II l MOM STATE GEOLOGICAL SURVEY 3 3051 00000 1697 Digitized by the Internet Archive in 2012 with funding from University of Illinois Urbana-Champaign http://archive.org/details/pennsylvanianfus67dunb STATE OF ILLINOIS DWIGHT H. GREEN, Governor DEPARTMENT OF REGISTRATION AND EDUCATION FRANK G. THOMPSON, Director DIVISION OF THE STATE GEOLOGICAL SURVEY M. M. LEIGHTON, Chief URBANA BULLETIN NO. 67 PENNSYLVANIAN FUSULINIDAE OF ILLINOIS BY CARL O. DUNBAR and LLOYD G. HENBEST WITH A SECTION ON STRATIGRAPHY BY J. MARVIN WELLER, LLOYD G. HENBEST and CARL O. DUNBAR ERRATA Bulletin 67 — Pennsylvanian Fusulinidae of Illinois. Page 64— first column, line 8— "Karl" should be Carl. Page 75 — second column, line 9 — "mural" should be spiral. Page 108 — second column, line 8 below chart — "distensa" should be distenta. Page 210 — first column, last line — "syntype" should be paratype. ILLINOIS GEOLOGICAL SURVEY 14 (41700) PRINTED BY AUTHORITY OF THE STATE OF ILLINOIS urbana, Illinois ILLINOIS GEOLOGICAL 1942 SURVEY 1 1 BRA; Glenn, L. C, Kentucky Geol. Survey, Rpt. Prog. 1910-11, p. 27, 1912. 10 Butts, Charles, Geology of Hardin County : Illinois Oeol. Survey, Bull. 41, pp. 225, 228, 1920. 11 Wanless, H. R., Stratigraphic Introduction, in White, David, Lower Pennsylvanian Floras of Illinois: U. S. Geological Survey (unpublished manuscript). 12 This sandstone overlies the DeKoven coal and is named from exposures at Palzo, ten miles southeast of Marion, in Williamson County, Illinois. It is correlated by Wanless with the Sebree sandstone of western Ken- tucky. in a cyclic manner. 13 Weller later ob- served that such cyclic repetition is characteristic of all parts of the Penn- sylvanian section in Illinois and In- diana, 14 and Wanless proved that such cyclical repetitions are persistent over extensive areas and can be readily traced and correlated. 15 Each of these cyclical repetitions of beds or cyclothems may include the following sequence al- though such a complete succession of beds has been observed at very few localities. In general the upper cyclo- thems of the Eastern Interior basin ex- hibit . this succession much more com- pletely than do the lower ones: 10. Shale with ironstone concretions 9. Marine limestone 8. Black sheety shale with black limestone concretions or layers 7. Impure, lenticular, marine lime- stone 6. Shale 5. Coal 4. Underclay 3. " Fresh-water " limestone 2. Sandy shale 1. Sandstone, locally unconformable on underlying beds. Weller originally suggested that each cyclothem be considered a formation 16 but it is now apparent that some cyclo- thems are too thin or too indistinct to warrant recognition as separate forma- tions. 17 MARINE HOEIZONS Marine fossils are confined, with few exceptions, to beds 7 to 10 of the typical cyclothem. These beds present a great range in lithologic characters and each type of sediment includes its own more or less typical faunal assemblage. The "middle" limestone (No. 7) almost everywhere contains a great abundance of invertebrate remains, but the shells 13 Udden, J. A., Geology and mineral resources of the Peoria quadrangle: U. S. Geol. Survey Bull. 506, pp. 47-50, 1912. 14 Weller, J. M., Cyclical sedimentation of the Penn- sylvanian and its significance: Jour. Geol. vol. 38, pp. 97-135, 1930. 15 Wanless, H. R., Pennsylvanian cycles in western Illinois: Illinois Geol. Survey Bull. 60, pp. 179-193, 1931. 16 Weller, J. M., op. cit., p. 101. 17 Wanless, H. R., and Weller, J. M., Correlaton and extent of Pennsylvanian cyclothems: Geol. Soc. Amer. Bull. vol. 43, p. 1003, footnote, 1932. STRATIGRAPHY 11 are commonly crushed and broken so that few good specimens can be obtained. Although individuals are abundant, the fauna is generally restricted to a few common species of which Ambocoelia and the irregular tubes of a small worm or hyperamminid foraminifers are most conspicuous. The fauna of the black sheety shale (No. 8) is a very restricted one, both in variety and numbers. Conodonts are present almost everywhere. Inarticu- late brachiopods, a few species of pecti- noids, dermal tubercles, spines, and scales of fishes, and Estheria occur lo- cally, the last in considerable abundance in some of the higher cyclothems. A dif- ferent and more varied fauna occurs in some of the black limestone concretions included in the black shale, although at many places they are entirely nonfossili- f erous. This fauna is almost exclusively molluscan. Pelecypods, generally of non-pectinoid types, predominate, with fewer gastropods and cephalopods. At a few places these concretions have yielded more ammonoids than has any other type of rock. The black shale grades upward into gray calcareous shale, and this in turn grades into the upper marine limestone (No. 9). In several of the cyclothems these gray shales yield some of the most diverse, most abundant, and best pre- served marine faunas found in the Pennsylvanian strata in Illinois. Mol- luscan species generally predominate, with such gastropods as the pleurotoma- rids, bellerophontids, Meekospira, and Soleniscus, and such pelecypods as Nu- culopsis. Brachiopods, however, are likewise common and include produc- tids, chonetids, spiriferoids, Composita, and Derbya. Other types of fossils gen- erally present are foraminifers, frag- mentary bryozoans, dismembered cri- noids, ostracodes, horn corals, and ortho- cerids. The limestone bed (No. 9) is the chief fusuline-bearing member of the cyclo- them and seems to represent the culmin- ation of the cyclic marine submergence. This bed is generally not only more uni- form and persistent but also purer than the other limestones of the succession. For purposes of identification it is gen- erally the most important single bed present in the cyclothem. Its fauna is typically molluscoidean except in algal facies where molluscs may be more com- mon. Collecting from this bed, however, is generally unsatisfactory because good specimens are difficult to obtain from the hard matrix except where they have weathered out upon the surface. At some places fossils are very scarce. The upper shale (No. 10) is generally nonfossilif erous although the lower part may be calcareous and have a fauna similar to that in the upper part of bed 8. Ironstone or limestone bands and concretions which are present at various levels in this bed may be fossiliferous, however. Molluscs are generally more abundant in the ironstone and brachio- pods in the limestone bands. A few marine molluscs are occasion- ally present in the shale bed (No. 6). Fossils likewise occur sparingly at a few horizons in the beds below the coal seam. The "fresh-water" limestone (No. 3) is generally barren, but at some places it does contain a very few species of tiny molluscs, ostracodes, and fish teeth that are all quite distinct from any forms present in the typical marine faunas noted above, and in addition Spirorbis. A few marine fossils, mostly large pele- cypods and brachiopods, occur in thin calcareous zones in a few of the basal sandstone beds. In certain areas such a zone is fairly persistent in the sand- stone of the Shoal Creek cyclothem, and a similar one occurs in the sandstone of the Lower Livingston cyclothem. A few other fossiliferous sandstones are known, but with some exceptions their local stratigraphic relations are not clear. GENERAL STRATIGRAPHIC SUCCESSION No single bed in the entire Pennsyl- vanian system is known to be developed everywhere in the Eastern Interior basin. Many of them occur only in more or less restricted localities, and most of them change markedly in thickness and lithology from place to place. In spite of this characteristic variability of the 12 PENNSYLVANIA* 7 FUSULINIDAE ' Limestone outcrop I {v 6 Greenup Is. Omega Is. L Livingston Is. end La Salle Is. SC Shoal Creek Is. B Brereton Is. C Curlew Is. S Seville Is. Coal Measures boundary Pig. A.— Outline map showing outcrops of some of the principal Pennsylvania!! limestones of Illinois. WESTERN ILLINOIS 13 Pennsylvanian strata, the cyclic repeti- tion of beds makes correlation by cyclo- thems possible wherever adequate out- crops are available for study. Uncer- tainties exist, however, concerning the correlation of the lower part of the sec- tion between southern and western Illi- nois. Also, the exact relations of certain local beds higher in the southern Illinois section to beds in the western Illinois section are as yet unknown. In some other parts of the State thick glacial drift and inadequate outcrops make cor- relations uncertain. For these reasons it is impossible at this time to present a single generalized succession of the Pennsylvanian system of the State that would not be confusing in some impor- tant respects. Therefore, it has seemed necessary to prepare for this report two general stratigraphic sections, one for western and another for southern Illi- nois, whose corresponding parts are pre- sented on opposite pages in order that they may be compared easily. Such problems of correlation as are involved in the study of the fusuline-bearing beds are considered later in this chapter. Western Illinois The best known Pennsylvanian succes- sion is present in a series of excellent outcrops in western Illinois west of Illi- nois River. It includes 20 cyclothems most of which can be correlated fairly satisfactorily throughout the entire Eastern Interior basin. A general sec- tion for this area is as follows (see also fig. 1, p. 14). The nomenclature em- ployed in this and subsequent lists is tentative. 20. Shoal Creek* 19. Trivoli* 18. Gimlet* F 17. Sparland* F 16. Brereton* F 15. St. David* F 14. Summum* F 13. Liverpool* F 12. Lower Liverpool 11. Greenbush* 10. Wiley* * Beds with marine fossils are present in those cyclo- thems marked with an asterisk, and the presence of fusulines is indicated bv an F. 9. Seahorne* F 8. Lower Seahorne 7. Upper DeLong 6. Middle DeLong 5. Lower DeLong 4. Seville* F 3. Pope Creek* 2. Tartar* 1. Babylon* Not all of the cyclothems included in the foregoing list are equally well de- veloped. Some of them, although wide- spread, are so incomplete that their cyclic nature is not evident. As most of these are traced southward, however, they acquire new beds, thicken, and gradually attain developments similar to the more complete cyclothems. The western Illinois section also in- cludes a few local developments of other beds which do not seem to fit into the characteristic cyclic succession of strata in that part of the State. As the Pennsyl- vanian section thickens southward, how- ever, recognizable but more or less in- complete new cyclothems appear at most of these horizons, and these beds of western Illinois are therefore believed to be the marginal developments of cyclo- thems which are more completely rep- resented in other areas. About twice as many cyclothems have been distinguished below the Shoal Creek cyclothem in southern Illinois as are present in the western part of the State. The additional cyclothems recog- nized in southern Illinois are distributed fairly regularly throughout the entire succession except that the greatest ex- pansion appears to occur adjacent to the Gimlet and Seahorne cyclothems and at the base of the section. The additional cyclothems seem to be rarely associated with the recognized cyclothems which are most incomplete in western Illinois. The exact relation of many of the ad- ditional southern Illinois cyclothems to the western Illinois section is uncertain. The evidence that is available, however, indicates that most of them appear as a result of the introduction of new beds within the western Illinois cyclothems rather than by the introduction of new beds between the other cyclothems. Ac- cordingly, the strata that appear to con- 14 PENN8YLVANIAN FUSULINIDAE ? >*S< 1^ I 1 I No 8 coal Lonsdale Is. Piasa Is.-^ Brereton Is. No.6 coal St. David Is,- Springfield No. Hanover Is. No. 4 coal Fusulina lonsda/ensis Fusulina ex i mi a Fusulina acme Fusulina megisla Fusulina mysticensis Fusulina piasaensis Fusulina girtyi Fusulina illinoisensis . Fusulina haworthi ■■■ . 5 coal Fusulina spissiplicaia Oak Grove Is. Colchester No. 2 Isabel ss. coal ez Seahorne is. Wedekindellina euthysepta Wedekindellina ellipsoides Wedekindellina excenfnca ? (Fusulina pumila Wedekindellina ^ euthysepta Seville Is. Rock Is. No. I coal Fusulinella iowensis F iowensis var. stouti Fusulinella gephyrea Fig. 1. — Generalized columnar section of the Pennsylvanian formations of western Illi- nois (chiefly west of Illinois River), showing the stratigraphic distribution of the fusulines. All fusuline illustrations X 4. SOUTHERN ILLINOIS 15 8 o I 1 I Palzo ss. Base of Carbondale DeKoven coal Davis coal Stonefort Is. Bald Knob coal Curlew ss. Curlew coal Curlew Is. Wedekindellina excenirica ? Wedekindellina minuta Wedekindellina euthysepta Fusulina novamexicana Fusulina . sp.A Fusulina leei Murray Bluff ss. Delwood coal Delwood ss. Boskydell ss. Willis coal Grindstaff ss Fusulinella sp. Reynoldsburg coal 1 Pounds ss. J Caseyville formation extends downward; no fusulines known . Fig. 2. — Generalized columnar section of the Pennsylvanian formations (lower part) in. southern Illinois, showing the stratigraphic distribution of the fusulines. The ; section is continued upward in figure 3. All fusuline illustrations X 4. 16 PENNSYLVANIAN FUSULINIDAE stitute a single cyclothem in western Illi- nois may, therefore, become parts of two or more cyclothems in southern Illinois. Southern Illinois The thickest and presumably the most complete Pennsylvanian succession of Illinois is present in the southern part of the State, but only the lower beds are exposed in abundant and adequately connected outcrops, and these do not clearly exhibit the type of cyclical sedi- mentation that is so characteristic of most of the Pennsylvanian system in other parts of the State. The lower cyclothems are in fact so incomplete and so lacking in distinctive characters that many of them cannot be certainly recog- nized in different outcrops or correlated from place to place. Certain critical parts of the higher section are nowhere adequately exposed, and other good out- crops are so isolated that the beds cannot be adequately connected in a continuous section. Drill records are useful in many areas but identification of the beds penetrated is generally somewhat doubt- ful, and many thin but significant strata have probably not been distinguished. Consequently the complete succession of cyclothems in southern Illinois has not been, and possibly never will be, worked out satisfactorily. A general section for this part of the State as now understood is, however, as given below (see also figs. 2 and 3, pp. 15, 17) . Units whose names appear in italics undoubtedly include several incompletely developed cyclo- thems. 20. Shoal Creek* Collinsville* 19. Trivoli* Unnamed Brouillett* Unnamed 18. Gimlet* 17. Sparland Bankston Fork Jamestown* F 16. Brereton* F Crab or chard* 15. St. David* F 14. Summum* Lowell* 13. Liverpool* F 12. Lower Liverpool 11. DeKoven 10. Davis* 8-9. Stonefort* F 4. Macedonia* F 3. Delwood*? 2. Grindstaff* F Pounds 1. Battery Rock* Lusk* The numbers in the above list indicate correlation of the coals and limestones with similar beds in the western Illinois section. The correlations of these beds above the Lower Liverpool cyclothem are believed to be fairly well established and consequently the same member names are used in both areas. Below the Lower Liverpool, however, the correla- tions are less well established and a new series of names is introduced for southern Illinois. Some of these named units con- sist of several incompletely developed cyclothems and therefore are not strictly comparable to the units named in the list for western Illinois. The Stonefort and Macedonia formations are of this type and probably include the three De- Long cyclothems (Nos. 5 to 7) that are recognized in western Illinois. Central Illinois Strata above the Shoal Creek lime- stone underlie a large area in the cen- tral part of the basin where the follow- ing succession of cyclothems occurs (see also fig. 4, p. 19) : 33. Shumway* F 32. Woodbury* 31. Gila* 30. Omega* F 29. Upper Newton* 28. Newton* 27. Upper Bogota* 26. Lower Bogota* 25. Cohn* 24. Upper Livingston* 23. Lower Livingston* F 22. Macoupin* 21. Flannigan* 20. Shoal Creek* This section is characteristic of Clark, Cumberland, and Effingham counties but it has not been traced southward SOUTHERN ILLINOIS 17 GO -/•• I I I Cutler Is Bankston Fork Is Anvil Rock ss. Jamestown Is. Herrin Is. Herri n No. 6 Coal Coal No. 5 A Absher is. HarrisburgNo.5 Coal J Fusulina levicula Fusulina lucasensis FusulineIJa cadyi Palzo ss. Fig. 3. — Generalized columnar section of the Pennsylvanian formations (upper part) in southern Illinois, showing the stratigraphic distribution of the fusulines. All fusuline illustrations X 4. 18 PENN8YLVANIAN FUSULINIDAE successfully, and it is not known to what extent it expands in that direction. Altogether more than 50 cyclothems are believed to be present in the Penn- sylvanian system of Illinois. Beds that contain marine fossils are known, at least locally, in 40 or more cyclothems, and fusulines in about 16. FUSULINE-BEARING BEDS Fusulines are generally associated with molluscoidean faunas, and their fossilized shells commonly occur in or are closely associated with limestones. In many of the Pennsylvanian lime- stones of Illinois, however, they are ab- sent or so rare that they have not yet been discovered. Exactly what condi- tions limited the distribution of the fusulines are not known. They are as a rule most common in the purer light colored limestones that are character- istic of bed 9 of the succession in many of the cyclothems. Fusulines have been collected from every cyclothem except the Shoal Creek which has a widespread comparatively pure upper limestone bed (No. 9). This exception is peculiar because the Shoal Creek limestone is the most continuous and uniform bed of this type in the entire Pennsylvanian succession of Illi- nois. Some of the purer limestones which are more locally present in other cyclo- thems have likewise yielded specimens of fusulines although others so far have been unproductive. The stratum which most commonly contains fusulines is the Brereton limestone. This is the caprock of coal No. 6, and in many of the older geological reports it is termed the Fusu- lina limestone. Fusulines are rarely present in shales except the thin shale partings between layers of limestone. At a few places, however, they occur in considerable abundance in shale below bed 9 (Lons- dale limestone) in the Gimlet cyclothem. Fusulines, mostly of small size, have been found at a few places in impure and dark colored limestones of the Liv- erpool and Seville cyclothems. The Shumway cyclothem is the only one in which fusulines are known to occur in beds other than the upper limestone (No. 9) or closely associated shales. In it they are present in the middle lime- stone (No. 7). Known Fusuline-bearing Beds of Illinois Group Cyclotilem Upper McLeansboro group 17. Greenup (Omega?) limestone 16. Shumway "middle" limestone 15. Omega (Greenup?) limestone Omega? Shumway Omega Lower McLeansboro group 14. Lower Livingston limestone. 13. Lonsdale limestone 12. Piasa (Cutler) limestone 11. Bankston Fork limestone 10. Jamestown limestone 9. Brereton or Herrin limestone Lower Livingston Gimlet Sparland Bankston Fork Jamestown Brereton Carbondale group 8. St. David or Absher limestone 7. Hanover limestone 6. Oak Grove limestone St. David Summum Liverpool Tradewater group 5. Seahorne limestone 4. Stonefort limestone 3. Curlew limestone 2. Seville limestone 1. Boskydell? sandstone Seahorne Stonefort fm. Macedonia fm. Seville Grindstaff? fm. CENTRAL ILLINOIS 19 => 5 * 2 O i i i Greenup Is. Shumway Is. Triticites cal/osus Triticites mediocris Triticites mediocris var. angustus Triticites turgidus Omega Is ' L Triticites pauper Triticites ohioensis Triticites venustus U.Livingston Is. L Livingston Is. Triticites ohioensis Triticites venustus Shoal Creek Is. Pig. 4.— Generalized columnar section of the Pennsylvanian formations in central Illi- nois, showing the stratigraphic distribution of the fusulines. This continues the section upward from figure 3. All fusuline illustrations X 4. 20 PENNSYLVANIAN FUSULINIDAE BOSKYDELL SANDSTONE The Boskydell marine zone is a me- dium- to coarse-grained sandstone, fer- ruginous and somewhat calcareous, that is believed to overlie the Willis coal in the Grindstaff cyclothem. It is appar- ently equivalent to bed 9 of the complete cyclothem and is the only sandstone of this type that is known to occur in such a position in the Pennsylvanian system of Illinois. It has been recognized at a number of outcrops in the southern part of the State and is believed to have been identified in a diamond-drill core from Macoupin County. The fossils of the Boskydell sandstone constitute the oldest post-Morrow fauna known in Illinois. 