity, showing sonic-velocity stations (italic letters). Lines of measurement shown by short dashes. U.S. GEOL. SURVEY PROF. PAPER 501-B, PAGES B108-B111 B108DICKEY B109 Measured velocities and calculated elastic moduli for rock salt near the position of the okome explosion [All arrival times determined from comparison of two or more records from each line of measurement except those for line J-O. Only one acceptable record was obtained from line J-O. Line Y-Z, the preexplosion line of measurement, is 5M feet higher stratigraphically than the other lines. Measurements by D. D. Dickey and D. R. Cunningham] Line of measurement Distance from explosion point (feet) Length of line (feet) Travel time of first arrival (milliseconds) Velocity (fps) Poisson’s ratio Young’s modulus (10« psi) Shear modulus (10« psi) Bulk modulus (10® psi) Compressional Shear Compressional Shear Postexplosion measurements A-C 80-110 34. 99 2. 9 6. 05 12, 100 5, 800 0. 35 2. 6 0. 95 2. B-C 80-110 32. 15 2. 7 5. 6 11, 900 5, 750 . 35 2. 5 . 93 2. G-E 140-205 66. 80 5. 6 10. 4 11, 900 6, 400 . 30 3. 0 1. 1 2. G-F 140-205 67. 09 5. 7 10. 4 11, 800 6, 450 . 29 3. 0 1. 2 2. J-O 235-350 114. 74 8. 8 14. 9 13, 000 7, 700 . 23 4. 1 1. 7 2. J-K 235-325 90. 52 7. 0 13. 1 12, 900 6, 900 . 30 3. 5 1. 4 2. U-W 600-785 186. 22 13. 4 24 4 13, 900 7, 650 . 29 4 2 1. 6 3. Preexplosion measurement 5-85 81. 37 6. 05 11. 5 13, 500 7, 100 . 31 3. 5 1. 4 EQUIPMENT The equipment used in this study consisted of a Tektronix-535 oscilloscope, a Polaroid Land camera mounted on the oscilloscope, a time-mark generator, a preamplifier, accelerometers, steel plates bolted to the tunnel wall, and a hammer wired as part of the trigger circuit. PROCEDURE At the gnome site, steel plates were bolted solidly to the tunnel wall at the sending and receiving stations, and the distances between them were surveyed. At each receiving station, an accelerometer was fastened to the steel plate. Output from the accelerometer was fed through the preamplifier to the oscilloscope, which was adjusted to sweep once when triggered by an external circuit. The trigger circuit used in these tests was a 6-volt dry cell in series with the oscilloscope; the hammer and the steel plate at the sending station acted as the switch. The time-mark generator was used on the second channel of a dual-trace oscilloscope to provide timing marks. It was also used to calibrate the grid on the oscilloscope screen, which in turn was used for measuring time. This is virtually the same procedure as used by Warrick and Jackson (1961) to measure velocities in salt and potash ore. The actual observations were made as follows: After the shutter on the camera was opened the sending plate was struck sharply with the hammer, thus closing the circuit and starting the trace on the oscilloscope to sweep. The acoustic waves generated by the hammer blow were imposed on the sweeping trace. The camera shutter was closed and the photograph immediately developed. The process was repeated until two satis- factory photographs had been taken. Figure 2, one of the photographs taken for the G-F line of measurement (fig. 1), is a typical example. In this photograph the time required by the oscilloscope beam to move one vertical grid line to the next was 2 milliseconds. The trace was started on a grid line, and the time was easily measured from starting time to the first arrival of the compressional wave. The photograph was enlarged by projection in order to more accurately pick this time. The first arrival of the shear wave was picked with a little less certainty, but when two or more pictures were used, this value was quite accurate. On figure 2 the times for the compressional and shear arrivals were picked at 5.7 and 10.4 milliseconds, respectively. It should also be noted that variation in the manner of striking the sending plate produced variation in the relative amounts of compressional and shear energy. Deliberate attempts at producing more shear energy by striking the sending plates on the side or top sometimes sharpened the shear arrival and reduced the relative compressional energy. The elastic moduli-Poisson’s ratio (ratio of the transverse strain to the longitudinal strain of a body under longitudinal stress), Young’s modulus (force per unit area multiplied by the length of a body, divided by the change in length), shear modulus (stress-strain ratio for simple shear, or the force per unit area divided by the ratio of the change in length to the original length of a body in shear), and bulk modulus (decrease in volume with increase in density of a body under pressure) of the rock salt were calculated from the following formulas (Howell, 1959, p. 152, 158, 204, 207; Jaeger, 1956, p. 56-58) :B110 GEOPHYSICS Figure 2.—Photograph of oscilloscope trace measuring travel times of compressional and shear waves for line of measurement G—F shown on figure 1. Vertical grid lines represent a time interval of 2 milliseconds. Oscilloscope started to sweep when circuit was closed and sound wave was initiated (left side of picture). First arrival of compressional wave P was at 5.7 milliseconds and first arrival of shear wave S was at 10.4 milliseconds. Poisson’s ratio, where Vp is compressional velocity in feet per second, and V, is shear velocity in feet per second. Young’s modulus, E— PVv\ 1+*)(!-2,Q 1440(1 — Dutra (1961). > Isidore Adler, analyst. B146 U.S. GEOL. SURVEY PROF. PAPER 501-B, PAGES B146-B147WARING B147 agreement between the data for the ratios by this method and by X-ray fluorescence is very good, but there are no data with which the present results for the hafnium content can be compared. The direct-reading method is iy2 times faster than spectrographic procedures based on photography, densitometry, and plate calibration. The use of a 1-mg sample is advantageous both to the mineralogist and to the spectrographer. Earlier work showed that low values and erratic results are obtained with samples weighing more than 1 mg, because of incomplete burning caused by the highly refractory nature of zirconium. The zircon content of most of the rocks is low, requiring at least 25 pounds of crushed rock to yield enough purified zircon for the analysis. The use of small, 1-mg samples saves time and labor in completing the purification process. However, care should be taken to insure that the zircon sample separated is large enough to be representative. The spectrographic and the direct-reading techniques are not applied to the original crushed rock because of the lack of sensitivity of the equipment to the hafnium and zirconium and because of the undesirable effects produced by other elements in the rock. REFERENCES Dutra, C. V., 1961, Spectrochemical studies on some Brazilian zircons: Bol. Soe. Brasilian Geol., v. 10, no. 1, p. 25-37. Helz, A. W., 1964, A gas jet for d-c arc spectroscopy: Art. 159 in U.S. Geol. Survey Prof. Paper 475-D, p. D176-D178. Waring, O. L., and Worthing, H. W., 1956, A spectrographic method for determining the hafnium-zirconium ratio in zircon : U.S. Geol. Survey Bull. 1036-F, p. 81-90.GEOLOGICAL SURVEY RESEARCH 1964 A SPECTROGRAPHIC METHOD FOR THE DETERMINATION OF CESIUM, RUBIDIUM, AND LITHIUM IN TEKTITES By CHARLES ANNELL, Washington, D.C. Abstract.—Spectrographic determinations of cesium, rubidium, and lithium in tektites, in concentrations as low as 1 ppm, are made with a K2C03=sample mixture and a 15-amp d-c arc. Selective filtering at the focal plane permits measurable line intensities for the two exposure conditions required. A method for the detection of cesium in concentrations of < 10 parts per million in tektites was required in order to study its abundance relative to that of other alkali elements. Several methods have been reported for trace-alkali determinations in rock and ore samples (Ahrens and Taylor, 1961, p. 194-201), and one procedure has been described for the determination of cesium, rubidium, and lithium in Australian tektites (Taylor, 1960). A 1-ppm analytical limit for cesium was obtained using a 3-meter concave-grating spectrograph, a cylindrical quartz lens focusing the arc source on the grating, Eastman I-N emulsion, a 15-ampere d-c arc, and anode excitation of a mixture of a 10-milligram sample and 20 mg of K2C03 which acted as a buffer for the sample. The method was primarily designed to determine the cesium content of tektites, with adaptation to rubidium and lithium determinations. The most sensitive analytical lines were used for all three elements: cesium, 8521.1; rubidium, 7800.2; and, lithium, 6707.8. A special filter at the focal plane of the spectrograph was necessary to obtain measurable intensities of the lithium-6707.8 line relative to the other lines. EXPERIMENTAL PROCEDURE In order to minimize errors arising from spectral interferences, an “average” tektite matrix was prepared from high-purity compounds, based upon several analyses reported previously (Cuttitta and others, 1961). Eight common oxides (or carbonates) were thoroughly mixed in the proportions shown in table 1. The mixture was sintered at 800°C in a muffle furnace for 30 minutes. The cooled material was then ground for 10 minutes in an agate mortar. A standard lepidolite, NBS 183, containing 0.3 percent Cs20, 3.5 percent Rb20 and 4.1 percent Li20 was diluted with the tektite matrix to give a graded series of alkali concentrations. For each dilution, some of the previously prepared standard and a portion of the tektite matrix were ground for 30 minutes in an agate mortar. This gave an adequate range of alkali standards (in parts per million) : Standard 1: Cs, 100; Rb, 1,140; Li, 680 2: Cs, 46; Rb, 529; Li, 320 8; Cs, 0.5; Rb, 5.3; Li, 3.2 The silicate-rock standards G-l and W-l were also included as standards in this work, using the following recommended values (in parts per million) (Stevens, and others, 1960) : Cs Rb Ll G-l................ 1.5 220 24 W-l................ 1.1 22 12 Exposures of four or five of these standards were made along with the tektite samples for each analytical plate prepared. Table 1.—Composition of a synthetic tektite matrix Compound Percentage Compound Percentage Si02 76 CaO 2 AI2O3 14 MgO 1 Fe203 3 Na20 (Na2C03) — 1 k2o (K2C03) 2. 5 Ti02 0.5 Alkali buffers are frequently used to enhance the intensity of many low-energy spectral lines (Ahrens and Taylor, 1961; and Rusanov and others, 1959, for example). Potassium salts are more effective than sodium salts for the enhancement of cesium. This is due to the lower ionization potential of potassium (4.32 ev), compared to that of sodium (5.12 ev), which in- U.S. GEOL. SURVEY PROF. PAPER 501-B, PAGES B148-B151 B148ANNELL B149 creases the probability of populating the upper energy level (1.45 ev) of the cesium atom that is responsible for the 8,521 line. The same reasoning applies to the enhancement of the rubidium-7800 (1.58 ev) and lithium-6707.8 (1.84 ev) lines. The three lines of the alkali elements all involve ground-state transitions (energy levels are taken from Moore, 1945). Johnson, Matthey and Co., Ltd., “Specpure” K2C03 was used because it contained no detectable cesium and had a very low rubidium and lithium blank. After a series of tests, a mixture of 10 mg of sample and 20 mg K2C03 was found to provide the required cesium detectability and precision. Similar results were obtained for rubidium and lithium, although the period of lithium excitation generally extended slightly beyond the main “K arc”. A 10-mg finely ground sample or standard is mixed with 20 mg of powdered K2C03. The mixing is conveniently done in an aluminum weighing pan with a plastic or wooden toothpick. The mixture is tamped with a small glass rod into the crater of a high-purity graphite electrode. In a humid environment the K2C03 will absorb water and become difficult to handle. A “dry box” or a similar low-humidity system is necessary under these conditions. All electrodes are stored in a dessicator when loaded. Approximately an hour before arcing, the electrodes must be dried in an oven set at 110°C to drive off excess moisture. Failure to dry the samples will result in popping and frothing after the arc is struck. The lower or sample electrode (anode) is made from high-purity ^-inch graphite rod. The electrode is machined to give a cup 0.24-inch deep having an inner diameter of 0.144 inch and outer diameter of 0.174 inch. The outside is machined to a shoulder 0.40 inch below the cup opening. The upper electrode is a straight ^-inch-diameter high-purity graphite rod (cathode). The electrodes are maintained at a 4-mm gap during arcing. The preheated electrodes are arced within 10 minutes after removing from the oven. An initial current of 5 amps d-c is used for 5 seconds to minimize any frothing or sample loss. The current is then increased to 15 amps for the remainder of the period. The output current remains remarkably steady at 15 amps throughout the arcing period, until the potassium has volatilized. Then a slight drop in the output current is noted along with a more erratic behavior. The exposure conditions for cesium are slightly different from those for lithium. Since the spectrograph used for these determinations covers a spectral range of about 1,300 A in the first order, it is necessary to take separate exposures. The first exposure can include cesium 8521.1 and rubidium 7800.2, and the second exposure includes rubidium 7800.2 and lithium 6707.8. The cesium-8521 line has a slight interference from a carbon band which can be ignored, provided the exposure is stopped when the potassium is gone. The loss of potassium from the electrode is marked by a change from a bluish-gray to a bright-blue color in the arc, as well as by the variation in the output current. The time required for this change in a 15-amp arc is approximately 90 seconds. The exposure for lithium and rubidium determinations is extended approximately 120 seconds, until there is complete sample consumption. No interferences are noted for lithium 6707.8 or rubidium 7800.2. A 450-mm cylindrical quartz lens focuses the source on the grating, which is masked to exclude background radiation from the electrode tips. A 25-micron slit is used. On the optical bench between the collimating lens and the slit, at the Sirk’s focal point, a filter holder is fixed. For the cesium and rubidium determinations a filter is selected so that the cesium-8521.1 line in W-l (1.1 ppm) gives an intensity value at least twice that of the standard deviation (table 2). This will give a cesium working range of 1-20 ppm when using I-N emulsion. The rubidium-7800.2-line intensity must be further attenuated to provide a measurable density in the 20-220-rubidium range. This is accomplished by using a 7-percent neutral filter mounted in a special holder which can be affixed at the focal plane in the casette (fig. 1). The lithium-rubidium determinations are made using about a 5-percent transmission filter in front of the slit and an additional 50-percent filter at the focal plane for the lithium-6707.8 line, permitting a workable lithium range of 4-150 ppm. In addition to neutral filters, an ultraviolet and blue-green absorbing filter is used to eliminate second-order spectra. The plates contain exposures of 5 or 6 standards and 5 or 6 samples, in duplicate. A calibration spectrum of a G-l/W-1, 1:1 mixture, using a 50/100-percent transmission-step filter, is exposed between the duplicate sets of standards and samples. The visible-red-sensitive I-N emulsion (Eastman) is used for all determinations. The plate is processed in D-19 developer for 4 minutes at 18 °C, placed in an acetic acid short stop 30 seconds, and acid fixed for 5 minutes. The plate is dried with a warm-air blower. Plate calibration is based on the two-step method (Churchill, 1944). A few lines in the 7300-8500-A region are selected for measurement with a densitometer.B150 ANALYTICAL TECHNIQUES Figure 1.