Water-Supply and Irrigation Paper No* 167 G B 102>5 UsRs benes I Q^ Underground Waters, 63 ■sM DEPARTMEiMi Ub THE INTEKiOR ITED STATES GEOLOGICAL SURVEY CHARLES D. WALCOTT, Director UNDERGROUND WATER IN THE VALLEYS OF UTAH LAKE AND JORDAN RIYER, OTAH BY G. B. RICHARDSON WASHINGTON GOVERNMENT PRINTING OFFICE 1906 Pass G[l ^l02.S Book U ^1^5 f f Water-Supply and Irrigation Paper No. 157 S«ri«<; i ^' Descriptive Geology, 86 ^®^^®^ \ 0, Underground Waters, 53 DEPARTMENT OF THE INTERIOR UNITED STATES GEOLOGICAL SURVEY CHARLES I). WALCOTT, Director y^y- UNDERGROUND WATER IN THE VALLEYS OF UTAH LAKE AND JORDAN RIVER, UTAH BY G. B. RICHARDSON WASHINGTON GOVERNMENT P R I N T I N (i C) F I<' I C E 19 06 VjX CONTENTS Page. Introduction 5 Topography and drainage 5 Geology 7 Literature 7 Descriptive geology of the highlands 8 Late geologic history 11 Tertiary 11 Quaternary 11 Climate 13 Precipitation 14 Temperature 15 Wind velocity 16 Humidity 16 Evaporation 17 Summary 17 Hydrography : 18 Streams tributary to Utah Lake and Jordan River 18 Utah Lake 23 Jordan River 24 Great Salt Lake 25 Underground water 27 General conditions 27 Source 27 Distribution 29 Quality 30 Recovery 35 Suggestions 38 Occurrence 38 West of Jordan River 38 Divisions of area 38 Upland area 39 Lowland area 41 East of Jordan River 43 Salt Lake City 43 South of Salt Lake City i 45 Utah Lake Valley 48 Lehi and vicinity 48 American Fork, Pleasant Grove, and vicinity 49 Provo and vicinity 51 Springville and vicinity 52 Spanish Fork, Payson, and vicinity 53 Goshen Valley ■'yn West of Utah Lake 56 3 4 CONTENTS AND ILLUSTRATIONS. Underground water — Continued. Page. Well data 56 Method of measurement 56 List of typical wells 59 Index 77 ILLUSTRATIONS. [Yate I. Wasatch Mountains from Liberty Park, Salt Lake City 5 IL Map of the valleys of Utah Lake and Jordan River, showing drainage area 6 III; A, Northern end of Utah Lake; B, Head-gate of Jordan and Salt Lake City canal 12 IV. A, Gate at head of Jordan River; B, Dead Man's Falls, Cottonwood Canyon. 24 V.'- Well sections 28 VI. Sketch map showing depth to ground water in the valleys of Utah Lake and Jordan River 30 VII.' Map showing the area in which flowing wells are obtained in Jordan River Valley 38 VIIL= Map showing the area in which flowing wells are obtained in Utah Lake Valley. 48 IX. A, Valley of Provo River below mouth of canyon; B, American Fork at mouth of canyon. 50 Fig. 1. Diagram showing variation of annual precipitation at Salt Lake City 17 2. Diagram showing mean monthly precipitation at Salt Lake City 18 3. Diagram showing fluctuation of the surface of Utah Lake, 1889-1904 23 4. Diagram showing fluctuation of the surface of Great Salt Lake, 1873-1903. . . 26 5. Diagram illustrating flow from vertical and horizontal pipes ^ 57 I- .E Z CD 3 -^ O -1 X o UNDERGROUND WATER IN THE VALLEYS OF UTAH LAKE AND JORDAN RIVER, UTAH. By G. B. Ric;hardson. INTRODUCTION. The valleys of Utah Lake and Jordan River are situated in north-central Utah, in the extreme eastern part of the Great Basin. The lofty Wasatch Range (PI. I), the western- most of the Rocky Mountain system, limits the valleys on the east, and relatively low- basin ranges — the Oquirrh, Lake, and East Tintic mountains — determine them on the west. The valleys trend north and south, and are almost separated by the low east- west Traverse Range, the slopes of which constitute a dam for Utah Lake, which drains through Jordan River to Great Salt Lake. The area under consideration is the most populous and flourishing part of the State. Salt Lake City and Provo, the first and tliird cities in the State, and many other thriving settlements are there located. At Bingham Junction and Murray a number of smelters treat the ores from near-by mines, but agriculture is the main industry. Water for irriga- tion is supplied by mountain streams, and intensive farming is successfully pursued. The practice of irrigation was begun by the Mormon pioneers in 1847, and has been dis- cussed in several publications; little attention, however, has been given to the under- ground water resources, and, so far as the writer is aware, they have not before been described. The present paper outlines conditions of occurrence of the subterranean waters and describes their development in the valleys of Utah Lake and Jordan River. TOPOGRAPHY AND DRAINAGE. The drainage area of Utah Lake and Jordan River is approximately 3,300 square miles, of which 2,600 are tributary to Utah Lake and 700 to the Jordan north of the Traverse Mountains (PI, II). About 2,000 square miles of the watershed are in the Wasatch Mountains, while the valleys themselves cover a little less than 1,000 square miles. Utah Lake Valley is about 38 miles long, averages 15 miles in width, and occupies about 560 square miles, including Utah Lake. Jordan Valley is approximately 28 miles long, 15 miles wide, and comprises 420 square miles. These valleys in late geologic time aw re occupied by Lake Bonneville, the Pleistocene predecessor of Great Salt Lake, and to that fact is due their characteristic topography. Almost flat unconsolidated lake sedi- ments underlie the broad valleys, the borders of which are marked by a unique series of terraces that characterize the shore lines of the old lake. Descriptive details of these features will be given in the sections devoted to geology and to the occurrence of under- ground water. The range in elevation is considerable. The present level of Great Salt Lake is approxi- mately 4,210 feet above the sea, and that of Utah Lake is about 4,480 feet. From these lowest elevations the two valleys rise to their outer borders, which may conveniently be taken as the highest level occupied by Lake Bonneville, at approximately the 5,200-foot contour, above which the Wasatch Range towers up to 12,000 feet. The mountains on the west are narrow north-south ranges that rise abruptly from broad valleys. The b UNDERGROUND WATER IN VALLEYS OF UTAH. Oquirrh Mountains, west of Jordan River, are 30 miles long, 5 to 10 miles wide, and their summits rise to elevations of about 10,000 feet. The Lake Mountains, west of Utah Lake, are about 15 miles long, 5 miles wide, and 3,000 feet above the lake. They are connected by low hills with the Oquirrh Mountains on the north and with the East Tintic Mountains on the south.- The East Tintic Mountains border Utah Lake Valley on the southwest, rising above it about 3,000 feet. A spur from these mountains extends north- eastward, constituting the southern border of Utah Lake Valley, and almost unites with the Wasatch Range. The steep western face of the Wasatch Mountains rises about 7,000 feet abruptly above the broad valley and constitutes the dominant topographic feature of the region. To the east the range slopes away gradually in a series of broad ridges and narrow valleys to the mountainous plateau region. The western scarp is deeply dissected by canyons, through which the entire Wasatch drainage flows to Great Salt Lake, the chief streams being Bear, Weber, and Jordan rivers. Utah Lake is a body of shallow water about 21 miles long and 7 miles wide (PI. Ill, A), covering a maximum area of 93,000 acres. Its depth over much of its extent is only 8 feet or less, and the maximum depth in the main body of the lake is about 13 feet. In its northwestern part, however, recent soundings have revealed the presence of several deep holes, due to springs (p. 49). The shore line of the lake is subject to considerable variation, owing to the changing relations of evaporation, precipitation, and inflow, and the margins are characteristically swampy. Two large, shallow bays extend eastward and southward from the main body of the lake, one south of Provo and the other north of Goshen. West of the lake the Pelican Hills approach close to the shore, and the region is barren, but on the north, east, and south the land rises gently toward the base of the mountains and is dotted with flourishing settlements which are supported by irrigation. The principal streams tributary to Utah Lake, beginning at the north and proceeding southward, are: Dry, American Fork, Battle, and Grove creeks, Provo River, Hobble Creek, Spanish Fork, and Peteeneet, Santaquin, and Currant creeks. Of these, Provo River is the largest, being approximately 70 miles long and having a drainage area of 640 square miles. It rises in the Uinta Mountains near the sources of Weber, Bear, and Du Chesne rivers, flows westward and southward through Kam.as and Provo valleys, and passes through the Wasatch Mountains in a deep canyon. On entering Utah Lake Valley Provo River flows almost due south for 5 miles, skirting the great Provo delta, and thence westward, entering Utah Lake about 3 miles west of Provo. Spanish Fork has a watershed about equal to that of Provo River, but not so great a discharge. It rises near Soldier Summit, and, after receiving two main tributaries. North and Thistle creeks, flows in a canyon through the main ridge of the Wasatch Moun- tains and enters Utah Lake Valley at the head of the large embayment that extends between Payson and Springville, Salt Creek rises in the southern Wasatch Mountains, on the eastern slope of Mount Nebo, and, after crossing the border of the plateau region, emerges into the broad valley at the southwestern base of the Wasatch Mountains where, in summer, it ceases to flow at the surface. The drainage way continues, in a narrow canyon, through Long Ridge which par- tially connects the East Tintic and the Wasatch mountains, and enters the southern end of Utah Lake in Goshen Valley, where the stream, which is fed largely by seepage, is known as Currant Creek. The other tributaries of Utah Lake are relatively small. The chief ones rise in the Wasatch Mountains and occupy canyons in their mountain courses, where they maintain perennial flows. At the mouths of the canyons canals divert the water and distribute it over the valley, so that in the irrigation season practically all of the available supply is thus used and the beds of the streams in Utah Lake Valley are commonly dry; but in the late spring and early summer, during the period of melting snow, large volumes are dis- charged directly into the lake. Jordan River heads at the northern end of Utah Lake and flows northward in a meander- ing course of about 40 miles to Great Salt Lake. For the first 5 miles the river flows slug- --^•^^sik*. l]L^^^'^y TOPOGRAPHY AND DRAINAGE. Y gishly in a broad valley, and in that distance falls only about 10 foot. In tho "narrows," however, the river occupies a constricted channel and descends rapidly; in the first mile below the intake of the canals its fall amounts to about 70 f(ct. Below the ''narrows" the valley spreads out and at its greatest width is about 18 miles wide. The country rises gradu- ally toward the adjacent highlands to the base of the terraces that mark the shore lines of Lake Bonneville, whence tho ascent is by successive steps. Between Salt Lake City and Great Salt Lake the topography is almost flat, and a numl)er of small lakes of shifting out- line occupy local depressions. As the shore of Great Salt Lake is approached there is a faint slope of the surface which becomes increasingly marshy. This area west of Salt Lake City in general is barren and desolate and the surface in many places is white with alkali. On the uplands, away from the lake, alkali is scarce, but the western part of the valley, because of the lack of water, suffers in comparison with the cultivated eastern part, which is supplied by streams from the Wasatch Mountains. North of the Traverse Mountains the principal tributaries of Jordan River are City, Red Butte, Emigration, Parleys, Mill, Big Cottonwood, Little Cottonwood, Dry Cottonwood, and Willow creeks, all of which issue from the Wasatch. In their mountain courses these creeks generally occupy narrow canyons from which they emerge on the lowlands and flow in broad open valleys to the Jordan. Within the mountains they are all perennial streams, but at the mouths of the canyons their flow is largely diverted by irrigation ditches, so that, in the dryest part of the year, their lower courses are generally dry. They rise in the main crest of the Wasatch and have small watersheds. Big Cottonwood Creek, draining about 48 square miles, being the largest. This stream rises at the base of Clayton Peak, is fed by a number of small lakes, and discharges a considerable quantity of water through a narrow canyon (PI. IV, 5). The vegetation is scanty. The valleys in their natural state are occupied by sagebrush, greasewood, and kindred desert plants, but wherever water is available there is a marked contrast, and the irrigated areas of these valleys rival in productiveness an}^ in the country. Sugar beets are grown in quantity; alfalfa, potatoes, corn, etc., are common crops; and on the bench lands a variety of fruits are successfully cultivated. The mountains on the western border are generally barren; sagebrush and occasional cacti are the chief growths on the slopes, while scrub oak and stunted spruce and pine here and there grow in patches; the summits are usually bare. The Wasatch Mountains are more favored, but they do not support a heavy growth of trees. At the heads of the valleys scattering pine, juniper, mountain mahogany, and quaking aspen locally occur, and cottonwood, birch, and maple are often found near the stream beds. The slopes are commonly covered with underbrush in varying degrees of thickness, sagebrush and scrub oak being prominent. GEOLOGY. LITERATURE. This area has been studied by prominent geologists and has inspired some classic works on American geology. King, Emmons, and Hague of the Fortieth Parallel Survey « inter- preted the main features of the region, and Gilbert made it famous by his investigation of Lake Bonneville. t But although this interesting region lies contiguous to one of tho main transcontinental routes and has been visited by many geologists, yet comparatively little detailed work has been done in it. Walcottc has studied tho Big Cottonwood Cambrian section, G. O. Smith and G. W. Tower rf have examined the Tintic district, J. E. Spurrf has a King, Clarence, Systematic geology: Rept. Geol. Explor. 40th Par,, vol. 1, 1872; Hague, Arnold, and Emmons, S. F., Descriptive geology: Ibid., vol. 2, 1877. b Gilbert, G. K., Lake Bonneville: Mon. U. S. Geol. Survey, vol. 1, 1890. cWalcott, C. D., Bull. U. S. Geol. Survey Nc. 30, 1880, p. 38. d Tower, G. W., and Smith, G. O., Geology and mining industry of the Tintic district, Utah: Nine- teenth Ann. Rept. U. S. Geol. Survey, pt. 3, 1898, p. m\. s little information concerning the relations of the two main mountain masses, because the o Emmons, S. F., Am, Jour. Sci., 4th sor., vol. U\, August, 19(«, j). 139. 10 UNDERGKOUND WATER IN VALLEYS OF UTAH. Traverse Mountains are largely composed of younger lavas, which conceal the rocks upon which they lie. In the '' narrows " where Jordan River flows through the Traverse Mountains, practically horizontal Pleistocene gravels, which form the great embankment at the point of the mountain, are unconformably underlain near the river level by fine-textured sediments that dip southeastward at an angle of 40°. The lower part of these sediments consists of light calcareous clay and the upper part of fine sand and gravel. No fossils were found, but the marked unconformity and the character of the material suggest that the age of the lower deposits is Tertiary. East of Utah Lake the great Wasatch fault is impressively shown by the remarkable alignment of the base of the mountains extending from Spanish Fork Canyon to the Trav- erse Mountains in an approximately straight line, and by the abrupt rise of the mountains above the broad valley. Second and third lines of faulting, lying parallel to the main fault and east of it, are suggested by the topography, which rises steplike, with two intervening treads between the ascents, to the top of the main ridge, and by the unusual thickness of limestone exposed, which apparently requires repetition by faulting for the explanation of its occurrence. In this part of the range a disturbed belt of rocks with prevailing steep westerly dips occurs along the western base of the mountains, beyond which the strata dip eastward at low angles and the summits of the main ridge are capped by limestone lying almost flat. The streams that cross the mountains, therefore, flow transversely to the strike of the rocks, in marked contrast to the creeks farther north, whose courses lie approximately parallel to the strike. Excellent sections can be measured along the canyons, but very little detailed work has yet been done. The rocks in general are quartzite and limestone of Carboniferous age, but locally Cambrian sediments also occur. In Rock Creek Canyon, east of Provo, in the lower end of the gorge, the rocks are much disturbed and are complexly folded. Here a considerable thickness of white quartzite outcrops, overlain by a great mass of limestone. In a thin bed near the base of the limestone G. H. Girty obtained a few Cambrian fossils, and about 600 feet above, in massive. gray limestone, the beds being apparently conformable, he found Lower Carboniferous fossils. South of Hobble Creek easterly dips prevail from the base of the mountains as far as Spanish Fork, beyond which the range has been very little studied. It trends southwest- ward and terminates at Mount Nebo, the main mass of which is composed of steeply west- dipping limestone and subordinate quartzite of upper Carboniferous age. The highland farther south consists of a series of plateaus, which are underlain by low-lying Mesozoic and Tertiary rocks. The highlands that border the valleys of Jordan River and Utah Lake on the west are for the most part composed of the same rocks that occur in the Wasatch Mountains, but the structural relations are completely hidden by the deep filling of the intervening valleys. The Oquirrh Range is composed mainly of Carboniferous limestones and quartzites, which, in the southern part of the mountains, are folded into two parallel anticlines with an intervening syncline. The axes of folding are obliquely transverse to the topography, the range extending in a north-south direction while the structural trend is northwestward. The structure of the northern part of the mountains is little known, but the range is proba- bly terminated by a fault. Rocks of Cambrian age are exposed locally by a fault in the vicinity of Mercur, and igneous rocks, both extrusive and intrusive, also occur. The intrusive rocks include both acidic and basic porphyries, which are conspicuous in the vicinity of the mining camps of Bingham and Mercur; the extrusive rocks, largely andes- itic, occur principally along the eastern base of the range and in the Traverse Mountains. The Lake Mountains, or Pelican Hills, west of Utah Lake, are composed of Carbonif- erous limestones and quartzites which constitute a low synclinal fold, and are separated from the Traverse Mountains by a narrow strip of Pleistocene deposits. A line of hills, GEOLOGY. 11 composed chiefly of west-dipping limestone, separate the Lake Mountains from the East Tintic Range — the succeeding highland mass to the south. The northern end of these hills is capped by horizontal basalt with which light pumiceous tuff is associated. The East Tintic Range, a complex mass of sedimentary and igneous rocks, forms the southwestern border of Utah Lake basin. As in Rock Canyon, the sediments consist of Cambrian quartzite and Carboniferous limestone in juxtaposition, indicating the al)sence. of the Ordovician, Silurian, and Devonian. The main structure of the sedimentary rocks is synclinal, but these constitute a relatively small part of the outcrops, igneous rocks, rhyo- lite, andesite, monzonite, and basalt occupying most of the region. These are of both extrusive and intrusive origin, and are of Tertiary age. The low spur of the Tintic Moun- tains known as Long Ridge, which lies south of Goshen and connects with the Wasatch — save for a narrow Pleistocene strip south of Santaquin — consists of andesite in its southern part, while southeast-dipping Carboniferous limestones outcrop in the gorge of Currant Creek. T.ATE GEOLOGIC HISTORY. The above resume implies for this region a complex geologic history which need not here be discussed. A statement of late geologic events will, however, add to a clearer under- standing of the valley deposits in which the underground water is stored. TERTIARY HISTORY. After many thousands of feet of sediments had accumulated in Paleozoic and Mesozoic time, during which the general region was occupied by oceanic waters, profound continental uplift occured in early Tertiary time. Since then the ocean has not invaded the interior of the continent and during Tertrary time much of the Cordilleran region is believed to have been occupied by a number of lakes in which a considerable thickness of rocks accumulated. During the Eocene, according to the geologists of the Fortieth Parallel Survey, a great fresh- water lake occupied the Wasatch Mountain area, and toward the close of this epoch the mountains were finally uplifted and the relative depression of the Great Basin originated. The late Tertiary witnessed the formation of several lakes whose positions were determined by different crustal movements, and these lakes persisted with varying relations into the Pleistocene epoch. The end of Tertiary time was marked by further earth movements that divided the Great Basin area into two main depressions, following the bases of the recently uplifted Wasatch Mountains and the Sierra Nevada. In Quaternary time the bordering mountains were occupied by glaciers, and enormous lakes accumulated in the marginal depressions of the Great Basin. The two largest of these have been named after early explorers. Lake Lahontan covered an immense area in western Nevada and Lake Bonne- ville occupied a considerable part of western Utah and extended into adjacent parts of Nevada and Idaho. QUATERNARY HISTORY. The existence of Lake Bonneville is borne witness to by a number and variety of facts, chief of which are the remains of shore lines and shore deposits, and the great thickness of sediments that accumulated in the lake and that now constitute the valley floor. At its greatest extent the water of Lake Bonneville was approximately 1,000 feet above the present surface of Great Salt Lake. This large body of water abutted against the adjacent highlands and the outline of the lake was intricate. Deep bays and jutting promontories marked the shores, and lone mountains, partly submerged, stood out as islands. The area considered in this report formed part of one of these bays. This — was divided by a close stricture into an outer bay and an inner, the outer covering the valley of the Jordan River and the inner spreading over Cedar, Utah, and tJoshen valleys and a part of Juab Valley. In the inner bay the Goshen Hills made two islands, and the Pelican Hills constituted one large and several small islands. Small estuaries occupied Emigi-ation and Little Cottonwood canyons, connecting with the outer bay, and the inner bay sent an estuary into Provo Canyon.a a Gilbert, G. K., Lake Bonneville: Men. U. S. Geol. Survey, vol. 1, 1890, p. 103. 12 UNDERGEOUND WATER IN VALLEYS OF UTAH. During the existence of Lake Bonneville sedimentation was practically continuous in its lowest depression, but toward the periphery oscillations of the water level alternately cov- ered the lake deposits and exposed them to subaerial influences. Evidence of the earliest Pleistocene history of the Bonneville region is furnished by alluvial cones that extend nearly to the bottom of the basin. These are composed of detritus derived from the adjacent highlands under subaerial conditions and could not have been accumulated when the level of the lake was high. It is therefore concluded that at this early period in the history of the lake comparatively arid conditions prevailed, for the stage of a lake in a closed basin is determined by the relation of evaporation to water supply. It has also been determined that at this period of the history of the lake it had no outlet and that the time of duration of low water was relatively long. Next succeeded a period of high water, when yellow clay, locally streaked with sand, was deposited in a large part of the lake. The base of the yellow clay has not been observed and good sections are rare, though an exposure 150 feet thick has been measured. The deposit locally extends to within 120 feet of the highest level attained by Lake Bonneville, but a study of the shore line shows that during the deposition of the yellow clay the water did not rise to the rim of the basin. In the lower part of the basin the yellow clay is unconformably overlain by a deposit of white marl, local streaks of alluvium occurring at the contact. The white marl is composed of a fine calcareous clay consisting of calcium and magnesium carbonates, microscopic siliceous organic remains, and fine clastic debris. These facts imply (1) that after the deposition of the yellow clay the lake water sub- sided, (2) that the clay was eroded, and (3) that a second period of high water subsequently ensued when the white marl was deposited. The extent to which the waters subsided is undetermined, but the possibility of complete desiccation is suggested by the difference in character between the yellow clay and white marl. The extent of the second period of high water is determined by the highest shore line traceable along the adjacent mountain flanks. This level is approximately 1,000 feet above Great Salt Lake and is known as the Bonneville shore line. The lake then outflowed through Cache Valley into the Snake River basin. The Bonneville shore line marks the highest stage of Lake Bonneville and the level of its initial outflow. Beneath this level the drainage channel was cut down by the outflow of the lake to a depth of approximately 375 feet. That the lake maintained its level at the stage of lowest outflow for a relatively long time is attested by the well-developed shore phenomena at the corresponding elevation. This stage determined the Provo shore line, so named from its great development near that town. The present conditions have been brought about by the recession of the lake's surface, due to the excess of evaporation over inflow, so that now Great Salt, Utah, and Sevier lakes are the sole remnants of the former great body of water. The recession has uncovered the great expanse of lake beds that underlie the intermontane plains and constitute the fertile lands at the base of the Wasatch Mountains, and has also exposed the remarkable shore phenomena that testify to the history of Lake Bonneville, so completely worked out by Gflbert. The Bonneville basin is preeminently characterized by its many shore lines (PI. Ill, B), the highest of which impinges against the mountains and the lowest of which that can be recognized incloses the area covered by the lake sediments. Through a vertical interval of 1,000 feet the story of the rise and fall of this body of water is recorded by the super- position of shore line upon lake sediment and of lake sediment upon shore line. The record is not in all cases perfectly legible, but the main features are unmistakable. The work of waves is recorded by cliffs and wave-cut terraces, from which the debris was carried along the shore to make benches, bars, spits, and terraces. The streams loaded with the waste of the land areas deposited their burdens in the lake, the coarser detritus being laid down near shore while the finer sand and clay were carried far out before sedi- mentation occurred. Deltas were formed at,the mouths of the larger creeks where so much debris was carried that the shore currents could not distribute it. Since the recession of A. NORTHERN END OF UTAH LAKE. Oquirrh Mountains in background. 