18 The number of species is small and many of the shells are waterworn or otherwise poorly pre- served. A few specimens of Fusulinella have been obtained from sandstone sim- ilar to the Boskydell in Pope County (Sta. 248) but their poor preservation makes specific identification impossible. Local stratigraphic evidence suggests that perhaps the fossiliferous stratum at this place should be referred to the Delwood rather than the Grindstaff formation. If such an assignment should be correct, this fossiliferous member is one that has not previously been recog- nized elsewhere. Seville Limestone The Seville limestone is the caprock of the Rock Island (No. 1) coal of west- ern Illinois. It is finely crystalline and dark gray to nearly black where fresh but weathers to a light color. This bed is not persistent but occurs in elongated areas less than one mile wide; it appar- ently accumulated in depressions on the uneven surface of the basal sandstone of the Seville cyclothem. In the midst of these areas the limestone may be six feet thick but toward the borders the sandstone thickens abruptly, and the underclay, coal, black sheety shale, and limestone wedge out. w A fauna from the Sellers limestone, locally present in the Battery Rock formation of the Caseyville group in Hardin County, is believed to be of Morrow age. In some respects it is similar to the Sharon ore fauna of Ohio. 19 Wanless, H. R., and Weller, J. M M Correlation and extent of Pennsylvanian cyclothems: Bull. Geol. Soc. Am. vol 43, pp. 1003-1016, 1932. In parts of Rock Island and Mercer counties the Seville limestone is over- lain by as much as 25 feet of very dark bluish-gray impure slabby limestone which is probably a calcareous phase of the upper shale (No. 10) of the cyclo- them. At the top of the "blue rock", as this is locally known, occurs a persist- ent bed of dark gray chert. The Seville limestone is not known south of Schuy- ler County. This is the lowest bed in western Illi- nois to yield fusulines, and studied col- lections from four localities contain only representatives of the genus Fusulinella. The species are small, and although specimens are locally abundant they are easily overlooked. F. iowensis Thomp- son predominates in each of these col- lections. Two of the collections have likewise yielded F. gephyrea n. sp. A single fine axial section of F. iowensis var. stouti Thompson was obtained from a specimen collected at one place. None of these forms are known from any other Illinois localities although an unidenti- fied Fusulinella occurs in the Boskydell sandstone and F. cadyi n. sp. is present in the Absher limestone. Curlew Limestone The Curlew limestone of southern Illi- nois is lighter colored than the Seville, very siliceous and cherty, and locally grades into a bed of solid chert. It also is quite variable in thickness and attains a maximum development of five to six feet. The cyclothem (part of the Mace- donia formation) which includes this limestone is thin. It contains no black sheety shale and the limestone is im- mediately underlain by a thin coal and underclay. The shale above the lime- stone is rarely more than three feet thick. The Curlew limestone is known from Williamson County, Illinois, to Butler County, Kentucky. Wanless and Weller have correlated the Curlew limestone of southern Illi- nois with the Seville limestone in the western part of the State on the basis of stratigraphic studies. 19 However, the occurrence of only Fusulina leei Skinner in the Curlew and of Fusulinella iowen- sis Thompson in the Seville leads Dun- bar and Henbest to conclude that these STONEFORT LIMESTONE 21 limestones cannot be equivalent and that the Curlew is younger than the Seville. They contend that these two species, or their near relatives, characterize two clearly marked nonoverlapping zones in Ohio, Illinois, Iowa, and Oklahoma. Weller recognizes that Fusulina leei occurs at horizons above the range of Fusulinella iowensis, but he does not believe that studies in any area have definitely established that the ranges of these species do not over- lap. He therefore believes it possible that they existed contemporaneously in Illinois but were restricted to different parts of the State by environmental conditions. between the Seahorne limestone and the Seahorne sandstone. This part of the section is more completely developed in southeastern Iowa where another lime- stone appears between these two coal horizons. The Seahorne beds of western Illinois therefore probably include parts of two different cyclothems. The characteristic fusuline species of the Seahorne limestone is Fusulina pu- mila Thompson. It occurs very sparsely in each of the three collections obtained from this bed and in only one of them is it known to be associated with Wedekin- dellina euthy septa (Henbest) (?), rep- resented by a single specimen. Seahorne Limestone The Seahorne limestone is the first im- portant marine stratum above the Seville limestone and is one of the most characteristic beds of the Pennsylvanian section in western Illinois. It is a hard massive limestone, medium gray in color, and weathers nearly white. It rarely shows signs of bedding and at many places is pseudoseptarian, brecciated, or conglomeratic, and its upper surface is commonly very rough and irregular. In some areas it is a persistent and uniform bed and is locally nearly 10 feet thick, but elsewhere it grades into rounded boulders surrounded by clay and in some extensive areas is entirely absent. It is known from Bock Island County to Madison County and is characterized al- most everywhere by a peculiar fauna containing many small gastropods. The Seahorne limestone is almost in- variably directly overlain by the under- clay of the next higher cyclothem. Coal is generally absent beneath the lime- stone, and where present it is rarely more than two inches thick. An unusu- ally light-colored underclay and thin very fine-grained pure quartz sandstone are however persistently present beneath it. At many places in western Illinois there seem to be two coal horizons, sepa- rated by a foot or less of greenish clay, Stonefort Limestone The Stonefort limestone of southern Illinois is a persistent bed one to two feet thick that is medium gray, weathers brownish, and is only sparingly fossili- ferous. It occurs in the midst of a suc- cession of thin beds including several coals that are not well known because they crop out at few places. Another thin limestone without marine fossils oc- curs locally a few feet above the Stonefort. The Stonefort limestone is the first marine horizon above the Curlew lime- stone of southern Illinois and occupies a position in the section approximately equivalent to the Seahorne limestone in western Illinois. These two beds cannot be correlated, however, with any degree of certainty and there are reasons for concluding that the Stonefort may be equivalent to the Lower Seahorne lime- stone of Iowa rather than the original Seahorne limestone of western Illinois. The Stonefort limestone has yielded five species of fusulines and its fauna is, therefore, one of the most varied fusu- line faunas of the State. The most abundant species is Wedekindellina euthy septa (Henbest). This species is likewise common in the Oak Grove and may also occur in older strata, for it is present in the limestone of questionable age at station Bl near Murphysboro. As- sociated with this species in the Stone- 22 PENNSYLVANIAN FUSULINIDAE fort limestone are W. minuta (Hen- best), known only from this bed, and W. excentrica (Roth and Skinner) which also is present in the Oak Grove. The second most common species in the Stonefort limestone is Fusulina nova- mexicana Needham, a form unknown elsewhere in Illinois except in the un- identified limestone near Murphysboro. Although the Stonefort limestone is believed to be similar in age to the Sea- horne, the dominant Seahorne species F. pumila Thompson is not known in the Stonefort, and only a single specimen of the common Stonefort species W. euthy- septa has been found in the Seahorne in each of two collections. Oak Grove Beds The Oak Grove beds of western Illi- nois are a series of alternating thin lime- stones and shales above the Colchester (No. 2) coal, the most uniform and per- sistent coal seam in that part of the State. They correspond in part to bed 9 of the ideal cyclothem. The typical succession is as follows : Ft. In. k. "Ironstone" with fossils pre- served as casts 3-6 j. Shale, gray, may contain "iron- stone" layers 1-3 i. Limestone, impure, brown- weathering, with Ambocoelia and Linoproductus abundant. ... 3-9 h. Shale, black, with Aviculopec- ten rectilaterarius 1-3 g. Limestone, nodular, impure, with abundant pelecypods y^-Q f. Shale, dark gray, silty, with a few Marginifera 6-9 e. Shale, dark, calcareous , with abundant Mesolohus 3-6 d. Cone-in-cone 1-8 c. Limestone, impure, gray, may be septarian, with abundant Marginifera muricatina y 2 -2 b. Shale, dark gray, slightly fos- siliferous, may contain thin limestone layers 1-4 a. Limestone, hard, dark bluish- gray, fine-grained, rather local. 0-12 These beds appear to be distinct throughout most of western Illinois al- though the succession is incomplete at many places. In LaSalle County the Oak Grove beds consist of two or more impure f ossiliferous limestones, common- ly very sandy, and associated shales. In Jackson County they are represented by a single massive limestone about two feet thick, but farther east in southern Illi- nois these beds are nowhere known to be exposed. The Oak Grove beds are overlain by the Purington shale which is as much as 80 feet thick in some places. The Oak Grove beds are separated from coal No. ?■ by black sheety shale and the discon- tinuous gray Francis Creek sha ] e (bed 6 of the ideal cyclothem). The Francis Creek shale reaches its greatest thickness of about 50 feet in parts of McDonough and Fulton counties; elsewhere it is much thinner or absent. % The black sheety shale is present except where the Francis Creek shale is unusually thick. The Oak Grove fauna is similar to that of the Stonefort in that Wedekin- dellina euthy septa (Henbest) is the dominant species and both include W. excentrica (Roth and Skinner). The second most common species of the Stonefort, Fusulina novamexicana Need- ham is, however, unknown in the Oak Grove, but this higher horizon has fur- nished specimens of W. ellipsoides n. sp. and F. spissiplicata n. sp. which are un- known elsewhere. Hanover Limestone The Hanover limestone is the caprock of coal No. 4, a generally unimportant coal seam. This limestone is largely confined to the area between Schuyler and Randolph counties where it is a mas- sive hard fine-grained light gray bed that locally resembles the Seahorne lime- stone. It has a maximum thickness of about four feet but thins to the north, grades into a zone of argillaceous lime- stone nodules and disappears in Fulton County but is present in LaSalle Coun- ty. This bed is apparently absent or discontinuous and thin in southern Illi- nois east of Jackson County. The Covel conglomerate, 20 a peculiar stratum of gray limestone with black 20 Willman, H. B., The Covel conglomerate, a guide bed in the Pennsylvanian of northern Illinois: Illinois Acad. Sci. vol. 32, no. 2, 1940 ; Illinois Geol. Survey Cir. GO, 1940. ST. DAVID LIMESTONE 23 limestone pebbles and marine fossils, oc- curs at many places in northern Illinois slightly above the horizon of the Han- over limestone. The Pleasantview sand- stone beneath the Hanover limestone and coal No. 4 includes some of the most important channel deposits, 21 particu- larly in western Illinois. It is almost in- variably a thin-bedded and shaly sand- stone even where it occupies channels 75 or more feet deep and several miles wide. The Hanover limestone is sparingly fusuline-bearing in Illinois. It is cor- related by Wanless and Weiler with the lower Fort Scott limestone of the north- ern mid-Continent area which contains a fauna similar to that of the Brereton limestone in Illinois. Absher Limestone The Absher limestone, named from a village in southeastern Williamson County, overlies the Harrisburg (No. 5) coal in southern Illinois. It is a com- paratively thin and somewhat impure bed and in the vicinity of Harrisburg is generally separated from the coal by as much as 20 feet of shale (bed 6 of the complete cyclothem). It has been cor- related with both the Hanover and St. David limestones of western Illinois; at present the correlation with the St. David limestone is favored. 22 Collections from undoubted Absher limestone are scanty and have yielded only Fusulina levicula n. sp., F. lucasen- sis Thompson, and Fusulinella cadyi n. sp. Another collection from Randolph County (sta. 498) which may or may not be from the same horizon contains these species in greater abundance. None of them are known elsewhere in Illinois except for rare occurrences of F. luca- sensis Thompson in the Brereton-Herrin limestone. F. lucasensis was also found in a zone 10 feet below the Mystic coal in Iowa. The presence of Fusulinella, otherwise known in Illinois only from the Seville limestone and Bosky dell (?) 21 Ekblaw, Sidney, Channel deposits of the Pleasant- view sandstone in western Illinois: Illinois Acad. Sci. vol. 23, pp. 391-99, 1931. 22 Weiler, J. M., and Wanless, H. R., Correlation of minable coals of Illinois, Indiana, and western Ken- tucky: Am. Assoc. Pet. Geol. Bull., vol. 23, footnote p. 1390, 1939; Illinois Geol. Survey Cir. 48, 1939. sandstone, and the absence of Wedekin- dellina from this and all higher horizons are noteworthy. St. David Limestone The St. David limestone, caprock of the Springfield (No. 5) coal of western Illinois, is considered to be equivalent to the caprock of the Harrisburg (No. 5) coal of southern Illinois, the Peters- burg-Alum Cave (coal V of Indiana) and coal No. 9 of western Kentucky. If this correlation is correct, the bed is one of the most widely recognized strata in the Eastern Interior basin. The St. David limestone is best developed in Jersey, Madison, St. Clair, and Ran- dolph counties and has a maximum thickness of nearly 10 feet. It is hard, fine-grained, and light gray in color. To the north it thins, becomes a single mas- sive ledge in Fulton County, grades into a nodular or concretionary horizon in Peoria and Knox counties, and is absent in northern Illinois. It is locally absent in parts of Morgan, Greene, Macoupin, and Calhoun counties. In parts of Ma- coupin and Greene counties it grades in- to a discontinuous Chaetetes reef, and locally in Randolph County it appears to be represented by a bed of chert. The most distinctive feature of the St. David cyclothem is the absence of a basal sandstone everywhere in western Illinois. The St. David limestone in parts of western Illinois appears to bear the same fusuline fauna as the Brereton, includ- ing its commonest species, Fusulina gir- tyi (Dunbar and Condra) and F. illi- noisensis n. sp. with F. haworthi (Beede) less abundantly represented. However, the exact source of the single supposed St. David fauna that has been studied is somewhat questionable ( Collection W232). Limestones of Randolph and Jackson Counties Three fusuline collections have been secured in Randolph and Jackson coun- ties from limestones below coal No. 6 whose stratigraphic positions are more 24 PENNSYLVANIAN FUSULINIDAE or less uncertain. This region is sepa- rated from western Illinois by an outly- ing portion of the St. Louis Cheltenham clay district where the lower Pennsyl- vanian succession is greatly compress- ed, 23 and from southern Illinois by the Campbell Hill and DuQuoin anticlines where almost the entire Pennsylvanian succession abruptly expands. 24 At station Bl near Murphysboro, in the midst of the area of expanding Pennsylvanian strata in Jackson Coun- ty, a collection of fusulines was obtained from limestone about 30 feet above the Murphysboro coal. As a result of his stratigraphic studies, Wanless tentative- ly correlated this limestone with the Curlew limestone farther east. Dunbar and Henbest, however, have identified Wedekindellina euthysepta and Fusu- lina novomexicana from it and point out that neither of these species is known to occur in either the Curlew or Seville limestones. They suggest, therefore, that this limestone is younger than the Curlew, and because both species are present in the Stonefort fauna, tenta- tively correlate it with that limestone. The stratigraphic evidence indicates that the latter correlation may be correct but is not sufficient to confirm it. A second collection was secured from limestone near Wine Hill in Randolph County (sta. B3). This locality is iso- lated and the exposed stratigraphic sec- tion is not sufficient for correlation. The fusulines collected here are Fusulina pumila Thompson, F. aff. F. leei Skin- ner, and Wedekindellina euthysepta (Henbest) ( ?). The first is known else- where only in the Seahorne, but the other two occur in both the Seahorne and the Stonefort limestones. Typical Seahorne limestone is believed to have been identified in a good section near Campbell Hill, and it is probable, as the presence of F. pumila suggests, that the Wine Hill limestone is also Seahorne. Near Schuline in Randolph County (sta. 498) there is a good exposure of strata below the Brereton limestone 88 Wanless, H. R. and Weller, J. M., Correlation and extent of Pennsylvanian cyclothems: Geol. Soc. Amer. Bull. vol. 43, p. 1007. 1932. 24 Wanless, H. R., Pennsylvanian Correlations in the Eastern Interior and Appalachian coal fields: Geol. Soc. Ainer. Sp. Paper 17, p. 7, 1939. which differs from the succession north- west of Belleville in having only one prominent light colored limestone below coal No. 6 instead of two (St. David and Hanover). The St. David limestone is locally absent in the area adjacent to St. Louis where the succession is much com- pressed, and it is possible, therefore, that it is also absent near Schuline and that the limestone is the Hanover. It is also possible that the interval between the St. David and Hanover limestones has greatly expanded southeastward from Belleville so that only one of them is exposed near Schuline. The associa- tion of Fusulina lucasensis Thompson, F. levicula n. sp. and Fusulmella cadyi n. sp. in this bed, a fauna known else- where only in the Absher limestone, strongly suggests that the latter inter- pretation offered above is correct. Brereton or Herrin Limestone The Brereton limestone, also known as the Herrin limestone in southern Illi- nois, is the caprock of the Herrin (No. 6) coal. It is a persistent bed, generally hard and massive but somewhat argilla- ceous, and varies in color from nearly black, as in Randolph County, to brown- ish-gray, as in western Illinois, and to light gray, as in most of southwestern and southern Illinois. In outcrop its thickness ranges up to a maximum of about 10 feet in southwestern Illinois. However, drill records in Macoupin, Madison, and St. Clair counties and else- where report thicknesses of as much as 25 feet. As reported in these records, the limestone is commonly interbedded with several layers of calcareous shale and probably includes the Jamestown and possibly also the Bankston Fork lime- stones that are distinguishable in out- crops. Gray shale, bed 6 of the ideal cyclo- them, appears between the Brereton limestone and coal No. 6 near the Du- Quoin anticline in southern Illinois. The shale extends eastward with rapid varia- tions in thickness up to a maximum of 25 feet or more. The Brereton or Herrin limestone is generally fusuline-bearing, and about one-third of the collections upon which CUTLER LIMESTONE 25 this report is based were secured from this bed. The fauna is composed essen- tially of Fusulina girtyi (Dunbar and Condra) and F. illinoisensis n. sp. As- sociated with these are a few specimens of F. lucasensis Thompson and F. ha- worthi (Beede). This fauna is easily recognized and in southern Illinois is re- ported only in this and the overlying Bankston Fork limestone. In western Illinois it is present in the Brereton limestone, possibly also in the underly- ing St. David limestone. Jamestown Limestone The Jamestown limestone can be dis- tinguished from the Brereton only where they are separated by the Jamestown coal which thickens from a few inches in St. Clair County to minable thickness in Kentucky where it is known as No. 11 coal. The Jamestown limestone is light to bluish-gray, somewhat argillaceous, and resembles the Brereton limestone. It is rarely more than two feet thick. North of St. Clair County it may be included in the Brereton limestone or it may wedge out into the Sheffield shale which overlies that bed. The fusulines in the Jamestown lime- stone have not been studied. Bankston Fork Limestone The Bankston Fork is a hard gray brownish-weathering limestone which has a maximum thickness of about five feet and which appears to be persistent- ly present in the southern Illinois sec- tion. At its eastern outcrops it is over- lain by the Bankston coal. The promi- nent Anvil Rock sandstone of western Kentucky lies between the Herrin and the Bankston Fork limestones. The sparse fusuline fauna of the Bankston Fork limestone is very similar to that of the Brereton-Herrin limestone and consists mainly of specimens of F. girtyi (Dunbar and Condra) associated at a few places with F. illinoisensis n. sp. and F. knighti n. sp. The last species is known elsewhere only in the so-called upper Fort Scott limestone (Brereton) of the St Louis outlier in Missouri. 