—Closeup view of neutral filter mounted in a special brass holder (above) ; and view of spectrograph, showing position of filter and holder at the focal plane in the spectrograph (below). The cesium-line intensities are corrected for adjacent background. The selection of pure chemicals for the tektite matrix avoids any cesium contamination in the blank, but any further correction of the cesium blank results in an overcorrection of the analytical curve. The rubidium and lithium lines require no background correction when using the conditions described. Typical analytical curves for the alkali elements are shown in figure 2. The lithium and rubidium lines show reversal at the higher concentrations. No internal-standard lines could be found in the 6500-9000A region which were suitable for densitometry under these conditions. However, by means of voltage regulation at the source input coupled with the potassium buffering in the arc, satisfactory precision is obtained. A measure of the precision of the determinations is shown in table 2. Tektites having closely similar concentrations of trace alkalis are grouped together. One group of tektites from an area centered around Lee County, Tex., and commonly referred to as “bedia-sites”, have relatively low trace-alkali concentrations. The other group includes tektites from southeast Asia and Indonesia. The deviations of duplicate determinations obtained from the same spectrographic plates were used to calculate the standard deviations and coefficients of variation (Youden, 1951, p. 16-17; American Society for Testing Materials, 1960, p. 95). No accuracy tests were made because of a lack of analyzed samples. However, the level of trace-alkali concentrations in these groups of tektites is in agreement with the results reported by Taylor (1960, p. 89) for the australites. Table 2.— Trace-alkali •precision in analyses of two groups of tektites z (ovq. concentration, in Element Group ppm) S.D. C.V. n Cesium Bediasite (Texas) 2. 04 0. 22 10. 7 13 Tektite (southeast Asia and Indonesia). 5. 3 0. 35 6. 7 11 Rubidium_. Bediasite (Texas) 66. 5 3. 95 5. 9 8 Tektite (southeast Asia and Indonesia). 106 4 92 4 6 16 Lithium Tektite (southeast Asia and Indonesia). 46. 6 2. 76 5. 9 12 d=difference between duplicate values. n=number of duplicate determinations. x=average of all determinations in a group. S.D.=^5^- =standard deviation. C. V.=100S..D.=coefficient of variation. x 1 Lithium in bediasites was determined by another spectrographic method.INTENSITY INTENSITY ANNELL B151 Figure 2.—Analytical curves for the determination of cesium, lithium, and rubidium in tektites, based on G-l, W-l, and synthetic-tektite standards. REFERENCES Ahrens, L. H., and Taylor, S. R., 1961, Spectrochemical analysis, 2nd. ed: Reading, Mass., Addison-Wesley Pub. Co., Inc., 454 p. American Society for Testing Materials, 1960, Methods for emission spectrochemical analysis, 3rd ed: Philadelphia, p. 685. Churchill, J. R., 1944, Techniques of quantitative spectrographic analysis: Indust, and Eng. Chem., anal, ed., v. 16, p. 653. Cuttitta, Frank, Carron, M. K., Fletcher, J. D., and Chao, E. C. T., 1961, Chemical composition of bediasites and philippinites, in U.S. Geological Survey astrogeologic studies semiannnual progress report to NASA, February 25, 1961 to August 25,1961: p. 15-47. Moore, C. E., 1945, A multiplet table of astrophysical interest, rev. ed: Princeton, N.J., Princeton Univ. Observatory, 96 p. Rusanov, A. K., Khitrov, V. G., and Botova, N. T., 1959, Use of low temperature carbon arc as a source for excitation of Rb, Cs, T1 and In spectra in the spectrographic analysis of silicates: Zhur. Anal. Khim., v. 14, p. 534-541 [in Russian], Stevens, R. E., and others, 1960, Second report on a cooperative investigation of the composition of two silicate rocks: U.S. Geol. Survey Bull. 1113, 126 p. Taylor, S. R., 1960, Abundance and distribution of alkali elements in australites: Geoehim. et Cosmochim. Acta, v. 20, p. 85-100. Youden, W. J., 1951, Statistical methods for chemists: New York, John Wiley and Sons, Inc., 126 p.GEOLOGICAL SURVEY RESEARCH 1964 STAINING OF PLAGIOCLASE FELDSPAR AND OTHER MINERALS WITH F. D. AND C. RED NO. 2 By RUPERTO V. LANIZ,-1 ROLLIN E. STEVENS, and MEADE B. NORMAN, Palo Alto, Calif.; Menlo Park, Calif. Abstract.—Procedures are given for sequentially staining plagioclase red with F. D. and C. Red No. 2 (amaranth) and K-feldspar yellow with cobaltinitrite in rock slabs, thin-sections, and mounted sands. Although amaranth staining is not specific for plagioclase, it is frequently useful because other minerals can be distinguished by the hue and depth of the stain. Addition of a calcium chloride dip is necessary to stain Na-rich plagioclase. Bailey and Stevens (1960) proposed the staining of plagioclase feldspar red by treatment of the rock surface, etched with hydrofluoric acid, first with a solution of barium chloride and then with one of potassium rhodizonate. Barium ion is preferentially adsorbed on the etched plagioclase and forms insoluble barium rhodizonate, staining the plagioclase brick red. This staining technique for plagioclase was combined with yellow staining of K-feldspar with cobaltinitrite. Success with other dyes for staining plagioclase has also been reported. Robert F. Gantnier and James A. Thomas (written communication, 1961) used several pH-indicator dyes. Reeder and McAllister (1957) used hematein, and Graham (1955) malachite oxalate for staining plagioclase. This article describes the staining of plagioclase with the fruit dye F. D. and C. Red No. 2, after the mineral has been etched with hydrofluoric acid and dipped in barium chloride solution. This method can be combined with the well-known staining of K-feldspar with cobaltinitrite (Gabriel and Cox, 1929; Keith, 1939a, b; Chayes, 1952; and Rosenblum, 1956) to stain K-feldspar yellow and plagioclase red in rock slabs, in mounted sand grains, and in thin sections. Unlike the potassium rhodizonate the fruit dye is inexpensive and can be obtained from many dyestuff distributors. F. D. and C. Red No. 2 (amaranth) is listed as C. I. 16185 in the Colour Index of the American Association 1 Stanford University. B152 of Textile Chemists and Colorists (1957, p. 3084). It was formerly called amaranth, and was listed in older Colour Indexes as C. I. 184. The dye has the formula This dye and similar compounds are reactive toward metallic ions, which form ring structures by replacing the H in the OH group and joining to one of the N atoms with a coordinate link. Deep-red staining of the plagioclase is obtained by first adsorbing barium ion on the etched plagioclase surface, as in the rhodizonate staining technique, and then dipping the specimen in the amaranth dye. The resulting barium salt is slightly soluble and is retained on the etched plagioclase if the specimen is washed only briefly. Although the barium-dye compound is much more soluble than barium rhodizonate, washing techniques for the dye were developed which color all plagioclase surfaces in the rock slabs a brilliant purple-red that contrasts sharply with the color of K-feldspar (stained yellow by cobaltinitrite), unstained quartz, and dark ferromagnesian minerals. Pure albite fails to stain with either this dye or rhodizonate, but it can be stained by first dipping the etched specimen in calcium chloride solution. Other minerals containing alkaline earths or lead can be stained distinctive shades with the dye. DETAILED STAINING PROCEDURE The step-by-step procedure for staining rock slabs is as follows: 1. Prepare a smooth flat surface with No. 400 to 800 grit on a lap. If the rock is porous, first fill the surface with molten Lakeside before grinding it smooth. NaOjS ■N=N HQ SOiNa SOiNa U.S. GEOL. SURVEY PROF. PAPER 501-B, PAGES B152-B153LANIZ, STEVENS, AND NORMAN B153 2. Etch the surface for 10 to 15 seconds In concentrated hydro- fluoric acid (52-percent HF). 3. Dip the slab once in water. 4. Immerse the slab in a saturated solution of sodium cobalti- nitrite for 1 minute. 5. Remove the excess cobaltinitrite by rinsing the slab gently in tap water. 6. Dry the slab under a heat lamp. 7. Immerse the slab for 15 seconds in 5-pereent barium chloride solution (W/V). 8. Dip the slab once quickly in water, and dry gently with compressed air. 9. Immerse the slab for 15 seconds in amaranth solution (1 oz. F., D. and C. Red No. 2, 92 percent pure coal-tar dye, in 2 liters of water). 10. Dip the slab once quickly in water. 11. Direct a gentle stream of compressed air onto the stained surface to sweep off the remaining excess of amaranth solution. 12. Where milky white areas suggestive of albite remain after the above treatment, repolish, repeat steps 1 to 3, dip in calcium chloride solution, dry, then proceed as in steps 4 to 11. For staining sand grains, mount them in melted Lakeside containing lamp black to make it opaque; cool; grind a surface smooth to expose the sand grains; and etch and stain as directed for rock slabs. For staining thin sections the procedure is as follows: 1. Etch the uncovered rock section for 15 seconds in hydro- fluoric acid vapor. 2. Immerse in the cobaltinitrite solution for 15 seconds. 3. Rinse briefly in tap water. 4. Immerse for a few seconds in the barium chloride solution. 5. Dip in distilled water. 6. Immerse for 1 minute in the amaranth solution. 7. Dip once in water. 8. Sweep away the excess amaranth solution, still left on the slide, with a gentle stream of compressed air. AMARANTH STAINING OF OTHER MINERALS The etched plagioclase feldspars are not the only minerals stained by the amaranth. Various other minerals containing akaline earths or lead may also be stained, the depth of color depending upon the content of these elements in the mineral reacting with the dye, and upon the extent to which the mineral is etched with hydrofluoric acid. Silicate minerals containing alkaline earths or lead are readily stained because a significant etch residue is left on the mineral. Deep-red stains were obtained, after etching, on the following minerals: benitoite, celsian, cordierite, dolo- mite, hydrogamet, pectolite, vesuvianite, witherite, wollastonite. Very faint or insignificant stains were obtained on anglesite, anhydrite, barite, calcite, and celestite because these minerals do not leave an etch residue to retain the stain. That the amaranth stain is not specific for plagioclase is frequently an advantage in that certain other minerals may be delineated in the specimen because the depth of red produced on them contrasts with the shade of red of the stained plagioclase. For example, in a stained rock slab the deep red of stained cordierite contrasted well with the less intense red of the stained plagioclase, and the structural relationships in the rock could be plainly seen, showing a complex assemblage of deep-red-stained cordierite, less-red plagioclase, yellow-stained K-feldspar, uncolored quartz, and dark ferromagnesian minerals. Dolomite is stained a deep red with amaranth, and calcite a faint pink. These results have been repeated on a number of samples and the test was found to be diagnostic for distinguishing calcite from dolomite. In samples with intergrowths of calcite and dolomite the deep red of the stained dolomite contrasted clearly with the faint pink of the calcite. REFERENCES American Association of Textile Chemists and Colorists, 1957, Colour index, v. 3, 2nd ed., 1956: Lowell, Mass., Lowell Technol. Inst. Bailey, E. H., and Stevens, R. E., 1960, Selective staining of K-feldspar and plagioclase on rock slabs and thin sections: Am. Mineralogist, v. 45, p. 1020-1025. Chayes, Felix, 1952, Notes on the staining of potash feldspar with sodium cobaltinitrite in thin sections: Am. Mineralogist, v. 37, p. 337-340. Gabriel, Alton, and Cox, E. P., 1929, A staining method for the quantitative determination of certain rock minerals: Am. Mineralogist, v. 14, p. 290-292. Graham, E. R., 1955, Rapid determination of quartz, potash minerals, and plagioclase feldspars: Chemist-Analyst, v. 44(2), p. 37-38. Keith, M. K., 1939a, Selective staining to facilitate Rosiwal analyses: Am. Mineralogist, v. 24, p. 561-565. ----—1939b, Petrology of the alkaline intrusive at Blue Mountain, Ontario : Geol. Soc. American Bull., v. 50, p. 1795-1826. Reeder, S. W., and McAllister, A. L., 1957, A staining method for the quantitative determination of feldspars in rocks and sands from soils: Canadian Jour. Soil Sci., v. 37, p. 57-59. Rosenblum, Samuel, 1956, Improved technique for staining potash feldspars: Am. Mineralogist, v. 41, p. 662-664.GEOLOGICAL SURVEY RESEARCH 1964 SUCCESSFUL SEPARATION OF SILT-SIZE MINERALS IN HEAVY LIQUIDS By ROBERT SCHOEN and DONALD E. LEE, Menlo Park, Calif. Abstract.—Routine separations of particles as small as 10 microns are possible by centrifuging fine fractions in heavy liquids. Rapid application of centrifugal force allows separation of particles to precede flocculation. One of the major stumbling blocks in the application of theoretical geochemical principles in earth science is the inability to determine the precise chemical composition of natural coexisting phases. Many rocks are so fine grained that their mineral phases cannot be purified for chemical analysis. Fine-grained igneous rocks, hydrothermally altered rocks, and many sedimentary rocks are subject to this problem. The geochemical analysis of some of the most interesting natural systems often founders because an approximate or ideal composition for one or more of the phases must be assumed. The usual sink-float techniques of mineral separation in heavy liquids fail, when applied to small particles, for two reasons. First, the rate of sedimentation of very small particles is slow in liquids whose specific gravity is close to that of the particles. Second, and more important, the relatively large surface area in relation to weight of small particles leads to their aggregation into floes whose individual grains can no longer sink or float independently. Two recent papers (Loughnan, 1957; Kittrick, 1961) describe methods by which expansible clay minerals may be purified by sink-float techniques. Both methods depend upon the ability of particular clays to change their specific gravity appreciably when they adsorb certain liquids. Unfortunately, the methods are limited to expansible clay minerals and possibly to zeolites, and are restricted to relatively large particle sizes, because of the tendency of the grains to flocculate. As part of a geochemical study of hydrothermal alteration, a method was developed to make routine heavy-liquid separations of particles as small as 10 microns in diameter. Particles smaller than 10 microns can be separated if large density differences exist among the phases, as for instance in pyrite and quartz. The success of this method depends upon its ability to overcome the two previously mentioned obstacles common to ordinary sink-float techniques. A centrifuge capable of producing 1,500-gravities acceleration must be used in order to speed up the sinking or floating of the mineral grains (Hutton, 1943). Kepeated short high-speed centrifugations, with intermittent stirring, are necessary to allow separation to occur before flocculation. Familiarity with the general principles of heavy-liquid techniques (Twenhofel and Tyler, 1941, p. 67-84; Hutton, 1950) is assumed in the following discussion and description. Particular care must be used to avoid inhalation of vapors from any of the organic liquids, many of which are highly toxic. EQUIPMENT The following special equipment is useful in making clean separations and minimizing loss of sample: 1. Heavy-wall centrifuge tubes of special shape (fig. 1) are necessary to avoid breaking of tubes and to minimize contamination of concentrates (Hutton, 1943, p. 76). This shape allows the light fraction to be poured off and the top of the tube rinsed without contamination of the heavy fraction. Such tubes may be obtained on special order from a glassblower. In conjunction with this tube, a stopper (fig. 1) must be used to seal off the lower bulb of the tube. The stopper may be made by attaching to a metal rod a plug of hard rubber that has been shaped to fit the constriction in the centrifuge tube, or a plug may be made by shaping molten polyethylene inside a wet centrifuge tube to fit the constriction. 