7;. HEAD-GATE OF JORDAN AND SALT LAKE CITY CANAL, LOOKING SOUTH. Embankment at point of the mountain in background. GEOLOGY. 13 the lake from its old shores the streams which formed the deltas have begun their destruc- tion by cutting them in two in their progress toward the shrunken body of water. The Bonneville is the most conspicuous of all the shore lines, not because of the relative duration of time during which it was formed but because being the topmost of the series, it emphasizes the contrast between the sharply carved subaerial erosion features of the main land and the broad horizontal lines due to the influence of the lake. Study of the levels of bars at this stage shows that the record is complex and that the water surface alter- nately rose and fell a few feet during the formation of the shore phenomena that mark the general Bonneville level. Below the Bonneville there are a number of plainly marked shore lines which represent stages in the level of the lake when it was practically constant for relatively long periods. Of these shore lines the Provo is the most remarkable, for it records the longest occupancy of one approximate horizon of any of the stages of the lake. Its embankments are the most massive and its wave-cut terraces are the broadest, notwithstanding the fact that the lake at the Provo stage was considerably smaller than when the surface of the water was 375 feet higher, its area having shrunk from 19,500 to approximately 13,000 square miles. The Provo shore line is characterized particularly b}^ its deltas, which were formed at the mouths of all the larger streams that entered the lake. The fall from the Bonneville to the Provo level was apparently without interruption and comparatively rapid. But below the Provo stage there are remnants of shore lines and terraces at a number of horizons that record temporary halts of greater or less extent in the gradual shrinkage of the lake. The most conspicuous of these lower shore lines, at an elevation of approximately 750 feet below the Bonneville level, has been named the Stans- bury shore line, from its prominent development on Stansbury Island, but the others have not been correlated. As many as ten distinct shore lines can be traced on the west side of Jordan Narrows. In connection with the different shore lines it is of interest to note that Gilbert has found evidences at a few localities of oscillations of the lake level between the Provo and Bonne- ville horizons, which appear to record halts in the rise of the lake as it approached its maximum. This is unusual, for most of the observed shore phenomena were formed during the retreat of the lake. Local deposits of calcareous tufa occur associated with the various shore lines, but are most abundant at the Provo horizon. The tufa appears to have been deposited by precipita- tion from the lake waters due to aeration of the waves, especially during storms, and con- sequent loss of carbon dioxide by which the carbonate of lime was held in solution. The tufa occurs as a cement to gravel and as a more concentrated deposit, from a few inches to a few feet in thickness, coating exposed surfaces. Below the Provo horizon, lake beds consisting of subhorizontal or gently lake ward-sloping sediments are associated with shore deposits until, as the valley bottom is approached, shore markings become indistinct and the lake beds prevail. The deposits of yellow clay and white marl previously mentioned as being widely distributed in the Bonneville basin apparently are not typically developed in the bay of the old lake, which occupied the area under consideration. A number of deep wells have been sunk into the valley deposits and their records indicate the general composition of the sediments (PI. V). The beds are at least 2,000 feet thick, and consist of gravel, sand, and clay, which constitute the reservoirs in which ground water is stored. CLIMATE. Weather observations have been systematically recorded at Salt Lake City for thirty- one years, and at near-by stations, including Provo, Thistle, Heber, and Park City, for eight to fourteen years. The most important meteorologic data, compiled from reports of the United States Weather Bureau, are summarized in the following tables, which give details of precipitation, temperature, wind velocity, humidity, and evaporation, on which the supply of underground water directly depends. 14 UNKEBGROUND WATER IN VALLEYS OF UTAH. PRECIPITATION^. Monthly and annual precipitation at Salt Lalce City, 1875 to 1904.. [Inches.] Year. Jan. Feb. Mar. Apr. May. June. July. Aug. Sept. Oct. Nov. Dec. Annual 1875. 1876. 1877. 1878. 1879. 1880. 1881. 1882. 1883. 1884. 1885. 1886. 1887. 1888. 1889. 1890. 1891. 1892. 1893. 1894. 1895. 1896. 1897. 1898. 1899. 1900. 1901. 1902. 1903. 1904. 3.05 1.23 .87 1.07 1.87 .29 1.24 1.50 1.47 .71 1.48 1.91 2.36 1.52 .73 3.67 .74 1.61 .82 1.31 1.32 1.26 1.16 .58 .84 .44 .95 2.11 1.45 0.79 1.52 .38 3.49 .71 1.02 2.44 .42 .72 2.23 1.56 1.36 1.41 1.22 .81 2.05 .76 .68 1.64 .83 .85 .69 3.81 .38 2.98 1.30 1.77 1.17 .82 2.25 Mean. 1.44 1.33 2.81 4.00 2.93 2.54 .67 .43 .88 1.12 1.75 3.69 2.64 2.60 -.35 2.18 1.64 1.12 4.66 2.21 2.68 1.73 .81 1.99 2.20 1.71 2.93 .33 2.48 1.22 1.35 1.50 2.09 2.14 2.63 3.26 2.37 2.37 3.81 2.92 2.89 3.47 4.43 1.87 .99 1.52 .94 1.49 1.90 2.72 1.67 .73 2.53 2.00 1.30 .81 2.91 .87 3.69 1.11 2.20 2.91 4.30 3.49 2.50 .10 1.85 2.55 .26 .98 1.78 2.49 .06 .73 .34 2.97 .16 .72 1.65 1.68 1.22 2.29 3.67 .98 4.19 2.50 .44 4.27 .33 3.55 3.08 0.90 .09 .80 .35 1.34 .01 .28 2.24 .33 .33 2.67 1.02 .37 .98 .01 .32 1.08 1.21 .04 1.38 .99 .25 .52 1.45 .96 .08 .49 .37 .74 .27 1.01 .83 .02 1.08 .07 .20 .21 .30 .10 .27 .58 T. 1.23 .24 .08 .02 .47 T. 1.19 .82 .42 1.35 .69 .18 .42 .32 .31 .56 .14 .59 0.25 .92 .28 .81 .06 .74 1.61 1.61 .62 .73 .90 .59 .69 .63 .92 .79 .46 .05 .71 .87 .02 1.47 .33 1.35 1.06 .72 1.22 .15 .43 1.22 .42 .90 3.15 .01 .56 .43 .37 .13 1.91 1.29 1.88 .55 .51 .52 T. 1.19 .12 1.30 2.87 .95 .52 .48 .15 T. 1.44 .66 .05 .84 .12 1.36 3.27 2.41 1.39 1.62 .40 2.19 2.89 2.24 .30 .80 3.85 1.44 1.26 1.58 1.02 1.01 .24 .70 1.91 1.57 2.85 1.99 .98 .52 .81 1.18 5.81 .81 1.02 .63 .32 1.17 1.44 .54 1.78 .50 3.10 1.79 .25 2.00 1.04 T. .90 .72 1.18 .28 2.44 3.15 1.19 1.95 1.52 1.40 .92 1.24 2.21 .00 2.03 1.80 1.11 .11 3.08 1.90 1.24 .92 1.20 2.12 .92 1.27 1.55 2.21- 4.37 .42 2.19 2.35 2.37 1.28 .89 .84 1.47 1.28 .61 .16 1.16 1.31 .51 .90 2.03 2.21 1.62 ,79 53 1.54 1.36 Monthly and annual precipitation at Parle City, 1899 to 1904- [Inches.] Year. Jan. Feb. Mar. Apr. May. June. July. Aug. Sept. Oct. Nov. Deo. Annual. 1899 0.90 3.50 1.40 1.80 1.30 2.20 1900 0.93 2.24 1.90 3.88 2.15 1.87 2.35 1.18 1.34 5.00 0.38 3.15 4.04 2.60 7.85 3.56 1.92 1.96 .95 1.69 0.30 1.50 .67 2.89 2.44 T. 0.20 0.10 .90 0.32 1.40 2.23 .45 0.90 .18 15.39 1901 17.89 1902 1903 T. .92 .30 .55 .00 .95 1904 1.99 CLIMATE. 15 Monthly and annual precipitation at Provo, 1899 to 1904^. [Inches.] Year. Jan. Feb. Mar. Apr. May. June. July. Aug. I Sept. Oct. Nov. Dec. Annual. loqq 1.54 .45 .22 .35 2.65 1.72 2.89 .35 2.06 1.12 .65 2.27 2.45 .05 1.09 1.30 1.80 3.75 0.39 1.65 .29 2.14 .51 1.56 1.37 .32 .39 .36 2.69 2.11 0.00 1.13 2.79 .66 T. .68 .55 0.94 3.50 .85 1.55 1.14 .00 1.05 .12 .98 1.28 .49 1.05 loni 0.18 .10 .30 .42 T. 0.11 .39 .39 1902 0.20 .42 .45 .72 1903 12.31 1904 .04 1.56 15.32 Monthly and annual precipitation at Heher, 1899 to 190Ji.. [Inches.] Year. Jan. Feb. Mar. Apr. May. June. July. Aug. Sept. Oct. Nov. Dec. Annual. 1899 2.95 5.85 3.00 0.89 1.14 0.97 1.61 2.10 1 0. 15 3. 20 0. 85 1.55 14.26 1900 1.06 1.50 .34 2.53 .16 .20 .25 .31 1.20 1.47 4.42 .22 13.66 1901 2.20 2.20 1.56 .31 1.72 .08 . 40 2. 06 . 16 1. 70 1.40 1.50 15.29 1902 .50 2.17 2.10 1.03 .07 3.00 1.46 1.95 3.48 1.88 .78 .49 1.42 .37 .25 .73 . 15 . 50 .69 .02 .29 1 .88 . 45 . 45 1.17 .76 . 16 ! 1. 22 1.77 1.90 .00 1.04 1.33 1.91 10.09 1903 13.32 1904 .96 2.01 16.74 Monthly and annual precipitation at Thistle, 1899 to 190^. [Inches.] Year. Jan. Feb. Mar. Apr. May. June. July. Aug. Sept. Oct. Nov. Dec. Annual. 1899 1.60 .30 2.40 .47 2.35 2.05 1.30 .00 2.40 2.00 0.05 1.77 1.15 2.23 1.75 .90 0.88 .05 .85 .35 1.60 2.65 T. 0.10 .05 .00 .35 0.40 .75 1.15 .41 1.43 .27 2.08 1.80 .93 2.10 .80 .00 1900 0.10 .11 .35 .53 .32 0.46 3.05 .20 .10 .46 1.00 .25 .85 .66 1.90 0.30 2.00 1.45 1.40 1.50 7.10 1901 1902 i.« 13.89 1903 1904 1.90 1.55 TEMPERATURE. Mean monthly and annual temperature at Salt Lake City, 1873 to 1904. January 27. 9 February 33. March 41.6 49.5 April. May. June. July. 57.8 67.0 75.5 August 74. 8 September 64. 3 October 52. 3 November 39.8 December 32. 7 Annual 51. 4 Mean monthly and annual temperature at Provo, 1890 to 1904- January 26. 6 February 29. 3 March 39 . 3 April 49. 1 May 58. June 64. 7 July 73.2 August 70. 7 Soptomhor 59.8 October 48. 7 November 38. 4 Doceml)er 29.2 Annual 49. 2 16 UNDERGROUND WATER IN VALLEYS OF UTAH. Monthly maximum temperature at Salt Lake City, 1899 to 1904. [°r.] Year. Jan. Feb. Mar. Apr. May. June. July. Aug. Sept. Oct. Nov. Dec. 1899 54 57 51 43 53 48 51 55 55 62 42 66 67 72 65 58 65 63 80 78 79 78 80 78 83 89 88 88 86 83 96 101 90 98 91 92 97 99 101 96 96 97 91 94 95 98 98 94 91 88 86 92 92 92 73 76 85 81 77 83 63 68 67 70 70 66 59 56 59 1900 1901 1902 58 45 55 1903 1904 .... Mean 51 55 65 79 86 95 98 95 90 79 67 55 Monthly minimum temperature at Salt Lake City, 1899 to 1904. Year. Jan. Feb. Mar. Apr. May. June. July. Aug. Sept. Oct. Nov. Dec. 1899 16 20 4 - 4 15 7 -10 10 15 12 - 4 6 20 26 25 21 14 19 30 30 15 32 25 30 25 40 43 35 33 36 34 47 40 42 54 44 51 53 49 43 46 51 46 52 56 52 48 46 46 32 39 35 37 38 30 27 36 36 32 28 28 28 29 21 I 9 2 1900 1901 11 1902 15 1903 14 1904 7 Mean 11 10 21 ■ 27 35 44 49 50 38 32 25 10 TVIND VELOCITY. Average wind velocity at Salt Lake City, 1900 to 1904- [Miles per hour.] Year. Jan. Feb. Mar. Apr. May. June. July. Aug. Sept. Oct. Nov. Dec. Annual. 1900 3.4 5.0 3.8 4.8 4.1 5.2 4.0 5.5 4.5 6.3 6.3 6.2 6.9 6.8 7.3 7.3 7.8 6.7 7.3 7.2 6.8 7.3 7.1 6.1 6.8 6.5 6.6 6.7 6.6 6.5 6.0 6.3 6.7 7.2 6.5 6.4 5.8 6.5 6.2 5.7 6.5 7.0 6.7 6.3 6.0 6. 5 5. 5. 4. 9 5. 7 1 6.0 4.5 4.8 4.7 3.7 4.9 5.9 1901 5.9 1902 6.1 1903 5.3 5.4 5.4 4.7 5.8 1904 6.0 Mean 4.2 5.1 6.7 7.2 6.8 7.0 6.5 6.1 6.5 5.6 5.2 4.5 5.9 HUMIDITY. Mean relative humidity at Salt Lake City, 1900 t@ 1904- [Per cent.] c Year. Jan. Feb. Mar. Apr. May. June. July. Aug. Sept. Oct. Nov. 62 57 56 64 45 Dec. Annual. 1900 78 69 83 73 75 65 73 62 74 62 40 55 58 52 64 59 42 48 44 46 41 44 43 48 49 25 36 31 38 38 24 26 27 30 33 24 39 27 28 38 36 30 32 38 34 48 50 40 45 53 63 71 65 75 60 47 1901 49 1902 . .. 48 1903 51 1904 5® Mean 76 67 54 18 45 34 28 31 34 47 57 67 49 CLIMATE. K^' APOll^VTlON . Depth of evaporation at Utah Lake a from August, lOOS, to August, 190 Jf. 17 [Inches.] 1903. August 8. 40 September (J. 78 October 3. 86 November 2. 50 December 1-50 1904. January 1.50 1 o Fig. 1.— Diagram showing variation of annual precipitation at Salt Lake City. of Utah and Great Salt Lakes and the Wasatch Mountains. The tables show that the climate is characterized by low annual precipitation, moderate temperature, moderate wind velocity, low relative humidity, and considerable evaporation. The mean annual precipitation at Salt Lake City is 10.19 inches, ranging between a maxi- mum of 23.64 inches in 1875 and a minimum of 10.33 inches in 1890. Since 1900 it has averaged 2.2 inches below normal (fig. 1). Only about 18 per cent of the annual total o Computed from daily mciisurements of a tank 3 feet in diameter. Tests were made by the engi- neer of Salt Lake City from 1901 to 1903. and since then they have been kept up by the Reclamation Service under G. L. Swendsen. See also Newell, F. II., Fourteenth Ann, Rept. U. S. Ceol. Survey, pt. 2, 1894. p. 154. IRK 157—06 2 18 UT^DERGKOUND WATER IN VALLEYS OF UTAH. occurs from June to September, and for these four months amounts to less than 3 inches. Between October and May the variation is not marked, but the greatest precipitation occurs in March and April (fig. 2). This precipitation is unusually high for the Great Basin. The Wasatch Mountains serve to condense the moisture, originally derived in large part from the westerly winds from the Pacific Ocean, that remains in the air after crossing the Sierra Nevada. Probably the precipitation is greater on the summits than at the stations where records have been kept, but data are not available. The melting snow of the winter's accumulation is ihe chief supply of the streams of the area under consideration. The mean annual temperature of -Salt Lake City is 51.4°. The mean monthly maximum ranges from 98° in July to 51° in January, while the mean monthly minimum varies between 10° in December and February and 50° in August. The dryness of the atmosphere is indicated by the mean relative humidity of 49 per cent, varying from 28 per cent in July to 76 per cent in January, and by the amount of evapora- tion from a free water surface, which, according to the latest measurements, is about 60 Per cent 14- Jan. Feb. Mar Apr May June July Aug. Sept. Oct. Nov. Dec. /2 10 , - e ■ 6 4- B 1 1 n 1 Jnches 1.44 1.33 2.03 2.21 1.62 .79 .53 .72 .93 L54 1.36 /.64 Fig. 2.— Diagram showing mean monthly precipitation at Salt Lake City. Mean annua/ I6./9 inches a year. Yet the chmate is not nearly as dry as in other parts of the Great Basin. The dryness lessens the effect of the summer's heat, so that the "sensible temperature" is not so great as would be suggested by the thermometer, being modified by the cooling effects of evaporation. HYDROGRAPHY. STREAMS TRIBUTARY TO UTAH LAKE AND JORDAN RIVER. Seepage from surface streams, as shown hereafter, is the most important source of supply of underground water in the valleys of Utah Lake and Jordan River. A summary of discharge measurements therefore throws important light on the subject and, with other data, furnishes facts for roughly estimating the amount of water available for the annual replenishment of the underground reservoirs. The figures here given have been compiled from records of the United States Geological Survey and from data obtained through the courtesy of the city engineer of Salt Lake City, and are now published for the first time. Satisfactory measurements of the flow of all the streams in the two valleys have not been made. However, records have been kept for a number of years of the discharge of several of the more important, and the combined data, with due consideration for varying con- ditions, may be taken as typical of the drainage of the entire watershed. The measure- HYDROGRAPHY. 19 merits wore made at the mouths of the canyons. Below tliese points, (hiring the irrigation season, the water is diverted and conducted over the valley in an intricate .system of ditches, so that the stream beds in their lower stretches are then often dry. During the flood season the streams discharge directly into either Utah Lake or Jordan River. Fol- lowing are tables of monthly measurements for 1904, to which annual summaries for several years are added where figures are available: Estimated discharge {at mouths of canyons) of streams tributary to Jordan River and Utah Lake. CITY CREEK. [Drainage area, 19 square miles.] Date. 1904. January February March April May June July August September. . . October November... December Year. 1903. 1902. 1901. 1900. Discharge. Maxi- mum. Sec. -feet. 6.7 7.9 11.0 28.8 70.1 57.0 26.5 15.3 11.4 9.3 8.7 9.2 70.1 63.1 58.2 72.0 31.3 121.9 Mini- mum. Sec-feet. 6.0 6.0 7.3 11.0 28.8 26.6 16.2 11.5 9.4 8.7 8.2 7.7 6.0 4.3 3.6 5.0 5.4 3.2 Mean. Sec. -feet. 6.2 6.6 8.1 22.1 55.6 39.2 19.7 13.4 10.4 9.1 8.5 8.0 17.2 13.0 12.3 12.7 9.8 20.0 Total. A cre-feet. 381 380 516 1,315 3,419 2,332 1,211 824 619 609 506 12,604 9,440 8,910 9,251 7,054 14,491 Run-off. Per square mile. Sec-feet. 0.326 .347 .442 1.160 2.926 2.063 1.037 .705 .547 .479 .447 .421 Depth. Inches. 0.376 .374 .510 1.294 3.373 2.301 1.195 .813 .610 .551 .499 .485 Relation to rain- fall. Per cent. 20.9 10.3 8.6 66.7 122.2 852.2 202.5 71.9 508.3 46.7 .908 12.381 .685 9.323 .647 8.811 .668 9.126 .517 7.040 1.053 14.306 53.9 Rainfall.a Inches. 1.80 3.62 5.92 1.94 2.76 .27 .59 1.13 .12 1.18 .00 .90 61.2 63.1 69.5 53.9 52.5 80.1 20.23 14.77 12.67 16.94 13.41 17.85 EMIGRATION CREEK. [Drainage area, 19 square miles.] 1903. January February. . . March April May June July August September. . October Noveml)cr. . December. .. Year. . 6.3 0.7 1.1 ()8 0.058 0.069 2.3 .8 .5 .6 33 .032 .033 3.1 11.7 .4 . 3.0 184 .158 .182 9.2 , 12.8 3.7 8.0 476 .421 .470 4.5.6 19.3 5.5 9.5 584 .500 .576 17.9 18.1 4.0 8.6 512 .453 .505 136.5 4.0 1.6 2.8 172 .147 .169 120.7 1.7 .6 1.0 61 .053 .061 14.2' 1.1 .6 .8 48 .042 .047 5.3 2.0 1.1 1.2 74 .063 .073 13.3 3.2 1.0 1.3 77 .068 .076 5. 5 .8 .6 . 7 43 .037 .043 5.9 19.3 .4 3.2 2,332 .169 2.304 15. 6 2.99 1.08 1.97 1.03 3.22 .37 .14 .43 1.38 .73 14.77 1 The record of rainfall given under City, Emigration, Parleys, and Mill creeks is the mean precipita- tion for Salt Lake City and Park City; that under .Vmerican Fork and i'rovo River is for Provo and lleber; that under Spanish Fork is for Provo, Thistle, and Soldiers Summit. 20 UNDERGROUND WATER IN VALLEYS OE UTAH. Estimated discharge (at mouths of canyons) of streams tributary to Jordan River and Utah Lake — Continued. PARLEYS CREEK. [Drainage area, 50 square miles.] Date. 1904. January February . . . March April May June July August September . . October November . . December . . . Year . . 1903 1902 1901 1900 1899 Discharge. Maxi- mum. Sec-feet. 9.2 18.1 39.3 207.3 208.5 137. 5 41. 1 20.2 13.0 13.7 11.8 10.8 208.5 133.7 95.3 109.5 39.0 227.5 Mini- mum. Mean. Sec-feet. 4.8 4.2 9.4 69.8 88.1 28.5 19.5 11.8 9.4 11.8 2.5 2.1 2.2 3.0 2.9 4.0 Sec-feet. 7.1 10.3 19.6 123.2 168.5 52.6 26.1 16.0 11.4 12.9 10.3 8.3 38.9 20.5 16.7 19. y 12.6 59.8 Total. Acre-feet. 437 592 1,205 7,331 10,361 3,130 1,605 984 679 793 613 510 Run-off. Per square mile. Sec-feet. 0.142 .206 .392 2.464 3.370 1.052 .522 .320 .228 .258 .206 .166 28,240 14,879 12,116 14,490 9,0^8 39,722 .777 .410 .334 .398 .251 1.196 Depth. Inches. 0.164 .222 .452 2.749 3.886 1.174 .602 .369 .254 .297 .230 .191 10. 590 5.581 4.544 5.429 3.431 14. 884 Relation to rain- fall. Per cent. 9.0 6.1 7.6 141.8 140.8 434.8 102.0 32.7 211.7 25.2 21.2 52.3 37.8 35.9 32.0 25.6 83.4 Rainfall. Inch es. 1.80 3.62 5.92 1.94 2.76 .27 .59 1.13 .12 1.18 .00 .90 20.23 14.77 12.67 16.94 13.41 17.85 MILL CREEK. [Drainage area, 21 square miles. 1904. January February... March April May June July August September . . October November. . December . . . Year . . 1903 1902 1901 1900 13.0 13.0 13.0 25.1 58.2 55.9 29.7 16.8 15.9 14.0 13.0 n.3 58.2 34.4 39.5 47.4 30.8 66.0 6.6 3.7 9.3 11.3 25.1 29.7 20.8 13.0 13.0 13.0 11.3 1.0 LO 2.9 1.9 L4 L4 2.4 9.9 609 0.471 9.9 569 .471 11.2 G89 .486 18.8 1,120 .895 41.4 2,545 1.971 40.9 2,434 1,948 25.7 1,580 L224 14.9 916 .710 15.0 893 .714 13.7 842 .652 12.4 738 .590 8.6 529 .410 18.5 12.3 12.1 12.9 11.5 19.6 13, 464 8,916 8,753 9,391 8,296 14, 193 .878 .586 .575 .615 .549 .932 0.543 30.2 .508 14.0 .560 9.4 .999 51.5 2.272 82.3 2.173 804.8 1.411 239.2 .819 72.5 .797 664. 2 .752 63.7 .658 .473 52.5 11. 965 59.1 7.964 5.3.9 7.814 61.7 8.383 49.5 7.466 55.7 12. 669 77.1 L80 3.62 5.92 1.94 2.76 .27 .59 L13 .12 L18 .00 .90 20.23 14.77 12.67 16.94 13.41 17.85 HYDROGRAPHY. 21 Estimated discharge (at mouths of canyons) of streams Uihutary to Jordan River ami Utah Lake — Continued. BIG COTTONWOOD CREP^K. [Drainage area, 48 square miles.] Dato. 1902. January FeV)ruary . . . March April May June July August. September.. October November. . December . . . Year. 1901. Discharge. Maxi- nuun. Sec-feet. 27.6 2S. 4 27.7 142.9 369. 7 309.5 92.3 38.9 31.6 29.0 28.8 29.3 369.7 407.3 Mini- mum. Sec-feet. 13.6 17.2 20.4 27.0 108.9 91.7 40.9 28.4 25.2 21.4 21.8 10.1 Mean. Sec-feet. 23.1 24.2 24.6 70.4 210.2 194.5 62.2 33.0 27.9 26.3 24.8 22.8 Total. 13.6 11.3 62.0 68.3 L cre-feet. 1,421 1,344 1,513 4,189 12,925 11,574 3,825 2,029 1,661 1,617 1,476 1,402 44,976 49,639 Per square mile. Sec-feet. 0.481 .504 .512 1.470 4.380 4.050 1.300 .688 .581 .548 .517 .475 Run-off. 1.292 1.422 Depth. Inches. 0. 555 ..525 .590 1.640 5. 050 4. 519 1.499 .793 .648 .632 .577 .548 17. 576 19. 381 Relation I Rainfall, to rain- fall. , Per cent. \ Inches. AMERICAN FORK. [Drainage area, 66 square miles.] 1904 January February. . March April May June July August September. October November.. December. . Year. 17 15 16.1 990 0.244 0.281 14.7 L91 16 15 15.4 886 .233 .251 9.5 2.64 24 15 19.1 1,174 .289 .333 9.2 3.62 109 23 46.9 2,791 .711 .793 63.0 1.26 379 95 216.0 13,280 3.27 3.77 183.0 2.06 310 131 201.0 11,960 3.05 3.40 596. .57 147 ()() 95.3 5,860 1.44 1.66 488.0 .34 - 64 44 52.8 3,247 .800 .922 140.0 .66 43 35 38.1 2,267 .577 .644 644.0 .10 41 34 35. 9 2,207 .544 .627 45.1 1.39 34 28 28 18 30.0 25.3 1,785 1,556 .454 .383 .507 .442 .00 29.8 1.48 379 15 06.0 48,000 1.00 13. 62 85.0 16.03 .22 UNDERGROUND WATER IN VALLEYS OF UTAH. Estimated {at mouths of canyons) of streams tributary to Jordan River and Utah Lalce — Continued . PROVO RIVER. [Drainage area, 640 square miles.] Date. Discharge. Maxi- mum. 1904 January February. . . March April May June ... July August September . . October November.. December . . Year. 1898 1897 1895 Sec-feet. 290 861 2,153 1,625 326 182 184 146 190 205 2,153 1,212 2,600 1,760 Mini- mvrai. Sec-feet. 196 253 331 353 461 371 136 134 80 79 113 113 79 146 225 192 Mean. Sec-feet. 244 373 388 486 1,145 1,131 202 149 117 113 139 149 386 "571 423 Total. A cre-feet. 15,000 21,460 23,860 28,920 70,410 67,300 12,420 9,162 6,962 6,948 8,271 9,162 279,900 279,000 414,000 306,400 Run-off. Per square mile. Sec-feet. O.08I .583 .606 .759 1.79 1.77 .316 .233 .183 .177 .217 .233 .604 ,60 Depth. Inches. 0.439 .629 .699 .847 2.06 1.98 .364 .269 .204 .204 .242 8.20 8.19 12.12 9.07 Relation to rain- fall. Per cent. 23 24 19 67 100 347 107 41 204 15 Rainfall. Inches. 1.91 2.64 3.62 1.26 2.06 .57 .34 .66 .10 1.39 .00 1.48 16.03 16.71 17.76 a 14. 63 a Approximate. SPANISH FORK. [Drainage area, 670 square miles.] 1904. January February... March April May June July.. August September.. October November.. December.. Year. 113 .58 77.6 4,771 0.116 0.134 8.1 126 58 79.1 4,550 .118 .127 7.4 240 63 85.8 5,276 .128 .148 4.4 229 110 174. 10,350 .260 .290 28.0 415 236 343.0 21,090 .512 .590 25.0 , 255 111 162.0 9,640 .242 .270 41.0 121 80 94.6 5,817 .141 .163 39.0 92 67 75.8 4,661 .113 .130 19.0 75 65 68.0 4,046 .101 .113 13.0 69 65 67.8 4,169 .101 .116 . 11.0 fiQ 49 61 5 3,660 3,339 092 102 77 40 54.3 .081 .093 8.7 415 40 112.0 81,370 .167 2.28 15.4 1.66 1.71 3.36 1.02 2.33 .85 1.01 .00 1.07 14.78 Comparison of ttie discliarge of several streams shows marlied differences. For instance, during 1901 and 1902, tlie only years when complete measurements of both Parleys and Big Cottonwood creeks are available, the discharge of Big Cottonwood (drainage area, 48 square miles) averaged 47,308 acre-feet, while that of Parleys, with a drainage area slightly greater (50 square miles), averaged only 13,303 acre-feet. Again, during 1904 the dis- charge of City and Emigration creeks, each having drainage areas of approximately 19 square miles, amounted, respectively, to 12,604 and 2,332 acre-feet. Provo and Spanish Fork rivers also afford similar results. The drainage area of Provo River (640 square miles) HYDROGRAPHY. 23 is slightly loss than that of Spanish Fork (070 square miles), yt't the discliargc of the former in 1904 was more than three times that of the latter. It will be noticed that the flows of Spanish Fork and of Emigration Creek, streams which in the above comparisons figured poorly, have much in common, though their drain- age areas difi'er greatly. The flow of the two streams, expressed in second-feet per square mile of their drainage areas, averaged 0.167 for Spanish Fork and 0.169 for Emigra- tion Creek, which may be compared with an average of 0.746 for City Creek and 0.69 for Provo River. The amount of discharge, expressed in depth of inches, over the watershed is 2.28 for Spanish Fork 2.30 for Emigration Creek, and 10.33 for City Creek. The run-off is approximately 15 per cent of the precipitation for Spanish Fork and Emigration Creek, and about 63 per cent for City Creek. These and other discrepancies are due to a complex set of causes, chief of which are differ- ences in precipitation, topography, vegetation, soils, and rocks of the several drainage areas, and the care that is taken to prevent fires, grazing, and destruction of timber on the water- sheds. Though in general the main streams in the Wasatch Mountains have many features in common, the valleys of some of them are narrow and steep, whil'e those of others are broader and more open. Some valleys are better adapted than others, by configuration and position, to collect and keep snow. Some of the streams head in lakes, while others do not. All are poorly clothed with trees, but some are less fortunate in this respect than others. The soil covering in general is thin, particularly on the steep slopes and in areas where the absence of much vegetation allows the products of rock disintegration to be washed into the valleys. But where the slopes are comparatively gentle and vegetation protects the accu- mulated rock debris, more of the precipitation is absorbed and (escaping flood discharge) seeps slowly into the valleys to maintain the perennial flow of the streams. Differences in the porosity of the bed rocks and in the character and quantity of debris in the stream beds, whereby greater or less amounts of water are absorbed, also greatly influence the amount of run-off. UTAH Lake. Utah Lake is fed from several sources, including surface streams, seepage, springs l^eneath the lake, and the precipitation that falls upon it. The measurable factors were determined tttv.T OU 1889 1890 1891 1892 1893 1894 1895 1896 FEcr 4491 90 89 .68 87 86 85 84.' 83 82 - A /\ A A ^\ / \ ^\ ^\ ^ r /\ / \ / \ . y " \ / -^ V ' A / \J \ / \y 1897 1898 1899 1900 1901 1902 1903 1904 - y\ /\ ' \ / ^^^^ _ /-x X/"^ \y \ ^■^ \ . / \ .-^ /^ /' \^ Vy \ / \ / V^ \^ / r; Fig. 3.— Diagram showing fluctuations oi the surface of Utah Lake, 1S89-1904. 24 UNDERGROUND WATER IN VALLEYS OF UTAH. for the period August 1903, to August, 1904, under the direction of G. L. Swendsen,o of the United States Reclamation Service, who found that of the total supply of 604,010 acre- feet only 471,140 were contributed by rainfall on the lake and by the measurable surface streams, leaving an unmeasured supply of 132,870 acre-feet. This considerable amount appears to be contributed by seepage and by springs, some of which have recently been found in the northwestern part of the lake. The surface of the lake is subject to considerable variation in elevation in consequence of the changing relations of evaporation, precipitation, inflow, and outflow. Fig. 3, pre- pared by the Reclamation Service, shows fluctuations of the surface from 1889 to 1904. There is a seasonal variation of 1 to 4 feet, ranging from a minimum in the late fall to a maximum in late spring and early summer. The diagram also shows the variation in the mean level of the lake. The lowest elevation shown occurred in 1903, when the lake was about half a foot lower than it was in 1889. Following 1889 was a period of ten years of relatively high water. JORDAIS^ RIVER. During the last few years anomalous conditions have existed at the outlet of Utah Lake. The water level of the lake has fallen so low that the normal flow has ceased, and in order to supply the canals in Jordan Valley it has been necessary to resort to pumping. Accord- ingly a pumping plant has been in operation at the head of Jordan River since August, 1902. (PI. IV, A.) The following table of discharges has been prepared by Mr. J. Fewson Smith, jr., water commissioner: Discharge of Jordan River and the canal systems in Jordan Narrows, and of Jordan River at pumping plant, April to October, 1904. [Acre-feet.] Month. North Jordan. East Jordan. City. South Jordan. Utah and Jordan Salt River at Lake. weir. Sum of preced- ing. Jordan River at pumping plant, a 1904. April May June July August September . . October 963 2,970 3,384 3,233 2,662 753 650 3,036 5,701 5,369 5,186 5,280 1,920 452 3,199 3,090 1,373 399 647 5,167 6,648 5,407 5,031 5,357 2,134 720 4,150 7,878 6,719 7,110 7,992 3,367 75 2,911 4,225 3,894 3,668 2,767 310 2,092 16,823 27,874 27,972 27,318 25,431 222 18,090 25, 110 25,210 24,720 23,330 8,363 Total. 