25 Piasa Limestone The Piasa limestone is a massive light gray bed that has a maximum thickness of five to six feet in Jersey and Macou- pin counties. It thins and disappears to the north and south. This limestone overlies the horizon of coal No. 7 but the two beds are not present in the same areas. Fusulines are locally very abundant in the Piasa limestone. The fauna is dominated by large elongated specimens which show an advanced stage of septal folding. The most common species are Fusulina eximia Thompson, and F. piasaensis n. sp. Also present are F. mysticensis Thompson, F. megista Thompson, and F. acme n. sp. With the exception of F. piasaensis these species all occur in the Lonsdale limestone of western Illinois and, except for F. mys- ticensis, in the Cutler limestone of south- ern Illinois. They are, however, unknown in other horizons in this State. For several years Wanless and Weller have correlated the Piasa with the Bank- ston Fork limestone but the fusuline fauna makes this correlation doubtful. The absence of F. girtyi and the pres- ence of a number of species showing a highly advanced stage of specialization, unknown at lower horizons, strongly suggests that the Piasa limestone is younger than the Bankston Fork. In view of these facts it seems possible that a marine horizon, recognized at a few places in western Illinois close above the Brereton limestone, is the equivalent of the Bankston Fork limestone rather than the Jamestown, as was formerly believ- ed. Likewise it now appears possible that coal No. 7 of western Illinois may be equivalent to the Bankston coal of the southern part of the State where coal No. 7 has not been recognized previously. Cutler Limestone The Cutler limestone of St. Clair, Perry, and Randolph counties is a light gray bed about five feet thick which lies 15 feet above the Bankston Fork lime- 25 Knight, J. B., The location and areal extent of the St. Louis Pennsylvanian outlier: Am. Jour. Sci. ser* 5, vol. 25, p. 44, 1933. 26 PENNSYLVANIAN FUSULINIDAE stone. Discontinuous thin coals are lo- cally present close below and close above it. At a few places in St. Clair County the upper surface of the limestone is dis- tinctly sun-cracked. To the east this bed is not so well known but appears to con- tinue as a brownish-gray limestone about 3 feet thick. The Cutler limestone has been cor- related with the Lonsdale 26 but a recon- sideration of the local stratigraphic sec- tion suggests that it is more probably equivalent to the Piasa, and its fusuline fauna furnishes some substantiation for this revised correlation. The fusuline assemblages of these three limestones are somewhat similar and all include Fusu- lina acme n. sp. and F. megista Thomp- son, but the Cutler fauna also contains F. piasaensis n. sp., one of the two most common Piasa species which is not known in the Lonsdale. In addition, the Cutler has at one place yielded another form suggestive 0/ F. haworthi (Beede). Loxsdale Limestone The Lonsdale limestone of western Illinois is an extremely variable bed which has a thickness of 25 feet or more in some places. It is light gray and commonly nodular or conglomeratic (possibly of algal origin) with irregular greenish shaly partings, but is locally massive and subcrystalline or very ar- gillaceous. The relations of the Lonsdale lime- stone to both the underhung and over- lying beds are variable and it is proba- ble that the beds referred to the Gimlet cyclothem actually represent several in- complete cyclothems. Throughout con- siderable areas in western and northern Illinois, red shale with a maximum thickness of about 15 feet underlies the Lonsdale limestone. Coal is absent from the cyclothem, and at many places no indication of a coal horizon or under- clay can be recognized, although black sheety shale is locally present. In some parts of western Illinois the limestone - ,; Wanless, If. R., Pennsylvanian correlations in the Eastern Interior and Appalachian coal fields: Geol. Soc. \m. sp. Paper 17, p. 81, 1939. rests directly on the basal sandstone of the cyclothem. Locally in Peoria Coun- ty the Lonsdale limestone is overlain bj^ as much as two feet of black slabby lime- stone containing Spirorbis, small gastro- pods, and poorly preserved leaves. At some places a thin clay or shale sepa- rates these beds. Large silicified stumps which are found along present streams are believed to have weathered out from the upper limestone. The Lonsdale limestone disappears to the south in Morgan County. It has previously been correlated with the Cutler limestone of southern Illinois although it now seems probable that the latter bed is equivalent to the Piasa. Certain restricted layers in or below the Lonsdale limestone locally carry abundant fusulines with F. acme n. sp. as the dominant form. F. eximia Thomp- son, F. megista Thompson, F. mysticen- sis Thompson, and F. lonsdalensis n. sp. are also present. All but the last of these species also occur in the Piasa limestone. The Lonsdale limestone marks the last appearance of Fusulina in Illinois, and the next known fusuline-bearing bed contains the earliest species of Triticites found in the State. The important faun- al break separating these genera coin- cides with the boundary between the DesMoines and Missouri series in Iowa, Missouri, and Kansas, and is corroborat- ed by the distribution of some species of larger fossils. Brachiopods and bryo- zoans indicate that the Lonsdale lime- stone is the youngest marine bed of Des- Moines age in western Illinois, and the Trivoli limestone, overlying coal No. 8, is the oldest marine bed of Missouri age. This faunal break is the basis for sepa- rating the McLeansboro group into a lower and an upper part. A new classification of the Illinois Pennsylvanian based upon the arrange- ment of cyclothems into groups in ac- cordance with the latest paleontological and physical evidence is needed but such a classification has not yet been com- pletely formulated. \Vhen it is, the faunal and physical break between the Gimlet and Trivoli cyclothems should receive the recognition that it deserves. GREENUP LIMESTOXE 27 Livingston Limestone The Livingston limestone of east-cen- tral Illinois, with a total thickness of 20 feet or more, consists of two hard fine- grained light gray limestones, massive or unevenly bedded, separated by a few feet of shale or clay. Southward the shale or clay increases in thickness, coal and underclay appear, and it becomes obvious that two cyclothems are repre- sented which are provisionally termed Lower and Upper Livingston. One or both beds of the Livingston limestone have been correlated with the LaSalle limestone of the upper Illinois Valley. Similar limestone has been traced along the west side of the Illinois basin as far south as Fayette County which at one place is separated into two parts by an intervening thin coal and underclay. It has been provisionally correlated with the Livingston. Fusulines occur in the Livingston lime- stone of Edgar County (sta. 286) and in an algal limestone in Christian County (sta. 490) which are believed to be equiv- alent. Two beds of the Livingston lime- stone have not been recognized at either of these localities, and the specimens are tentatively referred to the Lower Livingston although it is possible that the two limestone beds have merged. Col- lections from both localities have fur- nished specimens of typical Triticites ohioensis Thompson with which T. venu- stus n. sp. is associated at the Christian County locality. Omega Limestone The Omega limestone is generally a light gray fine-grained hard pure lime- stone four to five feet thick. It is well developed and persistent in Marion, Clay, and Effingham counties. In part of Shelby and more locally in Clay County it thickens greatly but at the same time becomes impure and grades into a very silty or argillaceous but mas- sively bedded limestone as much as 25 feet thick and medium to dark bluish- gray in color. In Marion County and to the north a persistent coal horizon, locally represented b} r a one-foot coal bed and underclay, occurs beneath the Omega ' limestone. In Shelby County, where the limestone is thick and impure, it rests on sandy shale. Fusulines are abundant in the upper part of the Omega limestone at a num- ber of localities. Triticites venustus n. sp. is the common species but T. ohioen- sis Thompson is also present at one lo- cality. The Omega limestone has been cor- related at various times with the Shoal Creek, LaSalle (Livingston), and Green- up limestones. The species of Triticites listed above suggest that the second cor- relation may be correct, but recent strat- igraphic field work indicates that the Omega limestone is probably equivalent to the Greenup limestone although Hen- best and Dunbar believe the Greenup to be much younger. Calhoun Limestone The Calhoun limestone 27 is a lenticu- lar bed with a maximum thickness of about three feet which overlies a persis- tent coal in western Lawrence and east- ern Richland counties. It is light gray, more or less argillaceous, and locally grades laterally into calcareous sandy shale. This limestone and its underly- ing coal have not been definitely identi- fied and were formerly doubtfully cor- related with the LaSalle (Livingston). However, the probable structural trends in this part of the State strongly suggest that the limestone occupies a higher po- sition in the section and it is now pro- visionally correlated with the Omega. The Calhoun limestone has yielded a few small and poorly preserved speci- mens of Triticites venustus n. sp. which do not help in solving this correlation problem. Greenup Limestone The Greenup limestone of Cumber- land County consists of about 4 feet of light gray earthy limestone that is dis- tinctly nodular at most places. It thins southward so that in Jasper County it is only locally represented by a foot of hard brownish-gray limestone or a more or less inconspicuous zone of limestone nodules. No coal or underclay is present -' Named from Calhoun in Richland Countv. 28 PENNSYLVANIAN FUSULINIDAE beneath the Greenup limestone, and lo- cally it is in direct contact with the un- derlying sandstone. The Greenup lime- stone has not been definitely recognized farther south although lenticular but locally prominent limestones in Law- rence, Richland, and central Wayne counties are tentatively correlated with it. Fusulines are locally abundant in the Greenup limestone. Triticites mediocris n. sp. is the most abundant, its variety angustus n. var. is less common, but T. callosus n. sp. is the largest and most conspicuous form. None of these are known elsewhere. The correlation of the Greenup lime- stone is somewhat doubtful. Weller and Newton, 28 on the basis of extensive field studies, have concluded that the Green- up is stratigraphically equivalent to the Omega limestone of Effingham, Clay, and Marion counties and probably is equivalent to the Calhoun limestone of Lawrence and Richland counties. Dun- bar and Henbest, however, point out that T. callosus n. sp., which they assign to the group of T. ventricosus (Meek and Hayden) is indicative of a much higher horizon, probably upper Shawnee or Wabaunsee in age, and suggest that the Cumberland County succession may be interrupted by an important and un- recognized hiatus. Shumway "Middle" Limestone The lower of the two marine lime- stones (middle limestone or bed 7) of the Shumway cyclothem is known only in Effingham County where it occurs in sections above the Omega limestone. It is a dark bluish-gray argillaceous but hard and massive bed which disin- tegrates upon weathering. It has a maxi- mum thickness of 1% feet, but is lenti- cular and discontinuous. A thin coal or coal horizon occurs everywhere beneath this limestone. Above it is a persistent black sheety shale and an "upper" lime- stone, one to three feet thick, that is dark gray, hard, fine-grained and somewhat earthy, weathering to a light ochreous color. 28 Newton, W. A., and Weller, J. M., Stratigraphic studies of Pennsylvania!] outcrops in part of southeastern Illinois: Illinois Geol. Survey Rpt. Inv. 45, 1937. This bed has furnished two small species of Triticites, T. turgidus n. sp. and T. pauper n. sp., which are un- known elsewhere. MAJOR FAUNAL ZONES Four well-marked faunal zones can be recognized in Illinois on the basis of the fusulines. These, and some of their sub- zones, are equally distinct throughout, the mid-Continent region, west Texas, and New Mexico. Insofar as fusulines occur in the Appalachian coal fields, the zones are well marked there also. These faunal zones and their subdivisions, therefore, furnish a major framework for the general correlation of the Penn- sylvanian formations of the entire con- tinent. Zone of Fusulinella Throughout most of the northern hemisphere, wherever the lower part of the Pennsylvanian system contains nor- mal marine beds, the lowest fusuline fauna is characterized by Fusulinella. The older species of this genus are as- sociated with such primitive genera as. Staffella, Ozawainella, and Fusiella but younger ones occur with W edekindellina and the more primitive species of Fusu- lina. In the northern mid-Continent, Eastern Interior, and Appalachian re- gions, the lower part of the Pennsyl- vanian system consists largely of non- marine beds and, except for a few hori- zons in the upper part of the Fusulinella zone, has not yielded identifiable speci- mens. In Oklahoma and in central and western Texas, however, • this zone is more fully recognizable and appears to extend much lower than the oldest fusuline-bearing beds of Illinois. Subzone of Fusulinella iowensis The small ventricose species, Fusulin- ella iowensis Thompson, is found throughout the interior states but ap- pears to occupy a rather limited strati- graphic range. It is known only in the Seville limestone of Illinois, at a single horizon in Iowa (90 feet below the Whitebreast coal) that is probably Check List of Pennsylvanian Fusulinidae in Illinois 1. Fusulinella iowensis Thompson. . . . 2. Fusulinella iowensis var. stouti Thompson >: M co O pq ? % x x X X u O X o f-i o CO >. d § s +^ x X X d o 02 X x ? X X 03 d Sh o A a 03 x X X X 03 d g CO W +3 X ? X X CD > o s-( O -a o X X X X X X c o m 5b ^h X X X X 03 CO < X X X ■> Q +-> X X X X 'p S3 w 1 d o += X d O d .2 H a . a a a a a a a o3 d % o hH" a o o o o o o o o -t-3 d Ph «i « £ fc £ £ & fc fc & > >* ** 44 d d£ d CD PI 03 03 d 03 73 +3 ■+3 c— e>- 03 [> o CO ^ £N £V d 03 d 03 J33 73 o3 '£ 13 13 CO co o3 C3 o o © 03 03 73 c-~ p- o- p~ E JO Ph JO JO fi ^ v ft d O ft d o3 03 o3 3 d o3 1=1 44 d 03 o3 O !H* o S 1 t1 ^_^ •— >> ^^ O +3 g d o3 03 r-j d 73 73 73 & Ph d Is i—i 03 03 03 bC •"-N 43 ^3 73 O 73 O 73 o 3 +3 CO 03 o3 o o3 o 13 a d d 03 ft 18 03 CO d 03 Jh 03 JH 03 £ JO JO JO o ? JO s B 03 r^ 43 75 ^ s c^T _, ■+3 o 73 03 O- o JO Ph d o d o +3 03 CO O ft # d 75 o3 +3 e— v — f "03 3 g ;§d «3 C— >> e— is d o JU +3 d P -(-3 CO d o3 PQ -1-3 co 03 a o3 _d 75 03 w &H 03 43 CO 42 <1 d 03 co 3 X 03 •+3 O 3 a d o a, o 03 d o -1-3 CZ2 J^3 75 d U 73 44 CO O pq d d 0) o3 a o3 bO 03 -i-3 CO bC d Jh 5 a '£ o 02 o 3 03 o 05 13 73 CO d o o3 CO o3 Sh 03 40 03 44 O Ph d 03 CO d o -+■3 03 Jh 03 PQ 73 03 Q h-3 02 U 03 ► o d 03 w > o o -a o 03 d O 43 o3 03 +3" d 03 CO 40 JU 03 02 44 d 03 o3 44 03 JO "o3 03 o O h- 1 03 a o3 43 3 .a >> o CO o3 co a o3 o a o o O 73 d 4^ 75 1 O o O +3 W M o d o w 44 o •4l 4? 03 o3 s 03 o a 73 <5 03 e o ■a 03 (X; +3 d s 12 3 d 03 CO CD 3 3 o IdO O Q *CQ o3 co CO § s / +3 +3 o 03 -1-3 o o t» 03 03 03 1 43 03 & d 03 h5 +3 d o a o3 < 03 o3 Ph 03 Ph h4 -1-3 o to (32 ■4-3 u O to h4 03 O a 73 < -f3 d 03 CO 03 3 -t-3 d 03 CO 03 Jh 3 CORRELATIONS 33 The upper Pennsylvania!! strata in western Kentucky are restricted to a small area and apparently are not com- pletely exposed. Equivalents of the Livingston, Omega, and Shumway lime- stones may be present but they have not been identified. The Ohio and Illinois successions dif- fer considerably in the details of their development. In Ohio, marine lime- stones are absent from the upper part of the Allegheny and lower part of the Conemaugh formations. The higher marine limestones of Ohio are probably equivalent to important marine lime- stones in Illinois, and on the basis of their faunas and stratigraphic positions, the Brush Creek and Ames limestones of Ohio are tentatively correlated either with the Omega and Livingston or with the Livingston and Macoupin limestones in Illinois. The Pennsylvanian strata of southern Iowa and northern Missouri have re- cently been studied in some detail by D. G. Stookey, L. M. Cline, and others 35 but formal names have not yet been proposed for all of the beds, particularly those in the lower part of the section. The Ardmore limestone was formerly known as the Bevier sump rock in Mis- souri and the Two-layer limestone in Iowa. The Blackjack Creek limestone is the caprock of the Mulky coal in Missouri. The Houx limestone is the caprock of the Summit coal in Missouri. The Myrick Station limestone is the cap- rock of the Lexington coal in Missouri and the Mystic coal in Iowa. The Coal City, Worland, and Cooper Creek lime- stones were formerly termed 17 -foot, 50- foot, and floating rock in Appanoose County, Iowa. Both the Seahorne and Seville limestones of Illinois have been recognized in Iowa but not named. 36 In western Missouri and Kansas the strata from the Fort Scott limestones up are now fairly well known and corre- lations with the Iowa section have re- cently been made by Jewett. 37 The different nomenclature formerly used in western and northern Missouri is the result of miscorrelations. 38 In 35 Cline, L. M., Traverse of Upper Des Moines and Lower Missouri series from Jackson County, Missouri, to Appanoose County, Iowa: Am. Assoc. Petroleum Geologists Bull. vol. 25, pp.. 23-72, 1941. northern Missouri the Fort Scott lime- stones are the caprocks of the Mulky and Summit coals. The caprock of the Lexington coal is equivalent to the Brereton limestone of Illinois. The Jamestown and Bankston Fork lime- stones of Illinois have not been identi- fied certainly in Missouri or Kansas. The Bankston Fork and upper Pawnee lime- stones appear to occupy similar strati- graphic positions but their fusuline faunas are not the same and Dunbar and Henbest believe the Bankston Fork lime- stone to be the older. The Bevier and Tebo coals appear to have been miscorrelated from place to place in Missouri. The Tebo coal in Macon County is equivalent to the Col- chester (No. 2) coal of western Illinois, and the Ardmore limestone above the Tebo coal, commonly termed the Bevier sump rock, is the Oak Grove. In some other parts of the State, however, the lower of these coals seems to have been identified as Bevier so there the sump rock, if present, is probably equivalent to the Seahorne of Illinois. A fauna similar to that in the Seville limestone occurs a short distance beneath the Jor- dan coal of Vernon County, Missouri, but the details of these lower strata have not been satisfactorily worked out, and the stratigraphic position of this fauna is therefore not adequately known. The faunal break which occurs at the boundary between the DesMoines and Missouri series of the "Western Interior basin is recognized in Illinois between the Lonsdale limestone and the marine limestone of the Trivoli cyclothem of the McLeansboro group. The Piasa limestone is equivalent to part of the Altamont limestone west of the Missis- sippi, and the Lonsdale corresponds to one or more of the beds of the Lenapah limestone which occurs near the top of the Marmaton group. Correlations of the post-DesMoines beds in the Eastern Interior and the Western Interior basins are much less satisfactory than correlations of the 36 Wanless, H. B,., and Weller, J. M., op. cit. 37 Jewett, J. M., Classification of the Marmaton group, Pennsvlvanian, in Kansas : Geol. Survey Kan. Bull. 38, 1941/ 3S Hinds, Henry, and Greene, F. C, The stratigraphy of the Pennsvlvanian series in Missouri : Missouri Bur. Geol. and Mines, Ser. 2, vol. 13, 1915. 