2. A three-element filter of the millipore type is superior to an ordinary funnel for filtration of heavy liquids. The millipore filter has the advantage of rapid filtration because of its large area for filtration. There is no danger of the filter paper breaking as it is supported on a fritted glass disc. The cellulose filters supplied for normal use in a millipore filter must not be used, as they are soluble in organic solvents. Instead, a smooth hardened filter paper such as Whatman 50 is trimmed to fit on top of the glass disc. This results in a 300-percent saving in filter-paper cost. B154 U.S. GEOL. SURVEY PROF. PAPER 501-B, PAGES B154-B157SCHOEN AND LEE B155 3. An inexpensive water aspirator is preferable to a vacuum pump for producing suction in the vacuum flask. The poisonous and corrosive vapors produced by heavy liquids are difficult to trap, and their accumulation in a vacuum pump requires flushing and refilling with expensive oil. An aspirator, on the other hand, flushes these vapors away and there is no disposal problem. Although an aspirator produces less vacuum than a pump, the large filtration area of a millipore filter results in rapid filtration. The aspirator also causes less evaporation of heavy liquids. 4. Although a rubber stopper can be used to support the milli- pore-filter assembly, a rubber filter support and closure marketed under the trade name “Filtervac” will greatly speed up transfer of the filter assembly from flask to flask. The usual arrangement of the pieces of filtration equipment is diagrammed in figure 2. Figure 1.—Specially shaped centrifuge tubes (A, 40-ml and B, 10-ml capacity) with stoppers, for the separation of minerals in heavy liquids. 725-328 0—64-----11 PROCEDURE 1. Crush the sample to pass through a 200-mesh sieve and then size it as follows: Let the sample settle in a water-filled 10-cm-high vessel for 2 minutes; decant the suspension. Let the suspension settle for 10 minutes and decant again. This procedure gives three solid fractions whose approximate size limits are: 30-75 g, after 2 minutes; 10-30 g after 10 minutes; and less than 10 g in the remaining suspension. Dry the two coarse fractions under a heat lamp. A final washing with anhydrous acetone gives a powdery sample free from lumps. 2. Pour the size fraction whose largest grains are monomin- eralic onto a creased glazed weighing paper. Crush any lumps to form a free-flowing powder. 3. Pour the sample into the special centrifuge tubes. The 40-ml tube will hold 2 g or less and the 10-ml tube will hold % g or less. 4. Fill each tube to the same level with a heavy-liquid mixture of the proper specific gravity. If a complete separation of a rock is attempted, it is best to start with the heaviest liquid and work successively with lighter liquids. In this way, the bulk of the sample is always floating at the top of the tube where it can be stirred to free more heavy minerals. 5. Stopper the mouth of each tube, preferably with a neoprene or a plastic stopper, to prevent evaporation of the liquid and a consequent change in specific gravity. 6. Gently invert each tube several times to disperse the sample throughout the liquid. Quickly place the tubes into a centrifuge and rapidily accelerate it to 1,500 to 2,000 gravities. 7. Stop the centrifuge slowly after about 1 minute. Prolonged centrifugation only hardens the floating cake of mineral grains, making further separation difficult. 8. Stir the floating cake to redisperse it completely, but avoid mixing in the heavy fraction. After stirring, quickly put the tubes into the centrifuge and again rapidly accelerate it to high speed. 9. Three centrifugations are usually enough, but centrifuging should be repeated until no further addition to the heavy fraction is noted. Even if no heavy minerals separate during the first run, it is best to stir and centrifuge again. If the amount of heavy minerals separated seems disappointingly small, filter the liquid anyway as several hundred milligrams will appear insignificant if divided among several tubes. 10. Gently twist the specially-shaped stopper through the float- ing cake. This loosens the cake so that it can be poured off yet does not cause mixing of the light (solids) and heavy fractions. Seal off the lower bulb of the tube and pour the light fraction into the millipore filter. With the stopper held tightly against the constriction of the tube, rinse the upper portion with a jet of heavy liquid from a squeeze bottle until all the light fraction is on the millipore filter. Repeat step 10 for each tube. 11. After filtering the heavy liquid into a vacuum flask, break the vacuum, remove the vacuum flask containing heavy liquid, and insert a clean vacuum flask beneath the millipore filter. Wash the light fraction and the sides of the funnel with a jet of anhydrous acetone from a squeeze bottle. Filter off the acetone washings.ANALYTICAL TECHNIQUES B156 12. Carefully open the millipore filter holder and remove the filter paper. Scrape the grains sticking to the funnel onto the filter paper and dry under a heat lamp. Rinse the funnel with acetone and dry. Install a new filter paper and reassemble the filter. Pour off the heavy fraction from each tube. Rinse the tube with heavy liquid. Change the vacuum flask and wash with acetone as before. 13. The heavy-liquid filtrate can be reused after its specific gravity is checked and adjusted if necessary. The acetone washings should be saved in a large brown bottle for eventual recovery of pure heavy liquid by standard methods. An example of the purification routinely possible by this method is presented on figure 3. The rock, a hydro-thermally altered basaltic andesite, consisted of K-feld-spar, celadonite, and lesser amounts of pyrite and anatase. The 10-30 p fraction, A, consisted of individual grains of K-feldspar, celadonite, and pyrite with very small inclusions of anatase in otherwise pure mineral grains. Separated fractions of K-feldspar, B, and celadonite, 0, each with included anatase, are being chemically analyzed. The analyses will be corrected for anatase by subtracting TiOz (anatase) from each analysis. If more sample had been available, the concentrates illustrated on figure 3 could have been purified further. The careful application of this method will lead to cleaner separations and, therefore, to more meaningful chemical analyses. When a sufficient amount of sample is available, the purity of the fractions will depend largely on the patience of the investigator. Figure 3.—Photomicrographs of fine-grained mineral fractions purified with heavy liquids. A, the 10-30 p fraction of crushed basaltic andesite; B, separated K-feldspar fraction; C, separated celadonite fraction. The mineral grains are mounted in an oil, refractive index 1.535, that enhances the tiny anatase inclusions. Although apparently contaminated, the K-feldspar fraction, B, contains only 0.60 percent titanium.SCHOEN AND LEE B157 REFERENCES Hutton, C. O., 1943, Some features of heavy mineral separations: Royal Soc. New Zealand Trans, and Proc., v. 73, p. 76-83. ------ 1950, Studies of heavy detrital minerals: Geol. Soc. America Bull., v. 61, p. 635-716. Kittrick, J. A., 1961, The density separation of clay minerals in thallous formate solutions: Am. Mineralogist, v. 46, p. 744-747. Loughnan, F. C., 1957, A technique for the isolation of inont-morillonite and halloysite: Am. Mineralogist, v. 42, p. 393-397. Twenhofel, W. H., and Tyler, S. A., 1941, Methods of study of sediments: New York, McGraw-Hill, 183 p.GEOLOGICAL SURVEY RESEARCH 1964 EFFECT OF SEICHES AND SETUP ON THE ELEVATION OF ELEPHANT BUTTE RESERVOIR, NEW MEXICO By GEORGE L. HAYNES, JR.( Santa Fe, N. Mex. Abstract.—Recorded deviations from the normal water-surface elevation of Elephant Butte Reservoir occur as setup and seiche and are caused by wind and barometric pressure changes and by flash-flood waves from reservoir tributaries. Single-station weather data provide only a general indication of setup production and seiche excitation. Transitory surges of the water surface in reservoirs can introduce significant error in the computation of capacity. However, such errors can be reduced by careful selection of sites for gages and by correcting for known anomalies. Surges caused by wind, barometric-pressure changes, and flash-flood waves at Elephant Butte Reservoir on the Rio Grande in south-central New Mexico were studied to aid in establishing guidelines for locating reservoir and lake gages. Elephant Butte Reservoir is a long narrow lake whose major axis has a general north-south orientation; at maximum elevation, 4,231.5 feet, the reservoir has a capacity of 2,195,000 acre-feet and comprises two main bodies of water separated by a constriction called the Narrows. Deviations from the normal water surface recorded by the reservoir gage at the dam occur as static and dynamic surges or as a combination of the two. These surges are caused by wind and air-pressure changes and by flood waves from tributaries that discharge into the reservoir. Water-surface fluctuations are compared with weather observations at the Truth or Consequences, N. Mex., airport, 7% miles northeast of Elephant Butte Dam. Static surges classified as setup are caused primarily by strong winds of extended duration, but pressure difference over the water surface can augment or suppress the effect of wind. The U.S. Army Corps of Engineers (1955) found that pressure differences had to be accounted for in relating setup to hurricane B158 parameters on Lake Okeechobee in Florida. Irish and Platzman (1962) investigated the possibility of resonant coupling resulting from movement of the stress band accompanying frontal passages of cyclonic systems across Lake Erie. They concluded that resonance is almost entirely suppressed when the stress-band width is greater than the length of the lake; this is the case for Lake Erie, which has a length of about 200 miles—much less than the scale of cyclonic systems. Figure 1 shows the relation between the north or south component of wind velocity and setup or setdown as recorded by the reservoir gage. A more precise procedure would be to relate setup to wind force, (p„F2), Figure 1.—Relation between wind velocity and setup and setdown for Elephant Butte Reservoir during the period 1950-61. U.S. GEOL. SURVEY PROF. PAPER 501-B. PAGES B158-B162HAYNES B159 where pa is the air density and V is the wind velocity, and to adjust for pressure difference over the water surface. This procedure, however, would require weather data and water temperature at several points over the reservoir surface. The computation of setup requires data on fetch, depth, shear stress, and in some situations, barometric pressure and planform (shape of water body in plan view). The determination of shear stress is extremely complicated. Dynamic surges, or seiches, are oscillatory long-period standing waves whose periods are intermediate between those of lunar tidal waves and storm waves. The resonant oscillation of seiches is analogous to similar behavior of mechanical, acoustical, and electrical systems and may be expressed one-dimensionally by the differential equation for a linear-damped oscillating system with forced vibrations. Seiches may be excited by any force acting on the water surface, including wind, atmospheric pressure, flood waves, landslides, earthquakes, and rainfall. These forces may act singly or in combination to produce oscillations or to damp oscillations previously excited. Seiche periods for irregular basins may be computed by Du Boys’ (1891) equation y=2 rL dx ; k Jo -yfgd in which d is the depth corresponding to an increment of length, dx, g is acceleration of gravity, L is total length, and k is the number of nodes. Observed periods of oscillation on Elephant Butte Keservoir were compared with theoretical periods computed by Du Boys’ equation, using the method described by Shen (1961). The comparison, shown in figure 2, is influenced by several factors. Friction losses in shallow water cause observed wave celerities to be less than computed values. Seddon (1900), in his studies on Figubb 2.—Observed and computed periods of seiche oscillation on Elephant Butte Reservoir during the periods 1941-43 and 1950-61.B160 SURFACE WATER the Mississippi River, found the celerity in a reach to be dependent on the mean width of channel; this factor would probably affect long narrow reservoirs such as Elephant Butte in similar fashion. Extensive sedimentation, particularly in the upper reaches of the reservoir, also may affect the comparison. Computed periods are based on depths from the 1961 survey below the Narrows and the 1957 survey above the Narrows. The best agreement of observed and computed periods is for the period 1950-56, when the water surface was confined to the area below the Narrows. During the period 1957-59, the water surface occupied part of the area above the Narrows. The rise in elevation through the Narrows was accompanied by a gradual decrease in the observed period of primary oscillation from iy2 hours to 1 hour. As the water-surface elevation through the Narrows later dropped, the observed period increased to iy2 hours. Shen (written communication, 1963) suggests that the Narrows influences the seiche characteristics such that uninodal oscillation for elevations below the Narrows changed to trinodal above the Narrows and that during the transition the behavior was similar to that of an open-end basin. Figure 3 indicates the general classification of seiche mode with respect to reservoir elevation, and figure 4 illustrates how oscillations may have occurred under these conditions. With the reservoir at high stage in 1941-43 (fig. 2), trinodal oscillations apparently were replaced by uninodal primary oscillations accompanied by secondary oscillations of about the fourth or fifth harmonic. The uninode probably was located in the Narrows as indicated by figure 4. For the secondary oscillations, the reservoir may have behaved as two distinct open-end or closed basins separated by the Narrows. Figure 4.—Sketch showing probable mode of primary seiche oscillation on Elephant Butte Reservoir for different water-surface elevations. This study indicates that seiches on Elephant Butte Reservoir may be excited by wind and barometric-pressure fluctuations and by flood waves from tribu- Figure 3.—General classification of seiche mode on Elephant Butte Reservoir with respect to water-surface elevation during the period 1950-61. Wind direction t \ t \ / S t cc uj (0 i±j tr w H 3 X !£ W o o LlJ — ce z. < cl ± CD Figure 5.—Record of a seiche probably resulting from flash floods, and the relation of the seiche to associated weather conditions, July 12, 13, 1950, Elephant Butte Reservoir. For wind-direction symbols, north is toward top of page.HAYNES B161 taries to the reservoir. However, data observed at the single weather station provide only a general indication of the specific conditions responsible for seiche excitation. The largest seiche amplitudes recorded during the study period were apparently produced by flash-flood waves from tributaries to the reservoir. Figure 5 shows a seiche probably resulting from a flash flood of about 1,000 cubic feet per second out of Ash Canyon, noted on the chart by an observer at the reservoir. The associated weather conditions shown support this likelihood. A seiche probably excited by the sudden subsidence of strong winds is shown on figure 6. Weather conditions associated with other seiches studied indicated that excitation commonly resulted from sharp pressure changes and wind reversal. The excitation of some seiches studied was particularly obscure, emphasizing the limited applicability of single-station data in quantitative seiche analysis. Wind direction Figure 6.