13,965 27,142 ,109 30,391 37,936 17,850 136,; 125,045 Figures furnished by G. L. Swendsen. From these figures it appears that the gain in the flow of Jordan River between the pump- ing plant and the intake of the canals in Jordan Narrows, a distance of about 13 miles, April to October, 1904, was 11,348 acre-feet. The gain is partly supplied by seepage and partly by the flow of wells and springs. Between Jordan Narrows and the head of North Jordan canal, a distance of about 9 miles, Mr. J. Fewson Smith, jr., found that the seepage into Jor- dan River between May and September, 1904, amounted to 13,789 acre-feet. oThe writer acknowledges his indebtedness to Mr. Swendsen for many courtesies extended, both in the field and office, during the prosecution of the work. U. S. GEOLOGICAL SURVEV WATER-SUPPLY PAPER KO. 157 Pl. IV I! issi: iaea., i-mt >>t^t '.n i *>^^ ^. GATE AT HEAD OF JORDAN RIVER. DEAD MAN'S FALLS, COTTONWOOD CANYON HYDROGRAPHY. 25 No systematic data have been collected below the head of North Jordan canal, but in December, 1904, the following measurements were made by Mr; Caleb Tanner and the writer : Diacharge of Jordan River and tributaries between Little Cottonwood Creek ami the ford, in sec. i, T. 1 N.,R. 1 W., December 0-7, J90J^. Second-foet. Jordan River above mouth of Little Cottonwood Creek (il . 38 Little Cottonwood Creek 8-14 Flume at Taylorville roller mill 39. Hig Cottonwood Creek -tI-Z Ditch south of Mill Creek 2. 12 Mill Creek -^ -3. 94 Ditch, outlet of Decker Lake -* 2. 93 Parleys Creek, north and south ditches 8. 78 f:ighth South street ditch G. C9 Total 203. 58 Jordan River below North Temple Street Bridge 190. 22 190. 22 Loss between mouth of Little Cottonwood Creek and North Temple street 13. 30 Outlet of Hot Springs Lake 7. 64 Sewer ditch (estimate) 7. 50 Jordan River at ford, sec. 4, T. 1 N., R. 1 W 214.00 Total 205. 30 205. 30 Gain between North Temple Street Bridge and ford 8. 04 Loss in the flow of Jordan River, instead of expected gain, is thus shown between the mouth of Little Cottonwood Creek and North Temple Street Bridge at the time the measure- ments were made, while a slight gain is shown between the bridge and the ford in sec. 4, T. 1 N., R. 1 W. It appears that the seepage drains into the tributaries rather than directly into Jordan River in the area where the tributary streams are numerous and that farther north, where there are fewer tributaries, a small amount of seepage drains directly into the river. How far these figures represent conditions the year round remains to be determined. GREAT SALT LAKE. Except during a lapse from 1893 to 1896, instrumental records of the surface fluctua- tion of Great Salt Lake have been kept since 1875, and there is evidence less exact dating back to the survey of the lake by Stansbury in 1849-50. When that survey was made the level of the lake was extremely low, and since then it has varied considerably. In 1869 the water surface was approximately 11 feet higher than it was in 1850; a comparatively low stage was reached in 1873, after which the lake rose about 4 feet to a maxinumi in 1876, about equal to that attained in 1869. In 1883 the lake was about 7 feet below the maximum; then it rose 4 feet until 1886, since when it has gradually fallen until now it is at an extremely low stage, about 15 feet lower than the maxima of 1869 and 1876. Fig, 4 illustrates the changes since 1875. Besides the irregular fluctuations there is a regular annual variation ranging between 1 and 2 feet, the maximum occurring in June and the minimum in the winter This annual variation is due to the changing relations of precipitation, inflow, and evaporation, high water occurring after the spring floods, and low water during the season of fe(>ble stream di.s- charge and after the period of excessive evaporation. The irregular variation of the past can be accounted for chiefly by changes in rainfall, the earlier nuixima being associ- ated with unusually large amounts of precipitation. The gradual decrease of late years in tlie volume of the lake, after allowing for recent dry seasons, is apparently due to largely increased irrigation, by which the inflow of surface streams has been checked 26 UNDERGROUND WATER IN VALLEYS OF UTAH. through diversion into ditches. Because of the considerable evaporation and transpira- tion incident to such use of the water, only a small per cent of the run-off reaches the eo < ^ 20 < ^ •^ 10, < -- J> 0061 ^ V 66 < > 86 < s 16 < > s 96 < 96 <' > fr6 < \ £6 /^ > 26 < 16 ' > 0681 < > 68 ^ >• 88 V > 18 5 ^ 98 58 < s . 1^8 ^ ■— -, e8 < Z8 K, / 18 < 0881 ^ / ^ 6Z 5 s 8Z < 11 91 ^ ^ Ql / ;:: ^ CO lake, and with the spread of irrigation it may be expected that this cause will increasingly tend to keep the lake level at a low stage. SOURCES OF GROUND WATER. 27 UNDERGROUND WATER. GENEKALi CONDITIONS. SOURCE. The underground water supply in the valleys of Utah Lake and Jordan River, as is well known, is maintained by the snow and rain that fall on their drainage areas. In con.sid- ering the sources of the supply, the precipitation tributary to Utah Lake and Jordan River can conveniently be divided into that on the mountains and that on the main valley. It has been stated that the actual precipitation in the mountains probably exceeds the amount shown by the recorded data. Moreover, neither the rainfall nor the snowfall is evenly distributed. The precipitation is greater in the northern than in the southern half of the area under consideration, and in contiguous localities there are differences due to varying topographic conditions. More precipitation is likely to occur in the vicinity of the higher peaks, and in the mountain recesses that are well protected from the sun large quan- tities of snow linger long after the general mantle has disappeared. Of the total precipitation on the mountains, part is evaporated, part joins the run-ofl", and part becomes underground water. Evaporation occurs either directly — from snow, from a free surface of water, and from water contained in soils and brought to the surface by capillary action — or indirectly by transpiration through the growth of plants. Of the por- tion which joins the run-off part runs directly out of the mountains, part flows to small lakes at the head of Big Cottonwood Creek and Provo River, and part is absorbed by the soil and rocks over which the streams flow and joins the subterranean store. A final portion of the precipitation on the mountains becomes underground water directly by absorption by the surface on which the rainfall occurs. Part of this underground water reaches the surface again by capillary action in the soils and by the life activity of plants and is finally evaporated; another part after remaining underground a shorter or longer time reaches the surface again by springs and seepage, and, joining the run-off little by little, maintains the perennial flow of the streams; another part joins the more permanent supply of underground water. It is impossible, because of the complexity of the subject and the lack of data, to state the amount of water which annually replenishes this more permanent supply of underground water, but the quantity is equivalent to the precipitation minus the run-off and the amount evaporated. From the incomplete facts at hand it appears that the run-off, measured at the mouths of the canyons, although varying greatly, approximates 50 per cent of the precipitation, but the total evaporation is unknown. Although exact figures repre- resenting the amount evaporated can not be obtained, yet experiments on evaporation from snow, soils, and vegetation in the mountain areas would afford valuable data. The amount of precipitation in the valley is better known, and the figures for Salt Lake City and Provo are typical. Here, as in the mountains, part of the precipitation joins the run-off, part is evaporated, and part becomes underground water; but there are practi- cally no measurements of these different quantities. Direct run-off of the precipitation on the valley is comparatively small, owing to the open nature of the country and to the fact that no great accumulations of snow occur, and the seepage run-off probably consti- tutes the main amount. Evaporation from soils and vegetation dissipates probably the largest part of the rain that falls on the valley, especially during the summer. The increase of the more permanent underground water supply due to the rainfall on the valley is con- sequently small. A basis for judgment is furnished by comparing the condition of the valley east and west of Jordan River. Precipitation is perhaps slightly less in the western part of the valley, but the difference is not enough to cause the marked contrast. The scarc- ity of ground water within easy reach of the surface in the western part of the valley, com- pared with the abundance easily accessible in the eastern part, implies that the rainfall on the valley contributes a proportionally small amount to the store of underground water. Existing conditions are due to the fact that on the west only a few feeble and generally intermittent streams are tributary to the valley, whereas on the east a number of large perennial streams flow from the Wasatch Mountains, supplying water that is distributed 28 UNDERGROUND WATER IN VALLEYS OF UTAH. over the valley by canals. Seepage from these streams is the main source of underground supply in the valleys. The amount of water contributed to the valleys by streams from the Wasatch Mountains is capable of rough numerical statement. The drainage area in these mountains tributary to Jordan Valley is approximately 220 square miles, and measurements of five creeks in that region, given in the section devoted to hydrography, show an average flow of 0.66 second- foot per square mile of watershed. This amount is equivalent to a stream discharging 145 second-feet, or a total amount approximating 105,000 acre-feet a year. The average of measurements of Provo River and Spanish Fork in Utah Lake Valley gives a flow of 0.43 second-foot per square mile of drainage area, which, assuming the flow to be derived from rainfall on a watershed of about 1,670 square miles, is equivalent to a stream discharging 718 second-feet, amounting to 520,000 acre-feet a year. Of this amount of water annually contributed by streams to the valleys of Utah Lake and Jordan River, part permanently runs off and is added to the supply of Great Salt Lake by Jordan River. This quantity has not yet been systematically measured, but it is esti- mated to average about 200 second-feet. The residue either evaporates, directly and indi- rectly, or becomes underground water. Unfortunately, no figures are available whereby the amount lost by evaporation can be estimated, so that the annual replenishment of the underground supply is unknown. Only the crude statement can now be made that, in the presence of influences sufficient to cause an evaporation of 60 inches a year from a free body of water, the amount which is not thus lost from a supply of somewhat more than 600 second-feet joins the underground store. Seepage measurements which have been made at different times in both valleys from creeks and ditches offer concrete demonstrations of the manner in which the underground supply is maintained. Only a few such measurements have been made in Utah Lake Valley, but it has been shown that in IJ miles the Timpanogas canal lost slightly more than 25 per cent of the water taken in at its head.a Another set of measurements has been made on Provo River. The discharge a short distance above the mouth of the canyon was found to be 175.04 second-feet; at a station a mile west of Provo the river was dry, while the sum of several intermediate diversions amounted to 186.22 second-feet. The difference — 11.18 second-feet — represents the return seepage from the various canals. & In the valleys of creeks tributary to Jordan River more measurements have been made, of which those in Big Cottonwood and Mill valleys are typical. In Big Cottonwood Creek Valley Mr. E. R. Morgan selected for measurement two sections of the creek on which different conditions exist. In the upper section, immediately below the mouth of the canyon, the bed of the stream is composed of large loose bowlders resting on coarse gravel, and the land on either side is covered with comparatively scanty vegetation. In the lower section, below the head of Green ditch, the bed of the creek is comparatively smooth, and the land on both sides is irri- gated and covered with abundant vegetation The loss in the first section, in a distance of 2^ miles, was 7.36 second-feet, a percentage of 22 6, while in the second section, also 2| miles long, the loss was only 0.30 second-feet, a percentage of 2.4.c In Mill Creek Valley Mr. Morgan also made measurements in two sections where different conditions exist. In one section, 2 miles long, he found a loss of 22.7 per cent; in the other, three-quarters of a mile long, he found a loss of 3.6 per cent.d While seepage from the flow of the creeks and canals furnishes the chief supply of under- ground water to the valleys of Utah Lake and Jordan River, other sources are the underflow of the creeks at the mouths of the canyons, springs from bed rock, seepage at the base of the mountains, and the small addition, already mentioned, derived from rainfall on the valley. The underflow of the creeks at the mouths of the canyons is an important source, but the amount thus contributed is unknown. The quantity equals the remainder after subtract- ing the sum of run-off and evaporation from the precipitation, of which factors only the run-off is established, the precipitation being only approximately and the evaporation not at all known. The amount of the underflow can be directly determined, however, by a series a Bull. U. S. Dept. Agric. No. 124, Office Expt. Stations, 1903, p. 123. 6 Ibid., p. 126. c Morgan, E. R., Irrigation in Mountain water district, Salt Lake County, Utah: Bull. U. S. Dept. Agric. No. 133, Office Expt. Stations, 1903, pp. 60-61. d Ibid., pp. 44-45. U. S. GEOLOGICAL SUftvSv WATER-SUPPLY PAPER NO. 15? PL. V :^^ 3 7 8 eS ^ =^^^:^ ^^§ es 11 ---"---" ^-.zr-Ii--^ ss= •:-.«°o°o.-. .''/v'°=o " • '; '■'.-;■ ^^-- 13 14 15 Si==£^= -i^^ii ^XX^^ ^ o \'P °. = §=^3^r- y- —.. — [■/■■■r:\'.:': 22 23 24- 20 ^^ EXPLANATION W Soil Clay Sand Dark clay Coarse sand Sandy clay Fine sand Clay Quicksand Sand and gravel Hard clay Gravel Hardpan Clay and gravel Scale 60 loofoet '~^"£" i^g ^-,-~z^ '-'2^^. •"„}'" oj- s 3 C 1 WELL SECTIONS. No. 1, Oregon Short Line well at Kaysville; No. 2, Southern Pacific Company's well at Strongs Point; Nos. 3-24, location shown on Pis VII and VIII. SOURCE AND DTSTRrBUTION. 29 of measurements which should be made in estinmt ing the feasibility of constructing sub- surface dams. The amount of water cont'-ibuted to the valleys from bed-rock sources is also important. A remarkable series of thermal springs is a.ssociated with the great fault at the western base of the Wasatch Mountains. These occur at intervals along the entire extent of the range, and other warm springs, which may also })e connected with faults, are located within the area under consideration. Association with faults suggests a deep- seated origin, which accounts for the high temperature of the water. The last source of the valley water supply to be mentioned is the comparatively small amount which is derived by seepage from the base of the mountains from areas that are not drained by creeks. DISTRIBUTION OF UNDERGROUND WATER. From the outline of the geology given on pages 7-13 it will be seen that the valleys of Utah Lake and Jordan River are occupied by a considerable but unknown thickness of gravel, sand, and clay derived from the disintegration of the adjacent mountains and deposited in the valley under alternating subaerial and lacustrine conditions. In general, the deposits are arranged in broad, sheet-like accumulations, the coarser-textured materials abounding adjacent to the highlands and the finer debris preponderating farther out. The beds lie practically flat in the center of the basins, but are inclined slightly away from their source, the attitude of deposition being practically unaltered. Conditions of deposition, however, were so varied that over large parts of the area considered the deposits are not widely uniform. For instance, while clay was being laid down in one place sand was accumulating in an adjacent area and at their border the two deposits were merged. Consequently the arrangement of the beds is broadly lenticular, as is illustrated by the well records (PI. V). No two records are exactly alike, and in most cases it is impossible to correlate deposits in the different sections. Beds of clay are most widely distributed, but the more localized accumulations of sand and gravel, which are the most important reservoirs of underground water, are irregularly distributed. Underground water derived from the sources stated above occupies the spaces between the solid particles of the clay, sand, and gravel which constitute the valley filling. In general, these deposits are saturated below the horizon which marks the surface of ground water. The position of this surface varies, depending on the supply, on the ajnount used or the intensity of evaporation, and on the character and slope of the sediments. The water is seldom stagnant, but tends to flow with extreme slowness from a higher to a lower level, the chief factors in the movement being the number and size of the interstitial spaces in the deposits and the pressure gradient due to gravity. The highest velocity of ground water ever determined is about 100 feet in twenty-four hours, but the ordinary velocity is mucli less than this, common rates in sand being between 2 and 50 feet a day. The fluctuation of the surface of ground water is considerable. Since the chief replen- ishment of the supply occurs when the creeks discharge the most and when the irrigation canals are in full operation, ground water occurs nearer the surface in summer than in winter. Conditions in different areas cause a varied annual range, but 10 feet is connnon and 15 feet is not infrequent. In addition to the annual fluctuation a cumulative change is in progress, the ground-water surface being graduall}^ raised in the lower parts of the valley in consequence of irrigation and the custom of allowing artesian wells to flow uncetis- ingly, leading to swampy conditions in the valley bottom. Details regarding these changes arc given on subsequent pages. PI. VI illustrates the approximate average depths at which ground water occurs in the valleys of Utah Lake and Jordan River. The boundaries between the did'erent areas fluctuate andean not accurately be determined. A narrow belt contiguous to the base of the mountains is left blank on the map because of the varying and often unknown condi- tions that exist there, owing to seepage and the irregular distribution of water in the adjacent bed rocks. In the absence of topographic maps the position of the water table can not be shown by contours. Below the surface of ground water the saturated beds contain varying amounts, depend- ing on the character of the deposits. Coarse-textured gravel and sand, having a greater porosity than fine-textured clay, hold and transmit relatively more water. Beds of sand and gravel therefore constitute the chief underground reservoii-s. Typical illustrations of the distribution of sand and gravel are shown in PI. V. In sinking wells in this region, beds 30 UNDERGROUND WATER IN VALLEYS OF UTAH. of sand and gravel, ranging from a few inches to a hundred feet or more and separated by- varying thicknesses of clay, are encountered, water being commonly found in each porous deposit. Because of the prevailing inclination of the deposits away from the mountains, and of the presence of relatively impervious beds of clay above more porous sand and gravel, the contained water is under pressure. In the lowland areas this pressure is suffi- cient to cause the deep-seated water, when it is reached in a well, to rise and flow at the surface, and consequently artesian water is an important source of supply. Above the lowlands, where the surface elevation is too great for a flow to occur at the surface, the water rises in deep wells to a greater or less height according to the amount of pressure. aTTALITY OF UNDERGROUND WATER. The accompanying analyses, gathered from a number of sources and reduced to common terms, illustrate the character of the water in the valleys of Utah Lake and Jordan River. of water from streams and springs in valleys of Utah Lake and Jordan River.O' [Parts per million.] No. Source and date. Ca. Mg. Na. K. AI2O3 FezOa Si02. SO<. HCO3. CO2. CI. Total. CREEKS. 1 1 City, Dee., 1882. 55.3 18.9 2.6 24.3 2.0 19.9 7.3 95.1 19.5 244.9 2 Red Butte, Dec., 1882 88.8 31.3 • 25.6 Trace 3.3 35.2 100.6 108.8 22.9 416.5 3 Emigration, Dec, 1882 101.0 31.6 18.1 9.9 2.6 24.4 126.2 102.7 28.6 445.1 4 Parleys, Dec., 1882 85.1 22.5 31.5 2.6 1.8 27.2 56.5 122.1 19.7 369.0 5 Big Cotton- wood, Oct. ,1884 48.1 18.9 Trace. 8.6 1.6 12.6 42.1 63.6 7.9 203.4 6 Little Cotton- wood, Oct., 1884 17.5 8.2 5.9 1.7 1.3 39.9 12.3 32.2 2.8 ' 121.8 7 Dry Cotton- wood 17.0 45.0 27.0 24.0 15.0 4.0 14.0 10.0 34.0 42.0 121.0 145.0 14.0 Trace. 242.0 8 American Fork . 270.0 9 Payson 12.0 17.0 22.0 3.0 32.0 121.0 14.0 221.0 10 Santaquin 12.0 31.0 31.0 5.0 33.0 212.0 14.0 338.0 11 Currant Warm 47.0 114.0 54.0 48.0 89.0 381.0 44.0 92.0 115.0 114.0 181.0 333.0 15.0 28.0 211.0 703.0 756.0 1? 1,813.0 RIVERS. 13 Provo 51.0 68.0 29.0 36.0 28.0 46.0 22.0 17.0 44.0 64.0 205.0 277.0 28.0 28.0 397.0 14 Spanish Fork.. . Jordan: 1 536.0 15 Utah Lake (outlet), 1899. 67.6 13.8 233.7 2.0 236.7 23.7 316.5 894.0 16 Salt Lake Citv (near), 1899. WARM SPRINGS. 111.8 13.7 251.1 334.5 Trace 378.9 1,090.0 17 Salt Lake City, Oct., 1881... 535.2 138.4 3,039.0 178.0 0.7 21.3 787.5 442.9 4,968.0 10,284.0 18 Beck's (hot).. 694.3 109.5 3,754.9 196.9 9-0| 31.5 840.5 204.5 6,743.8 12,584.9 19 Sandy (8mi. s.). Mar. 1882 UTAH LAKE. 141.5 27.7 405.0 55.0 5.1 50.5 53.8 272.7 635.6 1,658.0 ?n 1883 55.8 67.0 18.6 86.0 17.7 230.0 2.0 22.0 10.0 28.0 130. 6 378.0 194.0 60.9 11.0 12.4 308.0 ■^l 1904 337.0 1,353.0 a Authorities.— Nos. 1-5, 17, 19, Kingsbury, J. T. Nos. 6-14, Soil survey of the Provo area, Utah: Bureau of Soils U. S. Dep-t. Agric, 1904, p. 22. Nos. 15, 20, and 21, Cameron, F. K. Water of Utah Lake: Jour. Am. Chem. Soc, vol. 37, No. 2, 1905. No. 16, ibid.. Kept. No. 64 U. S. Dept. Agric. No. 18, Riggs,R.B., Bull. U.S.Geol. Survey No. 42, 1887, p. 148. No. 20, Clarke, F.W. No. 21, Brown, R.E. . S. GEOLOaiCAL SURVEY WATER-SUPPLY PAPER NO. 157 PL. EXPLANATION ] Area in wh/'c/i grouna/ wafer //es \ wfh/r? /Ofeefoffhe surfcyce \ Area in w/iic/i groi/nc/ wo/er //es \ befwee/? /Oanc/ 50 feet b e/ofv the surface \Area inivhici) grounc/wa/er/ies surface Base of mountains, approximofe pos/fon offfeBonnei//ffe sfore f/ne SKETCH MAP SHOWING DEPTH TO GROUND WATER IN THE VALLEYS OF UTAH LAKE AND JORDAN RIVER. QUALITY OF UNDERGROUND WATER. 81 The average of analyses of 12 streams « coming from the Wasatch Mountains shows a total solid content of 319 parts per million, ranging from 122 to 536, the varying character of the water being duo to differences in the rocks of the respective watersheds. Examina- tion of these analyses shows that calcium is usually the most abundant base, with magne- sium a poor second, while sodium and potassium generally are much less plentiful and vary in relative amounts. Among the acid radicals, carbonic commonly preponderates, being often several times more abundant than the others; sulphuric ranks next, and in a few streams is important, while chlorine is generally of minor occurrence. Little Cotton- wood Creek ranks first, having only 121.8 parts per million of dissolved solids. It flows for most of its course through granitic rock and therefore contains but little calcium car- bonate. The total solids in Big Cottonwood Creek water are also low and relatively little lime is present because a large part of the drainage is over silicious rocks. The great abundance of limestone on most of the watersheds accounts for the abundance of calcium carbonate. Red Butte, Emigration, and Parleys creeks make a relatively poor showing, the sulphates being especially abundant, because these streams flow over Permo-Carbon- iferous and Mesozoic rocks containing more or less gypsiferous matter. Provo River and Spanish Fork drain large areas occupied by a variety of rocks, among which limestone is prominent, and the analyses show rather high amounts of total solids, the carbonates being particularly abundant. Currant and Warm creeks are exceptional. The unusual amount of sodium chloride present in Currant Creek is derived from salt deposits above Nephi. Warm Creek rises in the springs west of Goshen, and the character of its water, like that of similar springs in this area, is due to unusual conditions. The few analyses of the thermal springs in the area under consideration show the presence of abundant dissolved salts, of which the chlorides are the most plentiful, though consid- erable quantities of sulphates and carbonates are also present. Sodium is several times more abundant than any other base, calcium ranks second, and magnesium and potassium are present in small amounts. Some of the hot springs contain considerable hydrogen sulphide. Most, if not all, of these springs are associated with faults and have a deep- seated origin, to which their temperature and composition are due. The mineral matter is leached from the deposits through which the waters pass, much of the salt content being probably derived from old lake beds. Analyses of water from flowing wells are similar to those of surface streams. Different wells give different results, the quality of the water varying with the source and the nature of the deposits passed through underground. Analyses from the "Murray" and "Ger- mania" wells show an unusually small content of total solids, while those from the wells of the Utah Sugar Company at Lehi and near Provo show amounts above the average. In the area contiguous to Great Salt Lake the well water contains considerable salt, but no analyses were obtained. In general the water from flowing wells is of admirable quality and often forms a marked contrast to the supply from shallow wells. a Omitting Currant and Warm creeks, which are exceptional. 32 UNDERGROUND WATER IN VALLEYS OF UTAH. Analyses of water from wells, etc., in valleys of Utah Lake and Jordan River. f' [Parts per million.] No, Source and date. Mill Pond at Lehi, July ,1895 Artesian well,Murray Plant; Am. Smelting and Refin- ing Co Artesian well, Germania Plant, Am. Smelting and Refining Co U. S. Mining Co. well, Bing- ham Junction, Aug., 1902 U. S. Mining Co. well. West Jordan, Aug., 1902 Wm. Cooper's well, Bing- ham Junction Beet-cutting station, Utah Sugar Co.well,near Provo. Jan., 1899 '. Artesian well, Utah Sugar Co., Lehi, Jan., 1899 R. G. W. Rwy. well, Spring- ville, May, 1901 R. G.W. Rwy.well, Goshen, May, 1901 Ca. Mg. Na. AI2 O3. Fe2 O3. 