34 PENN8YLVANIAN FUSULINIDAE older beds. Outcrops of the Livingston, Omega, Greenup, and Shumway lime- stones in Illinois are far removed from outcrops of equivalent beds in the west- ern basin, and the characters of the strata in the two basins are so different that they cannot be correlated upon the basis of lithology and the details of the stratigraphic succession. Neither are the faunal variations thoroughly under- stood, and so it does not seem advisable to attempt to correlate these beds with specific members or formations. They are simply assigned to the groups of the Kansas section which probably include their equivalents. MORPHOLOGY OF THE FUSULINE SHELL Cael O. Dunbar and Lloyd G. Henbest GENERAL FEATURES The shells in this family are common- ly fusiform or subcylindrical, and are planispirally coiled about an axis that corresponds with their greatest diameter. For purposes of description, therefore, the geometric terms axis, poles, and equator are useful. But from the bio- logic point of view the equatorial plane is the middle or sagittal plane of this bilaterally symmetrical animal. At the center of the shell is a minute subspherical initial chamber, the pro- loculum, and enveloping it in an ex- panding spiral is the outer wall or spiro- theca of the several whorls (fig. 5). Thin meridional plates, known as septa, sub- divide the volutions into narrow, slender chambers that extend from pole to pole. The last volution ends in a steep face, the antetheca, which is formed by the sharp flexure of the spiral wall into a radial plane where it descends to meet the preceding volution. Inspection shows that the shell has grown by the addition of chamber after chamber, each enclosed by a short extension of the spiral wall and an antetheca. As each new chamber was added the preceding antetheca became a septum. The surface of the shell is divided into melon-like lobes by shallow meridi- onal grooves, called septal furrows be- cause they correspond in position with the septa, each being the depression where the outer wall bends in. As a purely arbitrary convention, the shell is commonly oriented so that the antetheca is on top and faces the ob- server. The outer wall then forms the roof of each volution and the surface of the preceding whorl its floor. Like- wise, the basal margin of the antetheca (or septum) is that which meets the floor, and the upper margin is that which joins the spiral wall or spirotheca. All but the last few septa are pene- trated near the middle by a low basal slit-like opening that provided communi- cation from one chamber to the next. This open passageway is the tunnel. In many of the fusulines it is bordered on each side by a levee-like ridge of sec- ondary shell deposit. These ridges are the chomata (singular, choma). Although the fusiform shape is char- acteristic of the fusulines, all possible variations of it are to be found. By elongation of the axis and filling out at the ends, subcylindrical shells were pro- duced, while less elongation has pro- duced melon-shaped forms. Inflation at the center and shortening of the axis y on the contrary, has produced thickly fusiform and spherical shapes. In a few genera extreme shortening of the* axis has led to nautiliform or discoidaL shells. External form is an important specific character, and in some instances it serves as a generic criterion, but homeomorphy is so common that identifications based upon external features alone are unre- liable — even generic identification on such a basis is generally insecure. In- ternal features such as the structure of the wall, the form of the septa, the na- ture of the secondary shell deposits, the shape of the tunnel, and the ontogenetic changes in size and shape from whorl to whorl, are the best clues to the biologic history and taxonomic relations within the group. These internal features are generally best studied in slices of the shell ground to transparent thinness. If preservation is exceptionally good and the filling of the shell is of clear calcite, well polished facets are also useful. Axial sections reveal the maximum number of char- acteristics but must be supplemented by sagittal sections (see fig. 11). In addi- [35] 36 PENNSYLVANIAN FUSVLINIDAK SP sf Fig. 5. — Shell morphology of a primitive fusuline. The left end has been cut off and portions of the last two volutions removed on the front side, a, antetheca; c. chomata; ch, meridional chamber; e, epitheca; p, protheca; s, septum; sf, septal furrow; sp, septal pore; st, spirotheca; t, tunnel. tion, tangential sections that cut the last two whorls are often very useful for the study of septal characters. In order to form a basis for comparison of one spec- imen with another, thin sections must be oriented in exactly the same way, and the only practical bases for orientation are the axis and the sagittal planes. Ax- ial sections must follow the axis very closely and must cut the center of the proloculum; sagittal sections should lie at right angles to the axis and must also cut the proloculum. The preparation of suitable thin sections is an art and a tedious obstacle to the study of this group, but it is essential. (See p. 65.) PROLOCULUM The proloculum is a minute, common- ly subspherical chamber with a single round aperture, like a pinhole, in one side. It is commonly assumed to be the external shell secreted about the very young foraminifer. Myers 1 has shown, 1 Myers, V/.tr] IT., Bull. Scripps Inst. Oceanography, Tech. Series, vol. 3, pp. 355-392, 1935. however, that this is not the case in the living foraminifer, Patellina corrugata Williamson, in which the proloculum of the megalospheric generation forms about the nucleus and within the cyto- plasm, whereas in the microspheric gen- eration it forms about a bud-like lobe on one side of the young foraminifer, not about the whole animal. But in Spirillina vivipara Ehrenberg he found that the proloculum is secreted about the entire young foraminifer. 2 There is reason to believe that the fusuline cor- responded to the latter species in this respect. Although the volume of a proloculum bears an extremely small ratio to that of the entire shell, there is a surprising- range of size in the prolocula of this family, not only from species to species but even within a species. Extremes from 20 microns to 750 microns in di- ameter are known, although the common range in Pennsylvanian genera is be- tween 100 and 300 microns. 2 Mvors, Earl H., Jour. Royal Microscopical Society, vol. 56, PP. 125-126, 1936. PROLOCULUM 37 The spherical or subspherical shape, so characteristic of the prolocula in this family as in all other Foraminifera, may have a purely physical basis. Before secreting its first shell, the young for- aminifer is a minute droplet of fluid protoplasm. Surface tension and per- haps cohesion would tend to keep such an object round, just as it does a drop of dew on a blade of grass or a drop of mercury on a table. A very small droplet of mercury assumes a nearly spherical form while a larger one spreads by its own weight into an oblate spheroid. Be- cause of surface tension the young for- aminifer, less than half a millimeter in diameter, would assume a subspherical form unless this force were overcome by some positive biologic tendency or some external influence such as crowd- ing or attachment to a solid object. The importance of surface tension in this regard is suggested by the fact that prolocula less than 120 microns in di- ameter are seldom far from spherical shape, whereas the greatest irregularity is found among those of larger size. At least two other factors seem to in- fluence the shape of the proloculum. One is the wall thickness of this cham- ber and the other is phylogenetic age. The wall of the proloculum is relatively thin in some species and thick in others, the range being from less than 10 to more than 60 microns. The reason for difference in thickness is unknown, for two species of the same genus occurring together may differ markedly in this re- spect. It is significant that thick-walled prolocula rarely depart far from a spherical form and that the maximum irregularity is seen in the thin-walled types. The reason for this is also ob- scure, since the wall of the proloculum was obviously calcareous and therefore rigid and brittle, hence the shape was fixed at the moment shell secretion be- gan. It should be noted that departures from the spherical form are of the na- ture of distortions, as though an en- velope, originally spherical, had shrunk unevenly or had been squeezed from one or more sides. Such irregularity in shape appears to be an individual and not a specific characteristic. It is con- ceivable that the prolocula were formed Fig. 6. — Diagrammatic equatorial section through proloculum and part of first volution of a megalospheric individual. p, proloculum; pa, aperture of prolo- culum showing the common, but not always present, depression of the lip of the aperture; 1-7, first to seventh chambers of the first volution. It may be noted that commonly the first and sometimes the second and rarely the third chambers have a spherical con- tour but with shortening radius. The presence of the valley (v) at the foot of the antetheca probably facilitates the change in contour. while the young fusulines were in a fission cyst comparable to that described by Myers 3 in Patellina, and that crowd- ing interfered with the symmetry of large amoebulae during their confine- ment. This, however, would have no ob- vious relation to the thickness of the wall. Another factor may have been the viscosity of the protoplasm in the young foraminifer. This may have af- fected the force of coherence and may have been correlated with virility or potency in lime secretion. A phylogenetic age factor is suggested by the fact that the greatest irregularity in shape is found in the prolocula of Parafusulina and Polydiexodina of late Permian age, but this may be due to en- vironment rather than time. There is clear evidence of abnormal salinity in many of the Permian seas and this doubtless involved not only the sodium chloride but other mineral salts as well, and may have affected the i^hysiology 3 Myers, Earl H., op. cit. 38 PENNSYLVANIAN FUSULINIDAE of shell secretion in certain of the fusu- lines either directly or indirectly. Double prolocula occur rarely in sev- eral of the genera of fusulines (e. g. PL 13, figs. 8, 9). This phenomenon has been recorded by several students and discussed at some length by Staff (1910, pp. 78-82) but its significance is still a matter of speculation. Each proloculum is commonly surrounded by about one volution of chambers coiled about itself without interference by its twin, and it appears evident that the twinning is due to the fusion of two young individuals after they had already started to form their shells. The double prolocula oc- cur only in the megalospheric genera- tion and the twinned young shells are approximately equal in size and stage of shell formation. Whether this means that they were members of a single brood or merely that fusion was possible only between individuals of the same age is uncertain. The resultant shell is commonly normal for the species so far as the size and form of its outer volu- tions are concerned, but in some in- stances it attains a size slightly larger than normal. The matter needs further study. WALL STRUCTURE The structure of the spiral wall in the fusulines is amazingly complex. It has been considered an important taxonomic character by nearly all students of the group and has been critically examined by many specialists, yet has received the most contradictory interpretations. That it is still a subject of controversy may seem strange to those who have not ac- tually attempted its study. Recent works by Henbest (1937) 4 and by Dunbar and Skinner (1937, pp. 543- 558) review the researches that have been made and present the latest points of view. These studies were made in- dependently and were in press at the same time (though the former appeared first) and include some differences in terminology that have been adjusted in the following account of the wall struc- ture. 4 References in parentheses appear in the bibliography at the end of this report. Two major types of fusuline wall were recognized by Moller as early as 1877 and were made the basis of generic separation. They have been named for genera in which they are clearly dis- played, the fusulinellid and the schwag- erinid types, respectively. They are il- lustrated by figure 7 and by plate 1, figures 1 and 3. In spite of the fact that the schwagerinid type was derived from the fusulinellid, and at one stage in the development of the family these types intergrade, they remain the most striking and useful basis for a major subdivision of the fusulines. Fusulinellid Type The typical fusulinellid wall (fig. 7 and pi. 1) appears to consist of four layers which differ in color and trans- parency. The thickest of the inner layers is the diaphanotheca, so called because it appears clear and transparent. Indeed, Moller mistook this layer for a filling of an originally open space by pure calcite. Bounding it on the outside is a very thin dark layer which has been named the tectum. The outer and inner layers, called tectoria, are alike in ap- pearance and in origin, are gray in thin sections, and are intermediate in density between the tectum and the diaphano- theca. Except at great magnification no further structures can ordinarily be observed. The wall structure appears simpler in the last few chambers of a well pre- served shell, whether it be immature or fully grown (pi. 1, fig. 2 and fig. 7A). Here the wall consists of a light gray layer covered externally by a thin and obscure film of darker material. These two layers clearly are the diaphanotheca and the tectum, the tectoria being ab- sent. Farther back in this volution, however, the chambers are lined not only on the roof, but on sides and floor as well, by a deposit that forms the tec- toria. Here the wall of the last volution consists of three layers, tectum, dia- phanotheca, and inner tectorium. Fur- thermore, this lining of the chambers forms the inner tectorium of the last whorl and the outer tectorium of the penultimate whorl. Since the outer vo- WALL STRUCTURE 39 lution shows these features at all stages of growth, it is evident that the dia- phanotheca and tectum constitute the first formed or primary element of the wall, the protheca, and that the tectoria represent a veneer of shell material, or an epitheca, added later as a lining of the chambers. Moreover, the inner tectori- um at any spot in the wall belongs to one volution, and the outer tectorium to the next. In spite of the existence of four layers, therefore, there are really but three elements involved in the wall, the diaphanotheca, the tectum, and epitheca. The tectum needs further investiga- tion. In many of the primitive fusulines it is so thin and obscure that some doubt is justified whether it is actually a shell layer or merely an optical illusion, like the Becke line in a rock section, due to the contact of two layers of shell differ- ing slightly in composition. The fusulinellid structure is the prim- itive type and is found with slight modi- fications in all the fusulines of early or middle Pennsylvanian (i. e., Bend — Des Moines or Moscovian) age. But although the four layers are distinct and are characteristic of Fusulinella, Fusulina, Wedekindellina, and some other genera, one or more of the layers appears to be absent from some of the primitive fusu- lines, and on this basis distinct genera have been set up, as clearly set forth by Lee (1933, p. 3). Thus Schubertella 5 was alleged to have but one dense layer, tectum ; Yangchienia to have two layers, tectum and diaphanotheca; Fusiella to have three, tectum and inner and outer tectoria. In some others, as Staffella, the differentiation is not clear, and in the genera mentioned the differentiation is commonly not clear in all parts of the shell. The taxonomic significance of these features would be clearer if we knew the cause for the differences observed in the wall layers. Gubler (1934 and 1935) has argued that the coloration in the wall is largely due to organic impurities intimately mixed with the calcite. He cites Averintzev's (1903, 1904) observa- / v****- mmw$^, e rnp. e _ 5 Although originally described by Staff and Wede- kind (1910, p. 121) as having a thin wall of one com- pact layer only, the genotype of Schubertella was re- cently shown by Thompson (1937, p. 120) to have a wall of two layers, tectum and diaphanotheca. Pig. 7.- — Comparison of (A) fusulinellid and (B) schwagerinid wall structure. Both are represented at the same magnification. In A the last two cham- bers of the last volution appear above. A is part of an excentric transverse section and B part of a sagittal section; a, alveolus; d, diaphanotheca; e, epi- theca; k, keriotheca; I, lamella of shell between alveoli; mp, mural or spiro- thecal pore; p, pyknotheca; sp, septal pore; t, tectum. tions that in living calcareous Foramini- fera the test is made of microscopic globules of calcite cemented together by an albuminoid organic substance known as tectine, which appears like chitin but 40 PENNSYLVANIAN FUSULINIDAE is chemically distinct. 6 Gubler succeed- ed in etching thin sections of fusulines with very dilute trichloric and formic acids and removing the calcite while leaving an organic residue sufficient to retain the form of the darker shell lay- ers. He concluded that the richer the layer in organic matter the darker its color. That is, the tectum is rich in tectine, the diaphanotheca is almost pure calcite, and the tectoria are an admix- ture of calcite with some organic matter. The idea is plausible. Myers 7 has re- cently observed that in the formation of the shell of the living foraminifer, Patellina corrugata, a film of organic matter is formed first and upon this base the calcareous wall is built. If Gubler 's interpretation is correct, Fusulinella began its shell with a thin layer, largely organic, which became the tectum, and immediately upon this it secreted nearly pure calcite to form the chief primary shell layer, the diaphano- theca ; then, for some unknown reason, the secondary shell material, added later to form the tectoria and chomata, con- tained an admixture of organic matter and calcite. In some living Foramini- fera it has been observed that at the moment before addition of a new cham- ber, enough material for its shell is held in solution in the protoplasm and is then quickly excreted. If this were true in the case of Fusulinella, there must have been a physiologic differentiation during the process of deposition, the organic constituent being excreted first and then the calcite, whereas in all shell material added later and more gradually to form the epitheca, both organic matter and calcite were excreted together. Failure of such a clear-cut differentiation would give less distinct shell layers, and might produce a three-layered wall as in Fusi- ella or a one-layered wall as commonly appears to be the case in Staffella and Ozawainella. Henbest (1937, p. 218) has recently expressed doubt that the tectum is al- 6 Averintzev, S., Tiber die Struktur der Kalkschalen mariner Rhizopoden : Zeitschr. fiir Wissensch. Zool., vol. 74, 1903. Beitrage zur Kemitnis mariner Rhizopoden: Mitt. Zool. Staz. Neapol., vol. 1.6, L903-1904. 7 Myers, Earl II., Bull. Scrippa Inst. Oceanography, Tech, Series, vol. 3, p. 359, L935. ways a distinct homogeneous layer of the protheca. He illustrated instances of its absence (pi. 34, fig. 1-4, and 14; and pi. 35, figs. 6 and 10) ; its occurrence as a zone of constriction in the outer end of the keriothecal pores (pi. 34, figs. 6 and 13 in part; pi. 35, figs. 4, 8, 9) ; and as a part of the basal deposit of epitheca in the overlying volution (pi. 35, fig. 1). He stated that in some shells this dark line is an optical illu- sion and in others it is probably a sec- ondary discoloration of the outer sur- face of the protheca by impurities before deposition of the epitheca. He conclud- ed that the tectum is heterogeneous or of several kinds of material. In most, if not all, of the later fusulines with a schwagerinid type of wall, however, the tectum is a well defined zone in the wall. Dunbar and Skinner (1937, p. 558 and fig. 96) accepted the tectum as a dis- tinct, normal primary shell layer, rich in organic matter according to Gubler 's hypothesis discussed above. If that in- terpretation be correct, it may obviously be thin or thick and it may be well differentiated from the underlying cal- cite layer or may grade into it. The finer microscopic structure of the shell has been a subject of controversy. At magnifications exceeding 200 diam- eters, and in suitably thin sections (pi. 16, figs. 15, 17), the shell material of the fusulines invariably appears finely granular. These particles are undoubt- edly calcite, but whether they are pellets secreted by the animal or foreign par- ticles picked up and built into the shell is not easy to determine. The difficul- ties of investigation are due to the smallness of the particles, which are generally 2 or 3 microns in diameter. The granules are thus several layers deep in an ordinary thin section, and a plane section through a single granule is rare because the grains in the shell are as fine as or finer than the usual abrasive powder. Even if plane sections are cut, the adjacent and underlying grains cause deceptive optical effects. Perhaps the most conclusive evidence for agglutinated structure is the granu- lar appearance at high magnification. On the other hand, the granules invari- ably seem to be calcite whether the mat- rix about the shells is limestone, shale. WALL STRUCTURE 41 or sandstone. Even this is difficult to prove decisively because only micro- scopic bits of the shell can be freed completely of matrix for examination; but tests for solubility in hydrochloric acid and for hardness, leave no doubt of the calcareous nature of the shell material. It is unreasonable to assume that the fusulines invariably selected calcareous particles and rejected all other foreign materials regardless of the surrounding bottom sediments, for that would demand an incredible degree of selectivity on the part of all members of a great family now numbering more than 500 species and ranging through two geologic systems. We are therefore inclined to believe that the fusuline shells are not agglutinated. Gubler's hypothesis that the fusuline shell is prismatic has been discussed re- cently at some length by Henbest (1937, p. 215) and by Dunbar and Skinner (1937, pp. 548-553), and rejected. SCHWAGERINID TYPE The schwagerinid type of wall (fig. 7B) has a distinctly different appear- ance from the fusulinellid. It common- ly includes only two layers ; one, the tectum, appears as a dark outer rind and is similar to the tectum of the fusu- linellid wall. The inner, and relatively thick layer, appears in thin sections to be transversely striped with dark lines about as dense as the tectum. These dark lines are the walls that separate deep prismatic or cylindrical alveoli. The gross structure (pi. 1, figs. 3, 5, 6) thus resembles that of honeycomb, and this alveolar layer is known accordingly as the keriotheca (Gr. kerion, honey- comb). In fusulines having this type of wall the epitheca has been generally re- duced to local deposits such as the cho- mata and, in some forms, as axial filling. Porosity of the fusuline shell has long been a subject of controversy. The problem was discussed at length by Hen- best (1937) and by Dunbar and Skinner (1937, pp. 544-558) and is reviewed briefly here. The schwagerinid type of wall was considered porous by many of the early workers, although there was confusion as to whether the dark lines crossing the wall were the pores or the shell ma- terial. These early