—Record of a seiche resulting from sudden subsidence of strong winds, and the relation of the seiche to associated weather conditions, May 27, 1953, Elephant Butte Reservoir. For wind-direction symbols, north is toward top of page. Two classes of weather systems have been identified as producing setup and in exciting seiches. Cyclonic systems produce most occurrences of setup; thunderstorm systems excite most seiches. Frequency of occurrence of setup and seiche during 1941-43 and 1950-61 is shown in figure 7; the number of occurrences of pure setup is small compared to the number of seiches. Thunderstorm systems are responsible for the greatest number of deviations from the normal water-surface elevation. Because of the small scale of thunderstorm systems, a comprehensive quantitative analysis of seiche excitation would require complete weather observations at a number of locations over the reservoir surface; fewer observations would be required for cyclonic systems because of their larger scale. A properly instrumented study might show that the phenomenon of resonant coupling resulting from thunderstorm systems is an important factor in exciting seiches or in augmenting seiche amplitude. Figure 7.—Monthly distribution of 256 occurrences of setup and seiches exceeding 0.10-foot amplitude on Elephant Butte Reservoir during 1941-43 and 1950-61. A knowledge of the characteristics, and an understanding of the principles, of setup and seiche occurrence are necessary for the proper interpretation and accurate computation of reservoir and lake-stage records and for the pptimum placement of gages to minimize or delineate seiche and setup effects. Formidable problems in gage location would be posed by the complexity of these characteristics when applied to reservoirs having irregular planforms and subject to large ranges in stage. REFERENCES Du Boys, P., 1891, Essai th^orique sur les seiches: Archives des Sciences Physiques et Naturelles, Geneve, p. 628.B162 SURFACE WATER Irish, S. M., and Platzman, G. W., 1962, An investigation of the meteorological conditions associated with extreme wind tides on Lake Erie: Monthly Weather Rev., U.S. Dept, of Commerce, Weather Bur., v. 90, no. 2, p. 39-47. Seddon, J., 1900, River hydraulics: Am. Soc. Civil Engineers Trans., v. 43, p. 217-229. Shen, John., 1961, Characteristics of seiches on Oneida Lake, New York: U.S. Geol. Survey Prof. Paper 424^B, p. B80-B81. U.S. Army, Corps of Engineers, 1955, Waves and wind tides in shallow lakes and reservoirs: Office of the District Engineer, Jacksonville, Fla., Summary Report, 46 p.GEOLOGICAL SURVEY RESEARCH 1964 FLOOD INUNDATION MAPPING, SAN DIEGO COUNTY, CALIFORNIA By L. E. YOUNG and H. A. RAY, Menlo Park, Calif. Work done in cooperation with the California Department of Water Resources Abstract. A flood-hydrology study of San Diego County streams indicates that flood magnitude-frequency relations can be estimated from drainage-area size and a dimensionless basin-shape factor. Floods of 50- and 100-year magnitude were estimated for selected sites and, by means of a simple reservoir-storage routing method, the peak discharges were adjusted, where necessary, for the attenuation that would result from storage in existing reservoirs. Areas of potential inundation are shown on topographic maps. In an investigation of flood hazard in San Diego County, Calif., a new approach was used to determine, from floods of 50- and 100-year recurrence intervals, the areas of potential inundation along five major rivers. A dimensionless flood hydrograph was used in adjusting regionalized flood-frequency results to allow for the attenuating effect of existing reserviors. This investigation consists of two major parts, (1) a flood-hydrology study of streams draining the western slopes of the Peninsular Range in San Diego County, and (2) determination of areas of potential inundation along the flood plains of the five major rivers, for annual floods of 50- and 100-year recurrence intervals. The regional concept of flood-frequency analysis was used in the flood-hydrology study because the flood series for an individual stream-gaging station is a random sample that may not be representative of the longterm average distribution of floods at that gaging station. The regional concept combines the experience at a number of gaging stations in a homogeneous area, thus providing more reliable flood magnitude-frequency relations. This method of analysis is described in detail in a recent U.S. Geological Survey report (Benson, 1962). Statistical multiple-correlation techniques were used to relate floods of selected recurrence intervals to hydro-logic and physiographic characteristics of gaged streams in the area. The equations relating the annual peak discharge of T’-year recurrence interval, Qt, to various basin hydrologic and physiographic parameters have the general form Qr=a BbCcDd, where B. C, and D = basin parameters (independent variables) , and a, b, c, and d=constants of the regression equation. The most significant parameters for use in estimating the 50- and 100-year floods were found to be drainage area and a dimensionless basin-shape factor. This shape factor, Sh, is defined as Sh=d/l, where d= diameter, in miles, of a circle with an area equal to the basin area, and 1= length, in miles, of the drainage basin measured parallel to the principal stream channel. The effects of mean annual precipitation, mean annual basin loss (precipitation minus runoff), main channel slope, and channel storage, on annual peak discharges were also investigated, but were found not to be significant for use in estimating the 50- and 100-year floods. To determine the area of potential inundation, the generalized equations from the flood-hydrology study were used to estimate magnitude of 50- and 100-year floods for selected locations along the San Luis Rey and San Dieguito River flood plains. These peak discharges were then adjusted, where necessary, for the attenuation that would result from reservoir storage. The degree of attenuation was determined by a simple reservoir-storage routing method whereby the storage and outflow discharge are assumed to be uniquely related (Carter and Godfrey, 1960). A composite dimensionless flood hydrograph, developed for the study B163 U.S. GEOL. SURVEY PROF. PAPER 501-B, PAGES B163-B164B164 SURFACE WATER area, was used in conjunction with the estimated peak discharges to construct hydrographs of hypothetical reservoir inflow. The dimensionless flood hydrograph, which relates percent of peak discharge to time elapsed since the beginning of storm runoff, was developed from the few available recorded flood hydrographs for the major rivers in the area. The standard step method of backwater analysis (Chow, 1959) was used to compute water-surface profiles for the adjusted peak discharges. This method uses the Manning equation for computing tranquil gradually varied flow. The hydraulic properties of the reaches of river channel under study were determined from field surveys and from large-scale topographic maps, These data, along with the appropriate peak discharges, were then applied in the equation, and by trial-and-error computation the water-surface profiles were determined. These profiles were adjusted for backwater effect from bridge constrictions, and the adjusted profiles were used to delineate the areas of potential inundation along the streams. The areas of potential inundation on the San Luis Rey and San Dieguito River flood plains for 50- and 100-year floods were shown on 7^-minute topographic maps. Two sets of maps (not shown) were prepared; one set shows the area that would be inundated if the floods occurred when reservoirs were initially half full, and the second set shows the inundated area if the floods occurred when reservoirs were initially full. REFERENCES Benson, M. A., 1962, Evolution of methods for evaluating the occurrence of floods : U.S. Geol. Survey Water-Supply Paper 1580-A, 30 p. Carter, R. W., and Godfrey, R. G., 1960, Storage and flood routing: U.S. Geol. Survey Water-Supply Paper 1543-B, 104 p. Chow, V. T., 1959, Open-channel hydraulics: New York, McGraw Hill, 680 p.GEOLOGICAL SURVEY RESEARCH 1964 THE RELATION OF DISCHARGE TO DRAINAGE AREA IN THE RAPPAHANNOCK RIVER BASIN, VIRGINIA By H. C. RIGGS, Washington, D.C. Abstract.—A family of curves relating discharge to drainage area, for discharges ranging from flood peaks to low flows, has been derived from gaging-station records in the Rappahannock River basin. The extrapolation of these curves to small drainage areas within the basin is verified by 4 series of 30 low-flow measurements in a portion of the basin. The curves may be used to estimate the magnitudes of low flows at selected frequencies. Stream discharge is commonly related to drainage area by the model Q=CA\ where Q is some selected discharge such as the 20-year flood, mean discharge, or drought discharge; and A is drainage area. The constants C and n will vary with the selected discharge. Thus, for a drainage basin, a family of curves is needed to cover the range in discharge. Such a family of curves is defined from gaging-station records in the Bappahannock Biver basin above Fredericksburg, Va. These curves may be extrapolated to small drainage areas within the basin, but without additional information the reliability of the extrapolated portion is unknown. Discharge measurements made on small streams at times of relatively steady flow verify the curve extrapolations in a portion of this basin. After defining the curve family and verifying the extrapolation to small drainage areas, one can estimate drought discharges from the measured small streams. The family of curves is developed from records for eight gaging stations in the basin. The basin and the gaging-station locations are shown on figure 1. The relation with mean discharge is defined by records for 7 stations, and an estimate for 1, for the period 1944—50. The plot shows considerable scatter. The amount of rainfall increases from north to south in this part of Virginia; consequently, the mean discharge per square mile from the southern drainage areas is greater than from the northern ones. This information can be used by adding to the relation a variable of latitude. Figure 2 shows mean discharge, both unadjusted and adjusted for latitude, plotted against drainage area. The equation of the relation is log 0.356+0.956 log A-0.0052 £, where Qm is mean discharge, 1944-50, in cubic feet per second; A is drainage area in square miles; and L, which ranges from 21 to 47, is latitude in minutes north of 38° N lat. Short records do not permit accurate definition of streamflow at specific probability levels. Therefore, 78 "00' Figure 1.—Map of the Rappahannock River basin above Fredericksburg, Va. Circles indicate gaging stations used in this analysis. U.S. GEOL. SURVEY PROF. PAPER 501-B. PAGES B165-B168 B165B166 SURFACE WATER Figure 2.—Relation of drainage area to mean discharge, 1944-50, in the Rappahannock River basin. concurrent discharges are used to develop other relations with drainage area throughout the discharge range. Peak discharges for the annual floods of 1942, 1955, and 1956 at the several gaging stations and at some miscellaneous stream-measurement sites are plotted against drainage area in figure 3 (curves 1, 2, and 3 respectively). Although not all the peaks for a particular flood have the same recurrence interval, the differences should not be great. Curve 4 (fig. 3) is the relation of drainage area to mean discharge, transferred from figure 2. Curves 5 through 9 are defined by minimum daily discharges for the following months of low flow: September 1955, September 1956, September 1954, October 1954, and October 1930. The ordinate scale is discharge plus 0.1 cfs so that a discharge of zero can be plotted. The relation curves are defined by the gaging-station records for drainage areas as small as 15 square miles. Downward extrapolations of these curves for discharges DRAINAGE AREA, IN SQUARE MILES Figure 3.—Relation of selected discharge to drainage area in the Rappahannock River basin.RIGGS B167 SCALE B 1 10 100 SCALE C 1 10 100 SCALE D 1 10 100 DRAINAGE AREA, IN SQUARE MILES Figure 4.—Discharge-drainage-area relations in the Hazel River basin. A, October 30 and 31, 1961; B, September 24 and 25, 1962; C, May 15 and 16, 1963; and fl, June 25 and 26, 1962. less than the mean have been checked by discharge measurements. Four sets of about 30 discharge measurements each, made in the Hazel River basin, a subbasin of the Rappahannock, are used to define the relations with drainage area shown in figure 4. The scatter of the points about the mean curves of figure 4 may be due to one or both of the following: (1) variation in base-flow yield, and (2) variation in recent precipitation experience among the basins. The curves describe the yield of an average subbasin of the Hazel River basin. If the meas- ured discharges of a stream are consistently above or below the average lines, that deviation is assumed to indicate no unusual precipitation influence and, therefore, a yield greater or less than the average. Some of the measurements in the Hazel River basin indicate an occasional influence of nonuniform precipitation over the basin, and others indicate definite differences in yield of certain subbasins. The curves of figure 4 have about the same slopes as the comparable curves of figure 3, indieating the hydrologic homogeneity of the Hazel River basin andB168 SURFACE WATER the general applicability of the curves of figure 3, when extrapolated, to small drainage areas in that basin. The extrapolated curves permit inferences as to the probable discharges of small streams in the Hazel River basin during droughts. For instance, extrapolations of curves 6 and 9 in figure 3 reach zero discharge at about 2 and 70 square miles, respectively, indicating that most streams draining smaller areas probably were not flowing at those times. The frequencies of these events can be estimated from gaging-station records. For streams on which measurements have been made, the respective drought discharges obtained from the average curves should be modified on the basis of measured discharges. Unless a base-flow measurement is available somewhere on a stream, the results from the average curves should be considered as first approximations. Differences in yield of subbasins are more pronounced at extremely low discharges. An additional set of discharge measurements made under drought conditions in August 1963 (fig. 5) shows this to be true. Thus, the generalized curves are least reliable under extreme drought conditions. 100 10 100 DRAINAGE AREA, IN SQUARE MILES Figure 5.—Discharge-drainage-area relations under drought conditions, August 6 and 7, 1963, in the Hazel River basin.GEOLOGICAL SURVEY RESEARCH 1964 THE ARTESIAN AQUIFER OF THE TIERRA DEL FUEGO AREA, CHILE By WILLIAM W. DOYEL and OCTAVIO CASTILLO U., Washington, D.C., Santiago, Chile Work done in cooperation with the Instituto de Investigaciones Qeoldgicas, Santiago, Chile, and under the auspices of the Agency for International Development, V.S. Department of State Abstract.