16.0 1 2.4 1 1.2 5 Tr. 4 90 SiOz. 14 9.7 14 13 16 58 12 18 80 SO4 dl96 dl4 dl2 d50 dl6 154 41 47 CO3. ?>135 42 64 56 c30 66 C180 c91 120 127 CI. 68 Na2 CO3 K2 CO3. 124 Na2 SO4 K2 SO4. Tr. 6.8 27 44 45 116 Na CI KCl, 152 28 87 58 87 103 287 Total sol- ids. 114 140 290 232 284 056 648 aAuTHORiTiES.— Nos. 22, 28, and 29, Dearborn laboratories. Nos. 25 and 26, Converse, W. A. No. 27, J. H. Parsons Chemical Co. Nos. 30 and 31, De Bernard, J. H. b From MgCOs. c From CaCOs and MgC03. d From CaSO^. No analyses of ground water obtained from shallow wells are available, but the general character of such water is known. In the upland areas above the canals the water from shallow wells is much like that commonly obtained throughout the region in deeper ones; it contains a moderate amount of dissolved salts, largely calcium carbonate, and is usually of good quality. But in the lowlands the surface water is quite different, generally con- taining considerable dissolved salts, among which alkalies are abundant. Where ground water lies within the scope of capillary attraction from the surface, evaporation causes the mineral matter which is held in solution to accumulate, and in this manner the soil becomes tainted with alkali. Consequently the water from surface wells in the lowlands is charac- teristically rich in dissolved salts. Abnormal conditions prevail locally in the vicinity of the smelters in Jordan Valley south of Salt Lake City. Smelter smoke has lately become a nuisance to farmers by injuring crops and animals in the path of prevailing winds. Sulphur dioxide is the most abundant deleterious substance contained in the smoke, and to a minor extent locally finds its way into the water supply. Occasionally also ground water may become poisoned from accumulations of flue dust containing copper and arsenic, a Natural gas occurs in a number of water wells in the area under consideration. Well drivers report the common presence of vegetable matter, chiefly fragments of wood, at different depths in many localities. This was entombed in the old lake deposits, and its decomposition may account for the origin of the gas. Though gas occurs in numerous wells it has been found in quantity in only a few localities, the greatest development occur- ing near the shore of Great Salt Lake, about 12 miles north of Salt Lake City, b Here several wells were drilled averaging about 500 feet in depth; and from September, 1895, a Widtsoe, J. A., Relation of smelter smoke to Utah agriculture: Bull. Agricultural College of Utah No. 88, 1903. b Richardson, G. B., Natural gas near Salt Lake City: Bull. U. S. Geol. Survey ll, to a depth of 1,073 feet. This is the deepest well in the area undei' consideration, and its record (p. 42), as given by the driver, Gus Westphal, is as follows: a A soil survey in Salt Lake Valley: Bull. U. S. Dept. of Agriculture No 64, 19fK). 1^ Boutwell, J. M., Oil and asphalt prospects in Salt Lake basin: Bull. U. S. (;eol. Survey No. 2(iO, p. 47L 42 UNDEKGROUND WATER IN VALLEYS OF UTAH. Record of Rio Grande Western Railway Company's well at Salt Lake City. Thickness in feet. Thin strata of clay and sand 130 Clay and hardpan 40 Red sand 30 Clay and hardpan. . . 60 Gray sand 5 Clay and sand 44 Sand 8 Clay 20 Sand 13 Hard clay 6 Sand 8 Clay 10 Sand 18 Clay 20 Sand 4 Clay 10 Blue sand 12 Clay 5 Blue sand 30 Hard clay 10 Sand and gravel 1 Clay 12 Gravel 4 Gray sandy clay 28 Tough blue clay 30 Hardpan 3 Depth in feet. 1-130 130-170 170-200 200-260 260-265 265-309 309-317 317-337 337-350 350-356 356-364 364-374 374-392 392-412 412-416 416-426 426-438 438-443 443-473 473-483 483-484 484-496 496-500 500-528 528-558 558-561 Thickness in feet. Sand Soft blue clay Sandy blue clay Hardpan Sand Sandy gray clay . . . . Red sand Gravel Blus clay Clay and sand, alter- nating every 12 or 18 inches Hardpan Sand and gravel Blue clay Gray clay Sandy gray clay . Quick sand Blue clay Sandy blu3 clay Quicksand Gray clay Fine blue sand Tough blue clay Hardpan Fine sand. Hard blue clay 40 40 2 16 18 36 10 76 84 8 11 16 24 13 15 21 11 10 11 3 12 2 21 4 Depth in feet. 561-569 569-609 609-649 649-651 651-667 667-685 685-721 721-731 731-807 807-891 891-899 899-910 910-926 926-950 950-963 963-978 978-999 999-1,010 1,010-1,020 1,020-1,031 1,031-1,034 1,034-1,046 1,046-1,048 1,048-1,069 1,069-1,073 Although the general composition of the old lake deposits is known, not enough informa- tion has been accumulated to enable very definite statements to be made concerning the detailed distribution of the sediments. A comparison of available well records shows that the alternating bads of sand, clay, and gravel, generally, can not be recognized as being equivalent in the several wells, and from the present evidence it appears that while there are great thicknesses of both sand and clay, which must have a more considerable lateral extent than the beds nearer the mountains, the lake deposits are lenticularly arranged. Sinc3 no correlation has been established, the structure of the lake deposits is not known. Apparently they are approximately horizontal, but with a. slight inclination toward the lake from the highlands. This is indicated by the pressure obtained in artesian wells and is proved in a few instances by well records. In the broad lowland west of Jordan River there is an abundance of water. Throughout practially all of this area ground water lies within 10 feet of the surface, and water is con- tained in the underlying deposits down to an unknown but considerable depth. Apparently flowing wells can be obtained anywhere within this area. Although the water is so gen- erally distributed, it is profitably recovered only from the more porous, coarser textured deposits of sand and gravel, which constitute natural reservoirs and in which the water moves more readily. Accordingly, water is found at several horizons in the course of , sinking a deep well. In the Rudy well, for instance, 1,002 feet deep, situated in sec. 5, T. 1 N., R. 1 W., 25 water horizons from which surface flows were obtained are reported. A record of this well is not available, but "good strong" flows besides minor ones were recorded, respectively, at 400, 508, 685, 753, and 881 feet. Though water is so abundant, this lowland region is thinly populated, the chief drawback to its settlement being the presence of much alkali in the soil over a considerable part of OCCURRENCE OF UNDERGROUND WATER. 43 the area. The Bureau of Soils of the United States Department of Agriculture, in coopera- tion with the Utah p]xperinient Station, is at present engaged in a d(>nionstration of the feasibility of reclaiming this land on a farm 3 miles west of Salt Lake Cit}'. But by no means all of the soils in this lowland area contain excessive amounts of alkali," especially along Jordan River and adjacent to the border between the lowland and highland areas there are thriving settlements. The map and list of wells show general conditions. The wells are grouped along the margins of the area, and few are located in the interior. In general they are 2 inches in diameter, but they vary in depth greatly. Although flows are obtained locally at only 30 feet bck)W the 'surface, 'commonly they are not encountered above 150 feet. Perhaps the avei-a^e well is between 200 and 300 feet in depth. It is a striking fact that flows may be obtained throughout the entire area at similar, but not at regular depths, indicating only a slight inclination of the water-bearing horizons and their lenticular character. The flows are usually small, averaging perhaps under 5 gallons a minute, though there are a number of 15-gallon flows. The supply generally is reported rather constant, except that the shallower well& a?e sirbject to seasonal variation. The pressure obtained, too, generally is small, being only enough to cause the water to rise either barely to the surface or a few feet above. In general the pressure and the flow are reported to increas.^ with the depth but measurements are not available. Both the flow and the pressure are considerable in the deep Rudy well, sec. 5, T. 1 N., R. 1 W. The conditions here noted apply mostly to the areas contiguous to the eastern and southern borders of the lowland west of Jordan River. Little information is available concerning the rest of this area (see list of wells pp. 59-75.) The few wells near Great Salt Lake were sunk to unusual depths beforeflowing water was obtained, this being apparentl}' due to the greater development of clay in that region, though no complete logs have been kept. The well at the Inland Crystal Salt Company's works, in which, at a depth of 560 feet, water was struck which rises about 9 feet above the surface and flows about 10 gallons a minute, is reported 720 feet deep. Underground water in the Pleistocene deposits near the lake contains considerable salt. EAST OF JORDAN RIVER. East of Jordan River the occurrence of underground water will be described under the following heads: Salt Lake City, lowland area south of Salt Lake City, and upland area south of Salt Lake City. SALT LAKE CITY. Salt Lake City is built principally on the floor of the main valley, ))ut its outskirts extend northward on the old delta of City Creek and eastward on the benches at the base of the Wasatch Mountains. Adjacent to the highlands the underlying deposits are very irregular in composition and distribution, consisting of sand and gravel with intercalated streaks of clay. But toward the valley proper the conditions become more regular and the prevailing clay is interbedded with sand and gravel, though from the records obtained no definite sequence appears to be applicable to any considerable area. In the lower purt of the city marshy areas occur, but conditions there have been much improved since the early days of settlement. Formerly the lower chaimels of City, Red Butte, Emigration, and Parleys creeks were ill defined and at high-water stage the part of the city adjacent to Jordan River was a great slough. But by erecting embankments, by confining the creeks to definite channels, and by draining the western part of the city much of the swampy land has been reclaimed. Shallow ground water, except on the benches, generally lies within 10 feet of the surface. The line separating flowing and nonflowing wells skirts the lower benclu's, so that in the larger part of the area occupied by the city artesian wells are obtained: Flows are found oSoil survey in Salt Lake Valley: Bull. U. S. Dept. Agric. No. 64, 1900. Reclamation of Alkali anda: Fifth Rept. Bureau of Soils, 1903, p. 1144. 44 UNDERaROUND WATER IN VALLEYS OF UTAH. at different horizons from about 50 feet downward, a common depth of wells being between 100 and 300 feet. The deepest well is that of the Rio Grande Western Railway Company near its station, the record of which appears on page 42. This well is 4 inches in diameter and 1,073 feet- deep. It was put down in 1895 and 15 horizons were passed through from which flows were obtained. At a depth of 1,048 feet the greatest flow occurred, amounting to 78 gallons a minute at 4 feet above the surface and to 37.5 gallons at ,25 feet above. The most notable group of wells in this vicinity is that put down by Salt Lake City adjoining Liberty Park. There are 16 or more of these ranging from 2 to 9 inches in diameter and from 100 to 600 feet in depth. About half a dozen different water-bearing horizons, each furnishing a flow, are said to have been encountered in driving the wells. The greatest pressure reported caused the water to rise in a pipe 35 feet above the surface. Discharge measurements, as furnished by the city engineer, are given in the following table: Discharge of city wells near Liberty Parle, Salt Lake City. No. of well. 1.... 2.... 3.... 4.... 5.... 6.... 7.... 8.... 9..-. Diam- eter. Inches. 9 9 8 8 8 2 2 2 2 Date of measurement. No. of well. Diam- eter. Date of measurement. Aug. 10, 1890. - July 17, 1900. Sept. 29, 1902. Aug. 10, 1890. July 17, 1900. Sept. 29, 1902. Gallons. 201,600 180,000 279, 132 Gallons. 120,000 297,000 280,000 215,000 5. 000 Gallons. 96,941 60, 588 302,940 193,882 11,459 5,876 610 206 19,784 10.... 11.... 12.... 13.... 14.... 15.... 16.... Inches. 2 2 2 2 2 9_ 2 Gallons. 43,200 33,230 36, 000 54,000 Gallons. 38,000 19,000 16,000 35,000 18,000 98,000 6,000 Gallons. 35, 644 15,892 14,213 20,626 13,316 36, 172 2,844 59, 040 14,400 10.000 16,000 27,000 54,000 1,000 500 25,000 997,602 1,183,500 830,993 In the immediate vicinity of these wells there are a number of springs whose supply is maintained chiefly by seepage. The combined flow from these springs and wells is esti- mated to amount to a maximum of 2,500,000 gallons a day. In order to utilize this supply in the city mains a pumping plant would have to be installed, and a further dis- advantage is the doubtful quality of the water. At present this source is used for street sprinkling and for feeding the lake in Liberty Park (PI. I). In the northern part of Salt Lake City several thermal springs occur, the most conspic- uous of which are the hot and warm springs. The hot springs issue at a temperature of about 130° from the Wasatch limestone at the western end of the spur of the mountains, with a discharge of about three-fourths second-foot,a and flow into Hot Springs Lake. The warm springs issue from unconsolidated deposits at the base of the spur about 2 miles southeast of the hot springs. The water is pumped to a slight elevation, from which it is piped to a sanitarium, the amount delivered being reported to average 350 gallons a minute. The temperature is 118° at the springs and about 100° at the sanitarium. Several other similar, but less important, springs occur, associated with the great Wasatch fault, along the base of the mountains between hot and warm springs. The municipal water supply of Salt Lake City is derived from mountain streams and dis- tributed through city mains. From this source there is an excellent supply of pure water under good pressure. The chief near-by available streams are City, Red Butte, Emigra- tion, Parleys, Mill, Big Cottonwood, and Little Cottonwood creeks. The discharges of some of these are given on pages 19-22. None of these except City Creek is entirely con- trolled by the city. Red Butte Creek is reserved for the army post at Fort Douglas, Emigra- tion and Parleys creeks partly contribute to the city supply, and the others are used entirely for a Measured by A. F. Doremus. OCCURRENCE OF UNDERGROUND WATER. 45 irrigation and domestic purposes, under water rights owned hy farmers. In order for Salt Lake City to utilize these streams it must huy the water rights or exchange with the farmers an equivalent amount of water obtained either from Utah Lake or from pumping plants. The present public supply accordingly is obtained from City, Parleys, and Emigra- tion creeks. The watei-slied of City Creek is protected from forest fires and from contam- ination, and many of its springs are developed. The flow is distributed from settling tanks near the mouth of the canyon and from a reservoir on Capitol Hill having a capacity of approximately 1,000,(J00 gallons. The surplus waters of City Creek are allowed to escape through flood ditches. Water from Parleys Creek to the extent of 81.8 per cent of its flow has been obtained by Salt Lake City in exchange for an equivalent amount of water from Utah Lake delivered through the Jordan and Salt Lake City canal. A settling reservoir, holding somewhat less than 1,000,000 gallons has been constructed at the mouth of Parleys Canyon, whence the water is conducted through a concrete conduit to a storage reservoir with A capacity of about 5,000,000 gallons situated on Thirteenth East street. An addi- tional supply is obtained from a trench in the bed of Emigration Creek half a mile above the mouth of the canyon. This trench is approximately 150 feet long, 10 feet wide, and 18 feet deep. It was dug in sand and gravel in the bed of the creek and at right angles to its course. A supply estimated to amount to 1,000,000 gallons a day is thus obtained, which is piped to the Thirteenth East street reservoir. No direct record is kept of the amount of water used by Salt Lake City, but discharge measurements of the creeks at the mouths of the canyons show the amount available. This is insufficient during the dry months and the use of water is restricted to a per capita consumption of 120 gallons a day, although it is considered desirable, in this dry climate, where lawns and gardens have to be irrigated, to maintain a per capita supply of approx- imately 300 gallons a day. It is planned to obtain in the immediate future a portion of the flow of Big Cottonwood Creek, by exchanging therefor water from Jordan River, delivered through the City canal, as is being done in the case of Parleys Creek, and to make the new supply available by constructing a pipe line from the mouth of Big Cottonwood Canyon to the mouth of Parleys Canyon, a distance of about 7 miles. SOUTH OF SALT LAKE CITY. Lowland area. — It will be convenient to divide the area south of Salt Lake City into a lowland and an upland portion, taking as the dividing line that which separates flowing and nonflowing wells. PI. VIII shows that this line extends contiguous to, but below, the Jordan and Salt Lake City canal as far as Little Cottonwood Creek, after crossing which it turns westward to the flood plain of Jordan River. The lowland area is traversed by Parleys, Mill, Big Cottonwood, and Little Cottonwood creeks, which flow in open valleys, with broad and low intervening divides. The general aspect of the country is that of a slightly dissected plain that rises gently toward the upland terraces. This area is relatively thickly populated, and intensive farming is widely practiced. The detailed character of the underlying lake sediments is not satisfactorily known, but from the well records conditions appear to be similar to those found elsewhere in the area under consideration. Beneath the lowlands the stratigraphy is more uniform than nearer the base of the mountains; fine-textured sediments are more abundant than coarse, and clay predominates. But a comparison of available well records fails to establish a correlation between the difl'erent beds of sand and gravel throughout the lowland. Well drivers state that all logs are different, and yet that, on the whole, general sections persist for certain areas in which the difl'erences are minor. It is believed that the sediments slope toward Jordan River at about the same angle as does the surface. The best-defined sequence that has been reported occurs immediately south of Salt Lake City, where in general light-colored clay at the surface overlies blue clay ranging from 30 to 70 feet in thickness, beneath which water-bearing sands and gravels occur at a depth of about 100 46 UNDERGROUND WATER IN VALLEYS OF UTAH. feet. At greater depths the succession appears to be more variable, but there are few satisfactory well records. Ground water now lies within 10 feet of the surface over practically the entire lowland area, but it is reported that in the early days it did not lie so near over so large an area. Present conditions are largely due to irrigation. Several old residents state that below the level of the Jordan River canals the ground-water surface has locally risen 40 or 50 feet since their construction. It has already been mentioned that along several of the drainage ways seepage water reappears at the surface and occasionally forms considerable streams, as at Spring Creek near its junction with Big Cottonwood Creek, where the Septem- ber flow is estimated to amount to 14,000,000 gallons a day. In many places also, especially along the bases of benches, lines of seep springs occur that furnish considerable flows, a notable occurrence being those at the nursery in the southeastern part of Salt Lake City. But locally, as along the bluff east of Jordan River, north of the Bingham Junction smelters, the water appears at so low an elevation as to be of comparatively little use. When pumping becomes more generally practiced in the valley this ground water that lies so near the surface can be easily developed. Flowing wells in this area are numerous. They are generally 2 inches in diameter and 100 to 400 feet in depth, and they commonly yield between 20 and 50 gallons a minute, though there are many variations. The pressure is low, generally less than '10 pounds. Well drivers say that their best results are obtained in belts extending northwest and southeast, parallel with the creeks, and that these productive belts are separated by rela- tively barren ones. The water-bearing sands and gravels apparently mark the courses of old waterways, while finer-textured material was deposited in the intervening areas. These distinctions have been noticed only in the upper parts of the lowland area, and near the river they are said to disappear. One of the best wells is at the plant of the American Smelting and Refining Company at Murray. It is 4 inches in diameter, 400 feet deep, and is reported to flow about 400 gallons a minute under a pressure of 3 pounds per square inch. The record of this well is given as follows, on the authority of H. F. Yeager, well driller: Record of American Smelting and Rejining Company's well at Murraij. Thickness in feet. Sand and gravel 5 Mud 3 Sand and gravel 4 Blue clay 6 Quicksand 10 Blue clay 8 Loose sand and gravel (good pump well at 42 feet) 16 j31ue clay 8 Quicksand (flow at 63 feet) 6 Blue clay 18 Yellow clay. 6 Loose sand and gravel (strong flow at 95 feet) 15 Yellow clay 3 Coarse gravel and rock (strong flow at 112 feet, and at this point the well at office stopped flowing). 8 Coarse gravel and rock 6 Quicksand 20 Clay, very hard 10 Quicksand 6 Gravel (small flow at 165 feet) 11 Depth in feet. 0-5 5-8 8-12 12-18 18-28 28-36 36-52 52-60 60-66 66-84 84-90 90-105 105-108 108-116 116-122 122-142 142-152 152-158 158-169 Thickness in feet. Hard pan, very hard 8 Blue clay 6 Quicksand (flow at 203 feet) . . 20 Quicksand 16 Blue clay 4 Quicksand 7 Blue clay . 8 Quicksand 18 Blue clay and quicksand in layers 2 feet thick 22 Quicksand . 8 Blue clay, very hard 12 River sand 2 River sand 7 Cemented gravel 12 Yellow clay . 7 Cemented gravel 17 Loose gravel 23 Yellow clay 2 Gravel. 7 Cemented gravel 12 Loose gravel 12 Depth in feet. 169-177 177-183 183-203 203-219 219-223 223-230 230-238 238-256 256-278 278-286 286-298 298-300 300-307 307-319 319-326 326-343 343-366 366-368 368-375 375-387. 387-399 OCCURRENCE OF UNDERGROUND WATER. 47 Decrease in flow and complete failure of some wells are reported throughout this area and are especially apparent in the vicinity of Murray. These results are directly traceable to the increased number of wells that have been sunk in recent years and to the fact that little economy is exercised in the use of the water. Well owners should more fully realize that the limited water supply comes from a common source, that the wastefulness of one counteracts the prudence of another, and that the common interest of all demands that the supply be conserved. Upland area. — The upland south of Salt Lake City includes the area lying between the base of the Wasatch and Traverse mountains and the area in which flowing wells can be obtained. This region is characterized topographically by the abundance and perfection of development of shore phenomena which mark different stages in the history of Lake Bonneville. As on the western side of the valley, the upland is in general a plain that rises toward the base of the mountains, but is interrupted by benches and escarpments and deeply cut by the creeks flowing from the Wasatch Mountains. The Bonneville terrace extends along the mountains like a narrow shelf, its horizontal lines contrasting strongly wdth the deep, vertical furrows on the mountains. Broad deltas formed by the larger creeks at the Provo stage extend down to the lowlands, and successive escarpments mark halting places in the retreat of Lake Bonneville. The most prominent of all the shore phenomena in the area covered by this report is the great embankment at the point of the mountains east of Jordan Narrows. Here the waves, gaining energy from the wide expanse of the old lake, carved a great sea cliff against the mountains and distributed the debris to form an enormous accumulation of sand and gravel. Prominent local features of this upland belt are the relics of glaciers adjacent to the mouth of Little Cottonwood Canyon and the evidences of recent faulting along the base of the mountains. Little Cottonwood Creek in Pleistocene time was occupied by a glacier which carved a broad U-shaped valley and deposited lateral and terminal moraines composed of a heterogeneous mass of coarse- and fine-textured debris. Along the entire front of the Wasatch Mountains Gilbert has found indications of recent dislocation associated with the great Wasatch fault. The evidence is varied, but escarpments in unconsolidated material breaking the even trend of alluvial slopes are conspicuous. The underlying deposits of the upland are mostly coarse textured, being near their origin, and consist chiefly of sand and gravel. The creeks, where they have cut deeply, expose good sections, but few deep-well records were obtained. This region in general is thinly populated, but where water is available there are settlements, and wherever the canals extend there are thriving farms. The contrast between the flourishing area which is supplied with water and the dry, barren region is striking. The map shows the distribution of the principal canal systems, which are supplied by the several creeks that flow from the Wasatch Mountains and by Jordan River. Underground water is used only to a limited extent. PL VI and the list of wells illustrate conditions. Under- ground water is recovered chiefly in the lower (western) part of the upland, where it lies at depths ranging from the surface to 50 feet below. In this productive area both dug and driven wells are used. The driven wells are commonly 50 to 200 feet in depth, and water is generally found beneath a bed of clay in sand or gravel under sufficient pressure to cause it to rise within pumping distance of the surface. In the eastern part of the upland area ground water generally lies at a greater depth than 50 feet below the surface, and in a number of places has not been found in test wells over 100 feet deep. In this (eastern) division of the upland, where the greater part of the valley deposits are coarse textured, the ground water sinks deep before a relatively impervious bed is encountered, and then it tends to move to the lower part of the valley. Away from the influence of seepage from the creeks little water is supplied to this area. Between the creeks the chief source of supply is seepage from the mountains. The most likely localities for sinking wells are along the courses of waterways, but over a large part of the upland the prospect is poor for obtaining imderground water in quantity within easy reach of the sur- face. In the mouths of the canyons there is the chance of developing the underflow by 48 UNDEKGROUND WATER IN VALLEYS OF UTAH, subsurface dams or by tunnels, mentioned on page 40. Other favorable localities for pros- pecting are adjacent to the base of the mountains, where water may be had by developing springs and by tunneling into the bed rock. Seep springs occur at several localities along the base of the mountains south of Salt Lake City, the most important, perhaps, being those about midway between Mill and Big Cotton- wood canyons. The feeble springs there issuing from sand and gravel were formerly allowed to go to waste, but by developing them a flow of about 2 second-feet was obtained, and a considerable tract of land thus became available for agriculture. About 4 miles southwest of the town of Draper, in sec. 12, T. 4 S., R. 1 \7., at some distance from the base of the mountains, there are four warm-water lakes that are fed by springs, some of which are said to be quite hot. The westernmost of the group is the largest and covers an area of about 5 acres. The temperature is reported to remain at about 70° the year round. Since underground water is so scarce beneath the upland, the most efficient manner of developing this area appears to be by the use, as suggested above (p. 38), of creek water in high-level canals to a greater extent than is now practiced. UTAH LAKE VALLEY. The following description of the occurrence. of underground water in the valley of Utah Lake begins at the north and proceeds east, south, and west around the lake, the several towns affording subheadings for convenient reference. (PI. VIII.) LEHI AND VICINITY. Lehi is situated in the main valley at some distance from the distinct terraces. Dry Creek lies adjacent to the town, but, as its name signifies, the creek, after supplying a num- ber of irrigation ditches, usually carries little or no water in its lower course. There is no public water system in the town, and the supply for domestic purposes is derived from numerous wells. A few shallow dug wells tap ground water at depths of 5 to 30 feet, but the majority are deeper and reach water under pressure. The sugar-plant mill pond is fed by springs and is an important local source of supply. Lehi was one of the first towns where artesian water was found in the Bonneville area, flowing wells having been obtained there about 1880. Formerly a feeble first flow was found in gravel about 60 feet from the surface and a stronger supply at a depth of about 160 feet, but in recent years flows, even from the second horizon, have failed during part of the season in consequence of the increased use of artesian wells in the area nearer the lake, and at times pumping has to be resorted to. However, when water does not actually flow it rises in the wells to within a few feet of the surface. The general section in the vicinity of Lehi, as reported by H. C. Comer, shows blue clay to a depth of 50 or 60 feet. Below this is the first water bed, consisting of about 50 feet of sand and gravel, separated from the second water horizon by 40 feet of light clay. This section does not apply in the eastern part of the town, where the log of the San Pedro Rail- road well shows coarse-textured material within 100 feet of the surface. In this well the main supply is derived from a depth of 330 feet, the water rising to within a few feet of the surface. These two logs illustrate the variability of adjacent sections. The Utah Sugar Company's plant at Lehi has several 2-inch wells, and the following flows in gallons per minute are reported: 80 feet, 15 gallons; 120 feet, 25 gallons; 150 feet, 20 gallons. Logs of these wells were not kept. The Rio Grande Western Railway well near the sugar factory is 3 inches in diameter and 165 feet deep. The water is reported to rise in a pipe to a point 30 feet above the surface and to flow about 50 gallons a minute at the level of the ground. Toward Utah Lake, below Lehi, there is a considerable development of flowing wells from which a number of square miles are irrigated. In this district there are several hundred flowing wells which average about 150 feet in depth. A close relationship has been established between the flow of the wells in the fields below Lehi and those in town. MAP SHOWING THE AREA IN WHICH FLOWING WELLS ARE OBTAINED IN UTAH LAKE VALLEY. OCCURRENCE OF UNDERGROUND WATER. 