workers, however, ignored the tectum. Girty (1904) called attention to the fact that in Triticites and similar forms the tectum is an in- tegral layer of the wall, and being un- able to detect pores in this layer he indicated that the fusuline shell was really imperforate. This idea was gen- erally accepted for the next quarter cen- tury, though Hay den (1909) observed that in certain Indian species the alveoli of the keriotheca are constricted to fine pores that pass through the tectum. Meanwhile it was supposed by all that the fusuline shell had an external aper- ture to provide for communication with the exterior; but the discovery that the tunnel is a secondary feature, due to resorption, and never reaches to the an- tetheca, led White (1932, p. 9) to the conclusion that the wall must be per- forate. He duplicated Hay den's obser- vations, apparently independently since he failed to mention Hay den's work. Henbest (1937, pi. 34, figs. 10-13) and Dunbar and Skinner (1937, pp. 544-553 and pi. 43, figs. 2, 3, and 4) have pub- lished the first convincing illustrations of pores in the tectum which have con- firmed the belief that porosity is proba- bly general throughout the fusulines. Porosity is commonly obscured in the fusulinellid type of wall because (1) the pores are extremely slender tubes and (2) where not functional they became filled or plugged with epitheca. Lee observed very fine pores in the diaphan- otheca in favorably preserved specimens of Staffella, Fusulinella, and Fusidina, and seemed to doubt the validity of a distinction between diaphanotheca and keriotheca. Galloway and Rvniker (1930, pp. 22-26 and pi. V, figs. 9-12 and legend) and later White (1932, p. 6 and fig. 95) observed very fine lines crossing the wall of primitive fusulines and interpreted the wall as fibrous. White, at least, considered the wall also to be porous. Henbest, in 1934, suc- ceeded in applying stains that resolved the structure and revealed tubular pores where they could not otherwise be ob- served, and in 1937 he discussed his observations at length with convincing illustrations. In the same year Dunbar 42 PENNSYLVANIAN FUSULINIDAE and Skinner (1937, pp. 553-558 and pi. 43, figs, i, 5, 6, 7 and pi. 44, fig. 5) de- scribed and illustrated pores in the wall of several fusulinellids. Henbest used the term alveoli for all tubular pores, whether large or small, constricted at one end or open, but Dunbar and Skin- ner drew a distinction between the tubu- lar pores which ran simply through the wall in the primitive fusulines, and the cell-like alveoli which characterize the keriotheca. This seems a desirable dis- tinction, both on etymological and prac- tical grounds. An alveolus is defined as "a small cavity or pit, as a socket for a tooth, or a cell or compartment of a honeycomb." Constriction or closure at one end is implied. This description fits the open spaces in the keriotheca of the schwagerinid wall, but not the simple capillary tubes that run through the fusulinellid wall. Henbest, as well as Dunbar and Skinner, however, treated the alveoli as highly specialized and en- larged mural pores, and the latter two authors indicated (1937, fig. 96) how the fusulinellid wall had evolved into the schwagerinid wall. The practical importance of the dis- tinction is evident at a glance on com- paring good thin sections of the wall of a typical early Pennsylvanian fusuline such as Fusulinella with thin sections of a late Pennsylvanian fusuline such as Triticites or a Permian form such as Schwa c/erina (e.g., pi. 1, figs. 1, 3, and text fig. 7). In either of the latter genera the spiral wall is 75 to 150 mi- crons thick and the tectum and kerio- theca are easily distinguished. In the keriotheca the shell material forms con- spicuous dark lines and the intervening alveoli are 5 to 10 microns in diameter. The compound wall of a primitive fusu- line, on the contrary, is commonly not more than 35 microns thick and displays the four layers previously described. The pores, if present, generally are so fine as to escape attention even at great magnification and can be observed only where they are naturally stained or where the shells have been favorably preserved. Artificial staining also will reveal them provided they have been filled by earthy matrix. Moreover, when the pores arc displayed they commonly pass through all layers of Ihe wall with- out constriction (see pi. 8, fig. 22; pi. 12, fig. 10) as tubular openings. To apply the term keriotheca to the wall in this case appears to the senior author to obscure a striking and significant dif- ference. SEPTA The septa are the radial walls between adjacent chambers of the same volution and appear to be inflected extensions of the spiral wall. In the primitive genus Staff ella they are flat partitions, and in the neoschwagerines and verbeekines they remain so through the racial his- tory. In most of the other genera the septa are more or less ruffled or folded, like a curtain ruffled by a gentle breeze, the upper margin remains straight and the lower part is thrown into a wave- like series of folds. In their evolution these septal folds appeared first near the poles and grad- ually spread toward the equator. In W edekindellina and Fusulinella they affect only the end zones and the septa remain flat, or plane, across the middle of the shell ; but in Fusulina the folds reach the equator, and the septa are strongly folded from end to end. Fur- thermore, the folds first affect the basal margin and in the course of specializa- tion extend eventually to the upper mar- gin. The folds of adjacent septa are al- ways opposed so that the backward fold of one is paired with the forward fold of the next. According to Staff (1910, p. 52) this is caused by a simple physical influence. He argued that as the proto- plasm outgrows the shell, it overflows and collects along the antetheca and when a certain increment has developed, it secretes a covering and thus adds a new chamber to the shell. If, before this addition to the shell, the previous ante- theca was folded, the overflowing proto- plasm would accumulate first in the re- entrants, where surface tension and co- hesion would round it up into a series of bead-like swellings. The new ante- theca, secreted to cover the front of this, would inevitably be folded forward where the preceding one was folded backward and vice versa. Although Staff's explanation appears plausible, SEPTA 43 the physiology of the process remains obscure. The width of a septal fold is measured from crest to crest or trough to trough ; its height is the distance it extends from the basal margin toward the roof; and its amplitude or depth is the distance a fold departs from the imaginary plane of the septum (fig. 8). The folding is considered shallow or slight when the amplitude is small in comparison with the distance between septa, and deep when it is great. With deep septal fold- ing the tips of opposed folds meet at or near the base and thus subdivide the meridional chambers into a series of cell-like chamberlets (pi. 17, figs. 9-11). These remain in open communication near the roof of the chamber where the intensity of the folding decreases. Dun- bar and Skinner (1937, p. 533 and pi. 42) have distinguished several different types of septal folds based on form. For example, the folding is regular when successive folds along a septum are similar in size and intensity; it is irregtdar when they are unequal in size and shape. Typically the regular folds run vertically up the septum (pi. 2, fig. 4), but in some fusulines they are not actually folds but blister-like irregular- ities developed chiefly in the end zones where the antetheca is high. Inasmuch as axial sections are cut vertically through the chambers and the septa, the sections of the septal folds appear as septal loops. Since the folds have their greatest amplitude near the base and die out upward, the size and length of the septal loops vary with the position in which the section happens to cross the fold, and if the septum is not straight, or the slice is not precisely parallel to it, the septal loops are very unequal and suggest an irregularity in the folds far greater than is actually true. In some species the septa are in- clined forward toward their base and this increases the probability that the folds will be cut by an axial section to form loops. A better understanding of the septal folding may be obtained from a tangential slice or, if the matrix is clear, from a polished tangential surface (cf. figs. 8 and 9 and 11 on pi. 10). The normal evolution of septal folds ^-su ^sf A Fig. 8. — Septal folds. In each view a portion of the spirotheca has been removed to reveal the septa. A, a primitive stage with plane septa (Fusulinella) ; B, an advanced stage with deep septal folds (Fusulina) ; 0, a highly special- ized stage with cuniculi (Parafusu- Una). 1). breadth of fold; c, chamber- let; cu. cuniculus; d. depth of fold; /. septal fold; sf, septal furrow; su, basal suture; us, upper margin of septum. is illustrated in figure 8. It was dis- played first among the primitive Fusu- lininae of the lower Pennsylvania!! which 44 PENN8YLVANIAN FUSULINIDAE began with Staffella and culminated in Fusulina, and it was largely repeated independently and at a later time by the Schwagerininae, which began with Tri- ticites in the upper Pennsylvanian and culminated in Par a fusulina and Poly- diexodina of the Permian. After the tips of opposed folds have met (see fig. 8), two further specializations are pos- sible. In Fusulina the backwardly di- rected folds tended to crowd over and rest upon the forwardly directed tips of the folds of the preceding septum. This was accomplished in only a few of the latest and most specialized species, and the result was to give the septal loops in axial sections the appearance of being pyramided (see pi. 15, fig. 15). On the other hand, when this stage of evolution was reached in certain Per- mian Schwagerininae, the tips of op- posed folds joined above the floor of the volution. This fusion formed a series of saddle-shaped arches between chamber- lets and left low passages around the shell which have been named cuniculi. This evolution gave rise to the genus Parafusulina in which the basal sutures, where the septa join the floor of the whorl, are at right angles to the axis instead of being parallel to it as they were primitively (see fig. 8c). This con- dition is best seen in tangential slices or polished facets cutting very close to the floor of one of the outer volutions. Whether cuniculi exist in the antetheca has not yet been decided. This problem and the process of their formation are now being studied by Henbest and Berthiaume in connection with Permian Fusulinidae from eastern Oregon. Ideally, it is possible to recognize six grades of septal folding, as follows : Grade I — septa plane from pole to pole. Ex. Rtaffella and early species of Wede- kindellina. Grade II — septa plane in the central re- gion but slightly folded in the polar regions. Ex. Fusulinella and certain species of Wedekindellina. Grade III — septa slightly folded across the central region and deeply folded near the poles. Ex. Species transitional be- tween Fusulinella and Fusulina; also many species of Triticites. Grade IV — septa deeply and regularly folded from poles to equator, tijos of op- posed folds meeting to subdivide the chambers basally into chamberlets. Ex. Fusulina and Hchwagerina. Grade V — as in IV except that backwardly directed folds are pyramided on the tips of those directed forward. Ex. A few of the latest species of Fusulina and of Schwagerina. Grade VI — tips of opposed folds join with- out reaching the floor, leaving cuniculi and composite basal sutures running around the shell. Ex. Parafusulina and Polydiexodina, and perhaps locally in the shells of late species of Fusulina. These are but arbitrarily chosen stages in a continuously evolving series. Moreover, they do not fully cover all cases. The septa necessarily converge toward the poles and are farthest apart at the equator ; hence, even if the folds were equally strong from pole to pole those of adjacent septa would meet first near the poles. In thickly fusiform or inflated shells, therefore, the septa may be strongly folded as in grade IV, yet fail to touch near the equator as in grade III. Furthermore, in its ontogeny a single shell may illustrate several of these stages. For example, the early species of Fusidina commonly are in grade II during the first three or four volutions before passing into grades III and IV. In judging the septal folding from axial sections it is important to distin- guish between simple oblique sections of a septum and true septal loops. The septa are commonly somewhat crooked regardless of the folding, and if so they will cross the plane of a section here and there even if free from folding. Or if the slice is somewhat oblique they will likewise cross it. Thus, for example, in the lower side of figure 13 plate 19, the first two lines crossing the penulti- mate volution on each side of the cho- mata are not septal loops. In structure the septa show some dif- ferences from the spiral wall in spite of the fact that each septum is a continua- tion of a segment of the spiral wall. In schwagerine shells the tectum continues from the outside of the spiral wall to form the front surface of the septum. The keriotheca bends in, becomes thin- ner, and loses its alveoli, passing down to form the main element of the septum as a compact layer of light gray calcite (pi. 1, figs. 3-6). No evidence of fine porosity, comparable to that of the spiral wall, lias been discovered and this TUNNEL 45 tissue may be termed the pyknotheca [Gr. pyknos, compact (as opposed to porous) -\- theka]. In sagittal sections the septa are inter- rupted by the tunnel and hang pendant into the whorl. Here the pyknotheca may thin or thicken distally. Com- monly the edge of the septum pendant over the tunnel is enveloped by epitheca, a part of the chomata. This greatly thickens the free ends of the septa seen in sagittal sections. To understand the structure of the septum alone, excentric cross sections may be studied to ad- vantage. In sagittal and excentric sections the pyknotheca commonly appears, at mod- erate magnification, like a wedge set into the wall, but greater enlargement (pi. 1, figs. 3-6) shows it to be a thin extension of the keriotheca. In the fusulinellid type of wall the tectum and diaphanotheca bend in, with little change in thickness or superficial appearance, to form the primary ele- ment of e^ch septum, which is later coat- ed over on both front and back surfaces by the epitheca. But whereas the dia- phanotheca has abundant fine pores, the pyknotheca has only scattered coarser septal pores. Septal pores are pinhole-like apertures in the septa, commonly appearing abun- dantly in the end zones of the outer volutions and more sparsely scattered across the middle of the shell; but in favorably preserved complete shells they seem to be as thickly scattered across the middle of the antetheca as they are in the end zones. They are much coarser openings than the pores of the diaphano- theca and commonly two or three times the size of the alveoli of the keriotheca (pi. 1, figs. 3, 5). Presumably they pro- vided the normal channels in many fusu- lines for extrusion of protoplasm. Norm- ally they are scattered at random, but a few specimens have been noted in which a row of such pores is concentrated along the basal margin of a septum in the outer whorl. An example in Wede- kindellina euthysepta is illustrated on pi. 8, fig. 21. The senior author has observed the same type of occurrence in a specimen of Triticites secalicus. It appears, however, to be a rare and in- dividual occurrence without taxonomic significance. Since the septal pores are commonly confined to the outer volutions, it might be assumed that they are a feature of the adult shell only ; but immature speci- mens also show them in the outer volu- tions even though corresponding volu- tions of adult shells appear to lack them. This suggests that pores may be present in the outer whorls at all stages of growth but that where not functional, in the inner whorls, they come to be closed by epitheca. This question needs further investigation. TUNNEL The tunnel is a low passageway cut- ting through the base of the septa in the equatorial zone and providing free com- munication from chamber to chamber. In axial sections it appears as an ellipti- cal or slit-like opening in the equatorial zone at the base of each septum, and in etched or weathered specimens it com- monly appears as a smooth girdle around the middle of the shell (pi. 2, fig. i.). Until 1932 it was generally supposed that the tunnel was merely the trace of an external aperture. However, shells with well-preserved antethecae never show such an aperture, and if sagittal sections are cut, it is found that the last several septa are complete at the middle of the shell. Since this is true at all stages of growth, it is evident that the tunnel is a secondary structure produc- ed by resorption at the base of the septa some distance back of the antetheca. This discovery was first announced by "White (1932, p. 13), had been made in- dependently by Henbest, and was fully discussed by Dunbar and Henbest in an unpublished manuscript submitted to the Illinois Geological Survey in May of the same year. That the tunnel is formed by resorption can be seen clearly in axial sections that happen to coincide with the distal end of the tunnel (pi. 16, fig. 17), where the opening is still irregular and ragged. Whether or not the fusuline possessed an external aperture in the earliest growth stages is still an unsettled prob- lem. There is reason to suspect that the 46 PENNSYLVANIAN FUSULINIDAE single round hole that invariably occurs in one side of the proloculum was a primary aperture. The first chamber of the spiral series is more or less hemi- spherical, and is always fitted over this hole as though the protoplasm that se- creted this first chamber had exuded through this pore and accumulated as a droplet on the side of the proloculum. In the first several chambers the tunnel is invariably narrow and elliptical even in species whose tunnel in later stages is wide ; but very young specimens having only one or two volutions have been ob- served in which the antetheca had not been penetrated by the tunnel. Whether these observations are generally repre- sentative or not, we are confident that after the formation of the first few volutions there was no external aper- ture. The tunnel is a feature of the sub- families Fusulininae and Schwageri- ninae only; the Verbeekininae and Neo- schwagerininae on the contrary having a single row of round openings along the base of each septum. No opportunity has yet been found to examine shells of these groups critically to see whether such openings are present in the ante- theca. Although there are exceptions, it is usual for the tunnel of spherical and very yentricose fusulinids to be narrow. In slender or cylindrical species, the tunnel is generally, though not always, wide. The elongated species in the Piasa and Lonsdale limestones have tun- nels that appear to widen as the shell elongates. CHOMATA In the primitive fusulines such as Fusulinella, in certain more specialized genera such as Fusulina and Wedekin- dellina, and in Triticites, a narrow ridge of secondary shell material lies along each side of the tunnel. These ridges are the chomata. They are heightened where they cross the septa, and com- monly merge into a narrow zone of epi- theca that extends up the margins of the septum beside the tunnel, and even along the pendant margin of the septum above the tunnel. The chomata are small, where present, in the last volution, and at all stages of growth fall just short of reaching as far as the tunnel with which they are so closely allied. This would indicate that they, like the tunnel, are secondary fea- tures. This is confirmed by their struct- ure which can be seen commonly in axial sections and which shows that they have grown thicker by the addition of successive lamellae of shell material (pi. 2, figs. 10. 