—Water flows from wells tapping the Los Olivos and Bellavista Members of the Palomares Formation of Tertiary age. Although the areal extent and hydrologic characteristics of these artesian aquifers are not known fully, considerable additional development of water supplies from them seems feasible. During the exploration for, and exploitation of, petroleum by the Empresa Nacional del Petroleo de Chile (ENAP) in the Tierra del Fuego area,1 artesian water was found in wells in the northern part of the Isla Grande de Tierra del Fuego and on the mainland north of the island (fig. 1). Some of the wells have as much as 70 meters of artesian head above land surface. Various ENAP geologists (Mordojovich, 1950; Alvarez, 1953; Duhart, 1955; and Marino and Mordojovich, 1955) have made brief studies of the occurrence of the ground water, and Gonzalez and Cortes (1953) have correlated the subsurface data with the surface geology. In 1962 the water was being utilized for public supply and industrial use at ENAP installations in the northern part of the Isla Grande de Tierra del Fuego. Additional study and subsequent exploitation of the artesian supply will help alleviate the shortage of water, which is handicapping further economic development of the area. The artesian system consists of two aquifers, the Los Olivos and Bellavista Members, which are separated by the Companario Member, all in the lower part of the Palomares Formation of late Tertiary age. The Tertiary units occupy a structural basin that is bounded on the south and west by the partly submerged Cordillera de los Andes. Rocks of Paleozoic and Mesozoic age crop out on the northeast flank of the Cordillera and dip toward the north and east. Tertiary rocks overlie and crop out in a band northeast of the Mesozoic rocks (fig. 1) and in the Rio Gallegos area of Argentina. The deepest part of the basin seems to coincide approximately with the Estrecho de Magallanes (Straits of Magellan) where it borders the north side of the Isla Grande de Tierra del Fuego. The description of the Palomares Formation given in the accompanying table is based on the work of Gonzalez and Cortes (1953) and applies only to the northern part of the Isla Grande and the southern part of the mainland north of the Estrecho de Magallanes. Although detailed studies of the late Tertiary sequence have not been made, the Palomares Formation is believed to be continuous throughout the Punta Arenas-Puerto Natales-Rio Gallegos area (fig. 1). Underlying the Palomares Formation is a lower Tertiary marine clay which has been identified only in wells (see table). B169 1 For the purposes of this report the Tierra del Fuego area is defined as the area shown in figure 1. U.S. GEOL. SURVEY PROF. PAPER 501-B, PAGES B169-B172B170 GROUND WATER 73° 72° 71° 70° 69° Rio Gallegos Puerto i Natales 50 KILOMETERS ARGENTINA CHILE Laguna Blanca Posesion o Punta Delgada anantiales Seno Seyring lanes Sombreo Nueva Cullen Seno Otway )PUNTA (ARENAS Porvenir Bahia Inutil ISLA/GRANDE DE t^TIERRA^DEL ■X^FUEGO Cameron Continental deposits Principally of glacial and glaciofluvial origin Basaltic and andesitic volcanic rocks CL < EXPLANATION Marine and (or) continental deposits Includes beds of coal and lignite; also includes Palomares Formation r_—-—1 I . . , 1 Marine deposits tx < i— CL LU U Marine and continental sedimentary rocks and volcanic rocks □ Granite (/) LU cn cl < CJ Volcanic rocks inter-layered with sedimentary rocks y < Metamorphic rocks Contact Glacier Not mapped Figure 1.—Geologic map of the Tierra del Fuego area. After geologic map of Chile by Institute de Investigaciones Geologicas, 1960.DOYEL AND CASTILLO U. B171 Stratigraphy of the post-Cretaceous deposits of the Tierra del Fuego area [After Gonz&lez and Cortes, 1963] System Formation Member Description Thickness (meters) Quaternary Principally poorly sorted glaciofluvial and morainal deposits filling valleys and covering flatland areas. Palomares Superior Tuff, white to yellow, fine- to coarse-grained, poorly sorted, irregularly stratified. Contains some plant stems. ±70 Primavera Sandstone and conglomerate, blue, poorly sorted, partially to well cemented; interbedded with white to yellowish-gray tuff. High content of basalt and pumice. The tuff contains some plant impressions. ±80 T ertiary Palomares Bellavista Sandstone and conglomerate, blue, poorly sorted, partially cemented, crossbedded; blue color due to staining on basalt grains. Contains pebbles and cobbles of basalt and pumice. Highly permeable; contains water under artesian pressure. ±30 Campanario Clay, gray to yellowish-gray; bentonitic in the upper part. Contains red tuffaceous clay near the base, stringers of lignite, and, in the lower part, many plant fossils. ±30 Los Olivos Sandstone, gray to grayish-blue, fine- to coarse-grained, poorly sorted, partially cemented, crossbedded; bluish color due to staining on basalt grains. Includes a high percentage of basalt grains. Highly permeable; contains water under artesian pressure. ±30 Unconformity Not identified in outcrop, but in the subsurface, marine clay underlies the Los Olivos and is underlain by a thick section of marine Tertiary sedimentary deposits. 500-1000 Cretaceous Marine sedimentary deposits. During the Pleistocene, the Tierra del Fuego area, and most of southern Chile, was subjected to glaciation. The Estrecho de Magallanes then probably was above sea level and was occupied by a tongue of glacial ice. Now, much of the lower lying part of the area is mantled with glaciofluvial and morainal deposits as much as 25 m thick. Conspicuous volcanoes distributed along an east-west line near the Chilean border with Argentina (52° south latitude) are post-Tertiary and may be of late Pleistocene or Eecent age. The outcrops of the highly permeable Los Olivos and Bella vista Members of the Palomares Formation in the north-central part of Isla Grande de Tierra del Fuego probably are the principal recharge area of the artesian aquifer system. The altitude of the land surface in the outcrop area ranges from about 100 to 110 m. Down the hydraulic gradient from the outcrop, the unnamed marine clay underlying the Los Olivos, the Campanario Member between the Los Olivos and Bellavista, and the Primavera Member overlying the Bellavista confine the water in the Los Olivos and the Bellavista Members. A piezometric map constructed by Duhart (1955) shows that wells tapping the Los Olivos and Bellavista in the northern part of the Isla Grande flow where the land-surface altitude is less than 100 m. The piezometric surfaces here slope northward. Available data are insufficient to determine the direction of the slope in the 725-328 0—64---12 area north of the Estrecho de Magallanes, but the geologic structure and stratigraphy suggest strongly that it is generally eastward. The aquifer system probably discharges along the coastline of the Atlantic Ocean and contiguous tidal-water bodies and possibly through submarine springs and by leakage upward through confining beds. The quality of the water is considered satisfactory for domestic and industrial use by the ENAP, the only user of the water in 1962. The results of chemical analyses made in the ENAP chemical laboratory show that the dissolved-solids content ranges from 300 parts per million in a well at Cullen to 901 ppm in a well in Posesion. No quantitative studies have been made, and hence the hydrologic characteristics of the artesian aquifer system are imperfectly known. In 1962, wells were producing sufficient water to supply the requirements of ENAP installations, with little or no evidence of decline in artesian head. The nature of the sedimentary rocks composing the aquifer system, the nearness of the recharge area to actual or potential points of withdrawal, the moderate rainfall well distributed throughout the year,2 and the yields of the wells indicate that the artesian aquifer system is capable of producing con- 2 The city of Punta Arenas has an average annual rainfall of 438 mm for the period 1901-56 (United Nations, 1960, p. 15).B172 GROUND WATER siderably larger quantities of water than now are being withdrawn. A marked decline in artesian head near tidal-water bodies, however, could result in the intrusion of salt water into the aquifers. The Quaternary deposits contain a shallow water-table aquifer throughout the basin area, and this aquifer is tapped by shallow wells for stock and domestic supplies. Because there are wide local variations in the horizontal and vertical permeabilities of the shallow aquifers, the possibilities for large-scale withdrawals are limited except in areas of exceptionally favorable conditions for the percolation of water both from the surface and laterally through the deposits. Water for domestic, municipal, and industrial use, and also for supplemental irrigation, can be obtained from the artesian system throughout the northern part of the Isla Grande and the area north of the Estrecho de Magallanes. Additional geologic studies and quan- titative and qualitative hydrologic studies, however, should be made before large-scale withdrawals. REFERENCES Alvarez, Jorge, 1953, Cuenca artesiana de la parte norte de Tierra del Fuego: Empresa Nacional del Petro leo de Chile open-file report. Duhart, Javier, 1955, Cuenca artesiana en la parte N.E. de Tierra del Fuego: Empresa Nacional del Petrdleo de Chile open-file report. Gonzalez, Eduardo, and Cortes, Raul, 1953, Levantamlento geoldgico en la parte noreste de Tierra del Fuego: Empresa Nacional del Petroleo de Chile open-file report. Marino, Mario, and Mordojovieh, Carlos, 1955, Posibilidades de agua subterr&nea en Flamenco y Cullen : Empresa Nacional del Petrdleo de Chile open-file report. Mordojovieh, Carlos, 1950, Cuenca artesiana en la peninsula Espora: Empresa Nacional del Petrdleo de Chile open-file report. United Nations, 1960, Los recursos Hidrfiulicos de Chile: Mexico City, Mex.GEOLOGICAL SURVEY RESEARCH 1964 A METHOD FOR EVALUATING OIL-FIELD-BRINE POLLUTION OF THE WALNUT RIVER IN KANSAS By ROBERT B. LEONARD, Topeka, Kans. Work done in cooperation with the Kansas State Department of Health Abstract.—Ratios of the concentration of major ionic constituents to the concentration of chloride in oil-field brine are used to determine the percentage of the dissolved-solids load that oil-field brine contributes to the Walnut River, Kans. Oil-field brine is a major source of dissolved solids in the Walnut River basin, Kansas (fig. 1), although marked improvement of the quality of both surface and ground water has resulted from an extensive pollution-abatement program of the Kansas State Department of Health. This article describes a method used to determine the approximate magnitude of oil-field-brine pollution from analyses of samples of river water and from published oil-field data. The method is based upon the premise that the concentration of chloride ion carried by the river can be used as a quantitative index of the degree of oil-field-brine pollution. It was developed as part of an extensive cooperative investigation of the quality of the water resources of the basin and is illustrated here by preliminary data obtained in a salinity survey made in 1962. In Kansas oil-field brines, the ratios of the concentration of calcium, magnesium, and sodium (as reported here the concentration of sodium includes concentration of potassium) to the concentration of chloride are virtually constant despite wide differences in dissolved-solids concentrations (Jeffords, 1948). Mean and weighted-mean ratios of the concentrations of selected constituents to the concentration of chloride in oil-field brine are listed in table 1. The ratios were calculated from analyses of 45 samples of brine from oil wells, separators, and brine-disposal ponds in the Walnut River basin (Schoewe, 1943; Rail and Wright, 1953). The samples represent nearly random geographic (figs. 1 and 2), stratigraphic, and compositional distribution. 97°00' Figure 1.—Map of the Walnut River basin in southern Kansas. Numbers refer to river sampling stations for which data are given on figure 2. Dots show brinesampling sites. U.S. GEOL. SURVEY PROF. PAPER 501-B, PAGES BS73-B176 B173B174 QUALITY OF WATER Table 1.—Mean and weighted-mean ratios of the concentration of selected constituents to the concentration of chloride in oil-field brine in the Walnut River basin All samples Samples with <90,000 ppm chloride Samples with >90,000 ppm chloride No. of analyses 45 29 16 Schloride (ppm) 2, 491, 778 707, 796 1, 783, 982 Mean Weighted- Mean ratio ratio mean ratio Sodium/chloride 0. 522 0. 5105 0. 5328 0. 5017 Calcium/chloride . 074 . 0769 . 0710 . 0793 Magnesium/chloride . 022 . 0229 . 0220 . 0234 Sulfate/chloride . 026 . 0115 . 0396 . 004 The concentrations of chloride in the 45 samples ranged from about 10,000 to 140,000 parts per million. As the concentration of chloride increased, the concentrations of the major constituents other than sulfate increased, the calcium/chloride and the magnesium/ chloride ratios increased slightly, and the sodium/chlo-ride ratio decreased (table 1). The sulfate/chloride ratio was less than 0.001 in many samples of concentrated brine, but it was as much as 0.14 in one sample. Because the total pollutive effect of equal volumes of brine varies almost directly with concentration of chloride, ratios weighted with respect to chloride are most applicable to this study of oil-field-brine pollution where neither the concentrations nor the exact locations of multiple sources are known. The method of computing the weighted-mean ratios (table 1) is illustrated by the computation of the weighted mean for the sodium/chloride ratio. The mean sodium/chloride ratio for each group (<90,000 ppm chloride, and >90,000 ppm chloride) was multiplied by the ratio of the sum of the chloride concentrations in that group to the sum of the chloride concentrations in both groups. The weighted-mean ratio is the sum of these products. The numerical computation is as follows: <**■ =weighted mean S0(^u™ ratio=0.5105 chloride If the calculated ratios are valid, an approximate anion-cation balance in equivalents per million should exist in a brine reconstituted by multiplying the ratios by an arbitrary concentration of chloride. The equation representing the concentrations of the major constituents of a typical oilfield brine is Na+1 + Ca+2 + Mg+2=S04-2 + Cl"1 The concentrations, in parts per million, of the various constituents, can be expressed as the products of an arbitrary chloride concentration and the appropriate ratios: Cations (ppm) Anions (ppm) Na+1=0.5105 CH S0r2=0.0115 Cl”1 Ca+2 = 0.0769 CH CH = CH Mg+2=0.0229 CH The concentrations can then be converted to equivalents per million (epm) and arranged as an equation: Cations Anions 0.0222 CH + 0.0038 CH + 0.0019 CH=0.0002 CH +0.0282 CH, which reduces to Cations Anions 0.0279 CH=0.0284 CH The percentage of error is approximately 1. Although low concentrations of bicarbonate and of other ions are commonly present in the oilfield brine, they apparently have no direct relation to the concentration of chloride. The small percentage of error substantiates the hypothesis that exclusion of these ions does not appreciably affect the accuracy of the method as applied in this area. The proportion of dissolved solids attributable to brine carried by the Walnut River during base flow can be calculated from the concentration of chloride in the river water. The amount of chloride introduced by oilfield operations, past and present, is approximately the difference between the natural and present chloride loads at a sampling station. The natural chloride load is determined from quality-of-water data obtained before 1914, the year that oil was discovered in the basin (Parker, 1911; Kansas State Board of Health, 1960), and from recent water-quality studies of tributaries draining geologically similar areas unaffected by oilfield activity. The concentrations of the other constituents derived from the brine can be determined by multiplying the concentration of chloride derived from brine by the appropriate R value shown in table 2. Table 2.—Computation of the contribution of oil-field brine to the dissolved solids content of the Walnut River at station A8, November 1, 1962 [Concentration in parts per million, except as noted; discharge of river 166 cfs] Total concen- tration Concentration attributed to oil-field brine Concentration attributed to natural sources Ri Calcium 161 2 20 141 0. 077 Magnesium. 35 2 6 29 . 023 Sodium 150 2 135 15 . 511 Bicarbonate. 332 0 332 Chloride 286 266 20 Sulfate 172 2 3 169 . 012 Dissolved solids (residue at 180°C). 1, 010 430 580 Dissolved solids (tons per day) _ _ 450 192 258 1 Weighted-mean ratio of concentration of indicated constituent to concentration of chloride, in oil-field brine; taken from last column of table 1. 