49 During the irrigation season, when the field wells are all flowing, those in Lehi practirally stop, hut during the winter it is a general custom to plug the wells used for irrigation, after which those in town begin to flow. Measurements liavc not been made, but the general facts are well established. Northwest of Lehi the line separating the areas of flowing and nonflowing wells continues to Jordan River, reaching it 3 to 4 miles north of Utah Lake. The line extends about half a mile west of the river and approaches close to the northv/est corner of the lake near Sara- toga Springs. In the flood plain of Jordan River flows can probably be obtained continuing into Salt Lake Valley, but outside of the line indicated the surface elevation is too great. The Salt Lake City authorities, about 1890, sank a number of wells in the flood plain of Jordan River in sec. 12, T. 5 S., R. 1 W., with the object of increasing the supply of the Jordan and Salt Lake Canal. These wells, about 130 in number, were mostly 2 inches in diameter, though a few were 6 inches, and arc said to average 100 feet deep. Clay was encountered down to the bottom of the wells, which were in gravel. It is stated that water rose in pipes 30 to 40 feet above the surface, and that individual wells flowed 125 gallons a minute. It is also stated that the combined flow amounted to 3,000,000 gallons a day. These wells soon interfered with neighboring ones, stopping their flow, and suit was brought against the city, with the result that the municipality was compelled to plug up its wells. After these had been plugged for some time a number of them were tempo- rarily opened, and in about twenty-four hours thereafter the water in one of the wells, the flow of which was interfered with, situated about half a mile above the city wells, had fallen 25 feet. The city wells were then capped again and in five hours the water in the well referred to had regained 7 inches of its lost level. Near the northwestern end of Utah Lake there is a group of hot springs which occin* both on shore and in the lake. On the shore there are several springs which support the Saratoga resort where the water, having a temperature of 111°, issues through the lake deposits and is used for ])athing and to a limited extent for irrigation. In the summer of 1904, during the survey of Utah Lake by G. L. Swendsen of the Reclamation Service, three groups of springs were found beneath the water of the lake. Their existence was shown by the pres- ence of depressions occupying areas of 100 square feet to 3 acres in extent and having depths of 20 to 80 feet. Since the prevailing depth of the lake is much less and the bottom is com- posed of slimy mud, a considerable discharge is thus indicated. Hot water that flowed above the lake surface was obtained by sinking pipes a short distance into the bottom. About 5 miles up Dry Creek from Lehi is the town of Alpine, located near the mouth of the canyon on the dissected Bonneville terrace. The settlement is supplied with water from irrigation ditches, and possibly not more than half a dozen wells have been sunk. These are 25 to 80 feet deep, and the water level is reported to vary considerably between winter and summer. Springs occur in Dry Creek Canyon, but they have not been developed. AMERICAN FORK, PLEASANT GROVE, AND VICINITY. The towns of American Fork and Pleasant Grove receive their main water supplies, respectively, from American Fork and from Battle and Grove creeks. These streams feed a number of irrigation canals, and are the chief source of underground water in this vicinity. (PI. IX, B.) American Fork is built at the base of a series of terraces on both sides of American Fork (creek), which has cut a narrow chaiuiel through the old lake deposits. Ascending the valley from American Fork, five distinct terraces can be traced up lo the broad Provo bench, between which and the Bonneville level, which forms a shelving bench against the mountains, traces of shore lines of pre-Bonneville age have been reported. In its lower course American Fork is dry throughout most of the year in consequence of th(> draft upon its waters for the canal system which supplies the uplands. Shallow wells in American Fork are commonly less than 50 feet in depth, avcMuging possibly 25 to 30 feet, and the ground-water level is reported to vary 10 to 15 feet between the winter minimum and summer maximum. The water generally is found in gravel. IRR 157—06 4 50 (JKDERGTIOUND WATER IN VALLEYS OF UTAH. Deep wells have been sunk in the extreme southwestern part of the town in search of flowing water. The water rises in these nearly to the surface, and furnishes the main sup- ply for domestic purposes. Well records show a variable succession of sand and gravel, with comparatively little clay. The city well is typical, and probably is the deepest in this vicinity. It is 440 feet deep and 6 inches in diameter. Two principal water hori- zons are reported, at 240 and 340 feet, and the water stands in the well at a depth of 22 feet. An electric motor pump supplies water for public purposes, but there is no water- works system. Individual families or groups of famihes maintain their own wells. The line separating the areas of flowing and nonflowing wells as mapped between Lehi and Pleasant Grove lies contiguous to the San Pedro Railroad, and here, as elsewhere, ground water commonly lies within 10 feet of the surface. Extensive areas of marshy land lie contiguous to the lake shore, where conditions have grown worse since the intro- duction of irrigation. The flowing wells in this vicinity vary in depth, but are commonly about 100 feet deep. As Utah Lake is approached more nearly uniform conditions are revealed by the logs. Clay is commonly present at the surface and continues to a depth of 90 or 100 feet, below which the water-bearing gravel occurs. In the deeper wells alter- nating sand, clay, and gravel are reported below the first gravel, and flows are obtained from every coarse-textured bed. One of the best wells in this vicinity is in sec. 23, T. 5 S., R. 1 E. It is 147 feet deep, 2 inches in diameter, and throws a stream 3 feet 8 inches above the pipe, having a capacity, therefore, of about 150 gallons a minute. A disturbed belt of rocks, dipping eastward, and locally covered by debris, lies near the foot of the Bonneville terrace between American Fork and Grove creeks. Springs occur at about this horizon, and prospecting for water in this belt, in sec. 17, T. 5 S., R. 2 E., has brought notable results. William Wadley & Sons, by tunneling into bed rock, have developed enough water to irrigate a number of acres of fruit land, which is bringing in handsome returns. Several tunnels have been dug, the most important of which lies about 200 feet below the Bonneville level and was driven 318 feet through black shale into broken and cavernous gray limestone, in which the water occurs. Pleasant Grove is located on alluvial slopes formed by Battle and Grove creeks. Its situation is so high that flowing wells can be obtained only in the extreme lower part of the town, which depends for its chief underground supply on wells from which water has to be pumped. Ground water can usually be obtained at 10 to 50 feet from the surface. No regular sequence of deposits underlies the town, but a variable succession of clay, sand, and gravel is encountered in wells, the water horizon usually being underlain by clay. In the southeastern part of Pleasant Grove no successful wells have yet been obtained, though prospecting for them has extended to a depth of 100 feet; not deep enough to find an impervious stratum. A continuous succession of gravel beds is reported. The high, almost flat Provo delta between Pleasant Grove and Provo is scantily pro- vided with water. The surface is generally gravel covered, and gravel is commonly found in wells to depths of 30 to 60 feet, below which sand is reported. Only a small amount of clay appears to be present. This tract of land is well adapted for the cultivation of fruit, but the present supply of water is insufficient for its complete development. Water was first brought to the delta by canals from Provo River in 1868, and the present supply, whereby a maximum diversion of about 116 second-feet is obtained, was established in 1888. Before irrigation was practiced on the bench the depth to ground water was considerably greater than it is now. Old wells are over 100 feet deep, but of late years the ground- water surface has risen so that on a large part of the area water can be obtained in wells averaging 50 to 75 feet deep. Toward the lower margins of the bench the depths to ground water is less than 50 feet. Here, as elsewhere throughout this entire area, ground water is lowest in the winter and highest during the irrigation season. The annual variation on Provo bench appears to range from 5 to about 17 feet. A few examples will illustrate general conditions. In 1875 a dry well 100 feet deep was dug in sec. 14, T. 6 S., R. 2 E. In the same section, during the winter of 1878-79, N. Knight dug a well 110 feet deep which afforded 3 feet of water in winter and 15 to 20 feet in summer. In 1899 N. J. Knight U. S. GEOLOGICAL SURVE> WATER-SUPPLY PAPER NO. 157 PL. IX A. VALLEY OF PROVO RIVER BELOW MOUTH OF CANYON, LOOKING NORTH. Shows Provo Bench and Bonneville terrace. B. AMERICAN FORK AT MOUTH OF CANYON. OCCURRENCE OF UNDERGROUND WATER. 51 dug a third well only 60 feet deep, near the second, which afrordcd about 3 feet of water in ^\inte^ and 20 in summer.^ Flowing wells can not be obtained on the bench because of its elevation, though several attempts have been made, without success. In 1887 and 1888 two deep wells were driven in the same section as those just referred to. The Colorado Fish Company put down a 3-inch well 250 feet deep and obtained water which rose to within 80 feet of the surface. This was pumped for several years. In 1888 Mr. Knight drove a 2-inch well 300 f(>ct deep in which water rose to within 90 feet of the surface. Both of these wells are now abandoned. From Provo to Pleasant Grove along the narrow belt of lowland lying between Provo bench and Utah Lake there is an abundance of underground water. The line that sepa- rates flowing and nonflowing wells coincides approximately with the San Pedro Railway, which also marks roughly the upper limit of the area in which ground water lies within 10 feet of the surface. Between the railroad and the base of the bench few wells have been driven and little is known of the conditions, but it is thought that water can be obtained at depths of 10 to 50 feet. Contiguous to the railroad a number of feeble seep springs occur along the base of a low bluff between which and the lake the ground is almost flat. Water occurs on the surface in many places, rendering the land unfit for use. Before irrigation was so exten- sively practiced it is reported that this lowland belt was fertile farming land, but in late years, due to the rise of the ground-water level, the land has materially decreased in value. Considerable areas of available land, however, are yet to be found in this area, and flowing wells are used to irrigate several hundred acres. Conditions can be much improved by drainage. The map and list of wells show the general conditions. The deep wells in this belt average slightly ov^r 100 feet and generally are 2 inches in diameter. North of Provo River the yield is inconsiderable, averaging, possibly, less than 15 gallons a minute pel*- well; but in the vicinity of Geneva, a resort on the lake below Pleasant Grove, the effect of Battle Creek drainage is experienced, and some of the strongest wells of the entire area covered by this report occur. Harry Gammon's wells, in sec. 7, T. 6 S., R. 2 E., are among the best. One of these is 3 inches in diameter, 110 feet deep, and jHlelds a flow of about 266 gallons a minute, the water rising in a pipe to approximately 28 feet above the surface. The section in this vicinity is shown on PI. V, the water occurring in gravel in the bottom of the well. PROVO AND VICINITY. Provo derives its water supply from Provo River. A number of canals tap the river (as shown on the map, PI. VIII), and distribute a good supply to the town; and water for household purposes is delivered through city mains from a direct source in the river near the mouth of the canyon. The quality is unsatisfactory, however, and a new system is being installed whereby a better supply is obtained from a number of springs that issue from unconsolidated debris along the base of the canyon for several miles above its mouth. Well records show fairly uniform stratigraphic conditions about Provo. Gravel usually imderlies the surface to a depth of from 10 to 20 feet, and is succeeded by 20 to 30 feet of sand, below which is a considerable thickness of clay, averaging possibly KK) feet, the upper 20 or 30 feet of which is yellowish and the lower part blue. Underlying the clay a bed of gravel occurs, which is said to be underlain by clay, though about Provo it has sel- dom been penetrated. With minor variations this section appears to hold good over a large part of the territory adjacent to the east shore of Utah Lake. Northwest from Provo the surface gravel disappears, but clay, light above and dark below and underiain by sand and gravel, is reported in the vicinity of Geneva, American Fork, and Lehi. South of Provo, in the vicinity of Springville, similar conditions prevail. (PI. V.) "These facts were obtained from Mr. Caleb Tanner, to whom the writer is indebted for many courtesies. 52 UNDERGROUND WATER IN VALLEYS OF UTAH. The beds about Provo appear to dip toward the lake at a low angle, approximately cor- responding to the slope of the surface, this being indicated by the fact that the depth at which the water-bearing gravel, is found over large areas is approximately constant. In the vicinity of Provo some direct data were obtained on this point. Wells have been driven along Center street from Academy street in Provo westward to the shore of the lake. The depths at which the top of the gravel was struck in some of these wells was obtained from the driver, J. Westfall, and a line of levels was run along the surface by the United States Reclamation Service, from which it appears that the lakeward inclination of the gravel is approximateljT^ 9 feet per mile, the rate decreasing as the lake is approached. Similar conditions probably exist throughout the area studied, the slope being greatest near the mountains, while beneath the broad lowlands the strata lie more nearly horizontal. Ground water in the vicinity of Provo can generally be obtained in the upper gravel within 10 feet of the surface. In the vicinity of the lake the gravel disappears and clay generally occupies the surface. Here, as is so general throughout the entire area, swampy conditions prevail, owing to the lowness of the region, the recession of the lake, and the rise of ground water due to irrigation. Flowing wells exist in great numbej- in this well-populated region, and in general an abundance of good water is obtained within 200 feet of the surface. The main water-bear- ing horizon is the bed of gravel that underlies the blue clay. Water is generally reached in this gravel at ] 50 to 200 feet from the surface, but conditions are not absolutely uniform at all places, and where the prevailing section is varied by local streaks of clay, sand, and gravel corresponding differences exist. Feeble flows are sometimes found at 100 feet, and a few wells obtain water from a depth of 360 feet, but this depth is unusual in the vicinity of Provo. The wells about Provo are generally 2 inches in diameter, and their flow may possibly average 50 gallons a minute. Among the best wells in this vicinity are those at the stations of the San Pedro, Los Angeles and Salt Lake Railroad and the Rio Grande Western Railway. These are 3 inches in diameter and 190 and 176 feet deep, respectively. In November, 1904, the Rio Grande Western well was found to flow approximately 120 gallons a minute at 2 feet above the surface under a pressure of 15^ pounds per square inch. SPRING VILLE AND VICINITY. Between Provo and Springville the lowland contiguous to Utah Lake extends to the Rio Grande Railroad, above which the surface rises at a steep grade to the base of the moun- tains. The lowland for the most part is marshy, and the line that separates flowing and nonflowing wells lies only a short distance east of the railroad. A low scarp, which appar- ently marks a Pleistocene fault, can be traced immediately west of the county road for a mile or more beyond the Utah County Infirmary toward Springville. Springs occur at the base of the scarp, and the large springs at the head of Spring Creek may be associated with faulting. A number of small lakes mark the presence of these springs, and Spring Creek, whose main supply is thus derived, flows about 1,600 second-feet. The deepest well in this area is that of the infirmary, situated near the road about mid- way between Provo and Springville. The well is 3 inches in diameter and 270 feet deep, and water is reported to rise in a pipe to a point 3 feet above the surface, flowing about 30 gallons a minute. In this vicinity a feeble first flow is reported at depths of 65 to 80 feet. Springville is situated on the plain about 3 miles below the mouth of Hobble Creek Can- yon, the channel of the creek passing through the town. During the irrigation season practically all of Hobble Creek water is diverted by canals that head near the base of the mountains. Ground water in Springville is obtained from wells that usually range in depth from 20 to 30 feet, the water occurring in the top gravel. The general level of ground water in the town is reported not to have changed since the early days, and only an annual difference of a few feet is noticed between winter and summer conditions. a aStevenson, J. B., well driver. OCCURRENCE OF UNDERGROUND WATER. 53 Records of wells in the vicinity of Springville show rather uniform conditions. The town generally is underlain by gravel 5 to 40 feet thick, below which blue clay occurs to a depth of about 130 feet, underlain by sand and gravel down to 180 feet; then about 50 feet of light-colored clay is encountered, followed by sand and gravel at a depth of about 230 feet. In the area nearer the lake the top gravel generally is wanting, but otherwise similar sections are reported in that locality. Flowing wells are obtained from the two lower gravel horizons at depths of approxi- mately 130 and 230 feet. The common occurrence of water at these two horizons implies unusual uniformity of underground conditions, and suggests a low lakeward dip, approxi- mately corresponding to the surface inclination. The wells are commonly 2 inches in diam- eter, though a few are 3 inches, and they yield on an average possibly 20 to 50 gallons a minute. One of the best in Springville is a 3-inch well belonging to A. Cox. It is 230 feet deep, flows about 120 gallons a minute, and its water is reported to rise in a pipe to a point 18 feet above the surface. The Rio Grande Railway Company has two wells in Spring- ville, which are 216 and 304 feet deep. In the deeper the first flow was struck at 126 feet, a second at 216, a third at 260, and a fourth at 292. The shallower well is 3 inches in diam- eter, and is reported to flow about 200 gallons a minute at the surface, which is reduced to about 12 gallons a minute at the top of a tank about 30 feet above the surface. Mapleton Bench is the local name for the Provo Delta, lying between Spanish Fork and Hobble Creek. The delta is here prominently developed, and constitutes valuable farm- ing land. Flowing wells are not obtained on Mapleton Bench because of its elevation, but there are a number of dug wells. It is reported that in the early days the wells on the bench were 60 feet or more in depth, but since irrigation has been practiced the ground- water level has been considerably raised, and now the wells average possibly only 30 feet in depth. There is a- marked difl'erence in the depth to ground water in winter and sum- mer, the range in some instances amounting to over 10 feet. Along the outer margin of the bench there is a line of springs, many of which did not exist before the ditches were dug. Big Hollow Creek, a stream that flows from the bench about 2 miles south of Spring- ville, is a conspicuous example. In the early days scarcely an}^ water is said to have flowed in its channel, whereas it now irrigates over 100 acres. Considerable amounts of water are obtained by a few tunnels that have been dug along the eastern edge of Mapleton Bench. The entrances to the tunnels are commonly at the sites of springs. Some begin and end in unconsolidated materials, while others penetrate bed rock. The longest noted is in sec. 24, T. 8 S., R. 3 E. Its length i^ 275 feet. Water enough to irrigate about 100 acres comes through crevices in bed rock. SPANISH FORK, PAYSON, AND VICINITY. The town of Spanish Fork is situated on the general lowland at the base of Mapleton Bench and immediately north of Spanish Fork, about 5 miles- below the mouth of its canyon. From the few well records available it appears that sand and gravel com- monly underlie the surface to a depth of about 30 feet and are succeeded by 150 feet of clay, below which water-bearing gravel is usually encountered at a depth of 180 feet. The log of the well recently completed at the San Pedrd' station, about a mile west of the town, shows a greater thickness of clay, amounting to 205 feet, beneath which sand and clay were found to 390 feet, where water-bearing gravel occurs. Spanish Fork is rather poorly supplied with underground water. Dug wells commonly reach water at depths ranging from 10 to 25 feet, but its quality is not good. Flowing wells were formerly obtained, but in recent years the flows generally have ceased and pump- ing has to be resorted to. A city waterworks system was installed in 1904, the supply being derived from Evans Spring, near the mouth of Spanish Fork Canyon, about 5 miles above the towm, and an excellent supply is now available. The line separating flowing and nonflowing wells now lies in the extreme northwest corner of the town. The fii-st flow occurs at a depth of about 180 feet and a second flow between 350 and 400 feet. The cream- ery well, 2 iuchei in diameter and 220 feet deep, is typical. Water was struck at 180 feet 54 UNDERGEOUND WATER IN VALLEYS OF UTAH. which in 1900 flowed 9 gallons a minute, while iii 1904 it stood about 4 feet below the surface with little or no variation. In 1904 the San Pedro, Los Angeles and Salt Lake Railroad Company put down a well 415 feet deep at its Spanish Fork -station and obtained a flow of 36 gallons a minute through a 2-inch pipe from gravel in the bottom of the well. Between Spanish Fork and the Goshen divide there are a number of settlements that are adjacent to the line separating flowing and nonflowing wells. Salem is situated at the lower end of the Provo Bench, about midway between Spanish Fork and Payson. In the northwestern part of the town the water table lies close to the sur- face and throughout the greater part of the settlement water can be obtained within 10 feet of the surface. There are many springs, the most important of which supply Salem Pond, which covers about 13 acres and averages possibly 12 feet in depth. The line separating flowing and nonflowing wells passes about midway through Salem. The flowing wells are gen- erally feeble and the quality of the water is poor. A first flow is commonly obtained at about 160 feet and a second at about 250 feet. Payson is situated on and near the delta formed by Peteneet Creek at the Provo stage of Lake Bonneville, part of the town being built on the delta and part on the subjacent plain. Flowing wells are not obtainable because of the elevation, and the underground water supply is furnished by dug wells. These vary considerably in depth because of the irregular distribution of the delta deposits. Their depth ranges from 15 to 115 feet and probably averages between 30 and 40 feet. As an instance of local variation it may be mentioned that in one well ground water is obtained at 18 feet while on the opposite side of the street a well was dug 90 feet without encountering water. The level of ground water is reported to fluctuate but little. A number of families in Payson are supplied by pipe lines, the water being derived from tunnels driven into the base of the bench. The town of Spring Lake is situated near the base of the mountains. The line separating flowing and nonflowing wells passes along the foot of the Provo Bench and lies about half a mile west of the town. In this locality ground water is found commonly within 10 feet of the surface and there are a number of shallow w^ells, but the chief supply comes from springs. Spring Lake covers an area of about 12 acres and discharges a stream of about 2 second-feet. It is made by damming a small creek that is fed by springs. Springs occur in the vicinity of the base of the mountains between Spanish Fork and Spring Lake. Most of them appear to be seep springs, but some that lie near faults that adjoin the base of the mountains may be of deeper seated origin. Many of the springs flow 20 to 50 gallons a minute. Santaquin is built on a delta of Santaquin Creek, near the base of the mountains, far above the general level at which flowing wells are obtained. The town is chiefly supplied with water for both household and irrigation uses by Santaquin Creek, and only a few wells have been dug. About a dozen wells strike water in gravel at depths of between 15 and 25 feet on a low bench in the southeastern part of the town. Tunnels are also dug into this bench, from which two pipe lines supply a number of families with water. Below the bench in Santaquin there are very few wells; two had to be dug about 80 feet before water was obtained. Below the line separating flowing and nonflowing wells between Hobble and Santaquin creeks the valley plain slopes gently to Utah Lake. Throughout this area ground water lies within 10 feet of the surface, and adjacent to the lake and in certain isolated localities swampy conditions occur. This area is mostly underlain by clay, which is reported to predominate in all of the wefls. Little or no gravel is encountered in well driving and the layers of clay alternate with layers of sand. Few satisfactory well records from this region have been obtained, and no correlation of the underground deposits has been possi- ble. Different conditions seem to exist in neighboring wells, indicating a lenticular arrange- ment of the deposits. The towns of Palmyra, Lake Shore, and Benjamin are situated below the line of flowing wells. Many farms are scattered over this area, but in a few localities — north of Spanish Fork, for instance — alkali is so prevalent as to discourage settlement. Much of the water used in irrigating this tract is derived from canals supplied by Spanish Fork, but flowing wells also are used to a considerable extent. OCCURRENCE OF UNDERGROUND WATER. 