11). The fact that material is resorbed to form the tunnel, and deposited to form the chomata, naturally leads to a suppo- sition that there is a simple transfer, the resorbed material being deposited again beside the opening. But the relation is evidently not quite so simple and direct as that, for the volume of material re- sorbed bears no direct relation to the volume of the chomata. For example, in Fusulinella where the tunnel is extreme- ly narrow we find the most massive cho- mata, and in Schwagerina or Parafusu- lina where the tunnel is wide and fully developed there are no chomata what- ever. Even in contemporary species of a single genus, as Fusulina or Triticites, there is no simple correlation between the width of the tunnel and the size of the chomata. It may be added that in Schwagerina, Para fusulina, and Poly- diexodina where chomata are lacking, some of the species have conspicuous epithecal deposits lining and even filling the chambers along the axis or in a belt bordering the tunnel. Such axial filling commonly far exceeds the volume of shell resorbed to form the tunnel and in- dicates an external source for such limy deposits. W edekindellina with an ex- tremely narrow tunnel has both chomata and a heavy axial filling. The function of the chomata, if any, is problematical. Resorption of the tun- nel weakens the shell against external stresses, and the chomata reinforce it at the weakest place. Thus, in the large, slender species of Parafusulina and Polydiexodina we commonly find the shell broken or cracked through the equator, apparently as the result of stresses caused by compaction of sedi- ments. At some localities it is difficult to find specimens that have not been RfiSUME 47 thus broken, but if such a shell is broken during fossilization the break almost in- variably passes through the tunnel. Species having chomata, on the con- trary, are seldom broken through the center. There has been a tendency, therefore, to look upon the chomata as a functional structure deposited to strengthen the shell. But it is not evi- dent that the shells of the living animals were subjected to any such stresses as would have broken them at the middle. Living in a fluid medium they were not subjected to breaking stresses like those imposed on the shell after burial. On occasion they may have been tossed about on the bottom by storm waves but the lack of evidence of attrition sug- gests that this was not a common men- ace. Moreover, if the chomata were really functional, it seems strange that they were gradually lost in the Schwag- erininae about the beginning of Permian time and are wholly lacking in the large, slender forms in which the danger of breakage at the middle was obviously greatest. R£SUM£ Relationship between mural pores, septal pores, chomata, and epitheca. — Evidence has been cited above that the shell wall consists of two elements, pro- theca and epitheca. The former is the primary or essential wall ; at all stages of growth it alone comprises the wall of the last-formed chambers. The epitheca is a deposit laid down subsequently, up- on the spiral wall of the septa. In the primitive fusulines it is a continuous sheath coating the roof, sides, and floor of the chambers and appears to be the outer and inner layer of the wall. The chomata are essentially only a special- ized thickening of this secondary de- posit along the edges of the tunnel. In the more advanced genera the protheca is commonly thicker and the epitheca greatly reduced. In Triticites of up- per Pennsylvanian age, epitheca com- monly was represented only by the cho- mata, but in many species of the Per- mian genera Schwagerina, Parafusu- lina, and Polydiexodina it was again prominent not as a simple layer of the wall but as a localized deposit, lining or even filling the chambers along the axis or in a wide belt on each side of the tun- nel. The protheca has been shown to be perforate. In the primitive fusulines the pores of the spiral wall are extreme- ly fine and apparently tubular, but in more advanced genera they expand into conspicuous alveoli transforming the chief wall layer into a honeycomb-like structure. Septal pores are most commonly seen in the outer volutions and particularly in the end zones. But they are also found in the outer whorls of immature shells. This suggests that they may have been present at all stages of growth but were functional only in the outer whorls and were progressively plugged and sealed by epitheca as they became useless in the inner whorls. Indeed it is difficult to see how the protoplasm of a growing animal would overflow the shell and readily accumulate along the front of the antetheca, as it obviously did, un- less the chief openings were along the antetheca. If, as inferred above, the pyknotheca was not finely perforated like the spirotheca and if the tunnel had no external opening, it seems reasonable to infer that septal pores must have been present at all stages of growth. The observed distribution seems to in- dicate that septal pores were normally abundant and subequally distributed from equator to poles (as they have been seen in the antetheca of favorably pre- served specimens of Fusulina, Wede- kindellina, or Triticites). However, there must have been a tendency for them to be rendered obsolete as the tun- nel was opened in order to provide free communication between chambers and as epithecal deposits were laid down. Septal pores were thus closed in the in- ner volutions, commonly disappearing first in the equatorial region where epi- thecal deposits are obviously thickest, and remaining open longer in the polar regions. Although fine pores can be demon- strated in the spiral wall of favorably preserved or stained specimens of the primitive fusulines (subfamily Fusu- lininae), such pores are commonly very obscure and at best are normally visible 48 PENNSYLVANIAN FUSULINIDAE only in the outer volutions or in local areas of the shell. Where preserved they may penetrate the epithecal deposits as well as the protheca. The reasons why they are so obscure and were so long overlooked in these primitive genera are, first, their extreme fineness and, second, the tendency to be closed by epithecal deposits. The first would render them difficult to see at ordinary magnifica- tion ; the second would either fill and obliterate them or prevent the infiltra- tion of noncalcareous matrix after bu- rial. In the outer volution they may have served as passageways for the pseudo- podia and provided for respiration, and in the inner whorls they may have served as channels of communication for the diffusion of digested food or the passage of respiratory products or hormones (if such existed). The tun- nel provided an obviously freer avenue of communication for mass movements of sarcode. INDIVIDUAL AND RACIAL DEVELOPMENT Dimorphism It is now known that many species of Foraminifera present shells of two dis- tinct forms, one being commonly larger than the other. This dimorphism was first suspected among the Eocene num- mulites in which pairs of "species", one large and the other small, are commonly associated. Munier-Chalmas in 1880 8 first suggested that these were but differ- ent forms of a single species, and coined the term dimorphism. Verification of the idea and explanation of the phe- nomenon came in 1895 when Lister, 9 in England, and Schaudinn, 10 in Germany were working independently on living Foraminifera, and discovered an alter- nation of sexually and asexually pro- duced generations which differed strik- ingly in size. The sexually formed in- dividual began with the fusion of two tiny gametes and initiated growth and shell formation while still very minute. Its shell, therefore, started with a very small proloculum. Asexually produced individuals, on the contrary, began as relatively large gamonts produced by the fission of the parent. Their shells started, therefore, with a relatively large proloculum. On this basis Lister dis- tinguished the shells of the sexually formed generation as microspheric, be- cause they had a minute sphere or pro- loculum, and the others as megalospher- ic. Curiously, the microspheric shells among the nummulites grew to the larg- er size. Recent experimental work of Myers 11 has given the first full and accurate ob- servations on the life history of dimor- phic species. Among other things he has found that, although in some species the microspheric generation grows to much larger size than the megalospheric, it does not in others. Observations on shells alone, both fossil and recent, have shown that the juvenarium of the micro- spheric shell commonly differs in form from the later whorls in ways suggesting a recapitulation of racial history. The considerable variation in size of the prolocula in many species of fusu- lines has led various students to distin- guish microspheric and megalospheric individuals, but in most such cases com- plete intergradation exists and the dif- ferences are probably not due to true dimorphism. In 1936, however, Dunbar, Skinner, and King (pp. 173-190) described strik- ing examples of dimorphism in the Per- mian genus Parafusulina. In these the megalospheric shells were formed of six to eight planispiral volutions and the prolocula were from 300 to 500 or 600 microns in diameter. The rare micro- spheric shells began with prolocula less than 50 microns in diameter and includ- ed a juvenarium of between one and two volutions of rounded or subspherical chambers coiled at nearly right angles to the ensuing whorls. The adult microspheric shells are about twice as 8 Munier-Ch:ilm;is, Sur 1e dimorphisme des Nummulites: Soe. poi. France Bull., vol. VJII, p. 300, 1880. 9 Lister, J, J., Contributions to the life-history of the Foraminifera: Royal Soc, London Philos. Trans., Ser. I',, Vol. 186, p- 401, 1895. 10 Schaudinn, P., tJber den Dimorphismus der Fora- miniicren. Sitzungsb. Oesell. Naturf. Freunde zu Berlin, No. 5, pp. 87-97, -]H<>:,. 11 Myers, Earl, The life history of Patellina cor- rugata, etc. Bull. Scripps Inst. Oceanography, Tech. Series, vol. 3, pp. 355>-392, 193f>. Morphogenesis of the test and biological significance of dimorphism, etc. ; ibid., pp. 393-402. The life cycle of Spirillina : Jour. Royal Microscopical Soc, vol. 50, pp. 125-126, 1936. DEVELOPMENT 49 large as the adult megalospheric shells. The juvenile part of the shell in these microspheric giants so closely resembles the shape of an adult Endothyra that it has been termed an endothyroid juve- narium. The same type of dimorphism was found by Dunbar and Skinner in the genus Polydiexodina. Curiously, in these Permian species the microspheric shells have no tunnel except in the first few fusiform whorls. Of course, the well developed cuniculi in these genera pro- vide for adequate communication be- tween chambers, and the tunnel seems to be superfluous, yet it is striking that the megalospheric shells have a well de- veloped tunnel and the microspheric have none at all except in the first two or three of the fusiform whorls. An extraordinary parallel to the dimorph- ism in these Permian fusulines was ob- served by Chapman in the Recent for- aminifer, Alveolinella quoyi. 12 In modern Foraminifera several asexual generations commonly succeed one another directly and a sexual gen- eration occurs only rarely; as a result megalospheric shells are commonly hun- dreds of times more abundant than the microspheric. This was clearly the case with the genera Parafusulina and Poly- diexodina, in which the microspheric giants are rare. In the early Pennsylvanian fusulines from Illinois, we have encountered a few shells that appear to be truly micro- spheric. One of these, belonging to Fusu- linella iowensis, is illustrated on plate 3, figures 15 and 25 ; another, belong- ing to Fusulina spissiplicata, is shown on plate 7, figure 12 ; and a third, of the species F. eximia, is shown on plate 23, figures 19 and 20. White (1935, pi. 18) has illustrated a closely similar occur- rence in a species of Fusulina and an- other^ in a species of Triticites from Oklahoma. In our Illinois shells the microspheric individuals agree closely with the associated megalospheric shells in size and external appearance. The distinction between the two is limited essentially to the early whorls which, in the megalospheric, are typically fusu- 12 Chapman, F., On Dimorphism in the Recent Fora- minifer, Alveolina boscii Defr. sp. Royal Micr. Soc. Jour., pp. 151-153, 1908, pi. 2 and 3. line from the first, and, in the micro- spheric, begin with a very small prolo- culum and have a well defined endothy- roid juvenarium. In these examples from the genera Fusulina and Fusu- linella, and in the Fusulina and Triti- cites figured by White, the tunnel and chomata are normally developed as in the megalospheric shells. It is desirable to distinguish clearly between such shells possessing a true en- dothyroid juvenarium and others, oc- casionally seen, in which the early whorls are fusiform but have the axis somewhat oblique to that of later whorls. In the latter only a slight migration of the axis during early growth is com- monly present but there is no fundamen- tal change in the shell ; the early whorls are fusiform and the chambers are long, like the lobes of a melon. In the endo- thyroid juvenarium the early chambers are subspherical in form and the shell is in no respect fusiform in shape or fusu- linoid in nature. In thin axial section, it is hard to distinguish the two types, but in thick axial sections or in sagittal sections the difference is evident. True dimorphism, with an endothy- roid juvenarium in the microspheric generation, appears to be more common in some of the oriental genera of fusu- lines, such as Misellina ( ? ) and Neosch- wagerina, than it is in the genera discuss- ed above. Although microspheric forms are extremely rare in many genera such as Fusulinella, Fusulina, and Triticites, it now appears probable that they must be expected in all the genera and in any species of the Fusulinidae. This suggests the need for a reconsid- eration of the taxonomic significance of an unsymmetrical juvenarium. It has been considered one of the chief criteria of such genera as Schubertella, Eoschu- bertella, Fusiella, Boultonia, and Yang- chienia ; but we should expect a megalo- spheric equivalent for each of these in which bilateral symmetry and a larger proloculum exists. Such may or may not differ notably in size from their microspheric counterpart. Field occur- rence and associations will apparently be our best guides in identifying such related forms. 50 PENN8YLVANIAN FUSULINIDAE Recapitulation In the classification of the Foramini- fera the idea of recapitulation is useful, but its importance varies from group to group. In some it is so obvious that it is admitted without question, but in other groups recapitulation is so uncer- tain that attempts to use it as a means of delineating racial history have led to rash conclusions. Ontogeny is represented by progres- sive changes in length, thickness, and proportions, and by changes in the mas- siveness or shape of the chomata, in tun- nel angle, and in the type and intensity of septal folding. Two shells which are very similar at maturity commonly differ much more in their younger whorls. Because such ontogenetic changes are so significant we have adopt- ed the policy of tabulating the measur- able features of each volution of several type specimens. Certain genera are distinguished by their ontogeny, notably Pseudoschwag- erina and Paraschwagerina, both of which differ from closely related forms by having a tightly coiled juvenarium followed by abrupt and marked inflation. Other genera have been distinguished on the basis of an un- symmetrical juvenarium, but as noted in the discussion of dimorphism, this may have a different significance. Within limits, the concept of recapit- ulation is useful in the study of the fusulines (as it is elsewhere in the For- aminifera). as a clue to phylogenetic re- lationships. For example, the geologi- cally older species of Fusulina have com- monly three or four inner volutions with massive chomata and almost plane septa, indicating their derivation from Fusu- linella, whereas this fusulinellid stage is more and more abbreviated in later spe- cies and finally omitted. The early whorls of Pseudoschwagerina have all the characteristics of Triticites, includ- ing well developed chomata and slightly folded septa, whereas the corresponding whorls of Paraschwagerina have very slight chomata and regularly and deep- \y folded septa as does Schwagerina s.s. Thf '(nstipctjly^eness oj: Pseudoschwag- ■ erina and Parascrm)a'g%rina is thus indi- cated by ontogeny. The geologically oldest species of Schwagerina have less deeply and less regularly folded septa than later ones and retain distinct traces of the chomata, thus indicating their origin in Triticites. The endothyroid juvenarium is com- monly believed to indicate the ancestral type of smaller Foraminifera from which the fusulines developed. The common explanation for dimorphic shell structure is that since the microspheric individual originates from amphimixis, it is primitively reproduced and its growth and form are profoundly con- trolled by the racial history of its fore- bears. The megalospheric individuals, being born of mitosis, supposedly origi- nate to a certain degree as did Athena from the head of Zeus (parthenogene- tically) and, accordingly, at birth are advanced ontogenetically beyond the stage of recapitulation. Thus the chron- ologic age and ontogenetic age of the individual may differ according to its kind of generation. Possibly it is signi- ficant that endothyroid juvenaria are most common in early members of the family such as Fusiella and Eoschuber- tella, or in persistently primitive ones like Schubertella, Boultonia, and Yang- chienia. The microspheric individuals of the Permian genera Parafusulina and Poly- diexodina, however, present a curious problem in that they have no tunnel. The tunnel is, of course, a secondary feature developed by resorption of the septa, but it is invariably present in all genera of fusulines from the most primi- tive to the last, with the exception of the microspheric individuals of these Per- mian genera. Does its absence in the microspheric generation of Parafusulina and Polydiexodina indicate reversion to an ancestral stage preceding the tunnel formation? Apparently not, because in similar microspheric individuals of the older genera Fusulinella, Fusulina, and Triticites, the tunnel is normally de- veloped. Does it then mean that by tachygenesis the tunnel has been com- pletely eliminated in these shells where it is no longer needed? If so, we have the strange contradiction of a persis- tence of the extremely remote ancestral RECAPITULATION 51 condition in the spiral juvenarium and at the same time the complete suppres- sion by tachygenesis of one of the most characteristic shell features of the fami- ly. Neither explanation seems satisfac- tory. This suggests the necessity for caution in the application of the principle of re- capitulation to the Foraminifera. The spherical proloculum is primitive in that it represents the most common basic arch- itecture seen in the Foraminifera. But to regard this as phylogenetically signi- ficant carries the assumption that the character of the ontogenetic develop- ment is unrestricted except by inherit- ance, and that its evolution of form is free of the ordinary vicissitudes of life that affect the parent and all other adults. But, as explained on page 37 it is a demonstrable fact that surface tension and cohesion are powerful forces in shaping minute fluid particles ; and the spherical form so general for small prolocula is probably due to the fact that the * ' embryo ' ' was unable or lacked incentive, or at least found it uneco- nomical of energy, to overcome these forces and produce any other shape. If it is granted that the incapacity, or at least the indisposition, of the "embryo" to assume other than a spherical form is continued until the strength of the in- nate form-controlling forces and the in- crease in size are together sufficient to overcome the external form-controlling forces, then we can understand the changes which take place toward de- veloping the adult idiomorphology as a succession of adaptations or compro- mises between opposing forces. In the development of the fusulinid shell this explanation fits the observ- able changes (see fig. 6, p. 37). The first chamber to be built after the proloculum has a more or less spherical contour, its exact form de- pending, we suppose, on the amount of growth of the sarcode before a new chamber was constructed, or it may de- pend upon the amount of sarcode ex- truded to take part in chamber building. If the increment of sarcode or the amount extruded were as great as the volume of the original mass, the second chamber (the first of the spiral series) would be spherical, with a radius com- parable to that of the proloculum, but of course it would be excentric. If, on the contrary, the growth, or the amount ex- truded, were only a small addition to the size of the sarcode, the form of the cham- ber would remain somewhat spherical but would reflect more strongly the in- fluence of the shape and capillarity of the proloculum. The second chamber of the spiral series would have, instead of a single spherical surface for a founda- tion, two curved surfaces intersecting to form a valley. This valley then makes it possible for the second chamber of the spiral series to be longer and more nar- row than the first one, provided that the body of sarcode actively engaged in chamber building is not large. The in- creased height of the second chamber relative to its width makes its front face steeper and thereby alters somewhat more the foundation for the third cham- ber ; and so on for the fourth and follow- ing ones. Accordingly, we would argue that if innate form-controlling forces are active at this stage, they can operate most effectively and economically by controlling either the amount of sarcode extruded to build a chamber or the fre- quency of chamber additions relative to the rate of growth of sarcode, both of which would achieve the same end. In microspheric individuals the first and occasionally the second whorl of cham- bers are rounded in transverse section, lie close to and conform with the spheri- cal proloculum, and are subject to aber- rations in direction of growth but gradu- ally become more extended at the poles and develop the fusuline morphology. Accordingly, the progressive change in the shape of the chambers from the spherical proloculum to the slender ones of the later stages can be viewed as a series of adaptations and as a struggle between the innate or indigenous and the external form-controlling forces. The external forces at first predominate but are gradually overcome by the indigen- ous ones as the size increases and the in- fluence of surface tension becomes pro- portionately less. The succession