2 R X 266 (concentration of chloride attributed to oil-field brine).LEONARD B175 Although calcium and magnesium are derived partly from oil-field brine, they are derived principally from the dissolution of limestone, gypsiferous shale, and gypsum of Permian age. Limestone crops out along and is present as float in all major stream courses, and gypsiferous strata are at or near the surface throughout much of the western part of the basin. Hardness (as CaC03) of water in the lower reaches of the main stem at low flow is characteristically greater than 300 PPm. Sodium is derived principally from oil-field brine, although minor amounts are naturally present. The sodium/chloride ratio of waters containing oil-field brine is normally less than 0.60. The concentration of sodium-plus-potassium in unpolluted surface water in the Walnut River basin commonly is <20 ppm, although concentrations ranging from 100 to 150 ppm are now common in the main stem. The concentration of potassium is uniformly low (5 to 6 ppm) at all sampling sites. Some sodium and potassium may be attributed to municipal sewage and to the use of fertilizers. Sulfate is derived principally from gypsum and gypsiferous shale of Permian age. Natural sulfate concentrations in some tributaries of the Walnut River normally exceed 200 ppm. Only a minor part of the total sulfate load is derived from oil-field brine and from oxidation of sulfurous materials associated with some oils. The sulfate/chloride ratio of natural water in the basin is commonly greater than one. In periods of low flow during the study, ratios were as high as 11 in tributaries draining the western part of the basin but as low as 0.03 in those draining oil fields. Chloride concentrations greater than 200 ppm are not uncommon during periods of low flow in the Walnut River. Under similar conditions, water unpolluted by brine from the eastern part of the basin commonly 70 60 50 40 DISTANCE ABOVE MOUTH, IN RIVER MILES Figure 2.—Chemical-quality profile of the Walnut River on November 1, 1962, showing the part of the dissolved-solids load derived from natural sources and the part due to pollution by oil-field brine.B176 QUALITY OF WATER contains less than 12 ppm of chloride, and water from the western part seldom contains more than 30 ppm. On the basis of concentration-discharge relations and data obtained prior to the discovery of oil, the natural chloride concentration is assumed to be 12 ppm in the part of the Walnut River upstream from Augusta (Al-A7, figs. 1 and 2) and 20 ppm in the part downstream from the confluence with the Whitewater River (A8-All). The assumed values are sufficiently accurate for illustration of the method; however, they may be changed slightly as a result of studies now in progress. Application of the method to data collected on November 1, 1962, at sampling station A8 in the water-quality study is presented in table 2; the results of similar computations for all river sampling stations are illustrated on figure 2. The utility of the method described is based on the assumption that the chemical analyses, sampling procedures, and discharge measurements adequately describe actual field conditions. Discharge measurements and chemical analyses are considered to be accurate within 5 percent, but other variables are difficult to evaluate as precisely. Slight errors in any of the variables could cause apparent inconsistencies in the results. For example, the computed loss of about 1 percent of the tonnage of total dissolved solids ascribed to brine in the reach between Douglass and Winfield (fig. 1) is well within the limits of accuracy for the method. The ratios of the constituents of brine polluting a particular reach or tributary may not conform to the computed ratios because of isolated and practically in- REFERENCES Jeffords, R. M., 1948, Graphic representation of oil-field brines in Kansas : Kansas Geol. Survey Bull. 76, pt. 1,12 p. Kansas State Board of Health, 1960, Chemical quality of surface waters in the Walnut River basin, 1906-1960: Topeka, Kans., Div. Sanitation, 57 p. determinate anomalies in the distribution and characteristics of the sources of brine. However, expected variations from the weighted mean are commonly minor. For example, the standard error of the sodium/ chloride ratio (0.5105) determined from the 45 available analyses is only 0.008. Inaccuracies in the assigned value of natural chloride concentration may affect adversely the results for sites in the basin where the natural concentration of chloride constitutes a large proportion of a low concentration of chloride. However, under these conditions such error is insignificant because the tonnage attributable to oil-field brine carried by the stream would also be low. Bicarbonate and minor constituents of the brine are disregarded in determining the magnitude of the brine component in the samples of the Walnut River water. The concentration of bicarbonate derived from brine is probably insignificant when compared with that derived from contact with calcareous rocks, the soil, and the atmosphere. Generally the concentration of the other disregarded constituents of brine is extremely low. . This study shows how analyses of water samples can be used to determine the percentage of the dissolved-solids load that oil-field brine contributes to the Walnut River, Kans. On the basis of preliminary data, oilfield brine accounted for about 40 percent of the dis-solved-solids load downstream from the confluence of the Walnut and Whitewater Rivers at the time of the survey described in this article. Parker, H. N., 1911, Quality of the water supplies of Kansas: U.S. Geol. Survey Water Supply Paper 273, 375 p. Rail, C. G., and Wright, Jack, 1953, Analyses of formation brines in Kansas: U.S. Bur. Mines Rept. Inv. 4974, 40 p. Schoewe, W. H., 1943, Kansas oil-field brines and their magnesium content, pt. 2 of Reports of studies: Kansas Geol. Survey Bull. 47, p. 37-76.GEOLOGICAL SURVEY RESEARCH COMPUTING STREAM-INDUCED GROUND-WATER FLUCTUATION By M. S. BEDINGER and J. E. REED, Little Rock, Ark. Work done in cooperation with the U.B. Army, Corps of Engineers Abstract.—Changes In ground-water level Induced by a fluctuating surface-water boundary can be analyzed by separating the surface-water stage hydrograph into a sequence of steady stages separated by instantaneous changes. Each change in ground-water level is considered to be the net effect of antecedent changes in surface-water stage weighted according to the drain function. the aquifer is proportional to and instantaneous with the corresponding change in ground-water level, the change in ground-water level induced by a change in the stage of a surface-water body from one steady stage to another is described by the following equation (Stall-man, in Ferris and others, 1962, p. 126): In places where surface water is hydraulically continuous with ground water, changes in the stage of a surface-water body commonly are the principal cause of water-level fluctuations in nearby wells. Ferris (1951), drawing from analogous expressions for heat flow, developed mathematical equations relating the amplitude of sinusoidal stage changes in a surface-water body to the amplitude of the corresponding water-level changes in the adjacent ground-water reservoir. Except for surface-water bodies affected by tidal forces, sinusoidally fluctuating bodies of water are rare. A method is presented here for analysis of ground-water fluctuations induced by either sinusoidal or irregular surface-water fluctuations. In this method the surface-water hydrograph is generalized as a sequence of instantaneous changes separating steady stages of equal duration. The effect of each unit duration of surface-water stage on the ground-water level at a specific location is analyzed separately. The changes in ground-water level are then considered to be the algebraic sum of the effects of independently acting antecedent changes in surface-water stage. The latter summation is based upon the principle of superposition which, in turn, is valid only if ground-water flow is described by linear differential equations. The procedure used is taken from the method developed by Lang-bein (1949) for the computation of soil temperatures. Consider an extensive uniform aquifer bounded by a stream. If a change in the amount of water stored in U.S. GEOL. SURVEY PROF. z where u2=x2S/4:Tt or, in U.S. Geological Survey units, u2= 1.87x2S/Tt; x is the distance from the surface-water body to the point at which the amount of head change, s, is to be determined; s0 is the abrupt change in surface-water stage at t=0; t is the time since the change in surface-water stage; and T and S are the coefficient of transmissibility and storage, respectively, of the aquifer. D(u)h replaces the quantity in brackets and represents the drain function of u for the constant-head situation. For leaky artesian aquifers, the following expression, developed by Hantush (1961, p. 79) with symbols changed to conform with Survey usage, applies instead of equation 1: s=| [V*V?W carf (u- Jrex'Jp'iTm' cerf Cxl2)s]P'ITm' )} (2) where P' and mf are the permeability and thickness respectively, of the leaky confining bed, cerf represents the complementary error function which is the same as the drain function of u for the constant-head situation [D(u)h\, and the other symbols are as defined previously. PAPER 501-B, PAGES B177-B180 B177B178 ANALYTICAL HYDROLOGY 1/u2 Figure 1.—Graph of equation 1, showing change in ground-water level in response to an instantaneous change in river level. Symbols are defined in text. The following procedures, although applied in this article only to equation 1, may be applied to equation 2. A graph for the solution of equation 1 is given in figure 1, where the ratio s/s0 is plotted as the ordinate and 1/u2 as the abscissa. Because s/s0 is a function of time, the graph illustrates the fluctuation in ground-water level in response to a permanent change in surface-water stage. To implement the method presented in this article, we must know the separate effects of a change of one time unit during subsequent units of time. Consider a point 2,500 feet from a river in an aquifer with a ratio of transmissibility to storage of 5.84 X106 gallons per day per foot. Arbitrarily choosing 1 day as the time unit we find this corresponds to l/w2=5.84X 106/ 1.87X6.25X 106=0.5. Values of 1/u2 and D(u)h, for the first 12 units of time, are listed in columns 2 and 3, respectively, of table 1, and identical values of D(u)m each offset by 1 time unit, are listed in column 4. The differences between the fourth and third columns, listed in column 5, are the coefficients of the distributive effect of a change of 1-day duration. For example, a rise in river stage of 10 feet at time 0 will effect a component of rise of 10X0.046=0.46 foot the first day, 10X0.111 = 1.11 feet the second day, 10X0.091=0.91 foot the third day, and so forth. Next, consider the changes in ground-water level at well A-4,1,700 feet from the Arkansas River in Jefferson County, Ark. The transmissibility of the aquifer at well A—4 was estimated from the lithologic log to be 108,000 gpd per foot. The coefficient of storage from pumping tests in the area averages about 0.02. The value of 1/u2 for 1 day equals 1.0. The drain function of u for the constant-head situation, D (u)j,, read at intervals of 1 day was used to determine the coefficients Table 1.—Coefficients of the distributive effect for changes of 1 unit duration [Symbols explained in text] Time, in days (1) 1 /u> (2) D(u)h (3) D(u) k offset by one time unit (4) Coefficient of distributive effect («) i. 0. 5 0. 046 0 0. 046 2 1. 0 . 157 . 046 . Ill 3 1. 5 . 248 . 157 . 091 4 2. 0 . 317 . 248 . 069 5 2. 5 . 371 . 317 . 054 6 3. 0 . 414 . 371 . 043 7 3. 5 . 449 . 414 . 035 8 4. 0 . 479 . 449 . 030 9 4. 5 . 505 . 479 . 026 10 5. 0 . 527 . 505 . 022 11 5. 5 . 547 . 527 . 020 12 6. 0 . 564 . 547 .017 of the distributive effect shown in column 5 of table 2. The daily component of rise after the twelfth day of a change in river stage is small and was neglected. The daily change in water level at the given point was therefore computed as the net effect of the preceding 12 daily changes in river stage, each weighted according to the coefficients of the distributive effect. Figure 2 shows hydrographs of the stage of the Arkansas River at Pine Bluff, Ark., and of the measured water-level fluctuation in well A-4, based on daily readings of continuous recorder charts at 7 a.m. Using the coefficients of distributive effects for well A-4, shown in table 2, and daily changes in river stage at Pine Bluff, daily water-level changes were computed for the location of well A-4. The computed daily changes, shown as circles in figure 2, agree closely with the measured fluctuations of the water level in well A-4. The differences probably represent variations in accretion to the aquifer and in hydraulic diffusivity.RIVER STAGE, IN FEET DEPTH TO GROUND WATER, IN FEET BELOW LAND SURFACE BEDINGER AND REED B179 Figure 2.—Hydrographs of (1) the stage of the Arkansas River at Pine Bluff, Ark. (below), and (2) measured water-level fluctuations in well A-4 (solid line) and computed stream-induced water-level fluctuations (circles) at the location of well A-4 (above).B180 ANALYTICAL HYDROLOGY Table 2.—Coefficients of the distributive effect at the location of well A-4 [Symbols explained in text] Time, in days (1) l/u* (2) D(«)» (3) D(u) A offset by 1 time unit (4) Coefficient of distributive effect (5) i 1 0. 157 0 0. 157 2 2 . 317 . 157 . 160 3 3 . 414 . 317 . 097 4 4 . 479 . 414 . 065 5 5 . 527 . 479 . 048 6 6 . 564 . 527 . 037 7 7 . 593 . 564 . 029 8 8 . 617 . 593 . 024 9 9 . 637 . 617 . 020 10 10 . 655 . 637 . 018 11 11 . 670 . 655 . 015 12 12 . 683 . 670 . 013 The example demonstrated in figure 2 required the use of 12 enumerations for each daily change in water level. For points farther from the river or with a smaller coefficient of hydraulic diffusivity, river-induced fluctuations will be smaller in amplitude and will occur with greater time lag. At such points the coefficient of daily distributive effect will be smaller and the water-level changes will be significantly affected by a longer period of antecedent river stages. Where the daily distributive effect is small, the number of computations can be reduced by generalizing the surface-water hydrograph as averages of segments of several days’ duration. As a guide to generalizing the surface- water hydrograph, it has been found that satisfactory results can be obtained if the effects of each change in surface-water stage are distributed over 12 to 15 successive time units whose coefficients total 0.65 to 0.70. The method presented here, because it can be done manually, is of advantage where construction of an analog or programming for a digital computer is not practical. Although the computations are tedious, the method is not unduly time consuming if the surface-water hydrograph has been conveniently generalized. This method permits the estimation of the T/S ratio for aquifers where water-level fluctuations are caused mostly by changes in river stage. Also, if the hydraulic coefficients of an aquifer are already known, it can be an aid in the analysis of complex hydrographs where changes in river stage are one of several factors causing water-level fluctuations. REFERENCES Ferris, J. G., 1951, Cyclic fluctuations of water level as a basis for determining aquifer transmissibility: Internat. Union Geodesy and Geophysics, Assoc. Sci. Hydrology Assembly, Brussels, 1951, v. 2, p. 148-155. Ferris, J. G., Knowles, D. B., Brown, R. H., and Stallman, R. W., 1962, Theory of aquifer tests: U.S. Geol. Survey Water-Supply Paper 1536-E, 174 p. Hantush, M. S., 1961, Discussion of “Intercepting drainage wells in artesian aquifer,” by D. F. Peterson: Am. Soc. Civil Engineers, Jour. Irrigation and Drainage Div., v. 87, no. IR4, pt. 1, p. 79-81. Langbein, W. B., 1949, Computing soil temperatures: Am. Geo-phys. Union Trans., v. 30, no. 4, p. 543-547.GEOLOGICAL SURVEY RESEARCH 1964 USE OF WATER-LEVEL RECESSION CURVES TO DETERMINE THE HYDRAULIC PROPERTIES OF GLACIAL OUTWASH IN PORTAGE COUNTY, WISCONSIN By EDWIN P. WEEKS, Madison, Wis. Work done in cooperation with the Wisconsin Geological and Natural History Survey Abstract.