55 Flowing wells have been obtained throughout this area at depths of 50 to 5(J0 feet, as shown by the list. Flows are usually found in every considerable bed of sand encountered in drilling, and six or more water-bearing beds are sometinus struck in a 40()-foot well. Shallow wells are not the rule in this i-egion, for, though many are 150 to 200 feet deep, the majority are nearer 400 feet deep. Because of the general absence of gravel and of persi.st- ent beds of sand there are few especially good wells. The flows obtained are generally under 50 gallons a minute and frequently are less than 10. The pressure is low, seldom being sufficient to cause the water to rise more than a few feet above the surface. At the southern end of the lake, north of West Mountain, just above low-water level there is a warm spring that was estimated to flow 200 gallons a minute. Its temperature is 88°. GOSHEN VALLEY. Goshen Valley can be divided into a highland and a lowland portion, a convenient line of division for present purposes being that which separates areas where ground water lies above 10 feet from the surface, from those in which it lies below that depth. The high- land lies contiguous to the mountains and merges into the lowland which adjoins the lower course of Currant Creek and the southern extremity of Utah Lake. The lowland is chiefly underlain by clay and the soils contain abundant alkali. a Throughout the entire area ground water lies close to the surface and marshy conditions exist, especially toward the lake. The area of flowing v/ells in Goshen Valley embraces about 15 square miles and extends from Utah Lake to within about a mile of Goshen. Within it flowing wells are obtained at depths ranging from 50 to 400 feet. From the few available records it appears that varying stratigraphic conditions exist in this area, the prevailing clay being irregularly interbedded with sand, usually in thin streaks, with very little gravel. The flows obtained are small, averaging possibly about 5 gallons a minute, and the pressure is sufficient to cause the water to rise only a few feet above the surface. Goshen itself is furnished with surface water from ditches supplied by Currant Creek and by springs located at the base of the hills about 2 miles east of the town. The underground supply is derived from wells that usually range from 25 to 75 feet in depth. The wells are put down through clay to sand in which water is found under pressure sufficient to cause it to rise almost to the surface, the usual depth to water being 3 to 20 feet. A number of unsuccessful attempts to get flowing wells have been made, the deepest being the railroad well put down near the station. It is 334 feet deep, and water is reported to have ri.sen in it to within a few feet of the surface. The highland area is underlain chiefly by coarse detritus derived from the adjacent mountains and distributed either as shore deposits in Lake Bonneville or as alluvial accumu- lations. This higher portion of Goshen Valley is poorly supplied with water, the chief sources being Kimball Creek, a small stream which seldom flows below its mountain course, and Currant Creek, which flows perennially and supplies the lower valley. The discharge of Currant Creek, however, is insufficient for the ne^ds of the upland. A reservoir has been built by damming Currant Creek at the entrance to its canyon course through Long Ridge, and a canal constructed which skirts the upper part of Goshen Valley, but the (enterprise has been a failure. A few springs occur along the eastern base of the Tintic Mountains and some successful attempts have been made there to develop underground water by tunneling. In the upper valley of Kimball Creek there are a number of springs which flow about 100 gallons a minute, and smaller ones o:'cur in several gulches. About 2 miles east of Goshen there is a group of springs at the base of Long Ridge, where water issues through debris and accumulates in several small ponds, the temperature of which is reported to stay at about 70° F. through- out the year. These springs constitute the source of Warm Creek, and their comi)ined flow in November, HK)4, was estimated at about 5 second-feet. Water has been devclopcnl o Sanchez, A. M., Soil survey of the Provo area, Utah: Bull. Bureau of Soils, U. S. Dept. Agric, 1904. 56 Ul^BERGROUND WATER IN VALLEYS OF UTAH. by tunneling at several localities along the eastern slope of the Tintic Mountains. In the valley of Kimball Creek, in sec. 11, T. 11 S., R. 2 W., there is a tunnel 200 feet long in vol- canic rock, which furnishes about 20 gallons a minute, and water sufficient for milling purposes has been developed by drifting into the alluvium and bed rock at the head of Homansville Canyon. a Away from the bordering mountains in the highland portion of Goshen Valley, very little underground water has been obtained, and considering the slight run-off and the small tributary drainage area, not much can be expected. The most favorable locations for sink- ing wells are along the courses of drainage ways. The most successful are along the course of Kimball Creek, but even there water commonly is not obtained at depths less than 150 feet. A number of dry wells have been sunk in the upland area. WEST OF UTAH LAKE. The narrow strip of lowland between the western shore of Utah Lake and the Lake Moun- tains is very scantily provided with water. The low, narrow mountains catch relatively little precipitation; there are no perennial streams, and the arroyos carry water only for a few days during the year. From the foot of the Bonneville and Provo terraces that extend along the base of the mountains the surface slopes gradually lakeward and is under- lain chiefly by coarse-textured deposits. Along the shore of the lake a number of seep springs occur near water level. They are most abundant from Lehi southward, and there are also a few 2 or 3 miles beyond Pelican Point, where their presence is marked by low, marshy areas, one of which is utilized in the culti- vation of a few acres of alfalfa. Near Pelican Point there is a feebly flowing well 90 feet deep, in which water was obtained at a depth of 60 feet ; and in a near-by well a feeble flow is also obtained, which is said to come from a depth of 154 feet. Few if any other attempts have been made to r.ecover underground water in this region. Judging from the wells at Pelican Point one might expect to obtain similar results along the western shore of the lake, but if flows were obtained the water would be at so low an elevation as to make it of little use without pumping. Away from the shore flows can hardly be expected. It may be, however, that limited amounts of water can be found to rise in wells to within pumping distance. Prospecting for shallow wells might be attempted in the arroyos, but because of the limited watershed and precipitation the prospect is not good for obtaining enough underground water for extensive irrigation. Pumping directly from the lake presents attractive possibilities. >VELI. DATA. The writer is indebted for the subjoined list of wells to Messrs. F. D. Pyle and T. F. McDonald. Mr. Pyle worked in Utah Lake Valley and west of Jordan River. Mr. Mc- Donald, whose assistance was obtained through the courtesy of Mr. George W. Snow, engineer of Salt Lake City, collected data east of Jordan River. The yield of flowing wells was commonly measured by means of tables which are here inserted, together with accom- panying explanation, because the method aroused popular interest and because the edi- tion of the bulletin in which the tables were published has been exhausted. METHOD OF MEASUREMENT. 6 Tables for determining the discharge of water from completely filled vertical and horizontal pipes were prepared a number of years ago by Prof. J, E. Todd, State geologist of Souih Dakota, who issued a private bulletin describing simple methods of determining quickly, with fair accuracy and with little trouble, the yield of artesian wells. In the following notes the tables and explanations relating to vertical and horizontal pipes are taken from this bulletin. The explanations have been appended by the present writer. a Smith, G. 0., and Tower, G. W., Description of the Tintic district: U. S. Geologic Atlas, special foUo 65, U. S. Geol. Survey, 1900. 6 Slichter, C. S.: Water-Sup. and Irr. Paper No. 110, U. S. Geol. Survey, 1905, pp. 37-42. WELL DATA MEASUREMENT. 57 In determining the flow of water discharged through a pipe of uniform diameter all that is necessarj' is a foot rule, still air, and care in taking measurements. Two methods are proposed— one for pipes discharging vertically, which is particularly applicable before the well is permanently finished, and one for horizontal discharge, which is the most usual way of finishing a well. The table [on page 58] is adapted to wells of moderate size, as well as to large wells. In case the well is of other diameter than given in the table its discharge can without much difficulty be obtained from the table Ijy remembering that, other things being equal, the discharge varies as the square of the diameter of the pipe. If, lo • example, the pipe is one-half inch in diameter its dischar[ e will be one- fourth of that of a pipe 1 i:ich in diameter for a stream of the same height. In a similar manner the discharge of a pipe 8 inches in diameter can be obtained In' multiplying the discharge of the 4-inch pipe by 4. In the first method the inside diameter of the pipe should first l;e measured, then the distance from the end of the pipe to the highest point of the dome of the water above in a strictly vertical direction — a to b in the diagram [fig. 5]. Find these distances in table [p. 58, A] and the corresponding figure will pive the number of gallons discharged each minute. Wind would not interfere in this case so long as the measurements are taken vertically. The method for determining the discharge of horizontal pipes requires a little more care. First meas- ure the diameter of the pipe, as before, then the vertical distance from the center of the opening of the pipe, or some convenient point corresponding to it on the side of the pipe, vertically downward G inches, a to 6 of the diagi'am, then from this point strictly horizontally to the center of the stream, b to e. Illil Fig. 5.— Diagram illustrating flow from vertical and horizontal pipes. With these data the flow in gallons per minute can be obtained from table [p. 58, B]. It will readily be seen that a slight error may make much difference in the discharge. Care must be taken to measure horizontally and also to the center of the stream. Because of this difficulty it is desirable to check the first determination by a second. For this purpose columns are given in the tables for corresponding measurements 12 inches below the center of the pipe. Of course the discharge from the same pipe should be the same in the two measurements of the same stream. Wind blowing either with or against th(> water may vitiate i-esults to an indefinite amount. Therefore measurements should b(^ taken while the air is still. Whenever fractions occur in the height or horizontal distance of the stream, the number of gallons can be obtained by apportioning the difference between the readings in the table for the nearest whole numbers, according to the size of the fraction. For example, if the distance from the top of the pipe to the top of the stream in the first case is 9J inches, one-third of the difference between the reading in the table for 9 and 10 inches must be added to the former to give the correct result. In case one measures the flow of a well by both methods he may think that the results should agree, but such is not the case. In the vertical discharge, there being less friction, the flow will lie larger; so, also, in the second method differences will be found according to the length of the horizontal pipe used. As pipes are occasionally at an angle, it is well to know that the second method can hv applied to them if the first measurement is taken strictly vertically from the center of the opening and the second measurement from that point parallel with the axis of the pipe to the center of the stream, as before. The measurements can then be read from the table. 58 UNDERGROUND WATER IN VALLEYS OF UTAH. Table for determining yield of artesian wells. [Gallons per minute.] A. — Flow from vertical pipes. B. — Flow from horizontal pipes. Diameter of pipe in inches. Hori- 1-inch pipe. 2-inch pipe. | Height of jet. zontal leigth of jet. 1. l\- IJ. 2. 3. 6-inch level. 12-inch level. 6-inch level. 12-inch level. Inches. Inches. i 3.96 6.2 8.91 15.8 35.6 6 7.01 4.95 27.71 19.63 1 5.60 8.7 12.6 22.4 51.4 7 8.18 5.77 32.33 22.90 2 7.99 12.5 18.0 32.0 71.9 8 9.35 6.60 36.94 26.18 3 9.81 15.3 22.1 39.2 88^3 9 10.51 7.42 41.56 29.45 4 . 11.33 17.7 25.5 45.3 102.0 10 11.68 8.25. 46.18 32.72 5 12.68 19.8 28.5 50.7 113.8 11 12.85 9.08 50.80 35.99 6 13.88 21.7 31.2 55.5 124.9 12 14.02 9.91 55.42 39.26 7 14.96 23.6 33.7 59.8 134.9 13 15.19 10.73 60.03 42.54 8 16.00 25.1 36.0 64.0 144.1 14 16.36 11.56 64.65 45.81 9 17.01 26.6 38.3 68.0 153.1 15 17.53 12.38 69.27 49.08 10 17.93 28.1 40.3 71.6 161.3 16 18.70 13.21 73.89 52.35 11 18.80 29.5 42.3 75.2 169.3 17 19.87 14.04 78.51 55.62 12 19.65 30.7 44.2 78.6 176.9 18 21.04 14.86 83.12 58.90 13 20.46 31.8 45.9 81.8 184.1 19 22.21 15.69 87.74 62.17 14 21.22 33.0 47.6 84.9 190.9 20 23.37 16.51 92.36 65.44 15 21.95 34.2 49.3 87.8 197.5 21 24.54 17.34 96.98 68.71 16 22.67 35.2 50.9 90.7 203.9 22 / 25.71 18.17 101.60 71.98 17 23.37 36.3 52.5 93.5 210.3 23 \ 26.88 18.99 106.21 75.26 18 24.06 37.5 54.1 96.2 216.5 24 28.04 19.82 110.83 78.53 19 24.72 38.6 55.6 98.9 222.5 25 29.11 20.64 115.45 81.80 20 25.37 39.6 57.0 101.6 228.5 26 , 30.38 21.47 120.07 85.07 21 26.02 40.6 58.4 104.2 234.3 27 31.55 22.29 124.69 88.34 22 26.66 41.6 59.9 106.7 240.0 28 ' 32.72 23.12 129.30 91.62 23 27.28 42.6 61.4 109.2 245.6 29 33.89 23.95 133.92 94.89 24 27.90 43.5 62.8 111.6 251.1 30 35.06 24.77 138.54 98.16 25 28.49 44.4 64.1 114.0 256.4 31 36.23 25.59 143.16 101.43 26 29.05 45.3 65.3 116.2 261.4 32 37.40 26.42 147.78 104.70 27 29.59 46.1 66.4 118.2 266.1 33 38.57 27.25 152.39 107.98 28 30.08 46.9 67.5 120.3 270.4 34 39.64 28.08 157.01 111.25 29 30.55 47.5 68.5 121.9 - 274.1 35 40.45 28.64 161.63 114.52 30 30.94 48.2 69.4 123.4 277.6 36 41.60 29.46 166.25 117.79 36 48 60 34.1 39.1 43.8 53.2 61.0 68.4 76.7 88.0 98.6 136.3 156.5 175.2 306.6 352.1 394.3 Continue by a : 1.15 dding fc 0.82 r each i 4.62 nch— 3.27 72 48.2 75.2 108.0 192.9 434.0 84 51.9 81.0 116.8 207.6 467.0 96 55.6 86.7 125.0 222.2 500.0 108 58.9 92.0 132.6 235.9 530.8 120 62.2 98.0 139.9 248.7 559.5 132 65.1 102.6, 146.5 260.4 585.9 144 68.0 106.4 153.1 272.2 612.5 Note.— To convert results into cubic feet, divide the number of gallons by 7.5, or, more accurately, by 7.48. The flow in pipes of diameters not given in the table can easily be obtained in the following manner: For |-inch pipe, multiply discharge of 1-inch pipe by 0. 25 For |-inch pipe, multiply discharge of 1-inch pipe by 56 For 1 J-inch pipe, multiply discharge of 1-inch pipe by 1-56 For 1 J-inch pipe, multiply discharge of 1-inch pipe by 2. 25 For 3-inch pipe, multiply discharge of 2-inch pipe by 2. 25 LIST OF TYPICAL WELLS. 59 For 4-inch pipe, multiply discharge of 2-inch pipe by 4. 00 For 4.i-iiich pipe, multiply discharge of 2-inch pipe by o.OO For 5-inch pipe, multiply discharge of 2-inch pipe by <>. 25 For f)-inch pipo, multiply discharge of 2-inch pipe l)y 9.00 For 8-inch pipe, multiply discharge of 2-inch pipe l)y Itj. 00 LIST OF TYPICAL WELLS. Wells in Jordan River and Utah Lake valleys. [Height of water above surface indicated by t)lus + ; below surface indicated by minus — .] Name of owner. B. Young J. L. Haywood R. R. Anderson C. R. Savage G. A. Hatch J . Howard Stockyards T. German F. S. Rudy J. E. Peterson J. Minegar Do R. A. Bosley J. C. Hansen W. S. McDonald Gun Club J. Herridge G. Baldwin C. A. Anderson P. Olene S. Bamberger G. Fritt J. Withers I. Langton G. Martin A. J. Davis F.W. Kettle A. M. Davis Do E. King Wantland J. J. Sears Do Do P. Cline R. Weisner J. W. Evans W. Pearson J. W. Haddock A.Elkins A. J. Ridges W. Spicer J. Sandborg H. Price Mrs. Winters R.Griffith Location. T. 1N..R.1 E., sec. 31 ....do ....do T. IN., R. IE., sec. 32 T. 1 N., R. 1 W., sec. 1 ....do T. IN., R. 1 W., sec. 3 T. 1 N., R. 1 W., sec. 4 T. 1 N., R. 1 W., sec. 5 T. 1 N., R. 1 W., sec. 9. T. 1 N., R. 1 W., sec. 10 ....do T. 1 N., R. 1 W., sec. 11 T. 1 N., R. 1 W., sec. 15 T. 1 N., R. 1 W., sec. 17 T. 1 N., R. 1 W., sec. 21 T. 1 N., R. 1 W., sec. 22 do T. 1 N., R. 1 W., sec. 23 do T. 1 N., R. 1 W., sec. 25 .^..do do.. T. 1-N., R. 1 W., sec. 2G do T. IN., R. 1 W., sec. 27 do T. 1 N., R. 1 W., sec. 34 do do do T. 1 N., R. 1 W., sec. 35 do do do .do. .do. T. 1 N., R. 1 W., sec. 36. do .do. .do. .do. .do. .do, .do. .do. Diame- ter. Inches. Depth. 1,002 497 150 250 50 479 400 450 160 330 28 26 60-70 80 70 400 140 154 208 408 250 320 350 140 210 350 135 1.30 08 93 95 123 100 75 75 75 96 200 Height of Yield per water. , minute. Feet. Feet. 75 61 35 18 312 GaUon.s -20-50 -I- + + -I- + 1 Many. 6 40 30 3-7 3 3 1-2 1 25 1 1 5 15 2 3 2 15 85 30 25 5-20 60 UNDERGROUND WATER IN VALLEYS OF UTAH. Wells in Jordan River and Utah Lake valleys — Continued. Name of owner. Location. Diame- ter. Depth. Height of water. Yield per minute. S. A. Gibbs T. IN., R. 1 W.,sec. 36 T. 1 N., R. 2 W., sec. 25 Inches. 2-3 Feet. 75-80 400 401 465 Feet. + Gallons. 40 F. Auerbach J. Bond T. 1 N., R. 2 W., sec. 29 + + ■ + + - 6 -12 - 6 - + + + + + + + + +35 + + + + + + + - 1 + + + + 12 -5-6 • -65 -30-50 -46 - 4-16 - 5-14 + + - 3-11 - 3 4 Do ' .. .do... . 9 Ciillen Dairy J. Walker T. 1 N, R. 2.W., sec. 35 2 T. 1 S., R. 1 E., sec 5 80 16 73 45 29 40 12 75 82 387 10 100 162 100 125 170 150 100-600 178 150-200 155 160 60 165 110 50 - 50 26 246 390 207 41 28 42 100 130 85 51 54 56 18 32 22 20 100 200 335 15 33 20 P. J. Stone do... J. Lunn do W. J. Kelson do S. McKay do Speirs do Do do J. E. Wesley.. T. 1 S., R. 1 E., sec. 6 do 2 2 7 H. S. Sampson do 8 W. Wheeler. . do T. Golightly .do 2 2 2 S. K: Hansen do 6-8 W. N. Sheets T. 1 S., R. 1 E., sec. 7 30 F. Sproul .do ^ G. Baiber do 12 F. Rogansky do 1 City, about 16 wells . . . E. 0. Butterfield do .do 2-9 2 (?) 600 2-3 J. S.Wooley and others do 20-50 T. Berg do .. 2 2 2 2 2 li 2 3 2 IJ 2 50 Do . .do 50 W. Colton . ...do 6 L. Badger. do 30 J. W. Hicks. .. . .do 35 A. Duncan T. IS. R. 1 E., sec. 8 T. Antisill... do 3 S.M. Alley . .do S. H. Calder do : 40 S. Sudbury... do . . 8 J.R.Miller ...do 50 P. Rosmason do do ... W. Pickens do . T. 1 S., R. 1 E., sec. 9 A S Martin T 1 S R 1 E sec 10 J. A. Shelter T 1 S R 1 E sec. 15 L. Hunt. . do A Hord T 1 S R 1 E sec 16 A. Martin do H. E. Thorp. do J S. Southern T 1 S R 1 E sec. 17 do J E Nailor do T. Y. Taylor do 2 2 2 (a) do 6 W H Miller do 50 W. H. Burnett . do M. C. Sandford a Owner's name unknown. LIST OF TYPICAL WELLS. 61 WeU.''i in Jordan River and Utah Lake valleys — Continued. Name of owner. Location. Diame- ter. Depth. Height of water. Yield per minute. T.IS. R. do... do 1 E., sec. 17 1 E., sec. 18 Inches. 2 2 2 2 Feet. 33 10 14 48 325 300 100 164 160 20 72-82 500 600 636 150 40 325-3C0 501 382 17 250-300 322 560 40 298 m 50 160-170 323 296 285 150 437 100 94 60 176 180 90 181 84 212 75 240 150 150-l(i0 23 20 65 40 162 156 21 Feet. -28 -43 + + + + + 4- + + + + + + + + + + + + + + + + + + + + + + 4- -20 4- 4- 4- -14-15 Gallons. G Hemslev do J. J. Ilurtt T. 1 S., R do 4-5 T Furgesou 30-40 W N Sheets do 30 M. Gray .do 10 F II Woodbury do 18 M P Holmes do. E. H. Stout .do... !'^'!^^"^'^^!!!^!"'!!^ 2 2 2 2 2 2 2 30-40 J. II. Cochran ....do... 5 F. Prittish do 12-14 Salt Lake Co .do... (?j 150 do... 10 F. Wittich do... 18 L. A. Kelsh .do... 30-40 D. Evans do... 80 Eriekson do... 3 (?) 100 I. Riches .do... do... 2 2 1-13 E. S. Pierce do 55 (") . .do... 20-30 W. II. Wolstezhoh do... do 1 E., sec. 19 3 2 2 n 3 2 2 2 2 2 2 2 2 2 2 2 2 2 3 2 C. B. Stock 10-12 .do... 5-6 H. Best do... 8 A. Best. do J. A. Bush T. IS., R do... J.H. Tipton 50-60 L. W. Burton. . .do 60 Do .. ..do... 25 Do do lO-SO Do .do... J. Riley do... 17-20 G. JIall do 1 J. C. Ilogan J. 0. Young R. B. Young M. W. Taylor L. II. Kimball Do W. C. Winder do... do... do.. . do... do... do... do... ':■■■ do... do... 18 20-25 20-25 (?)100 10 1 Do A. Walker («) E. P. Parrot 30 40 46 11. Behling T. 1 S.. R do... 1 E., sec. 20 H. Eldridge T. R. Cutler do S. Love do... 5-6 M. C. Morris do 1 N. .1. Hansen A. Uoskinson do... do... 28 a Owner's name unknown. 62 UNDEEGEOUND WATEE lis" VALLEYS OF UTAH. Wells in Jordan River and Utah Lake valleys — Continued. Name of owner. Location. Diame- ter. Depth. Height of water. Yield per minute. C. Hansen.. T. 1 S., R. 1 E., sec. 20 Inches. Feet. 22 158 18 22 23 100 33 184 27 55 68 68 26 194 187 40 260 190 200 184 215 208 209 245 245 141-143 100 120 202 24 200 128 251 104 235 240 110 216 218 130 100 Feet. - 18 + - 19 - 20 -104 - 25 _ - 37 + - 34 -16 + + + + + + + + + + + + + + + + + + + + + 6 + + + + + + + + + + Gallons. P. E,. Ryon do 80 G. Cusiman do W. C. Smoot do J; Neff T. 1 S., R. 1 E., sec. 26 C. Banford do J. Fisher T. 1 S., R. 1 E., sec. 27 .. ..do F. Ereickson T. 1 S., R. 1 E., sec. 28 J. Childs T. 1 S., R. 1 E., sec. 29 W. M. Tillman do F. Degenhart do 2 J. P. Gaboon do W. S. Timmons . ..do 2 2 9 J. T. Guest do R. Pike do ..do J. S. Gustavensen do 2 2 H. Hizzard do 2 Mrs. C. Green ..do 1 Do do 11 S. F. Evans do .do ,2 0. Reece 30 Do do 30 Do do 13 L. Stutts . ..do : 2 2 3 40 S. Hicks do 30 E. E. Keithley H. Burnett do (?) 100 . .do 27 Do ' do W. J. Miller do 2 2 2 20 . ..do 20 J. Tremayave G. Taylor T. 1 S., R. 1 E., sec. 30 20 .do . W. Chantron J J. Spencer do do 2 2 2 2 2 2 2 2 2 30 17 M. M. Listen. .do 5 J. Cobert do 24 Scbool do 12 G. Calder ..do 45 R Norman do Mrs. A. S. Berg do 28 do 175 8 (a) Murray Live Stock Co. do 30 .do 40-6® :.;..do 300 185-230 82-83 50 160 202 72 237 160 20 L. White do 60 E J Williams do 2 2 li 2 2 2 2 25 Do do. 1 C. Halford .do 10 A. M. Rymarson Do T. 1 S., R. IE., sec. 31 do . 35 6 L Parks do J.Hulse do + 20 a Owner's name unknown. LIST OF TYPICAL WELL8. 63 Wells in Jordan River and Utah Lake valleys — Continued. Name of owner. Location. Diame- ter. I)ei)th. Height of water. Yield per rninutc. Inches. Feet. Feet. Gallons. J. Hulse . ... . T. 1 S., R. 1 E.,sec. .-^l do 2 2 130 255 83 + 4- 20 Do 30 J. Pearson C. Bell do ..do 2 209 + 40 Do do 211 203 + 20 J. Bert ..do 2 12 C. Cramer ..do 1.50 4- C!) 110 Do .do 90 + N. White ..do ..do i;30 80 4- + 15 J. Anderson h S. Ilaslam ..do 2 244 -f 8 E. lluish 1 S., R. 1 E., SfiC. 32 2 210 + 28 Do ..do 70 + 35 S. W. Moylo ..do 196 + 6 J. Cormvell ..do 235 + 20 Do ..do ..do lOO 160 + + Do 1-12 Do ..do 2 165 193 + + S. A.Cornwpll 1 Do ..do 2 55 + A. Young ..do 33 - 24 E. Bailey ..do 25 - 22 L. E. Sowers .do 54-56 70-150 - J. \V. Murphy C. A. North 1 S., R. 1 E. sec 33 25 520 -419 W. H.Thuers ..do 3 P. C. Brizen ..do 3 350 + 25 Mrs. M. Cold 1S.,R. 1 W.,sec. 1 '. 1^ 2 317 300 + -f. 1 J. R. Morgan Mrs. E.R. Wadsen.... .do .- 20 T. ..do 2 3 202 120 1,100 + 2 (a) 1 S., R. 1 W., sec. 2 J. Harrison ..do 30 F.J. Guth ..do 2 114 + li Mrs. C. Bickson ..do 2 318 4- 6 J. H. Haward ..do.: 2 335 4- 4 J. Taylow ..do 1 95 4- 2i Rio Grande Rwy ..do 4 1,072 + 30 80 H. L. Eyler Mortensen T T. 1 S., R. 1 W., sec. 3. 2i 2 381 280 + 4- 16 IS., R 1 W.,sec. 4 3 R. Boss T. 1 S., R. 1 W.,sec. 5., 2 360 + 4i 7 E. B Swan -do 2 38.5 4- 6 J. Rodgers T. 1S..R. 1 W.,sec. 7 .do 2 154 405 4- Do 10 Do T. .do 1 S., R 1 W.,sec. 8 n 2 154 325 4- + 1 F. Schonfeld 1 Brighton School T. ] S., R. 1 W., sec. [) 2 320 98 4- + 1 5-6 11. J. Walk -do 1 H. E.Evans T. IS., R. 1 W.,sec. 10 3 624 + 30-40 W. Baden T. 1 S., R. 1 W.,sec. 11 2 377 4- 9 W. J. Kinsman .do 2 130 + 20-30 Cannon .do 165 + 6-7 Sudbury .do 2 2 4- + 25 A. Bailey .do 367-387 5-6 J.Cleveland ... .do 2 456 4- 60-70 a Owner's name unknown. 