of chamber forms de- scribed above is a matter of common ob- servation. CuKuingtanQs (3E©|^3G*a" SURVEY HDRVW JUL 29 tttt 52 PENNSYLVANIAN FUSULINIDAE fairly simple physical basis for this evo- lution of chamber form. The above ex- planation seems to be most satisfactory at the present time and we present it, though perhaps in an over-simplified form, for what it is worth. If this series of adaptations 13 follows a course that coincides with that of the evolution of the race it should not be surprising, because one may argue that the same external forces that participat- ed in controlling the morphology of the individual also shaped in the same meas- ure and manner the morphological evo- lution of the race. This principle is par- ticularly applicable to protozoan zoology because most of the life history of the individual is passed outside the influ- ence of or contact with the parent. Af- ter separation the so-called embryo is in contact with practically the same ele- ments as the adult. The expressions innate or indigenous form-controlling forces are used here with the understanding that an immi- nent origin of the forces is referred to. Historically these forces appear to have evolved from a compromise between the sometimes opposing and the sometimes coordinating forces from within and without those individuals that perpetu- ated the race. In conclusion we may point out sev- eral considerations that should be kept in mind when recapitulation and phylo- genesis are being considered. (1) Among foraminifers, most of the stages of supposed recapitulation are in all probability not passed within a par- ent but are passed while the individual is free living. It is possible, therefore, that the young become adapted to exter- nal forces just as adults do. If this were true, it would be possible for reca- pitulation to present a false record of the history of the race. (2) The process of recapitulation may represent a series of adaptations or compromises between indigenous and ex- ternal forces. (3) In animals in general, the reca- pitulation stage commonly represents a type rather than a specialized form. 18 The writers wish lo acknowledge the kindness of Professor Alexander Petrunkevitch, Department of Zool- ogy, Yale University, for his suggestive criticisms of Ihis section of our paper. In the light of the foregoing notions, it will be interesting to examine the Fusulinidae to determine the significance of the supposed recapitulation. It has been repeatedly observed that the juvenaria of most, if not all, fusu- line genera belong to but a very few types. The advanced species of Fusu- lina have a juvenarium not far different from that of a number of other genera in the family. Since this type is repre- sented in a great number of earlier and later genera of Foraminifera not belong- ing to the Fusulinidae, that phase of re- capitulation ceases to have significance. The supposition has repeatedly been expressed that the Fusulinidae descend- ed from Endothyra, but the microspher- ic juvenarium is in some respects as much like Glyphostomella and Bradyina as Endothyra. Moreover, the juvenarium in some genera resembles Endothyra more, but in others is more like Brady- ina, which is a disturbing situation if we treat the group Fusulinidae as mono- phyletic. Earlier species of Fusulina do exhibit a stage of shell building in the early part of the adult morphology in which septa are plane, walls are massive with epi- theca, chomata are wide, and form ratio is the same as in Fusulinella. For sev- eral reasons, historical, anatomical, etc, we consider Fusulinella as ancestral to Fusulina. We believe that this conclu- sion would have been made even if the repetition of the fusulinellid shell had not been seen in the early species of Fusulina. A large number of more or less ob- viously true examples of recapitulation can be pointed out among the Foramini- fera, but we are confident that the prin- ciple is often misapplied through un- critical use. Inasmuch as only a few fusulinids show a phase of ontogeny that can defi- nitely be recognized as recapitulation, and just as possibly a majority of the Foraminifera either lack unmistakable evidence of recapitulation or at best bear ambiguous or confused evidence, it would seem appropriate to say that ontogeny often recapitulates phylogeny. EVOLUTIONARY TRENDS 53 Evolutionary Trends The history of the Fusulinidae is characterized by a rapid evolution into several distinct branches, nearly all of which were short-lived. Only a few of the least specialized genera, notably Staff ella, Ozawainella, and Fusulinella, persisted through a geologic period. Amid the diversity of their evolutionary experiments, repetition of form and parallelism of trends have resulted in striking homeomorphy of external form. These homeomorphs are but still further evidence that the Foraminifera have often and independently repeated their evolutionary experiments. The history of external form among the fusulines is a case in point. It is more involved than one would at first suppose, a fact clearly reflected in the changing conception of fusuline tax- onomy. The original recognition of Fusulina cylindrica Fischer, 1829, was based mainly on its peculiar external form. It was not until 1877 that Vale- rian von Moller placed the classification of fusulines on a sound anatomical basis by using thin sections and inferentially demonstrating the fact that external form and internal structure are not al- ways to be correlated. Not until the last decade, however, did paleontologists cease basing identifications of fusuline genera and species on external form alone. When the phylogenetic relationships of the Fusulinidae as a whole are viewed it can be seen that there has been a gen- eral evolutionary trend in form from the spherical to the fusiform, which is the most common shape, and thereafter to one of two divergent extremes, the first reverting toward a spherical and the other progressing toward a slender subcylindrical form. This phenomenon is especially well shown first by Fusu- lina and later by Triticites, both of which originated as fusiform types and later developed the full range of ex- tremes from subglobular to subcylindri- cal shape. A similar history is displayed by each of the two subfamilies which they represent, i. e., the Fusulininae and the Schwagerininae as a whole. Such parallelism in the evolution of different genera, and even subfamilies, at different times would seem to indicate both that a physical, external, form- controlling force was present, and that, in a sense, evolution repeats itself. The earliest known fusulines had thick fusulinellid shell walls, plane sep- ta, and either chomata or a very thick layer of epitheca on the floor of each chamber. W edekindellina maintained these features throughout its history, but Fusulinella changed from a plani- septate form to one of regularly plicated septa in the latest volutions, such as Fusulinella iowensis Thompson from the limestone caprock of the Rock Island (No. 1) coal in northwestern Illinois. Several intermediate species such as Fusulinella bocki Moller have irregular plications in the polar zone. Although Fusulinella does develop septal plica- tions near the end of its history, even in species which were not in the line that gave rise to Fusulina, the ad- vanced or highly evolved fusulines retained much of the massive wall structure characteristic of typical Fusulinella. Fusulina at an early stage began increasing the depth and number of its septal plications, and correspond- ingly decreased the massiveness of its walls. The thickness of the protheca de- creased only gradually, but epitheca showed the most marked decrease. The earliest species of Fusulina ordinarily have epitheca whose thickness is greater than that of the protheca, but such highly evolved species as Fusulina girtyi (Dunbar and Condra) (from the Brere- ton limestone) and F. megista Thomp- son, and F. eximia Thompson (from the Lonsdale and Piasa limestones of Illi- nois) have tectoria that, except for the chomata, are thinner than or at least as thin as the protheca. The shape and size of the chomata have a similar history. In many speci- mens of W edekindellina and Fusulinella the chomata are relatively low and not sharply differentiated from the very massive floor deposit of epitheca. Also, the chomata do not rise high on the septa. Among the Fusulininae, chomata reach their most typical form in the lower Pennsylvanian fusulines in which 54 PENNSYLVANIAN FUSULINIDAE they are high, restricted in width of base, and have the typical natural levee- like form, but do not rise very high against the septa. In these same fusu- lines the rest of the epitheca is moder- ately thick ; the septa are not very deep- ly and regularly plicated ; and the shells are fusiform. The chomata undergo changes in the evolution of higher forms of Fusulina that correspond to the in- crease in depth of septal plications and decrease in thickness of the walls. In these highly evolved species, the chomata decrease in width of base and rise high against the septa, even extending on the septa over the tunnel. The change ap- pears to have been gradual. It has been thought that such highly evolved species as Fusulina girtyi (Dunbar and Con- dra) have no chomata, but if one has difficulty in finding them in thin sec- tions, they can easily be observed by dissolving or breaking away the spiral wall of a specimen and viewing them from above. The history of epitheca, chomata, and septal plications in the Schwagerininae has more points of similarity with that in the Fusulininae than one would sup- pose on casual reflection. The most primitive genus of the Schwagerininae yet known is Triticites. The earlier species, such as T. secalicus (Say), have epitheca, especially in the earlier por- tions of the shell. The septa are rather less deeply and regularly plicated and the chomata are more typically devel- oped than usual in that genus. In the highly evolved T. ventricosus (Meek and Hayden), whose shape and size is some- what comparable to that of T. secalicus, the septa are more deeply and closely plicated; the walls are more delicate; the chomata are less massive ; and the tectorium is almost completely absent except in the form of a very thin, widely distributed, more or less indistinguish- able veneer on the walls. It is almost certain that the form that gave rise to the family Fusulinidae had no chomata. Ontogenetically the chomata are in every respect secondary structures because they were formed in the individual after the primary struc- ture had already been completed. Never- theless, they wore one of the first de- veloped distinctive features of the fam- ily, appearing in Staffella and Fusulin- ella and all the other early genera. In Staffella they persisted into Permian time, meanwhile disappearing in the Schwagerininae. The Verbeekininae and Neoschwagerininae appear to have sprung from Staffella early in middle Permian time, originating in Eoverbeek- ina which retained a slit-like median tunnel while adding a row of round holes along the base of the septa. As these new passages developed, para- chomata appeared as ridges on the floor of the volution alternating with these passages. In origin and structure these are essentially duplicated chomata. Their late appearance is indicated in the ontogeny of Verbeekina wherein para- chomata are commonly lacking in the early volutions. If the Verbeekininae and Neoschwag- erininae evolved from Staffella, the de- velopment of their alveolar spiral wall out of the fusulinellid wall of Staffella forms an amazing parallel to the earlier development of the alveolar wall in the Schwagerininae. After the development of septal plica- tions, the development of keriotheca out of diaphanotheca probably rates as the greatest single advance in maintaining strength and decreasing the weight of the shell. Among the Schwagerininae, advances in shell structure took place by increasing the depth and complexity of septal plication or by a reversion to spherical form. Parafusulina developed a complicated system of fusion between the septal folds whereby it was able to resorb portions of the septa, and by the same act, to maintain great strength and lighten the shell structure, and estab- lish from pole to pole a system of numer- ous channels of communication between the chambers. The evolutionary trends in the shell structure of the main stem of the family resulted in great increases in the sar- code-housing capacity of the shell with- out impairing its strength and useful- ness. In other words, the changes ap- pear to be advantageous ones. The shells of Staffella, Fusulinella, and Wedekin- dellina were very heavy and afforded scant housing for sarcode, but by decreas- FORM AND ANATOMY 55 ing the thickness of the walls, by folding the septa, and by shaping the chomata more advantageously, strength of shell was maintained in the more advanced genera and housing capacity greatly in- creased without a corresponding in- crease in the weight of the shell. It would seem probable that the more high- ly developed forms with light shells were able to move about more easily and quickly and were able to compete more successfully for food. The tele- ological interpretation of these morpho- logical changes is hard to apply con- sistently, however, because, for example, some species, such as Schwagerina com- pacta (White) of the Permian, partly return to an early fusuline habit of de- positing an axial filling of epitheca. That this is in some way an adjustment to the environment and not merely an atavistic return to a primitive habit is suggested, however, by the fact that the axial filling is definitely localized and assumes a highly distinctive pattern in different Permian species. For example, it is limited to a narrow axial zone that extends to the poles in Schwagerina line- aris, but in 8. crassitectoria is limited to a belt on each side of the tunnel, and in 8. compacta occupies a conical area in each end of the shell. External Form and Internal Anatomy Although it may be said with some accuracy that there is no constant cor- relation between external form and in- ternal anatomy of the fusuline shell, a survey of the group as a whole reveals a few broadly generalized relationships which have significance, but which can- not be used consistently in the taxonomy of the family. Some of the subspherical genera, as well as all the lenticular ones, lack deep septal plications. For example, Staff- ella, Ozawainella, Leella, and Nankinella have almost entirely plane septa. There has been a tendency to interpret this to mean that the high arch of the wall in such forms gave sufficient strength, whereas in slender shells septal plication was a device for supporting the spiral wall. However, exceptions to any such correlation of shell form and septal fold- ing are so numerous that this conclusion seems unwarranted. For example, the highly inflated genus Pseudoschwager- ina has slightly folded septa, but its con- temporary, Par a schwagerina, has very deeply folded septa, even in species like P. kansasensis that are almost spherical. Moreover, subglobular species of Triti- cites, as T. plummeri, have septa as deeply folded as any in the genus and much more so than in its congener, T. moorei, which is thinly fusiform. Of the very slender forms, W edekindellina pos- sessed almost plane septa, whereas some of the early species of Triticites, as T. irregularis and T. ne~braskensis, were similar in shape and had but slightly folded septa. In the late Pennsylvanian and Permian strata, however, the slen- der forms of this subfamily all display deep septal plication. In short, lack of septal folding is a primitive character- istic in this family and deep septal fold- ing is a definite specialization which was achieved slowly in some branches of the family and more rapidly in others. The Verbeekininae and Neoschwag- erininae are mostly subglobular and do not show septal folds, but they attained great architectural strength by another device, namely the development of pend- ant septula which served as I-beams to strengthen the spiral wall. And it may be observed that we find in these large subspherical shells the maximum devel- opment of complexity and strength. All this would seem to imply that if shell strength was of selective value it was not strength against simple crushing stresses that was demanded. The width and number of tunnels do have a relation to the shape of the shell. Forms such as Fusulina cylindrica and Triticites irregularis commonly have a narrow tunnel at the early stage when the shell has the same shape as Fusu- linella, but at the same ontogenetic stage as that at which the shell undergoes its sudden lengthening, the tunnel widens to a corresponding degree. In such species, the angular width of the tunnel may change from 20° to 60°. There is nothing strange about this widening of the tunnel, because the housing capacity 56 PENNSYLVANIAN FUSULINIDAE for sarcode is greatly increased in these forms by the great lateral expansion without a correspondingly great increase in the equatorial diameter of the shell. The tunnel, which is the chief and, wherever the septal pores and keriotheca are filled, the only channel for commun- ication between the chambers, accord- ingly must have an increased size to accommodate such increases in shell space if the same rate of passage is maintained, unless the septal pores re- main open as they do in Fusulina girtyi (Dunbar and Condra) in the last three or four volutions. The last two genera of the Schwager- ininae, which are commonly very slen- der, developed two ways of increasing the avenues of communication between chambers. Parafusulina developed vaulted passageways (cuniculi) between alternate chamberlets, beneath the junc- tion of septal folds. Poly die xodina add- ed to these a series of accessory tunnels produced by resorption of parts of the septa. PREPARATION AND STUDY SECTIONS AND ILLUSTRATIONS Accurately centered and oriented thin sections are the fundamental basis for the interpretation of the fusulines. Au- thors careless of this elementary fact have introduced much confusion into the literature by basing their studies on hap- hazard oblique sections. Furthermore, too many species have been based on but one or two sections and have been de- scribed in general rather than precise terms, with the result that subsequent identifications are uncertain, many syn- onyms have been created, and confusion has crept into the literature. At least two sections, one axial and the other sagittal (equatorial), are re- quired to show the important shell fea- tures, and several of each should be crit- ically studied before a new species is proposed. We strongly recommend that in de- scribing a new species not less than three well oriented axial sections be illustrated at the standard magnification of 10 di- ameters, and that a full set of measure- ments be given for each volution of each of these shells. The last is important because ontogenetic changes in growth are more distinctive than actual size and proportions at maturity. Good illustra- tions are essential because there are many features that do not lend them- selves to measurement or precise de- scription. Such, for example, are the axial profile, the form and spacing of the septal loops, the distribution and massiveness of the epitheca in the form of chomata, axial filling, etc. It is ex- tremely important to make the illustra- tions at a standard magnification be- cause this alone permits comparison of these immensurable features by direct inspection. At least three axial sections should be illustrated because there are individ- ual variations, both actual and apparent, that no single section can represent. The actual variations concern the details of shape, the size of the proloculum and early volutions, the massiveness and dis- tribution of the epitheca, etc. The ap- parent variations result chiefly from the relation of the section to the plane of the septa, as explained on page 43. For example, in a shell having moderately folded septa, if the section happens to fall midway between two septa the volu- tions will appear to be open and free of septal loops and the chomata will appear abnormally small ; but if the section is close to the plane of the septum, septal loops will be abundant and the chomata will appear more massive; or, if the septa do not follow a strictly meridional course, they will cross the slice oblique- ly, producing local variations between the extremes mentioned above. ORIENTATION OF SECTIONS Axial Sections An accurately centered and oriented axial section follows the axis and there- fore intercepts the center of the prolo- culum and the poles. It reveals the length and diameter of the shell and shows its axial profile, not only when adult, but at all stages of growth; it shows the height of each volution, the width of the tunnel, and the massiveness of the chomata ; it also permits a study of the microscopic texture of the wall and septa. Both in the making of sections and in the selection of axial sections for study it is essential to be able to judge the orientation correctly. As one side of a fusiform specimen is ground away, the wall of successive volutions appears on the flat facet in various figures deter- mined by the orientation, as explained in figure 9. If the facet is parallel to the axis these figures are concentric, sub- elliptical, and bilaterally symmetrical [57] 58 PENNSYLVANIAN FUSULINIDAE Fig. 9. — Diagrams to illustrate orientation of sections. A-C, three facets