—Mathematical solutions derived for hypothetical “ideal” aquifers were used in determining, from data on water-level recessions following cessation of recharge, values of T/S for water-bearing glacial outwash. The results agree fairly closely with those obtained from a pumping test. Values for the hydraulic properties of aquifers, including the coefficients of transmissibility (T) and storage (S), are needed to determine the availability of ground water and to predict changes in the hydrologic system caused by water-resource development. One method of determining these properties for shallow unconfined aquifers entails an analysis of water-level recessions following a period of recharge. This method of analysis yields a value for T/S, from which T can be computed if S is known, or S can be computed if T is known. The analysis of water-level recession curves is made possible by idealizing the aquifer configuration and recharge conditions to the extent that water-level recessions may be analyzed mathematically. For the analyses, it is assumed that the aquifer is homogeneous and isotropic and that the aquifer approximates a simple geometric shape, such as an infinite strip, a rectangle, or a wedge, that is bounded by streams or by streams and impermeable rocks. Recharge to the aquifer is assumed to be distributed uniformly throughout the area and to occur either instantaneously or at an equilibrium rate (recharge equal to discharge) that ceases instantaneously. Despite the apparent restrictiveness of these assumptions, many aquifer configurations and recharge conditions may be idealized to fit the assumed conditions to the necessary degree of accuracy. This article describes the analysis of water-level recession curves to determine the ratio T/S of glacial outwash in the drainage basins of the Plover and Little Plover Rivers, in Portage County, central Wisconsin. The idealized aquifer configurations and recharge conditions assumed for the determinations include those for an infinite-strip aquifer recharged by an instantaneous slug, an infinite-strip aquifer recharged at an equilibrium rate ending instantaneously, and a wedge-shaped aquifer recharged by an instantaneous slug (% !)• Water-level recessions in five wells were analyzed. The recessions followed water-level rises resulting from recharge by infiltrating snowmelt and spring rains in 1960 and 1961. The large volume of spring recharge in 1960 could be idealized as an instantaneous slug because it occurred over a relatively short time and was followed by a relatively long period of little recharge. Because in 1961 the water level rose more slowly than in 1960 and remained at a fairly constant high level for some time before receding, recharge for some time immediately prior to the water-level recession was idealized as occurring at a constant rate in equilibrium with discharge and then ceasing instantaneously. The water-bearing glacial outwash south of the Little Plover River was idealized as an infinite-strip aquifer, whereas that between the Little Plover and the Plover Rivers was idealized as a wedge-shaped aquifer. The hydraulic boundaries of the infinite-strip aquifer are the Little Plover River on the north and the marshlands that parallel the Little Plover about 4 miles to the south. Those of the wedge-shaped aquifer are the Little Plover River on one limb, the Plover and a short stretch of the Wisconsin River on the other limb, and U.S. GEOL. SURVEY PROF. PAPER 501-B, PAGES B181-B184 B181WISCONSIN B182 analytical HYDROLOGY R. 9 E. EXPLANATION Pt-361 o Observation well Pt-279 © Irrigation well Bedrock contour Shows subsurface configuration of sandstone ridge; contour interval 20 feet X Sandstone outcrop Irrigation well sanusiuuv---- nouRE 1.—Map showing location of streams and observation wells and the limits of the assumed ideal aquifers used in the recession-curve analyses.WEEKS B183 an arbitrary arc of constant head assumed to be at a radius of 33,000 feet from the junction of the Little Plover and Wisconsin Rivers. The following equation, derived by Brown (1963, p. C89), expresses the relation of (1) decline in head (water-level recession) at a given point in an infinitely long strip aquifer which has been recharged instantaneously to (2) the factors of time since recharge occurred, aquifer width, and the hydraulic properties of the aquifer: h K 4 ^ 1 — 2-1 ~ exp 7T n-1, 3, 5,... n Tt \ . nirx 4a2s) Sm W’ where h0 = change in head due to recharge, h = residual change in head remaining at time t, T = coefficient of transmissibility, t =time since recharge occurred, 2a = distance between streams, S = coefficient of storage, and x = distance from observation well to stream. In analyzing the water-level recession that occurred in wells Pt-366 and Pt^376 (fig. 1) during the summer of 1960, type curves were prepared by plotting values of h/h0 versus log™ Tt/4a2S, the values of h/h0 being obtained by substituting assumed values for Tt/4a2S in the above equation. Type curves for the same infinite-strip aquifer under the condition of recharge at an instantaneously ending equilibrium rate were prepared by plotting values Tt of h/ho versus log10 , the values of h/h0 being obtained by means of the equation (Jacob, 1943, p. 566) A. hg £ 7i=l, 3, 5, 1 (n2i^Tt\ . utx .^exp-(wjsin- 2 a ^2, 1 . nirx 2J -j sm n=i,37s,...n3 2 a These curves were used in analyzing the water-level recessions occurring during the summer of 1961 in wells Pt-366 and Pt-376. The type curves prepared by Papadopulos (1963) from an integral equation derived by Jaeger (1942, p. 532) were used in analyzing the water-level recessions in wells Pt-357, Pt-361, and Pt-374. These wells are located in the wedge-shaped aquifer between the Little Plover and Plover Rivers (fig. 1). The water-level data from each well in the study area were prepared for analysis by plotting values of h/h0 versus log10£. As indicated in the hydrograph for well Pt-366 (fig. 2) the increase in head due to recharge is equal to the actual rise in water level plus the water-level decline that would have occurred in the absence of recharge. The water-level trend without recharge was found by preparing a semilog plot of the antecedent water-level recession and extrapolating the straight line best fitting those data. Values of h0 and of h for various times were obtained by subtracting the extrapolated water level from the observed water level. The data plots for wells Pt-366, Pt-376, and Pt-361 matched the type curves almost perfectly. The values for T/S obtained by analyzing the water-level recessions in these wells are given in the accompanying table. As the data plots for wells Pt-374 and Pt-357 did not match the type curves, reliable values for T/S could not be computed from them. It is likely that the buried ridge of sandstone that extends from sec. 2 to sec. 14, T. 23 N., R. 8 E., is so much less permeable than the glacial outwash that it affects water movement in the aquifer and, therefore, the shape of the water-level recession curves in these wells. Values of T/S determined from analysis of water-level recession Well No. Ideal aquifer configuration T/S (ft* per day) Transmissibility T (gpd per ft if S=0.2) Pt-366... (Infinite strip, instantaneous recharge 1. 8X 10s 270, 000 | Infinite strip, equilib-[ rium recharge 1. 7X 105 250, 000 P+ 37 A (Infinite strip, instantaneous recharge 1. 4X105 210, 000 | Infinite strip, equilib-( rium recharge.. 1. 3X105 200, 000 Pt-361... Wedge, instantaneous recharge 2. OX 105 300, 000 The values of T/S were multipled by 0.2, the storage coefficient determined from specific-yield data, to obtain values for aquifer transmissibility in units of square feet per day and by 7.5 to change the units to gallons per day per foot. The values of transmissibility are somewhat greater than the transmissibility of 140,-000 gpd per ft determined by a 3-day aquifer test made at well Pt-279, probably because of local differences in aquifer thickness. The thickness ranges from 0 at the sandstone outcrops to about 100 feet in the vicinity of wells Pt-376 and Pt-361 and is about 80 feet in the vicinity of well Pt-279. Differences in aquifer thickness probably also account for the range in transmissibility values determined for the several well sites. Transmissibility values determined from water-level recessions during 1960 in wells Pt-366 and Pt-376 agree quite closely with those from water-level recessions during 1961 in the same wells. Values for hydraulic properties obtained by the recession-curve method of analysis are those characterizing an areally extensive homogeneous and isotropic aquifer in which the water-level recession would matchB184 ANALYTICAL HYDROLOGY Figure 2.—Hydrograph of well Pt-366, showing the water-level recessions in the summers of 1960 and 1961 and the extrapolated water-level trends used to determine the head due to recharge. Datum is mean sea level. that observed in the real aquifer. Because of this, local variations in transmissibility are masked and the results may be somewhat different from those of a pumping test at a given site in the aquifer. Values for the hydraulic coefficients determined by recession-curve analysis are more useful than pumping-test results in predicting areal effects of water-resource development, whereas pumping-test results are more useful in predicting local effects of pumping in the vicinity of the test site. The methods described in this report could be used to determine the hydraulic properties of aquifers in many other areas. Much water-level information for aquifers throughout the county has been collected during basic-data programs and areal-reconnaissance studies, and many of these aquifers are bounded by streams or impermeable rocks in such a way that they can be idealized as wedges, infinite strips, or rectangles. Water-level recessions following recharge from snowmelt, torrential rains, or irrigation could be analyzed to determine the hydraulic properties of these aquifers. REFERENCES Brown, R. H., 1963, Ground-water movement in a rectangular aquifer bounded by four canals, in Bentall, Ray, compiler, Shortcuts and special problems in aquifer tests: U.S. Geol. Survey Water-Supply Paper 1545-C, p. C86-C100. Jacob, C. E., 1943, Correlation of ground-water levels and precipitation on Long Island, New York; pt. 1, Theory: Am, Geophys. Union Trans., p. 564—573 [1944], Jaeger, J. C., 1942, Heat conduction in a wedge, or an infinite cylinder whose cross-section is a circle or a sector of a circle: Philos. Mag. and Jour. Sci., v. 33, no. 222, p. 527-536, Papadopulos, I. S., 1963, Preparation of type curves for calculating T/8 of a wedge-shaped aquifer: Art. 54 in U.S. Geol. Survey Prof. Paper 475-B, p. B196-B198.GEOLOGICAL SURVEY RESEARCH 1964 TREE GROWTH PROVES NONSENSITIVE INDICATOR OF PRECIPITATION IN CENTRAL NEW YORK By WILLIAM J. SCHNEIDER and WILLIAM J. CONOVER, Washington, D.C. Abstract.-—Correlation of tree-ring widths, as measured on increment cores taken from coniferous trees, with precipitation demonstrates that although the two variables are not completely independent, measurements of ring width are of little value in determining past precipitation in the humid continental climate of central New York. Previous studies (Fritts, 1962) have shown that in some areas, the rate of growth of trees can be related to hydrologic phenomena, particularly annual precipitation. A recent study by Schneider and Ayer (1962) has shown that a change in land use from abandoned farmland to coniferous woodland in 1933 reduced streamflow by 23 percent in the Shackham Brook watershed near Cortland, in central New York. Accordingly, an attempt was made to relate the rate of growth of trees in the Shackham Brook area to precipitation in order to understand more fully the interrelation between tree growth and hydrology. More than 100 trees were systematically selected for sampling. Because the reforestation in 1933 was done by planting blocks of one or two species, sampling was also done by blocks and species. In each block, a group of five trees of a single species were selected arbitrarily. Twenty-three groups studied consisted of 7 groups of Norway spruce (Picea abies), 6 groups of European larch (Larix decidua), 6 groups of red pine (Pinus resinosa), and 4 groups of Scotch pine (Pinus syl-vestris). Tree-ring widths, a measure of the annual growth of the tree, were measured on increment cores taken from each tree. Ring widths were compared with the amount of precipitation recorded for the period of ring growth. The precipitation data used are an average of precipitation recorded at two sites in the 3.12-square-mile watershed. A May 1 to October 31 semiannual period, corresponding to the growing season, and a May 1 to April 30 annual period were used in this study. Although reforestation was done in 1933, only data from 1940 on were used, thereby eliminating the early years of tree growth when ring widths tend to be disproportionately large. Only increase or decrease in ring size as compared to that of the preceding year was related to the increase or decrease in precipitation as compared to that of the previous year. In this manner, the test was kept as general as possible. The sequential probability-ratio test of Wald (1947) was used with the following hypotheses: H0: An increase (or decrease) in ring width corresponds to an increase (or decrease) in the total amount of precipitation for the period of ring growth (12 months ending April 30) with a probability p^0.7. IIx: The probability p of a correspondence is <0.7. The type-I error, that is, the probability of accepting H0 when Hx is true, was selected as 5 percent. The type-II error, that is, the probability of accepting Hx when H0 is true, was also selected as 5 percent. The zone of indifference—the values of p for which either H0 or Hx may be selected—is the interval from 0.65 to 0.75. In other words, if p, as defined by /Z0, is between 0.65 and 0.75, we regard it as sufficiently close to 0.7 so that it does not matter which hypothesis we accept. To use Wald’s test graphically, the number of trials (v) is plotted as the abscissa, and the number of “successes” (dv) as the ordinate. A “success” is defined as a comparison of ring size with precipitation in which both showed an increase over the previous year or half year, or in which both showed a decrease. A comparison in which one increases while the other decreases is a “failure.” If either variable does not change in successive values, thattrial is not counted. The boundary lines, based on the selections of type-I error, type-II error, and zone of indifference, are as follows: dv= 6.17+0.706 v dv= -6.17+0.706 v U.S. GEOL. SURVEY PROF. PAPER 501-B, PAGES B185-B187 B185B186 ANALYTICAL HYDROLOGY 8 16 24 32 40 48 56 64 72 NUMBER OF TRIALS, V Figure 1.—Sequential analysis of relation between tree-ring growth and precipitation for May 1-April 30 periods. The hypothesis H0 is accepted when the graph crosses the upper boundary. When the graph crosses the lower boundary, the hypothesis H1 is accepted. The experiment is continued until the graph crosses one of the boundaries. The sequential order of the data for plotting was determined as follows: For each tree, the data were used chronologically. For each species, the order of the trees was selected by random process. The results of the study for the yearly period May 1 to April 30 are shown in figure 1. The graphs for all four species cross the lower boundary and we therefore accept the hypothesis Hx. Results for the study for the growing season of May 1 to October 31 are shown in figure 2. Again, the hypothesis //, is accepted. This process was repeated four times for each of the study periods. In all cases, for each species and each period, the hypothesis Hx was accepted. Both figures 1 and 2 show that an increase (or de- crease) in the amount of tree growth for the study periods will correspond to an increase (or decrease) in precipitation <70 percent of the time. If the rate of tree growth and amounts of precipitation were completely independent, the probability of correspondence would be 50 percent. The results, therefore, do not indicate complete independence of the variables. On the other hand, the results do not justify the use of tree-ring widths as sensitive hydrologic indicators in the humid continental climate of central New York. REFERENCES Fritts, H. C., 1962, An approach to dendroclimatology; screening by means of multiple regression techniques: Jour. Geophys. Research, v. 67, no. 4, p. 1413-1420. Schneider, W. J., and Ayer, G. R., 1962, Effect of reforestation on streamflow in central New York: U.S. Geol. Survey Water-Supply Paper 1602, 61 p. Wald, Abraham, 1947, Sequential analysis: New York, John Wiley and Sons.NUMBER OF SUCCESSES, dv NUMBER OF SUCCESSES, dv SCHNEIDER AND CONOVER B187 NUMBER OF TRIALS, V Figure 2.