64 UNDERGROUND WATER IN VALLEYS OF UTAH. Wells in Jordan River and Utah Lake faZZej/s— Continued. Name of owner. E.Kidd A.H.White J. Anderson J. H. Shaffer Lambert Paper Co . R. Cutler J. Gabbot. (a) J. S. McCallan J. G. Gumman Schoolhouse S. C. Sudbury L. S. Hansen. .. N. Hansen S. Sorensen Gilchrist Rockhill P. Austin G.H.Walton...... B. Harmon (a) Murray C. J. Lambert L. Burden N. P. Peterson J. C. Poulton (a) T. P. Jones Do (a) J. P. Anderson (a) (a) Wolstenholm Spencer Oslen Butterworth T. West N. T. West J. Michaels J. Hayhoe Goodwin A. Cockerill Speirs J. Kersey Inland Crystal Salt Co . Salt Lake and Los An- geles Rwy. Co. P. J. Reid J. Bertock J. Neilson G. Coleman T. Newman T. Gundesser, jr Location. R. 1 W. R. IW. sec. 26. sec. 28. T. 1 S., R. 1 W., sec. 12. do T. 1 S., R. 1 W.,sec.l3. do do do do do T. 1 S., R. 1 W.,sec. 14. T. 1 S., R. 1 W.,sec. 16. T. 1 S., R. 1 W., sec. 17. T. 1 S.,R. 1 W.,sec. 18. T. 1S.,R.1 W.,sec. 21. T. 1 S., R. 1 W., sec. 24. do T.1S.,R. 1 W., sec. 25. do do do T. IS., T. 1 S., do T. 1S.,R. 1 W., sec. 29. do T. 1 S.,R. 1 W., sec. 31. do „... T. 1S.,R. 1 W.,sec. 32. T. 1S.,R. 1 W.,sec. 35. do T. 1S.,R. 1 W.,sec. 36. T. 1S.,R. 2 W.,sec. 1.. do T. 1S.,R.2 W.,sec. 14. T. 1 S., R. 2 W.,sec. 21. do do do T. 1 S., do. T. IS., T. 1 S., T. IS., T. IS., T. IS., T. IS., T. IS., do. R. 2 W., sec. 22. R.2W., sec. 23... R.2W.,sec. 26... R. 2 W., sec. 27... R. 2 W., sec. 29... R.2 W.,sec. 33... R. 2 W., sec. 34... R. 3W.,sec. 2.... T. 1S.,R.3 W., sec. 24 do T.2 S.,R. 1 E., sec. 3 do .....do T. 2S., R. lE.,sec. 4 a Owner's name unknown. Diame- ter. Inches. Depth. Feet. 475 300 400 18 177 315 380 275 355 330 400 412 145 385 130 120 145 350 350 290 182 70 50 60 290 345 75 140 160 260 150 30 68 150 175 40 40 90 177 27 118 84 166 720 330 134 73 540 62 65 18 Height of water. Feet. + 3 + 6 + -21 -14 -66 + 9 + 12 LIST OF TYPICAL WELLS. 65 Wells in Jordan River and Utah Lake valleys — Continued. Name of owner. Location. R. 1 E., sec. 5. R. 1 E., sec. 6. T. R. Brockbank T. 2 S., R. 1 E., sec. 4 Do do J. Southerland do Do do Do do Do do W. Templeman do F. Hopp do A. Fuller do Do ' do P. C. Brizen ' do J. Wright T.2 S. E. Pugh ' do S. A. Williams do Mrs. A. D. Park do 0. Lemon do H.J. Bullock T.2S. T . Powell do H. Park do W. Hill, sr do Do do W. Hill, jr do G. E. Christensen do J. Godfrey T.2 S., R. 1 E., sec. 7 1. Hackley do Mrs. B. Erickson do J. S. Williams do E. Williams do Williams do Martin do Warenski ' do E. Warenski do R. Miller T. 2 S. W.Noble do M. M.Miller do Do do T. H. Pierce C. West J. Walker State fish hatchery . Do Do A. Gillard H. Brinton J. R. Hansen L. B. Howard A. Scott H. Bagley Do W. Reynolds F. Brinton C. Bagley Do do do do do do do do do T. 2S. do do do do do do do do R. 1 E., sec. 9 R.Anderson T. 2 S., R. IRR 157—06- Diame- ter. Inches. Tv^^+v, Height of ^«P*^- I witer. 1 E., sec. 10 a Drv 9 months in year. 2 , R. 1 E., sec. 8 5 2 2 ! Feet. 104 102 76 78 225 70-100 65 335 122 200 108 180 90 384 100 194 90 255 80 255 210 150 115 80 315 100 190 189 230 300 215 230 85 82 80 172 80 310 120 148 2 I 275-250 100-103 92-96 100 14 Feet. + + + + + Yield per minute. Gallons. + 30 + 15 + 4 + 10 + 38 + + 2 («) 66 UNDERGROUND WATER IN VA.LLEYS OF UTAH. Wells in Jordan River and Utah Lalce valleys — Continued. Name of owner. Location. Diame- ter. Depth. Height of water. Yield per minute. A. Olander T. 2 S., R. 1 E., sec. 15 Inches. Feet. 18 15 20 78 18-20 20 22 18 113 60 60 92 58 83 14 250 40 46 50-60 60 45 175 90 190 75 80 125 20-30 90 70-80 200 22 75-100 75-100 110 18 50 22 10 12 22 10 16 13 50 6 12 80 96 125 18 22 35 Feet. - 16 - 10-11 - 4-17 - 40 - 8-10 - 10 - 11 - 12 - 9 + + + 16 + 8 . - 9 - 12 + 8 + + + + + + + + -117 - 10 - 4-13 - 10 + + + - 4 - 8 - 30 - 55 - 93 - Gallons. J.Sioiilet .. .do ..' J. Smith T. 2 S., R. 1 E., sec. 16 ' J. Hemmert do - S. Neilson .. .do S. F. Smith do A. L. Hansen do J. W. McHenry .....do ' J. Hobbs do J. Furgeson do 17 I . Furgeson do do J. Brighouse H.V.Ballard. T.2S., R. IE., sec. 17 .do li 2 30 50 do District school do R. Brown .do. .. ^ R. M. Ballard.. do li 2 35 Mrs. Shumann do 20 H. E. Howe do .. . 22 D. A. Rauser. do.. .. 60 J. T. Erickson do 2 2 2 li 2 2 F. C. Howe do 35 Do do 35 J. B. Thompson Do do 45 do 60 E. Taylor E. Gillen T 2 S., R. 1 E., sec. 18' ...do 2 3 H. Berger do C. Turner do . ...do 2 2 2 2 3 J Jones do J. H. Wheeler .do.. . 20 South Cottonwood do . . 40 Ward. Do. do 60 Mrs. J. Clark do... M. Sibbs T. 2 S., R. 1 E., sec. 19 2 ... .do T. 2 S., R. 1 E., sec. 20 H. Wheeler do. ... C. B. Walder.. do C. J. Wright do W. Barrett T. 2 S., R. 1 E., sec. 21. J. E. Brown... do. H. C. L. Russell do J. W. Fawlke T. 2 S., R. 1 E., sec. 22 A. Fawlke do S. Jones T. 2 S., R. 1 E., sec. 26 A. D. Brown T. 2 S., R. 1 E., sec. 27 (a) W. Baggas. . T. 2 S., R. 1 E., sec. 28 T. 2 S., R. 1 E., sec. 29 D. M. Griffin do J. A. Wagstaff do : ■ Owner's name unknown. LIST OF TYPICAL WELLS. 67 Wells in Jordan River and Utah LaJce valleys — Continued. Name of owner. Location. Diame- ter. N. Morquist I T. 2 S., M. Holmes ' T. 2 S., H. Chambers do . J. Jones do. O. G.Nelson i T. 2 S., C. G. Johnson do. G. L. Rosengren ' do . H. M. Pearson do. A. Neilson do . H. Larsen do . L. Jacobson do. W. Dugger T. 2 S., A. Hansen do. E. E. Osbund do. H. C. Monten T. 2 S., J. F. Proctor T. 2 S., W. Rasmanson T. 2 S., H. Covert do. Clark T.2S., J.M. Wood do. E. Erickson do. Lumston do . (b) \ do. Gleason do . J. Hays I do. J. Harper ' T. 2 S., J. M.Mantell ! do. J. Mackey ' T. 2 S., Barker do . R. 1 E. R. 1 K. sec. 29 . sec. 30. R. 1 E., sec. 31.... R. 1 E., sec. 32. R. 1 E., sec. 33. R. 1 E., sec. 34. R. 1 E., sec. 35. R. 1 W., sec. 1 R. 1 W., sec. 2. R. 1 W., sec. 3. C) T. 2 S., R. 1 W., sec. 6.. Parker T. 2 S., R. 1 W., sec. 8.. School do Snider do McAllister | T. 2 S., R. 1 W., sec. 9.. H. McKay T. 2 S., R. 1 W., sec. 10. H. Harker T. 2 S., R. 1 W., sec. 11. W. H. Hague j do P. Swendsen i do B. Williams I do G. Bueger T. 2 S., R. 1 W., sec. 12. Western Pickling Co...' do S. Benson do D. Adamson do Creamery do A. E. Erickson do J. C. Cahoon \ T. 2 S., R. 1 W., sec. 13.. Mrs. A. J. Plummer do. C) M. Bishop E. B. Tripp A. S. White R. P. Binghurst Jones ..do ..do 2S.,R. 1 W.,sec. ..do ..do ..do Inches. Depth. Height of Yield pw water. minute. Feet. 30 3.5 2(X) 22 40-50 29-30 51 90 53 26 15 100 14 200 22 40 50 40 40 100 287 140 90 65 280 372 240 212 260 56 157 120 150 110 141 315 222 323 85 100 350 249 117 345 180 (iO 9J 50 Feet. - 26-27 Gallons. 25-34 26 - 41 - CO -200 - 26 + + - 18 + - 10 - 25 - 37 - 60 - 50 Dry in winter. 09 _ 180 I + b Owner's name unknown. - 36 + 4- + - 8 - 30 - c^h - 10 - 40 - 12 - («) Dry, 20-35 40 2 22 25 35 68 UNDERGROUND WATER IN VALLEYS OF UTAH. Wells in Jordan River and Utah LaTce valleys — Continued. Name of owner. Location. Diame- ter. Depth. Height of water. Yield per minute. Inches. J. Anderson School W. Diamond M. Parker M. Hansen (a) C. Erickson E. Bateman (a) Bingham School J. B. Wright E. Gardner (a) Cooper W. D. Runsal A. L. Cooley Olsen Cannon Farm R. Egbert P. T. Rundquist M. Pusler J. Peterson N. L. Gardner G.Hunt S. M. Wilmore N. Nelson (a) P. Jansen P.J. Wolfi Olsen H. Brown W. L. Bateman E. Johnson C. Peterson T. 2 S., R. 1 W., sec. 15 do T. 2 S., R. 1 W., sec. 22 ....do do T. 2 S., R. 1 W., sec. 23 T. 2 S., R. 1 W., sec. 24 T. 2 S., R. 1 W., sec. 25 ....do ....do T. 2S. ....do T. 2S. ....do ...-.do T. 2 S., R. 1 W., sec. 30 T. 2 S., R. 1 W., sec. 33 T. 2 S., R. 1 W., sec. 34 ....do ....do T. 2 S., R. 1 W., sec. 35 do do T. 2 S., R. 1 W., sec. 36 do do : do 3 , R. 1 W. sec. 26 3 , R. 1 W. sec. 27 3 T. 2S.,R. 2 W., sec. 11. T. 2S., R. 2 W., sec. 27. T. 3S.,R. IE., sec. 2... T. 3S., R. IE., sec. 5... T. 3S.,R. IE., sec. 6... do , A. Yelter ' T. 3 S., R. 1 E., sec. 7. H. P. Hansen.. P. Anderson... R. Despain C. Williams... F. Olsen P. A. Yastrop. J. P. Jenson... E. N. Fish J. L. Johnson. J. W. Smith... H. Pearson J. Tarry N. Brown J. R. Stocking. A. J. Wilson... J. R. Allen J. Ennis J. Boulter F. B. Ladler... T. 3S., R. IE., sec. 8.. T. 3 S., R. 1 E., sec. 9.. T. 3 S., R. 1 E., sec. 11. T. 3 S., R. 1 E., sec. 17. T'. 3 S., R. 1 E., sec. 18. T. 3 S., R. 1 E., sec. 19. do T. 3 S., R. 1 E., sec. 21. T. 3 S., R. 1 E., sec. 22. T. 3 S., R. 1 E., sec. 28. T. 3 S., R. 1 E., sec. 29. do .....do do T. 3 S., R. 1 E., sec. 32. do do T. 3 S., R. 1 E., sec. 33. do a Owner's name unknown. Feet. 117 165 345 225 140 185 30 251 20 325 230 180 100 154 137 28 178 1,000 52 80 217 127 309 21 225 190 50 30 174 150 38-40 14-16 40 28 75 56 125 16 30 40 95 34 65 10 18 18-20 16 42 70 24 41 22 66 Dry In winter. Feet. - 50 - 50 -110 - 40 - 90 - 24 - 12 - 16 - 60 - 40 - 20 33 20-30 30 24 18 53 25 17 8 75 17 25 70 45-52 Gallons. LIST OF TYPICAL WELLS. 69 Wells in Jordan River and Utah Lake valleys — Continued. Name of owner. , Location. Diame- ter. Depth. Height of Yield per water. minute. P. Swindsen T. 3 S.. R. 1 W., soc. 1 E. Densley do C. Densley do D. Densley, jr do J F Palmer T 3 S R 1 W. sec. 2 Inches. 2 3 Feet. 323 2on Feet. + -40 Gallons. 5 30 3 412 3 236 250 212 3 137 3 1 156 3 ; 255 500 2 50 l\ 28 ' 30 3 .127 28 15 -.^>8 -43 TT Gardner T 3 S R 1 W sec 3 -20 -40 -45 -85 -75 J. A. Egbert do J Goff 1 T. 3 S., R. 1 W., sec. 12 B. Wellington i T. 3 S., R. 1 W., sec. 13 \ J Holt T 3S R 1 W. soc. 1.5 B. W. Osborne T. 3 S., R. 1 W., soc. 23 W. R. Wellington do C Erickson T. 3 S., R. 1 W., sec. 24... 12-15 12-15 -12 - 4 -40 E Atwood do R Carlson do A. Yoblong T. 3S.,R. 1 W., sec. 25 J Smith do 3 2 3 3 2 133 90 225 102 400 40 125 20 41 15 Creamery T. 3 s Ti i W.. spo. 2fi + 12 -60 G. H. Donzy C. H. Roberts I. Langton G. Newbold G. Sproul L. Andrews J. Ennis H.J.Allen W. H. Garfield W.Crane Alpine W. L. Parry M. Densley J. Stedman J. Beveridge Lehi Junction T. 3S., R. 1 W., sec. 27 T. 3 S. R. 3 W., sec. 26 T. 4 S., R. 1 E., sec. 5 + + -10 -35 - 8 3 . ..do do 2 T. 4 S., R. 1 E., sec. 6 T. 4 S., R. 1 E., sec. 32 do T. 4 S., R. 1 E., sec. 33. 42 21 25-80 30 9QJ do T. 4 S. R. 1 E .,sec. 24 T. 4 S., R. 1 W., sec. 3.. do 3 -40 do 3 1.30 ! -40 T. 5 S., R. 1 E., sec. 4 32 15-50 -20 -10-40 + 25 + + - 8-10 -22 + + + + - 8 T. 5 S., R. 1 E., sec. 5 I. Anderson. . T. 5S.,R. IE., sec. 7 .:...do 2 ; 134 ui 125 Thomas College J. Wanless do li 2 2 125 90-100 193 90-100 12 145 75 12 20 145 130 135 300 330 330 .300 G. Jacobs do 12 Do do D. J. Thurman do 55 H. T. Davis T. 5 S., R. 1 E., sec. 8 G. Gerney do li T. R. Jones do B. W. Brown J. Gough P. Austin («) J. Brown . .do.. . do T. 5 S., R. 1 E., sec. 9 2 2 li 2 2 li 3 do do 5 (a) do San Pedro, Los Ange- do les and Salt Lake R. R. Do do Do do 4 23 35 Do 1 do li 140 a Owner's name unknown. 70 UNDEEGKOUND WATER IN VALLEYS OF UTAH. Wells in Jordan River and Utah LaTce valleys — Continued. Name of owner. Location. Diame- ter. Depth. Height of water. Yield per minute. W. Hunger T. 5 S., R. 1 E., sec. 9 Inches. 2 14 li 2 li li 2 2 3 Feet. 145 140 158 132 130 145 270 201 460 160 160 140 150 543 263 33 162 130 90 Feet. - 2 + + - 6 + + -25 + + + + - ^ - 2 + ■ + + + + Gallons. (?)25 9 Rhodes do Wing .do Anderson do 20 Gilchrist do T. 5 S., R. 1 E., sec. 10 D. Wagstafi T. 5 S., R. 1 E., sec. 14 . . . A. L. Thornton do 2 American Fork, city do well. A. Green T. 5 S., R. \ E., sec. 15 J. B. Greene do 2 2 2 3 2h 6 14 2 2 2 2 40 J. Stewart T. 5 S., R. 1 E., sec. 16 . .do. .. . 10 A. K. Thornton do T. J. Chipman do J. Peters do A. Field do 5 Mrs. K. Fox -do 10 (a) (a) do 10 do 15 (a) .do 90 147 150 350 132 150 143 ' 140 140 164 200 165 195 156 147 135 160 20 (a) T. 5 S., R. 1 E., sec. 17 0. Ellington do 1^ 2 2 2 2 2 li 14 2 3 2 2 2 2 2 2 ■2 2 2 2 2 2 2 3 3 3 li 2 2 2 2 2 nown. + + + + + + + 3 +30 + 3 + 10 + + 46 + + + + + + + + + + + + + + + + -33 + 18 do do 20 D. J. Thurman do 10 J.Donaldson .do .. 20 J. Stewart do P. Jacobs do 5 J. Woodhouse do M. Evans do (?)100 Rio Grande Western do 50 Rwy. G.Webb T. 5 S., R. 1 E., sec. 18 40 S. R. Taylor do W. H. Chipman ... Do T. 5 S., R. 1 E., sec. 23 (?)150 T. 5 S., R. 2 E., sec. 11. (?)200 B. Willis T. 5 S., R. 2 E., sec. 18 do 30 (a) J. D. Godey T. 5 S., R. 2 E., sec. 19 20 -do.. . 290 150 200 40 100 264 S. E. Davis do 80 W. Howe T. 5 S., R. 2 E., sec. 20 20 Clarke .do . Lott T 5 S R 2 E sec 21 60 (a) T. 5 S., R. 2 E., sec. 23. 10 . ..do A. F. Adams do 280 280 15 American Fork City. . . W^ Anderson .do T. 5S., R. 2E., sec. 25 T. 5 S., R. 2 E., sec. 29. . . 10 W. D. West 64 70 74 200 70 15 Do .. do (a) Wadley ... .. . do 35-50 dc W. D. West do a Owner's name unk LIST OF TYPICAL WELLS. 71 Wells in Jordan River and Utah Lake valleys — Continued. Name of owner. Location. D. M. Smith (a) (a) L. Olsen F. Newman Do Pastures P. H. Aldred I. Fox Salt Lake City (about 130 wells). J. M. Roberts (a) M.Norman T. 5 S I.Cole : T.6S T. 5S., R.2E.,sec. 29. T. 5 S., R. 2 E., sec. 32. ....do ....do ....do T. 5S., R. 2 E., sec. .35. ....do T. 5S., R. 1 W., sec. 1.. T. 5 S., R. 1 W., sec. 12. ....do 1 W 13. T. 5S., R ....do R. 1 W., sec. 24 R.2E., sec. 5.. J. S. Johnson do H. Gammon T. 6 S., R. 2 E., sec. 7.. H. Gillies | do D. A. Gillis I T. 6S., R. 2 E., sec. 8.. J. K. Parcell | T. 6 S., R. 2 E., sec. 10. N. Knight j T. 6 S., R. 2 E., sec. 14. Colorado Fish Co do N.J. Knight do W. Knight do J. S. Park i T.6S. A. N. Holdaway. M. Holdway B. Larsen Wride& Allen... G. A. Slumway.. J. A. Loveless... A. L. Mechum. .. D. C. Daniels H. C. Scott J. H. Clinger Creamery J. W. Park W. G. Williams. . S. L. Aldred W. Gammon P. 11. Cluff T. W. Whisble... J. A. Johnson N. Lydian S. McFee A. Holliday W. Cox P. C. Bumrell.... Utah Sugar Co.. W. L. Camp N. A. Nelson R. A. Hills Provo resort G. Baum W. D. Roberts... T. 6S. do T. 6S. do T. 6S. R.2E. R. 2E. sec. 15. sec. 17. R. 2 E., sec. 18. T. 6S. do T. 6 S. do do T. G S. do T. OS. T. 7 S. do T. 7S. do do do T. 7S. do do do T. 7 S. T. 7S.; T. 7S., T R. 2E., sec. 21. S., R. 2 E., sec. 23. S., R. 2 E., sec. 24. S., R. 2 E., sec. 26. R. 2 E., sec. 28. R. 2 E., sec. 34. Diame- ter. Inches. 2 2 2 2 2 2 2 2-6 2-3 2 3 2 2 ,; , R. 2E. sec. 35 2 , R.3E. sec. 31 , R.2E. sec. 1 o' 2 2 2 2i 2 , R.2E. sec. 2 , R. 2 E. sec. 3 . ,R.2E. sec. 4 , R. 2 E. o , R. 2E. sec. 10 , R.2E. sec. 11 2 Depth. Feet. 115 150 80 160 150 90 100 100 100 100 258 112 160 210 130 110 112 110 72 110 250 60 300 72 12C-140 100 100 110 • 104 52 40 65 110 Height of Yield per water. I minute. Feet. + 20 + Gallons. + + 7ins. + 30 + + + 14 + + + + 11 + -67 -80 -40-55 -62 + 1-10 + + 12 + + -50 -36 -60 S., a Owner's name unknow 125 + 110 + 130 + 210 - 24 - 50 - 217 + 145 + 145 + 145 + 150 + 130 + 135 + 110 + 128 + 35 - .50 - 342 + 12 - 184 + 25 40-45 45 (?)2,000 32 (?)260 (?)100 (?) 1-200 30 (?)100 2& 72 UNDERGROUT^D WATER IN VALLEYS OF UTAH. Wells in Jordan River and Utah LaJce valleys — Continued. Name oi owner. Location. 1 Height of water. Yield per minute. Westron T. 7 S., R. 2 E. sec. 11 Inches. Feet. 2 180 li 160 2 ; 168-178 2 1 150 2 170 3 175 3 192 n 248 Feet. + + + + + + + 35 + 12 Gallons. W. B. Johnson M. Christensen B. Johnson W. Carter do 15 do 10 ..do 45 do 40 Rio Grande Western Rwy. San Pedro, Los Ange- les and Salt Lake R. R. W. R. Pike T. 7S., R. 2E., sec. 12 do (?)120 (?)150 do 40 Do- do 2 198 168 168 180 150 36 W. J. Woodhead H. Manney Hospital W.Scott S. W. Sharp Farris Bros S.Copp WatMns & Taylor (a) A. B. Johnson G. T. Peay A. W. Hanrer do + + + + 60 do 60 do :....do 2 2 55 do 197 i + 'l85 : + 175 i + 300 + 145 + 30 do 60 do 2 9 do 2 T. 7 S., R. 2 E., sec. 14 n 20 do 170 137 T. 7 S., R. 2 E., sec. 16 2 2 li 2 3 2 2 li 2 2 3 li li 2 2 3 2 2 2 2 + 5 30 T. 7 S., R. 3 E., sec. 6 140 +2 333 +20 40 T. E. Thurman do 35 T. 7 S., R. 3 E., sec. 8 150 270 180 220 299 128 +20 + +10 + 4 + + 15 Utah Co. Infirmary... H. M. Dougal Do T. 7S., R. 3E., sec. 17 T. 7 S., R. 3 E., sec. 29 70 40 T. 7 S., R. 3 E., sec. 30 20 Clubhouse Do do 5 do 10 P. Boyer Rio Grande Western Rwy. J. B. Stevenson T. 7 S., R. 3 E., sec. 31 150' 1 + 220 +30 232 - + 18 T. 7 S., R. 3 E., sec. 32 do 80 15 T. 7S., R. 3 E., sec. 33 101 131 240 230 135 115 128 105 22 + + + + 18 + + + + 12 D. Wheeler .do 25 D. Clark do A. Cox .... do (?)120 W. Findley do 25 (a) A. Oakley do 70 .do 30 J. McCurdey. . do 30 do (a) do 2 120 ! + 245 + 25 20 T. L. Mendenhall do 45 S. Fuller .do \ M. Dougal do 2 IJ li 2 2 n 230 130 132 145 217 138 160 100 + + + + + + 10 E. P. Brinton . do 20 do 10 Daley do 9 F. W. Phillips ....do 65 (a) do 30 W. Brookes T. 8 S., R. 1 E., sec. 11 10 (a) do - 4 + T. 8S.,R. IE., sec. 24 7 a Owner's name unknown. LIST OF TYPICAL WELLS. 73 Wdls in Jordan River and Utah Lake valleys — Continued. Name of owner. J. D. Evans E. L. Oltioon IT. Otis C. Barney («) J. Hall J. S. Bellows ■\V. J. Soloman R, Hunter J. E. Creer P. Poulsen do. P. Neilson T. 8 S. E. P. Thomas ....' do A. Green 1 T. 8 S. Do I do Location. R. 2E. R. 2 E. sec. -1. sec. 4. T. 8S. T. 8 S. ....do ....do ....do ....do T. 8S. T. 8S. ....do ....do T. 8 S., R. 2 E., sec. R. 2E. R. 2E. sec. I . sec. 8. R. 2 E., sec. 10. R. 2E., sec. 12. Creamery San Pedro, Los Ange- les and Salt Lake R.R A. T. Money R. W. Monej' W. R. Simmons A. M. Furgeson P. E. Nelson Irrigation Co Lake Shore Canal E. M. Robertson N. P. Hansen (a) (a) G. McClellan Do Do Do N. Thompson D. L. Hoff E. Ludlow C. Howe T. Cahoon (") (") O. Christensen D. C. Markham G. Hales (a) N. P. Jensen B. Isaac («) P. Thomas F. Malley Howe G. Howe («) Stewart's ranch Do T. 8S., R. 2E., sec. 13. ....do T. 8S., R. 2E., sec. 14.. ....do T. 8S., R. 2E., sec. 1.5.. ....do ....do ....do ....do T.8S., R. 2E., sec. 16.. ....do T. 8S.,R. 2E., sec. 18.. ....do T.8S., R. 2E., sec. 19.. do do do T. 8S.,R. 2E.,sec. 20.. T. 8S., R. 2E., sec. 21.. do do do T.8S., R. 2E., sec. 22.. do T. 8S.,R.2E., sec. 23.. do do T. 8S., R. 2E., sec. 2.5.. T. 8S., R. 2 E., sec. 26. do T. 8S., R. 2 E., sec. 27. do T. 8S., do. T. 8 S. do. do. do. R. 2 E., sec. 28.... R. 2 E., sec. 29. Diame- ter. Depth. Height of water. Inches. Feet. 438 366 380 175 112 175 225 400 230 350 400 390 142 430 280 260 220 405 380 423 I 374 380 400 j 500 373 i 160 I 380 450 I 412 ! 387 j 170 ; 130 i 45 I 475 j 333 250 560 400 286 385 3(i0 250 137 318-320 425 385 415 450 175 Feet. Yield yer minute. Gallons. + + 10 + 4- + + 12 + 10 + + + 10 « Owner's name unknown. 74 UNDERGEOUI^D WATER IN VALLEYS OF UTAH. Weils in Jordan River and Utah Lalce valleys — Continued. Name of owner. Stewart's ranch C. Hickman S. P. Lorensen. . P. J. Lundale J. Howe J. J. Hansen G. Staley , Do W. O. Creer Creamery J. Anderson M. C. King Do («) Sugar factory... T. B. Jones (a) H. A. Harlan J. P.Holt J. G. Robertson. G. LeBaron McBeath J. Webb F. Rouse J. E. Gardner... (a) (a) (a) (a) (a) (a) S. Douglas Do Dixon Bros P. Windward T. E. Daniels C. Long D. LeBaron («) A. Bingham Do Creamery C. Hanks A. Burke J. Sheen O. R. Thomas... H. Boyle J. Job Do W. M. Phillippi. . (a) Rudd estate A. Steele E. Hawkins H. Johnson Location. R. 2 E.,sec R. 2E., R. 2E., sec. 32. sec. 33. T. 8S., do. do. T. 8S., T. 8S., do do do T. 8S., R. 2 E., sec. 35. T. 8S., R. 3E., sec. 4.. T. 8S., R. 3E., sec. 5.. T. 8S., R. 3E., sec. 7.. do T. 8S., R. 3E., sec. 8.. ....do T. 8S., R. 3E., sec. 21. T. 8S., R. 3E., sec. 30. ....do ....do ....do.. T. 9 S., R. 1 E., sec. 7.. 1 E., sec. 12. 1 E., sec. 13. 1 E., sec. 32. 2E., sec. 1.. T. 9S., T. 9S., T. 9S., T. 9S., do. T. 9S., do. T. 9S., .....do. do. R. 2 E., sec' 2. R. 2 E., sec. 3. T. 9S., do. do. do. T. 9S., do. T. 9S., T. T. R. 2E., sec. 5. R. 2 E., sec. R. 2E., sec. 7. Diame- r»oT^+T1 Height of Yield per tor -L'epUl. WQtor miniito Inches. ., R. 2 E., sec. 10 ., R. 2E., sec. 11 , T. 9 S., R. 2E., sec. 29 T. 9 S., R. 2E., sec. 30 T. 9S., R. 1 W.,sec. 25 T. 9S.,R. 1 W., sec. 26 T. 9 S., R. 1 W., sec. 33 T. 9S., R. 1 W., sec. 35 T. 9 S., R. 1 W., sec. 36 T. 10 S., R. IE., sec. 6 T. 10 S., R. IE., sec. 17 T. 10S.,R. 1 W., sec. 2 ! a Owner's name unknown. Feet. 172 163 175 200 380 185 380 20 144 145 170 154 30 123 22 140 30 100 247 180 290 155 200 200 160 375 228 50 130 300 140 116 160 217 438 196 275 225 175 296 279 20 90-126 50- 60 220 165 200 58 85 130 407 water. Feet. + + + + + + + + 15 + 1 + 20 + 16i 125 80 LIST OF TYPICAL WELLS. 75 Wells in Jordan River and Utah Lake valleys — Continued. Name of ownor. Location. Diame- ter. Depth. Height of water. Yield per minute. W. M. Phillippi W, C. Albertson T. 10 S., R. 1 W., sec. 4 Inches. 2 2 2 2 2 2 Feet. 168 178 ' 307 300 420 77 412 70 334 160 8 50 70 60 53 116 238 138 Feet. -100 - 3 - 4 - 4 - 3 - 20 - 86 -222 Gallons. T. 10 S., R. 1 W., sec. 9 J. Riley do Do do Baxter. . .do P. Okleberry T. 10 S., R. 1 W., sec. 11 (°) T. 10 S., R. 1 W., sec. 12 ...do Rio Grande Western Rwv do W. Finch T. 10 S., R. 1 W., sec. 14 2 L. E. Thomas T. 10 S., R. 1 W., sec. 15 Goshen Wells do u 2 2 2 2 2 2 Do do . ..do H. L. Cook do Allen.-. T. 10 S., R. 1 W., sec. 21 T. 10 S., R. 1 W.,sec. 30 (°) T. 10 S., R. 1 W., sec. 33. . a Owner's name unknown. INDEX A. ■ Page. Alpine, water supply of 49 American Fork (town), water supply of, source of 49 wells in 49-50 American Fork (stream) , description of ... . 6, 49 discharge and run-off of, table showing. 21 view of 50 water from, analysis of 30 use of 49 American Smelting and Refining Company, well of, record of 46 wells of, water from, analysis of 32 Analyses of water from various streams and springs 30, 32 Artesian wells. See Wells, flowing. B. Battle Creek, description of 6 drainage of, effect of, on wells ..r 51 water of, use of 49 Bear River, description of 6 Beck's hot spring, water from, analysis of. . 30 Bed rock, water from 50, 53 water from, methods of obtaining 37, 40 Benjamin, underground water conditions at. 54 Big Cottonwood Creek, description of 7, 45 discharge and run-off of, table showing. 21,25 rocks on 9 water from, analysis of 30 use of 44, 45 Big Cottonwood Creek Valley, seepage measurements in 28 Big Hollow Creek, description of 53 Bingham, mines at, water in 37,40 rocks near : 10 water supply of, source of 40 Bingham Canyon, placer mining in 40 Bingham Consolidated Company, wells of. . 37 Bingham Creek, description of 39 Bingham Junction, smelters at 5 wells at, water from, analyses of 32 Bonneville region, Pleistocene history of... 12-13 Bonneville shore line, description of 12-13 Bonneville terrace, description of 47 Boutwell, J. M., on discharge of Ontario tunnel 37 on Park City and Bingham mining dis- tricts 8 on well drilled for oil 41 Brown, R. E., analyses of water by 30 Bureau of Soils, Department of Agriculture, experiments in reclaiming land near Salt Lake City made by 43 Butterfield Canyon, springs m 40 tunnels driven for water m 37 Butterfield Creek, description of 39 Butterfield tunnel, water in, litigation caused by 40 Page. Cambrian fossils, occurrence of I Cambrian rocks, occurrence of 9, Cameron, F. K., analyses of water by Cannon farm, well on I Capitol llill, reservoir on ! Carboniferous rocks, occurrence and char- acter of 9, City canal, discharge of City Creek, description of discharge and run-off of, table showing. rocks on water from, analysis of use of Clarke, F. W., analysis of water by Climate, character of Colorado Fish Company, well of, descrip- tion of Comer, H. C, on general section in vicinity of Lehi Converse, W. A., analyses of water by Cooper, William, well of, water from, anal- ysis of Cottonwood Canyon, view in Cox, A . , well of Currant Creek, description of reservoir on, failure of rocks on water from, analysis of use of 10 10 11 30 41 45 10 11 24 7 19 8 30 44 ,45 30 33 13 -18 Dalton and Lark tunnel, description of water in, occurrence of Dams, subsurface, recovery of underground water by De Bernard, J. H., analyses of water by Dead Mans Falls, Cottonwood Canyon, plate showing Dearborn laboratories, analyses of water by. Decker Lake, ditch at outlet of, discharge of. Devonian rocks, occurrence of 8,9, 11 Doremus, A. F., spring discharge measured by Drainage, character of Drainage area discussed, map showing Draper, warm-water lakes near, description of Dry Cottonwood Creek, description of water from, analysis of Dry Creek, description of Dry Creek Canyon, springs in Du Chesne River, source of 44 5-7 6 47 7 30 6,48 49 East Jordan canal, discharge of East Tintic Mountains, location and eleva- tion of structure of Eighth South street ditch, discharge of 77 78 INDEX. rage. Electric power, development of 37, 39 Emigration Creek, description of 7 discharge and run-off of, table showing. 19 valley of, rocks in 9 syncline developed in 37 water from, analysis of 30 use of 44, 45 Emmons, S. F., on descriptive geology 7 Evans Spring, water of, use of 53 Evaporation at Utah Lake 17 F. Fault in Wasatch Mountains, description of 8,9,10 Flowing wells. See Wells, flowing. Fort Douglas, water supply of, source of . . 44 G. Gammon, Harry, wells of 35, 51 Gas, natural, occurrence of 32-33 Geneva, wells at 51 Geologic history, discussion of 11-13 Geology of the region 7-13 Gilbert, G. K., on Lake Bonneville 7, 11, 13 on oscillations of lake level between Provo and Bonneville horizons. 13 Girty, G. H., fossils found by 10 Goshen, springs near 55 water supply of, source of 55 well at, water from, analysis of 32 Goshen Valley, underground water condi- tions in 55-56 Great Salt Lake, elevation of 5 fluctuations of ■ 25-26 natural gas near 32 supply of, sources of 28, 33 water of, analyses of 33, 34 Grove Creek, description of 6 water of, use of 49 Guffey-Galey well, description of 41 H. Hague, Arnold, on descriptive geology 7 Heber, rainfall at, table showing 15 Highlands, descriptive geology of 8-11 Hobble Creek, description of 6 Homansville Canyon, water developed in.. . 56 Hot Springs Lake, outlet of, loss in flow at . 25 Humidity at Salt Lake City, table showing. 16 Hydrography of the area 18-26 I. Igneous rocks, occurrence of 8,9,10,11 Inland Crystal Salt Company, well of 43 Irrigation by artesian wells 36 J. Jap Pond, water of, character of 40 Jordan and Salt Lake City canal, head gate of, view of 12 wells sunk to increase supply of 49 Jordan Narrows, Jordan River and canal systems in, discharge of 24 shore lines on west side of 13 Page. Jordan River, area west of, divisions of 38-39 discharge of 24-25 flood plain of, wells sunk in 49 gate at head of, view showing 24 lowland area west of, description of 41-43 sewage discharge into 34 source and course of 6-7 tributaries of 7, 18-23 underground water east of, occurrence of 43-48 underground water west of, occurrence of 38-43 upland area west of, description of 39-41 water from, analyses of 30 Jordan River Valley, area of 5 drainage area of, map showing 6 ground water in, depth to, map show- ing 30 flowing wells in, area of, map showing.. 38 location and trend of 5 seepage in 24-25 topography and drainage of 5-7 K. Kimball Creek, springs in upper valley of . . 55 water of, use of ^5 wells along 56 King, Clarence, on geology of the region ... 7 Kingsbury, J. T., analyses of water by 30 Knight, N. J., wells of, description of 50-51 L. Lake Bonneville, description of 11-13 location of 5 shore deposits of 39, 55 Lake Lahontan, location of 11 Lake Mountains. See Pelican Hills. Lake shore, location of 54 Lakes, warm water, occurrence of 47 Lehi, artesian wells at, irrigation from 36 flowing and nonflowing well near, line separating 49 wells at 48 flow of, decrease in 36 water from, analyses of 32 Lehi and vicinity, underground water con- ditions of 48-49 Liberty Park, wells at and near, flow of — 36,44 Literature, geologic 7-8 Little Cottonwood Canyon, glaciers adja- cent to, relics of 47 Little Cottonwood Creek, description of 7, 45 discharge of 25 rocks on 9 water from, analysis of 30 use of 44 " Little Cottonwood granite," age of 9 Long Ridge, springs at base of 55 structure of 11 Lower Carboniferous fossils, occurrence of. . 10 M. McDonald, T. F., acknowledgment to 56 Mapleton Bench, descripton of 53 INDEX. 79 Massachusetts State Board of Health, on preservation of water supply from contamination 34-35 Measurement of wells, method of 56-59 Mercur, rocks near K) Mesozoic rocks, occurrence of 10 Metamorphic rocks, occurrence of 8 Mill Creek, description of 7,45 discharge and run-off of, table showing 20,25 ditch south of, discharge of 25 rocks on 9 water of, use of 44 Mill Creek Valley, seepage measurements in 28 Morgan, E. R., seepage measurements by.. 28 Mormon pioneers, irrigation by 5 Murray, smelters at 5 well at, record of 46 well near, decrease in 47 N. Natural gas, occurrence of 32-33 North J ordan canal, discharge of 24 O. Ogden quartzite, thickness of 8 Oil, search for 41 Ontario tunnel, discharge of 37 Oquirrh Mountains, elevation and extent of. 6 springs in 40 structure of 10 Ordovician rocks, occurrence of 11 P. • Paleozoic rocks, occurrence of 8,9 Paleozoic section in Wasatch Mountains, table showing 8 Palmyra, location of 54 Park City, mines of, water in 37 rainfall at, table showing 14 Parleys Canyon, reservoir at 45 Parleys Creek, description of 7,45 discharge and run-oflf of, table showing 20,25 rocks on 9 water from, analysis of 30 use of 44,45 i';irsons Chemical Company, analyses of water by 32 Payson, artesian well at, irrigation from 36 location of 54 water supply of, source of 54 Payson Creek, water from, analysis of 30 Pelican Hills, location and altitude of 6 structure of 10-11 Pelican Point, flowing wells near 56 seep springs near 56 Permian rocks, occurrence and character of. 9 Peteeneet Creek, description of Pipes, flow from vertical and horizontal, diagram illustrating 57 Placer mining in Bingham Canyon 40 Pleasant Grove, location and underground water conditions of 50-51 water supply of, source of 49 Pleistocene fault, occurrence of 5? Page. Pleistocene rocks, occurrence of 10 water in, character of 43 Porous deposits, rainfall absorbed by 39-40 Pre-Cambrian rocks, occurrence and char- acter of 8,9 Precipitation, tables showing 14-15, 19-22 Provo, location of 5 rainfall at, table showing 15 sewage of, disposal of 34 temperature at, table showing 15 vicinity of, underground water con- ditions in 51-52 water supply of, source of 51 wells at , 32, 52 Provo horizon, tufa at, occurrence and character of 13 Provo River, discharge and run-off of, table showing 22 drainage area of 6 source and course of 6 valley of, below mouth of canyon, view of , '. 50 water from, analysis of 30 Provo shore line, description of 12-13 Pumping plants for irrigation, favoral)le conditions for 39 Pyle, F. D. , acknowledgment to 56 Q- Quaternary history of the region 11-13 R. Rainfall, tables showing 14-15. 19-22 Reclamation Service, levels run by 52 plans of, for Utah Lake project 39 " Red Beds," occurrence and character of.. 9 Red Butte Canyon, rocks in 9 Red Butte Creek, description of 7 water from, analysis of 30 use of 44-45 Reservoirs, profitable locations for 38 Richardson, G. B., on natural gas near Salt Lake City 32 Riggs, R. B., analyses of water by 30 Rio Grande Western Railway, wells of 32, 42, 44, 48, 52 Rock Creek Canyon, rocks in 10 Rose Canyon . springs in 40 Rudy Well , description of 35. 42, 43 S. Salt Creek, source and course of 6 Salt Lake City , authorities of, wells sunk by, inl890 49 humidity , mean relative, at 16, 18 location of 5, 43 lowland area south of, description of .. 45-47 natural gas supply of, source of 32-33 rainfall at 14, 17-18 rocks in vicinity of 8,9 sewage of, disposal of 34 temperature at 15. 16, 18 thermal springs at. description of 44 underground water conditions of 43-45 80 II^DEX. Page. Salt Lake City, upland area south of, de- scription of 47-48 water supply of, precaution to avoid contamination of 34 source of 44-45 wells at 42, 44 flow of , decrease in 36 wind velocity at, table showing average. 16 Salt Lake City Spring, water from, analysis of 30 Salem, location of 54 underground water conditions in 54 San Pedro, Los Angeles and Salt Lake Rail- road, wells of 48,52,53,54 Sandy Spring, water from, analysis of 30 Santaquin, location of 54 water supply of, source of 54 Santaquin Creek, description of 6 water from, analysis of 30 use of 54 Sedimentary rocks, occurrence of 8, 9, 11 Seepage, measurements of 28 Sewage, disposal of, precautions taken for. 34 Silurian rocks, occurrence of 8,9, 11 Slichter, C. S., on measurement of water flow from pipes 56 on method of measurement of wells 56-59 Smelters, smoke from, injury by 32 Smith, G. O., and Tower, G. W., on ground water in Homansville Canyon. . 56 on the Tintic district 7 Smith, J. F., jr., discharge data furnished by 24 Snow, G. W., acknowledgment to 56 South Jordan canal, description of 39 discharge of 24 Spanish Fork (town) , location of 53 water supply of, source of 53-54 wells at 53-54 flow of, decrease in. . . : 36 Spanish Fork (stream), discharge and run- off of, table showing 22 drainage area of .^ 6 source and course of - 6 water from, analysis of 30 use of ^ 54 Spring Creek, flow of 46, 52 Spring Lake, location of .' 54 water supply of, source of 54 Springs, occurrence of 40, 44, 47, 50, 55 water of, character of 31 Springs, hot, occurrence of 29, 49 Springville, description of 53 vicinity of, underground water condi- tions in 52-53 wells at 53 water from, analysis of 32 Spurr, J. E., or the Mercur mines 7-8 Stanbury Island, shore lines on 13 Streams, water of, character of 30, 31 Structure of the Highlands 8-ll Swendsen, G. L., acknowledgments to 24 hot springs discovered by '. 49 T. Page. Tanner, Caleb, acknowledgment to 51 discharge measurement by 25 Taylorville roller mill, flume at, discharge at 25 Temperature, tables showing 15-16 Tertiary history of the region 11 Tertiary rocks, occurrence of 8, 10, 11 Thistle, rainfall at, table showing 15 Timpanogas canal, seepage of 28 Tintic Mountains, springs in 55 Todd, J. E., on measurement of water flow from pipes t 56 Topography, features of 5-7 Tower, G. W., and Smith, G. O., on ground water in Homansville Canyon. . 56 on the Tintic district 7 Traverse Mountains, structure of 8-9, 10 Tufa, calcareous, occurrence and character of 13 U. Underground water. See Water, under- ground. United States Mining Company, wells of, water from, analyses of 32 United States Weather Bureau, meteoro- logic data from records of 13-17 Utah and Salt Lake canal, description of . . 39 discharge of 24 Utah County Infirmary, well at 52 Utah Experiment Station, experiments in .reclaiming land near Salt Lake City made by 43 Utah Lake, description of 6 elevation of 5 evaporation at 17 fluctuations of 23-24 hot springs at 49 northern end of, view of 12 sewage discharge into 34 streams tributary to 6, 18-23 supply of, source of 23-24 underground water west of, occurrence of 56 water from, analyses of 30 Utah Lake project, plans for 39 Utah Lake Valley, area of 5 drainage area of, map showing 6 flowing wells in, area of, map showing. . 48 ground water in, depth to, map show- ing 30 location and trend of 5 topography and drainage of 5-7 undergrond water in, occurrence of 48-56 Utah Sugar Company, wells of 48 wells of, water from, analysis of 32 Ute limestone, thickness of & v.. Vegetation, character of 7 Volcanic rock, outcrop of 8. INDEX. 81 W. Page. Wadley, Williair, & Sons, water developed bj ,unneling into bed rock .50 Walcott, C. D., on Big Cottonwood Cam- brian section 7 Wann Creek, source of 31,55 water from, analysis of 30 Wasatch fault, description of 8,9, 10 Wasatch limestone, occurrence, thickness, and dip of 8 Wasatch Mountains, elevation of 5,6 geology of 8-9 Paleozoic section in 8 rainfall caused by 18 vegetation on 7 view of 5 Water, analyses of 30,32 contamination of, precaution taken to avoid 34 sanitary character of 34 Water, underground, depth to, map show- ing 30 distribution of 29-30 occurrence of 38-56 quality of 30-35 recovery of 35-37 source of 27-28 Water resources, use of, efficiency in 38 Weber quartzite, occurrence, thickness, and dip of 8 Weber River, description of 6 IRR 157—06 6 Page. Well sections, plate showing 28 Wells, data concerning 56-75 method of measurement of 56-59 water from, analyses of 32 W'ells, flowing, area of, in Jordan stiver Val- ley, map showing 38 area of, in Utah Lake Valley, map showing 44 decrease in, cause of 36 location and description of 35-36, 46,50,52,53,54-55 recovery of water by 36 water of, use of 36 yield of, table for determining 58 Wells, shallow, recovery of water by 36 Wells, typical, list of 59-75 West Jordan, well at, water from, analysis of 32 West Mountain, warm spring near 55 Westfall, J., information furnished by 52 Westphal, Gus, well record furnished by... 42 Widtsoe, J. A., on effects of smelter smoke. 32 Willow Creek, description of 7 Wilson, H. M., on wind velocity required for windmills 36 Wind velocity at Salt Lake City, table showing average 16 Windmills, wind velocity required for 36 Y. Yeager, H. F., well record furnished by 46 CLASSIFICATION OF THE PUBLICATIONS OF THE UNITED STATES GEOLOGICAL SURVEY. [Water-Supply Paper No. 157.] The serial publications of the United States Geological Survey consist of (1) Annual Reports, (2) Monographs, (3) Professional Papers, (4) Bulletins, (5) Mineral Resources, (6) Water-Supply and Irrigation Papers, (7) Topographic Atlas of United States — folios and separate sheets thereof, (8) Geologic Atlas of the United States — folios thereof. The classes numbered 2, 7, and 8 are sold at cost of publica- tion; the others are distributed free. A circular giving complete lists may be had on application. Most of the above publications may be obtained or consulted in the following ways: 1. A limited number are delivered to the Director of the Survey, from whom they may be obtained, free of charge (except classes 2, 7, and 8), on application. 2. A certain number are delivered to Senators and Representatives in Congress, for distribution. 3. Other copies are deposited with the Superintendent of Documents, Washington, D. C, from whom they may be had at prices slightly above cost. 4. Copies of all Government publications are furnished to the principal public libraries in the large cities throughout the United States, where they may be con- sulted by those interested. The Professional Papers, Bulletins, and Water-Supply Papers treat of a variety of subjects, and the total number issued is large. They have therefore been classified into the following series: A, Economic geology; B, Descriptive geology; C, System- atic geology and paleontology; D, Petrography and mineralogy; E, Chemistry and physics; F, Geography; G, Miscellaneous; H, Forestry; I, Irrigation; J, Water stor- age; K, Pumping water; L, Quality of water; M, General hydrographic investiga- tions; N, Water power; O, Underground waters; P, Hydrographic progress reports. This paper is the eighty-sixth in Series B, and the fifty-third in Series O, the compete lists of which follow (PP= Professional Paper; B=Bulletin; WS= Water-Supply Paper) : SERIES B, DESCRIPTIVE GEOLOGY. B '2'6. Observations on the junction, between the Eastern sandstone and the Keweenaw series on Keweenaw Point, Lake Superior, by R. D. Irving and T. C. Chamberlin. 1885. 124 pp., 17 pis. (Out of stock.) B 33. Notes on geology of northern California, by J. S. Diller. 1886. 23 pp. (Out of stock.) B 39. The upper beaches and deltas of Glacial Lake Agassiz, by Warren Upham. 1887. 84 pp., 1 pi. (Out of stock.) B 40. Changes in river courses in Washington Territory due to glaciation, by Bailey Willis. 1887. 10 pp., 4 pis. (Out of stock.) B 45. The present condition of knowledge of the geology of Texas, by R. T. Hill. 1887. 94 pp. (Out of stock.) B 53. The geology of Nantucket, by N. S. Shaler. 1889. 55 pp., 10 pis. (Out of stock.) B 57. A geological reconnaissance in southwestern Kansas, by Robert Hay, 1890. 49 pp., 2 pis. (Out of stock.) B 58. The glacial boundary in western Pennsylvania, Ohio, Kentucky, Indiana, and Illinois, by G. F. WrJ.,3:ht, with introduction by T. C. Chamberlin. 1890. 112 pp., 8 pis. (Out of stock.) II SERIES LIST. B 67. The relations of the traps of the Newark system in the New Jersey region, by N. H. Darton. 1890. 82 pp. (Out of stock.) B 104. Glaciation of the Yellowstone Valley north of the Park, by W. H. Weed. 1893. 41 pp., 4 pis. (Out of stock.) B 108. A geological reconnaissance in central Washington, by I. C. Russell. 1893. 108 pp., 12 pis. (Out of stock.) B 119. A geological reconnaissance in northwest Wyoming, by G. H. Eldridge. 1894. 72 pp., 4 pis. (Out of stock.) B 137. The geology of the Fort Riley Military Reservation and vicinity, Kansas, by Robert Hay. 1896. 35 pp., 8 pis. B 144. The moraines of the Missouri Coteau and their attendant deposits, by J. E. Todd. 1896. 71 pp., 21 pis. B 158. The moraines of southeastern South Dakota and their attendant deposits, by J. E. Todd. 1899. 171 pp., 27 pis. B 159. The geology of eastern Berkshire County, Massachusetts, by B. K. Emerson. 1899. 139 pp., 9 pis. B 165. Contributions to the geology of Maine, by H. S. Williams and H. E. Gregory. 1900. 212 pp., 14 pis. WS 70. Geology and water resources of the Patrick and Goshen Hole quadrangles in eastern Wyoming and western Nebraska, by G. I. Adams. 1902. 50 pp., 11 pis. B 199. Geology and water resources of the Snake River Plains of Idaho, by I. C. Russell'. 1902. 192 pp., 25 pis. PP 1. Preliminary report on the Ketchikan mining district, Alaska, with an introductory sketch of the geology of southeastern Alaska, by A. H. Brooks. 1902. 120 pp., 2 pis. PP 2. Reconnaissance of the northwestern portion of Seward Peninsula, Alaska, by A. J. Collier. 1902. 70 pp., 11 pis. PP 3. Geology and petrography of Crater Lake National Park, by J. S. Diller and H. B. Patton. 1902. 167 pp., 19 pis. PP 10. Reconnaissance from Fort Hamlin to Kotzebue Sound, Alaska, by way of Dall, Kanuti, Allen, and Kowak rivers, by W. C. Mendenhall. 1902. 68 pp., 10 pis. PP 11. Clays of the United States east of the Mississippi River, by Heinrich Ries. 1903. 298 pp., 9 pis. PP 12. Geology of the Globe copper district, Arizona, by F. L. Ransome. 1903. 168 pp., 27 pis. PP 13. Drainage modifications in southeastern Ohio and adjacent parts of West Virginia and Ken- tucky, by W. G. Tight. 1903. Ill pp., 17 pis. B 208. Descriptive geology of Nevada south.of the fortieth parallel and adjacent portions of Cali- fornia, by J. E. Spurr. 1903. 229 pp., 8 pis. B 209. Geology of Ascutney Mountain, Vermont, by R. A. Daly. 1903. 122 pp., 7 pis. WS 78. Preliminary report on artesian basins in southwestern Idaho and southeastern Oregon, by I. C. Russell. 1903. 51 pp., 2 pis. PP 15. Mineral resources of the Mount Wrangell district, Alaska, by W. C. Mendenhall and F. C. Schrader. 1903. 71pp., 10 pis. PP 17. Preliminary report on the geology and water resources of Nebraska west of the one hundred and third meridian, by N. H. Darton. 1903. 69 pp., 43 pis. B 217. Notes on the geology of southwestern Idaho and southeastern Oregon, by I. C. Russell. 1903. 83 pp., 18 pis. (Out out stock.) B 219. The ore deposits of Tonopah, Nevada (preliminary report), by J. E. Spurr. 1903. 31 pp., 1 pi. (Out of stock.) PP 20. A reconnaissance in northern Alaska in 1901, by F. C. Schrader. 1904. 139 pp., 16 pis. PP 21. The geology and ore deposits of the Bisbee quadrangle, Arizona, by F. L. Ransome. 1904. 168 pp., 29 pis. WS 90. Geology and water resources of part of the lower James River Valley, South Dakota, by J. E. Todd and C. M. Hall. 1904. 47 pp., 23 pis. PP25. The copper deposits of the Encampment district, Wyoming, by A. C.Spencer. 1904. 107 pp., 2 pis. PP 26. Economic resources of northern Black Hills, by J. D. Irving, with chapters by S. F. Emmons and T. A. Jaggar, jr. 1904. 222 pp., 20 pis. PP 27. Geological reconnaissance across the Bitterroot Range and the Clearwater Mountains in Mon- tana and Idaho, by Waldemar Lindgren. 1904. 122 pp., 15 pis. PP 31. Preliminary report on the geology of the Arbuckle and Wichita mountains in Indian Terri- tory and Oklahoma, by J. A. TafE, with an appendix on reported ore deposits in the Wichita Mountains, by H. F. Bain. 1904. 97 pp., 8 pis. B 235. A geological reconnaissance across the Cascade Range near the forty-ninth parallel, by G. O. Smith and F. C. Calkins. 1904. 103 pp., 4 pis. B 236. The Porcupine placer district, Alaska, by C. W. Wright. 1904. 35 pp., 10 pis. B 237. Igneous rocks of the High wood Mountains, Montana, by L. V. Pirsson. 1904. 208 pp., 7 pis. B 238. Economic geology of the lola quadrangle, Kansas, by G. I. Adams, Erasmus Haworth, and W.R.Crane. 1904. 83 pp., 1 pi. SERIES LIST. Ill PP 32. Geology and underground water resources of the central Great Plains, by N. H. Darton. 1905. 433 pp., 72 pis. WS 110. Contributions to hydrology of eastern I'nited States, 1904; M. G. Fuller, geologist in charge. 1905. 211 pp., 5 pis. B 242. Geology of the Hudson Valley between the Hoosic and the Kinderhook, by T. Nelson Dale. 1904. 63 pp., 3 pis. PP 34. The Delavan lobe of the Lake Michigan glacier of the Wisconsin stage of glaciation and as.sociated phenomena, by W. C. Alden. 1904. 106 pp.. 15 pis. PP 36. Geology of the Perry Basin in southeastern Maine, by G. O. Smith and David White. 1905. 107 pp., 6 pis. B 243. Cement materials and industry of the United States, by E. C. Eckel. 1905. 395 pp., 15 pis. B 246. Zinc and lead deposits of northwestern Illinois, by H. F. Bain. 1904. 56 pp., 5 pis. B 247. The Fairhaven gold placers of Seward Peninsula, Alaska, by F. H. Moffit. 1905. 85 pp., 14 pis. B 249. Limestones of southwestern Pennsylvania, by F. G. Clapp. 1905. 52 pp., 7 pis. B 2.50. The petroleum fields of the Pacific coast of Alaska, with an account of the Bering River coal deposit, by G. C. Martin. 1905. 64 pp., 7 pis. B 241. The gold placers of the Fortymile, Birch Creek, and Fairbanks regions, Alaska, by L. M. Prindle. 1905. 89 pp., 16 pis. WS 118. Geology and water resources of a portion of east central Washington, by F. C. Calkins. 1905. 96 pp., 4 pis. B 252. Preliminary report on the geology and water resources of central Oregon, by I. C. Russell. 1905. 138 pp., 24 pis. PP 36. The lead, zinc, and fluorspar deposits of western Kentucky, by E. O. Ulrich and W. S. Tangier Smith. 1905. 218 pp., 15 pis. PP 38. Economic geology of the Bingham mining district of Utah, by J. M. Boutwell, with a chapter on areal geology, by Arthur Keith, and an introduction ongeneral geology, by S. F. Emmons. 1905. 413 pp., 49 pis. PP 41. The geology of the central Copper River region, Alaska, by'W. C. Mendenhall. 1905. 133 pp., 20 pis. B 254. Report of progress in the geological resurvey of the Cripple Creek district, Colorado, by Walde- mar Lindgren and F. L. Ransome. 1904. 36 pp. B 255. The fluorspar deposits of southern Illinois, by H. Foster Bain. 1905. 75 pp., 6 pis. B 256. Mineral resources of the Elders Ridge quadrangle, Pennsylvania, by R. W. Stone. 1905. 86 pp., 12 pis. B 257. Geology and paleontology of the Judith River beds, by T. W. Stanton and J. B. Hatcher, with a chapter on fossil plants, by F. H. Knowlton. 1905. 174 pp., 19 pis. PP 42. Geology of the Tonopah mining district, Nevada, by J. E. Spurr. 1905. 295 pp., 23 pis. WS 123. Geology and underground water conditions of the Jornada del Muerto, New Mexico, by C. R. Keyes. 1905. 42 pp., 9 pis. WS 136. Underground waters of Salt River Valley, Arizona, by W. T. Lee. 1905. 194 pp., 24 pis. PP 43. The copper deposits of the Clifton-Morenci district, Arizona, by Waldemar Lindgren. 1905. 375 pp., 25 pis. B 265. Geology of the Boulder district, Colorado, by N. M. Fenneman. 1905. 101 pp., 5 pis. B 267. The copper deposits of Mi.ssouri, by H. F. Bain and E. O. Ulrich. 1905. 52 pp., 1 pi. PP 44. Underground water resources of Long Island, New York, by A. C. Veatch and others. 1905. 394 pp., 34 pis. WS 148. Geology and water resources of Oklahoma, by C. N. Gould. 1905. 178 pp., 22 pis. B 270. The configuration of the rock floor of Greater New York, by W. H. Hobbs. 1905. 96 pp., 5 pis. B 272. Taconic physiography, by T. N. Dale. 1905. 52 pp., 14 pis. (Out of stock.) PP 45. The geography and geology of Alaska, a summary of existing knowledge, by A. H. Brooks. with a section ofi climate, by Cleveland Abbe, jr., and a topographic map and description thereof, by R. U. Goode. 1906. 327 pp., 34 pis. B 273. The drumlins of southeastern Wisconsin (preliminary paper), by W. C. Alden. 1905. 46 pp.. 9 pis. PP 46. Geology and underground water resources of northern Louisiana and southern Arkansas, by A. C. Veatch. 1906. I'P 49. Geology and mineral resources of part of the Cumberland Gap coal field, Kentucky, by G. H. Ashley and L. C. Glenn, in cooperation with the State Geological Department of Kentucky, C. J. Norwood, curator. 1906. 239 pp., 40 pis. PP 50. The Montana lobe of the Keewatin ice sheet, by F. H. H. Calhoun. 1906. B 277. Mineral resources of Kenai Peninsula, Alaska: Gold fields of the Turnagain Arm region, by F. H. Motfit, and the coal fields of Kachemak Bay region, by R. W. Stone. 1906, WS 154. The geology and water resources of the eastern portion ot the Panhandle of Texas, by C. N. Gould. 1906. 64 pp., 15 pis. B 278. Geology and coal resources of the Cape Li.sburne region. Alaska, by A. J. Collier. B 279. Mineral resources of the Kittanning and Rural Valley quadrangles, Pennsylvania, by Charles Butts. IV SERIES LIST. B 280. The Rampart gold placer region, Alaska, by L. M. Prindle and F. L. Hess. B 282. Oil fields of the Texas-Louisiana Gulf coastal plain, by N. M. Fenneman. WS 157. Underground water in the valleys of Utah Lake and Jordan River, Utah, by G. B. Richardson. 1906. 81 pp., 9 pis. SERIES O— UNDERGROUND WATERS. WS 4. A reconnaissance in southeastern Washington, by I. C. Russell. 1897. 96 pp., 7 pis. (Out of stock.) WS 6. Underground waters of southwestern Kansas, by Erasmus Haworth. 1897. 65 pp., 12 pis. (Out of stock.) WS -7. Seepage waters of northern Utah, by Samuel Fortier. 1897. 50 pp., 3 pis, (Out of stock.) WS 12. Underground waters of southeastern Nebraska, by N. H. Darton. 1898. 56 pp., 21 pis. (Out of stock.) WS 21. Wells of northern Indiana, by Frank Leverett. 1899. 82 pp., 2 pis. (Out of stock.) WS 26. Wells of southern Indiana (continuation of No. 21), by Frank Leverett. 1899. 64 pp. (Out of stock.) WS 30. Water resources of the Lower Peninsula of Michigan, by A. C. Lane. 1899. 97 pp., 7 pis. (Out of stock.) WS 31. Lower Michigan mineral waters, by A. C. Lane. 1899. 97 pp., 4 pis. (Out of stock.) WS 34. Geology and water resources of a portion of southeastern South Dakota, by J. E. Todd. 1900. 34 pp., 19 pis. WS 53. Geology and water resources of Nez Perces County, Idaho, Pt. I, by I. C. Russell. 1901. 86 pp., 10 pis. (Out of stock.) WS 54. Geology and water resources of Nez Perces County, Idaho, Pt. II, by I. C. Russell, 1901 87-141 pp. (Out of stock.) WS 55. Geology and water resources of a portion of Yakima County, Wash., by G. O. Smith. 1901 68 pp., 7 pis. (Out of stock.) WS 57. Preliminary list of deep borings in the United States, Pt. I, by N. H. Darton. 1902. 60 pp (Out of stock.) WS 59. Development and application of water in southern California, Pt. I, by J. B. Lippincott 1902. 95 pp., 11 pis. (Out of stock.) WS 60. Development and application of water in southern California, Pt. II, by J. B. Lippincott, 1902. 96-140 pp. (Out of stock.) WS 61. Preliminary list of deep borings in the United States, Pt. II, by N. H. Darton. 1902. 67 pp (Out of stock.) WS 67. The motions of underground waters, by C- S. Slichter. 1902. 106 pp., 8 pis. (Out of stock.) B 199. Geology and water resources of the Snake River Plains of Idaho, by I. C. Russell. 1902. 192 pp., 25 pis. WS 77. Water resources of Molokai, Hawaiian Islands, by Waldemar Lindgren. 1903. 62 pp., 4 pis. WS 78. Preliminary report on artesian basin in southwestern Idaho and southeastern Oregon, by I. C. Russell. 1903. 53 pp., 2 pis. PP 17. Preliminary report on the geology and water resources of Nebraska west of the one hundred and third meridian, by N. H. Darton. 1903. 69 pp., 43 pis. WS 90. Geology and water resources of a part of the lower James River Valley, South Dakota, by J. E. Todd and C. M. Hall. 1904. 47 pp., 23 pis. WS 101. Underground waters of southern Louisiana, by G. D. Harris, with discussions of their uses for water supplies and for rice irrigation, by M. L. Fuller. 1904. 98 pp., 11 pis. WS 102. Contributions to the hydrology of eastern United States, 1903, by M. L. Fuller. 1904. 522 pp. WS 104. Underground waters of Gila Valley, Arizona, by W. T. Lee. 1904. 71 pp., 5 pis. WS 110. Contributions to the hydrology of eastern United States, 1904; M. L. Fuller, geologist in charge. 1904. 211 pp., 5 pis. PP 32. Geology and underground water resources of the ceiitral Great Plains, by N. H. Darton. 1904. 433 pp., 72 pis. (Out of stock.) WS 111. Preliminary report on underground waters of Washington, by Henry Landes. 1904. 85 pp. ipl. WS 112. Undertiow tests in the drainage basin of Los Angeles River, by Homer Hamlin. 1904. 55 pp., 7 pis. WS 114. Underground waters of eastern United States; M. L. Fuller, geologist in charge. 1904. 285 pp., 18 pis. WS 118. Geology and water resources of east-central Washington, by F. C. Calkins. 1905. 96 pp., 4 pis. B 252. Preliminary report on the geology and water resources of central Oregon, by I. C. Russell. 1905. 138 pp., 24 pis. WS 120. Bibliographic review and index of papers relating to underground waters published by the United States Geological Survey, 1879-1904, by M. L. Fuller. 1905. 128 pp. WS 122. Relation of the law to underground waters, by D. W. Johnson. 1905, 55 pp. SERIES LIST. V WS 123. Geology and underground water conditions of the Jornada del Muerto. New Mexico, by C. R. Keyes. 1905. 42 \>\k. y pis. \VS 136. Underground waters of the Salt River Valley, by \V. T. Lee. 1905. 194 pp., 24 pis. B 2M. Record of deep-well drilling for 1904, by M. L. Fuller, E. F. Lines, and A. C. Veatch. 1905. 106 pp. PP 44. Underground water resources of Long Island, New York, by A. C. Veatch and others. 1905. 394 pp., 34 pis. WS 137. Development of underground waters in the eastern coastal plain region of southern Caliioniia, by W. C. Mendenhall. 1905. 140 pp.. 7 pis. WS 13S. Development of underground waters in the central coastal plain region of southern Califor- nia, by W. C. Mendenhall. 1905. 1G2 pp., 5 pis. WS 139. Development of underground waters in the western coastal plain region of southern Cali- fornia, by W. C. Mendenhall. 1905. 105 pp., 7 pis. WS 140. Field measurements of the rate of movement of underground waters, by C. S. Slichter. 1905. 122 pp.. 15 pis. WS 141. Observations on the groundwaters of Rio Grande Valley, by C. S. Slichter. 1905. 83 pp., 5 pis. WS 142. Hydrology of San Bernardino Valley, California, by W. C. Mendenhall. 1905. 124 pp.. 13 pis. WS 145. Contributions to the hydroR)gy of eastern United States; M. L. Fuller, geologist in charge. 1905. 220 pp., 6 pis. WS 148. Geology and water resources of Oklahoma, by C. N. Gould. 1905. 178 pp., 22 pis. WS 149. Preliminary list of deep borings in the United States, second edition, with additions, by N. H. Darton. 1905. 175 pp. PP 46. Geology and underground water resources of northern Louisiana and southern Arkansas, by A. C. Veatch. 1906. WS 153. The underfloAV in Arkansas Valley in western Kansas, by C. S. Slichter. 1906. WS 154. The geology and water resources of the eastern portion of the Panhandle of Texas, by C. N. Gould. 1906. 64 pp., 15 pis. WS 155. Fluctuations of the water level in wells, with special reference to Long Island, New York, by A. C. Veatch. WS 157. Underground water in the valleys of Utah Lake and Jordan River, Utah, by G. B. Richardson. 1906. 81 pp., 9 pis. The following papers also relate to this subject: Underground waters of Arkansas Valley in eastern Colorado, by G. K. Gilbert, in Seventeenth Annual, Pt. II; Preliminary report on artesian waters of a portion of the Dakotas, by N. H. Darton, in Seventeenth Annual, Pt. II: Water resources of Illinois, by Frank Leverett, in Seventeenth Annual, Pt. II: Water resources of Indiana and Ohio, by Frank Leverett, in Eighteenth Annual, Pt. IV; New developments in well boring and irrigation in eastern South Dakota, by N. H. Darton, in Eighteenth Annual. Pt. IV; Rock waters of Ohio, by Edward Orton, in Nineteenth Annual, Pt. IV; Artesian well prospects in the Atlantic coastal plain region, by N. H. Darton, Bulletin No. 138. Corre-sjpondence should be addressed to The Director, United States Geological Survey, April, 1906. Washington, D, C. o 26 J906 Lo H 06 Xi'^