—Sequential analysis of relation between tree-ring growth and precipitation for May 1-October 31 growing seasons. 5* 725-328 0—64- ■13SUBJECT INDEX [For major subject headings such as "Economic geology," “Geophysics," “Sedimentation,” see under State names or refer to table of contents] A E Page Acoustical methods, use in study of explosion effects on rock salt.............. B108 Alluvial fans, glacial, Missouri............... 130 Amaranth dye, use in staining feldspar....... 152 Anomalies, geochemical, Nevada.................. 92 Apatite, rare-earth silicatian, New York..... 64 Aquifers, artesian, southern Chile............. 169 effect of streams on....................... 177 Arkansas, ground water, east-central part.... 177 Ash-flow sheet, Nevada, petrology............... 74 B Barometric pressure, effect on lake levels.... 158 Bed form, of stream channels, variables affecting............................ 140 Beryllium, distribution in igneous rocks...... 100 potential area for exploration in Utah.... 13 Big Stone Gap Member, Chattanooga Shale, Virginia, definition.................. 43 Brine, oil-field, pollutant of surface water.. 173 c Page Ervay Member, Goose Egg Formation, Wyoming, stratigraphy.. ....... B58 F F.D., and C. Red No. 2 dye, use in staining feldspar........................... 152 Facies relations, sedimentary rocks, Ken- tucky-Tennessee-Virginia............ 25 Faulting, complex, eastern Nevada............... 20 low angle, west-central Utah................ 13 thrust, eastern Tennessee................ 112 Feldspar, new staining technique............... 152 Floods, effect on lake levels.................. 158 mapping, California........................ 163 Florida, clay deposits, northern part.......... 116 Foraminifera, in Marshalltown Formation, New Jersey.......................... 61 Forelle Limestone Member, Goose Egg Formation, Wyoming, stratigraphy.. 58 Fractionation, of uranium isotopes.............. 84 Freezeout Shale Member, Goose Egg Formation, Wyoming, stratigraphy.................. 59 Inundation mapping, California............... B163 K Kansas, quality of water, south-central part.. 173 Karst topography, Puerto Rico, new term for solution feature.................. 126 Kentucky, stratigraphy, southeastern part... 25,30 structural geology, Bluegrass region........ 9 L Lake levels, effect of wind, air pressure, and floods on.......................... 158 Landslides, retrogressive, Puerto Rico....... 123 Lee Formation, Kentucky-Virginia, stratigraphy. ......................................... 30 Lithium, determination in tektites............. 148 Little Medicine Member, Goose Egg Formation, Wyoming, stratigraphy.................. 59 Little Stone Gap Member, Hinton Formation, Virginia, definition................ 39 M Calderas, Nevada, structural geology............ 16 California, floods, San Diego County........... 163 geochemistry, southern California batho- lith................................ 88 Cambrian, Tennessee, structural geology...... 112 Utah, structural geology.................... 13 Cesium, determination in tektites.............. 148 ion-exchange behavior with glauconite____ 95 Chadwell Member, Lee Formation, Ken- tucky-Virginia, definition.......... 34 Chattanooga Shale, Virginia, stratigraphy____ 43 Chile, ground water, Tierra del Fuego area... 169 Clay deposits, Georgia-Florida, structural control............................ 116 Colorado, petrology, Walsenburg area............ 69 Conasauga Shale or Group, Kentucky-Ten- nessee-Virginia, stratigraphy.... 25 Cretaceous, New Jersey, paleontology............ 61 Cryptoexplosive structure, Kentucky.............. 9 o Dark Ridge Member, Lee Formation, Ken- tucky-Virginia, definition.......... 34 Devonian, Virginia, stratigraphy............ 43,49 Difficulty Shale Member, Goose Egg Formation, Wyoming, stratigraphy_________________ 58 Dikes, composite, south-central Colorado.... 69 welded-tuff, southern Nevada................ 79 Discharge, stream, relation to drainage area.. 165 Domes, Nevada, structural geology............... 16 “Down-structure” method of tectonic analysis, use in Texas............................... 1 Drift, glacial, method of estimating lithology. 143 G Georgia, clay deposits, southwestern part.. 116 structural geology, southwestern part.. 116 Glacial deposits. See Alluvial fans, Drift, Outwash, Till. Glauconite, use as scavaging agent for nuclear wastes............................ 95 Glendo Shale Member, Goose Egg Formation, Wyoming, stratigraphy............. 57 Gnome project, New Mexico, effect of nuclear explosion on rock salt........... 108 Goose Egg Formation, Wyoming, stratigraphy....................................... 53 Green River Formation, Wyoming, mineralogy....................................... 66 Ground-water fluctuation, stream-induced, computation...................... 177 H Hafnium, content in zircon, southern Cali- fornia batholith.................. 88 determination in zircon, spectrometric method........................... 146 Hawaii, geophysics, islands of Hawaii, Maui, and Oahu......................... 105 Heavy-liquid mineral separations, new technique....................................... 154 Hensley Member, Lee Formation, Kentucky- Virginia, definition.............. 36 Hinton Formation, Virginia, stratigraphy___ 39 Middlesboro Member, Lee Formation, Ken- tucky-Virginia, definition......... 35 Mineral separations, new heavy-liquid technique......................................... 164 Minnekhata Limestone Member, Goose Egg Formation, Wyoming, stratigraphy............................................ 55 Miocene, Florida, economic geology........... 116 Georgia, economic geology----------------- 116 Puerto Rico, geomorphology................ 123 Utah, structural geology.................. 13 Mississippian, Virginia, stratigraphy________39. 43 Missouri, glacial geology, Mississippi River valley......................... 130 N Nevada, geochemistry, Cortez area.............. 92 petrology, Nevada Test Site..............74,79 structural geology, Ely area............... 20 Nevada Test Site....................... 16 Nevada Test Site, geological studies.....16,74.79 New Jersey, paleontology, southwestern part. 61 New Mexico, lake-level study, Elephant Butte Reservoir......................... 158 New York, glacial geology, Adirondack Mountains......................................... 143 mineralogy, Adirondack Mountains........... 64 relation of tree growth to precipitation- 185 Northupite, ferroan variety, description----- 66 Nuclear explosions, cause of sonic T-phases... 105 effect on rock salt....................... 108 Nuclear wastes, use of glauconite as scavenging agent.............................. 95 B189B190 SUBJECT INDEX o Page 011-fleld brine, cause of surface-water pollution. B173 Ollgocene, Puerto Rico, geomorphology..... 123,126 Opeche Shale Member, Goose Egg Formation, Wyoming, stratigraphy............. 65 Ordovician, Kentucky, structural geology--- 9 Tennessee, structural geology............ 112 Outwash, method of estimating lithology.... 143 method of determining hydraulic properties.................................. 181 occurrence as alluvial fan, Missouri... 130 p Paleozoic, Nevada, structural geology......... 20 Texas, structural geology.................. 1 See also Cambrian, Ordovician, Devonian, Mississippian, Pennsylvanian, Permian. Pennsylvanian, Kentucky-Virginia, stratig- raphy................................ 30 Permian, Wyoming, stratigraphy................... 63 Piapi Canyon Formation, Nevada, petrology.. 74 Pinnacle Overlook Member, Lee Formation, Kentucky-Virginia, definition____ 33 Plagioclase, new staining technique............. 162 Pleistocene, Missouri, glacial geology.......... 130 Washington, glacial geology................ 135 Pliocene, Utah, structural geology............... 13 Pollution, surface water, by oil-field brine_ 173 Precipitation, effect on tree growth............ 186 Profiles, river, study of concavity............. 119 Puerto Rico, geomorphology, northern part. 123,126 R Radioactive disequilibrium, of uranium in sandstone.......................... 84 Random-walk models, use in study of river profiles.......................... 119 Rare-earth oxides, unusual abundance in apatite............................ 64 Recession curves, water level, use in determining hydraulic properties of glacial outwash........................... 181 Red beds, Wyoming, stratigraphy................ 53 Page Rivers, with uniform discharge, study of profiles......................... B119 Rome Formation, Kentucky-Tennessee-Vir- ginia, stratigraphy.................. 25 Rubidium, determination in tektites............. 148 s Salt, rock, effect of nuclear explosions on.. 108 Seiches, effect on lake levels.................. 158 Seismic recording, of artificially produced T- phases.............................. 105 Separations, silt-size minerals,.new technique. 154 Setup, effect on lake levels.................... 158 Silica, relation to beryllium in igneous rocks.. 100 Spectrographic methods, use for Cs, Rb, and Li determination in tektites..... 148 Spectrometric methods, use in analysis of zircon............................................ 146 Staining techniques, new, for feldspar.......... 152 Streamflow, effects of temperature and channel width on............................ 140 relation to drainage area.................. 165 Streams, effect on ground-water fluctuation... 177 Strontium, ion-exchange behavior with glauconite.......................................... 95 T T-phases, seismic recordings, Hawaii............ 105 Tectonic analysis, “down-structure" method. 1 Tektites, determination of Cs, Rb, and Li content............................. 148 Tennessee, stratigraphy, northeastern part... 25 structural geology, eastern part........... 112 Tertiary, Chile, ground water................... 169 Colorado, petrology......................... 69 Nevada, structural geology.............. 16,20 See also Ollgocene, Miocene, Pliocene. Texas, sedimentation, Rio Grande................ 140 structural geology, western part............. 1 Till, glacial, method of estimating lithology... 143 glacial, occurrence in Washington.......... 135 Tree growth, relation to precipitation.......... 185 Triassic, Wyoming, stratigraphy.................. 53 Tuff, welded, dike-forming material.............. 79 u Page Uranium, isotope study, in granite and sand- stone.............................. B84 Uranyl tricarbonate, new form................... 82 Utah, economic geology, Juab County.......... 13 structural geology, Juab County............. 13 v Velocity studies, longitudinal and shear waves, in rock salt______________ 108 Virginia, stratigraphy, southwestern part. 25, 30,39,43,49 surface water, Rappahannock River basin. 165 Volcanism, Timber Mountain caldera, Nevada............................ 16 w Washington, glacial geology, Olympic Peninsula......................................... 135 Water-level recession curves, use in determining hydraulic properties of outwash........................ 181 Wildcat Valley Sandstone, Virginia, definition.......................................... 49 Wind, effect on lake levels.................. 158 Wind River Formation, Wyoming, geochemistry......................................... 84 Wisconsin, ground water, central part...... 181 Wyoming, geochemistry, Wind River basin.. 84 mineralogy, southwestern part............. 66 stratigraphy, southeastern part........... 53 x y z Yucca Mountain Member, Piapi Canyon Formation, Nevada, definition... 74 Zanjon, term for solution feature, definition... 126 Zircon, hafnium content, southern California batholith...................... 88 hafnium content, spectrometric determination............................. 146 Zirconium, determination of ratios in zircon.. 146 relation to hafnium in zircon.......... 88 %AUTHOR INDEX A Page Annell, Charles........................... B148 B Bedlnger, M. S...............—.........— 177 Bemold, Stanley.......................... 100 Black, D. F. B............................... 9 Bumgarner, J. G.........................— 112 c Carr, W. J.................................. 16 Castillo XT., Octavio.................... 169 Christiansen, E. L......_................. 74 Conover, W. J______________________________ 186 Crandell, D. R............................. 136 D Denny, C. S................................ 143 Dickey, D. D............................... 108 Doyel, W. W................................ 169 Drewes, Harald.............................. 20 E Page Houston, P. K............................ B122 Huddle, J. W................................ 43 I Ingram, Blanche............................ 64 j Janes, W. W_________________________________ 92 Johnson, R. B............................... 69 K King, P. B.................................. 1 Krlvoy, H. L.............................. 105 L Langbeln, W. B............................ 119 Lank, E. V................................. 152 Lee, D. E................................. 154 Leonard, E. B.......................... 173 Lindberg, M. L..........-................ 64 Lipman, P. W.............................74,79 M Englund, K. J............................... 30 Eppley, R. A............................... 105 Erickson, R. L.............................. 92 F Fahnestock, R. K........................... 140 G Garner, E. L............................ 84 Gottfried, David............................ 88 H Harris, L. D.............................. 4,25 Haynes, G. L., Jr........................ 158 Maddock, Thomas, Jr......—.............. 140 Marranzino, A. P_.............-......... 92 Masursky, Harold....................... 92 Maughan, E. K........................ 53 May, Irving............................. 95 Mello, J. F............................... 61 Meyrowitz, Robert.......................66,82 Miller, R. L........................ 39,43,49 Milton, Charles_______________________ 66 Minard, J. P.............................. 61 Monroe, W. H.........................- 123,126 N Naeser, C. R.............................. 95 Norman, M. B............................. 162 o Page Oda, TJteana.............................. B92 Owens, J. P.._____________________________ 61 P Postel, A. W............................... 143 R Ray, H. A................................... 163 Ray, L. L................................... 130 Reed, J. E.................................. 177 Ricketts, J. E.............................. 112 Riggs, H. C................-.............. 165 Roen, J. B................................ 43,49 Rosholt, J. N.............................. 84 Ross, D. R................................. 82 Ross, Malcolm.............................. 82 s Schneider, W. J............................... 185 Schnepfe, M. M................................. 95 Schoen, Robert______________________________ 154 Sever, C. W................................... 116 Shawe, D. R................................ 13,100 Shields, W. R.................................. 84 Stevens, R. E............................... 162 w Waring, C. L........................ 88,146 Wedow, Helmuth, Jr...................... 112 Weeks, E. P............................. 181 x y z Young, L. E. 163 B191 A UA. GOVERNMENT PRINTING OFFICE; 1964 O—725-328