cut on the same specimen; A, facet parallel to axis; B, facet oblique, too deep at right end; G, facet still more oblique and cutting through the axis at the right end. D and E, sections of an elongate shell having a curved axis; D, section in the plane of curvature; E, section at right angles to D and following the line a — b. (fig. 9A) ; but if the facet is oblique, the figures are ovoid and narrower at the end which is closer to the axis (fig. 9B). In the latter instance it is neces- sary to grind more rapidly on the blunter end until the facet becomes bilaterally symmetrical. If this is not done, the one end of the facet will soon intercept the axis and the closed figures will then merge into an oblique spiral (fig. 9C). It is then too late to correct the orienta- tion and get a correct axial section, and a new specimen should be selected for sectioning. If the facet is parallel to the axis the ellipses will enlarge as the cutting pro- ceeds and new volutions appear at the middle, but they will remain bilaterally symmetrical. As the axis is closely ap- proached and the umbilici at the ends of the shell are intercepted, the elliptical -figures will break into a series of offset and opposed hemiellipses as in figures 10 and 11 B, C. This is an infallible criterion of perfect orientation. In actual practice it is common to find that in well oriented sections some, or all, of the elliptical figures remain closed, or they may remain closed at one end. Dunbar and Skinner incorrectly interpreted the breaking of the closed figures into offset hemiellipses as due to the failure of the spiral wall to arch com- pletely down to the axis at the end of the shell. Actually, since it is impossible for the volutions of a coiled shell to overlap progressively beyond its axis, the perfect axial section must ideally display a series of offset sections of whorls half a volution apart, as represented in figure 10. Therefore, when the spiral wall passes unbroken around the end of a volution, we must assume that the axis at that point does not quite coincide with the plane of the section. This is a common experience, even in the best possible sections of fusulines, because the axis is generally not perfectly straight and in any volution may be* slightly above or below the average plane and thus may be missed by the slice. But since even slight obliquity across the axis inevitably transforms the section of the wall into a continuous oblique spiral, we may be sure that a section with symmetrical elliptical sec- tions of the whorls is parallel to the axis, and if at the same time it cuts the proloculum, it is very close to the ideal axis and is satisfactory for shell measurement. In case the axis is bent or arched, as it commonly is in long slender species, the facet should be cut so that the sec- tion will lie in the plane of curvature, as figure 9D. Thus the section is com- SAGITTAL SECTIONS 59 plete to the ends, the dimensions are all correctly shown and the amount of curvature of the axis is evident. But if the section be cut at a high angle to the plane of curvature, it may be made to follow the axis approximately in one end of the shell but will then cut ob- liquely across the other end (as the line a — b in fig. 9D). In this instance the elliptical figures will be asymmetrical, one end being long and the other short and blunt (fig. 9E). Obviously such a section does not represent the true shape or dimensions of the shell, but the longer end will, in any case, approach the cor- rect form more closely. Wherever free specimens are avail- able, it is desirable to orient the section so that it will include one of the last two or three chambers next to the ante- theca, thus giving the maximum dimen- sions and adult characters of the shell. The importance of this is suggested by comparison of the sections represented in figures 11B and 11C, both cut from a single shell. Oblique sections do not represent either the true shape or dimensions of a shell. This fact cannot be too strongly emphasized. Its importance is suggested by figure 11. Here the actual length, thickness, and profile of a shell are shown by the axial section, fig. 11B. An oblique section of the same shell cut along the line u' — u" would appear like the section shown in figure 11D. Since both sections cut the proloculum, they give the correct sagittal dimensions, but the length is greatly foreshortened in the oblique section and the poles appear much blunter and the slopes more con- vex than they should. Tangential Sections Sections of this type are, however, very useful as a supplement to the axial section, especially for the study of the plan and depth of the septal plication. A tangential section is one tangent to the surface and, unless otherwise speci- fied, the term should be applied to a section parallel to the axis and cutting only one or two of the outer whorls; it thus differs from an excentric axial sec- tion only in that the latter cuts deeply Axis Fig. 10. — Ideal axial section of a spheroidal shell to illustrate positions for measur- ing axial dimensions. Lengths of full volutions are b — b', d — d\ f — f, and h — h', respectively; the lengths at y 2 , IV2, 2V2 volutions, etc., are indicated by a — a', c — c', e — e\ etc. The emerg- ence of the axis is at po and po'. P proloculum; 0, center of proloculum. into the inner whorls but misses the proloculum. The tangential section is especially useful in the study of the septal plica- tion, particularly in large species and those in which the septal folding is com- plex. Such sections are indispensable in the study of Schwagerina, Parafusu- lina, and Polydiexodina, and are useful in many other genera. For example, the usual axial section of a species hav- ing rather deep septal folds shows a maze of septal loops of varying height and shape, giving the impression that the septal folds are quite irregular in size and depth (pi. 17, figs. 7, 8), even though the folds are actually very regu- lar and uniform (pi. 17, figs. 9, 10). The tangential section shows them cor- rectly, in plan. Sagittal Sections The sagittal (or equatorial) section is at right angles to the axis and intercepts the center of the proloculum. Its chief use is to show the number of septa and chambers, but it is also the best section for illustrating the rate of equa- 60 PENNSYLVANIAN FUSULINIDAE C D Fig. 11. — Diagrams to illustrate correct shell measurement. These are four ideal sec- tions of a single shell. A, sagittal section; B, perfectly oriented axial section lying in the direction of G — G' in figure A; C, axial section lying along line H — H' of figure A; D, oblique section lying along line U' — U" of figure B and at right angles to that section. torial expansion. The microscopic tex- ture of .the wall and the septa can also be determined from the sagittal section. The sagittal section intercepts the middle of the tunnel and, accordingly, the septa all fall short of reaching the floor of each volution. In making such sections the correct orientation may be judged by watching for this interrup- tion of the septa as the grinding ap- proaches the sagittal plane ; since the tunnel widens progressively it is en- countered first in the outer whorl, and if the section is at right angles to the axis the septa should be interrupted in about the same number of volutions on all sides of the shell as the proloculum is approached. If the interruption ap- pears first on one side, or if it extends deeper into the inner whorls, grinding should be accelerated at the opposite margin until symmetry is attained. If the tunnel is crooked it may be im- possible to cut a section so that it will follow the tunnel in all volutions. In that case, if chomata are present, they may appear Locally in the section. SHELL MEASUREMENT It may seem a very simple thing to measure the length and diameter of the shell, the size of its proloculum, the width of its tunnel, etc. but two ob- servers of the same section may record measurements differing by as much as the difference in size between two volu- tions. The need for a standard way of measuring was recently discussed by Dunbar and Skinner (1937) and is re- peated here. Radius Vector Versus Diameter In our measurements we have record- ed the half length and the radius vector instead of the full length and the di- ameter, the radius vector being the ra- dial distance in the sagittal plane from the center of the proloculum to a point on the surface at the end of a given whorl. Our reasons for this choice are both practical and theoretical. For example, MEASURING LENGTH 61 in reading half lengths under the micro- scope, whether by means of a graduated movable substage or by a calibrated scale in the ocular, we set the zero end of the scale at the center of the proloculum and read the distances to the ends of successive whorls; but if the full length of each were to be measured it would be necessary to count out in one direction, place the zero point at one end of the whorl, and then count across to the op- posite end of the same whorl, a process which would have to be repeated inde- pendently for each volution. In actual practice, the half lengths of all volu- tions in a shell can be read in a fraction of the time required to measure the full lengths, and with much reduced chances of error. Furthermore, this avoids the waste of sections that are incomplete or poorly preserved at one end and do not show the full length ; since fusulines are bilaterally symmetrical animals it is safe to measure the good end and double its value if the full length is required. Also, in case the axis is curved or bent and one end is foreshortened as in figure 9E, the required measurements can be secured from the longer end. Similar advantages are found in mea- suring the radius vector instead of the diameter. The zero point of our scale is set at the center of the proloculum and the distance to the surface of suc- cessive volutions is read directly. But if the full diameter were required the scale would have to be reset for each measure- ment. Furthermore, satisfactory mea- surements can frequently be made from one side of a section even though the opposite side is poorly preserved or in- complete. The chief disadvantages of our system are that (1) in comparing the new mea- surements with those of old descriptions expressed in length and diameter, it is necessary to double our figures, and (2) this introduces a slight systematic dis- crepancy since, due to growth, the ra- dius vector at the end of any volution is slightly more than half the diameter of that volution. However, experience has convinced us that the advantages far outweigh these disadvantages. Measuring the Length or Half- Length It may be assumed that the given measurements of any volution of the shell are its maximum dimensions when the volution is complete. Thus, for ex- ample, the length, or diameter, of the third volution should be measured at the end of that volution. Actually, this ideal can rarely be attained, and more ingenuity is required to measure the ax- ial dimensions of the inner volutions than any other part of the shell. The difficulties may be explained by means of figure 11, which represents four ideal sections of a single shell. In the sagittal section (fig. 11 A) it is easy to see where each volution begins and ends, but since the initial point of coil- ing cannot be seen from the outside of the shell the orientation of the axial sec- tion with respect to the ends of the several volutions is purely fortuitous. Figure 11B represents an axial sec- tion in the position G — G' of the sag- ittal section, falling exactly in the ideal plane so that the upper half of the sec- tion coincides exactly with the ends of the several volutions. But even here a choice must be made as to which side of the section to measure. The assumed relation to the sagittal section makes it clear that measurements on the lower half of this section (i. e., p — p', q — q' ', and r — r') really would indicate the length at %, iy 2 , and 2 J / 2 volutions, respectively. But in practice the orientation of the axial section with respect to the ends of the volution has to be inferred. In figure 11C, the section is represented as lying at 90° to the desired plane (i. e., along the line H — H' of fig. 11A). In this section the shell appears smaller than in the former, for it only shows 2% whorls of the shell. In it the hemi- ellipses on the upper half give the di- mensions of %, 1%, and 2 3 /4 volutions while those of the lower half correspond to %, 1%, and 2*4 volutions. It is therefore impossible to measure the full dimensions of any volution from this section. But obviously if we choose the side which gives the largest figures the results are most nearly correct. 62 PENNSYLVANIAN FUSULINIDAE The section may lie in some inter- mediate position, as k — k f of figure A. In this instance, the smaller half would show the shell at %, 1%, and 2% volu- tions, and the larger half would repre- sent %, 1%, and 2% volutions. In this case we approach closest to the true di- mensions if we ignore the first tiny sec- tion of a volution and call the next one the first volution. If the expansion and elongation of the shell is relatively rapid, the experienced student can safely infer from the size and shape of the first tiny whorl section whether it lies within the first quarter volution; but if the elongation is slow and gradual there is more uncertainty. In the latter case, however, an error of judgment is less serious than in rapidly elongating shells. To summarize, the rule for deciding which side of an axial section to measure is as follows : If the smallest whorl sec- tion is inferred not to lie within the initial % volution, measure the side op- posite to it, i. e., the side which will give the larger dimensions for corresponding whorls; but if the first tiny whorl sec- tion lies within the initial % volution, measure the side in which it occurs, but ignore this apical section and call the next whorl section number one. A further difficulty in measuring the linear dimensions of the inner whorls is that the ends of the volutions are com- monly obscured in a maze of septal loops. The diagram of a perfect axial sec- tion of a spherical fusulinid (fig. 10) represents an important principle that will serve as a guide both for locating the end of a volution and for recogniz- ing the position of the axis when mak- ing a thin section. The axis is repre- sented by the line hoh'. The equatorial plane, being perpendicular to the plane of the axial section, intersects the axial section along the line ZOZ'. The center of the proloculum (P) is indicated at o. Assuming that the growth of the shell stopped exactly at the end of the fourth volution, the length of the shell as seen from the outside is represented on this specimen not by the distance between the poles po-p'o' but by the distance hh' . The diameter of the shell is the distance ZZ' '. Before the last half of volution four had grown, the length of the shell at stage 3% was gg'. At volution three the length was ff' ; at 2y 2 volutions it was ee' • and so on. This illustrates the principle that in axial sections the profiles of the spiral walls on one side of the axis are offset relative to those on the opposite side of the axis. If the section is parallel to the axis but ex- centric, the profiles will be represented by slightly asymmetrical but closed loops resembling those of a tangential section. In sectioning, the change from closed profiles to offset profiles is an in- dication that the axis has been closely approached. In measuring the axial or the half axial length, the location of the polar extremities of some volutions is more obscure than others. A way out of this difficulty is to observe the general trends of growth in the shell at hand and, by using the principle of offset profiles, the probable true position can be interpolated. Measuring the Radius Vector The radius vector may be measured from both sagittal and axial sections. In the former it can be determined pre- cisely since the beginning and end of each volution can be observed. Thus, in figure 12 the correct position for measur- ing the radius vector is along the line OR. This is a slight departure from the practice adopted by Dunbar and Skinner, who measured along the line O'R' which runs through the first cham- ber. The objection to the latter is that the measurement is exaggerated by the abrupt elevation of the spiral as cham- bers 15 and 16 are superposed upon chamber 1. In the early whorls this dis- tortion may be relatively large, though it is of little importance in the outer whorls. In axial sections the difficulties are like those encountered in measuring the length, and the same criterion should be used in deciding which side of the section falls most closely along the de- sired plane at the ends of the several volutions. The radius vector should be measured from the center of the proloculum to the TUNNEL ANGLE 63 tectum of each volution. Wherever epitheca covers the floor of the tunnel it should not be included because it be- longs to the next whorl. Wall Thickness The spiral wall is normally thickest near the middle of the shell, thinning progressively to the poles; also it is thinnest in the early volutions and tends to thicken gradually in successive whorls except that in some genera it declines again in the last. Obviously, therefore, a wide range of thickness might be found, not only from whorl to whorl but from center to ends of a single whorl. We have followed the practice, therefore, of measuring the maximum thickness for each volution, i. e., the thickness at a point about half way be- tween the septa in the equatorial plane. Measurement of the protheca near the septal furrows will, in some species, give an exaggerated thickness. Even so, complications are presented by epithecal deposits such as the cho- mata and axial or chamber filling which locally increase the thickness of the wall. Since these are secondary and somewhat inconstant in thickness, we avoid such local and accessory deposits by measur- ing the thickness under the tunnel. This practice has the double advantage that it avoids secondary thickening and that it localizes the measurements so that dif- ferent observers will measure the same places and get comparable results. Septal Count Counting the chambers in ordinary specimens requires no special skill. By reference to figure 12, it may be seen that the proper position to count from is represented by the line OR which rep- resents the beginning and end of each volution. This position is obtained by running a line from the center of the proloculum through the posterior side of the first chamber of the spiral series (number 1 of figure 12). Thus the first volution contains 14 chambers (frac- tions not stated) and the second 23 chambers. The position OR' has been used by some as marking the beginning Fig. 12. — Sagittal section to illustrate the correct measurement of radius vector and septal count. P, proloculum; 0, center of proloculum; OR, line mark- ing ends of volutions; OR', incorrect position for measuring radius vector and counting septa; 1-14, chambers of the first volution; 15-37, chambers of the second volution. The rise in the spiral wall of chamber 15 is slightly exaggerated to show the error of measuring radius vector along the di- rection OR'. and end of volutions, but the use of this position introduces error in the cham- ber count and an error in measuring the radius vector, as explained on page 62. Although an experienced student can gain some notion of the closeness of septa from an axial section, an actual septal or chamber count is possible only by means of an equatorial or nearly equatorial section. Proloculum Several students have measured the inside dimensions of the proloculum, but since outside dimensions are invariably the ones measured in all later volutions it is proper to measure the outer di- mensions of the proloculum. Tunnel Angle This is the angle subtended at the center of the proloculum by the width of the tunnel in any given volution. <64 PENNSYLVANIAN FUSULINIDAE Since the width of the tunnel commonly increases at an accelerated rate in the outer volutions, the tunnel angle changes from whorl to whorl and no single mea- surement can satisfactorily represent it. The angle can be measured on a re- volving substage, but a goniometer eye- piece such as that supplied by Karl Zeiss is much more efficient. Pig. 13. — Diagram to illustrate the effects of unequal prolocula. The pyramids are exact duplicates except that A has four apical segments not represented in B. Segments 1-5 of B correspond ex- actly with segments 4-8 of A. Allowance for Unequal Prolocula Even though the sections are correctly oriented and the measurements are prop- erly selected, a further obstacle to inter- pretation of the data is frequently en- countered because shells closely alike at maturity may have very unequal pro- locula. Dunbar and Skinner have dis- cussed this difficulty and pointed out that the size of the proloculum varies inversely as more of the early on- togeny is represented. Accordingly, the first volution in a shell having a large proloculum represents a different stage of growth from the first whorl of a shell of the same species having a small proloculum, and should not be compared with the same whorl but with the second or third whorl of the latter shell. The situation is illustrated by fig. 13 which represents in purely idealized form two shells, one of which begins at •an early and the other at a later onto- genetic stage. For the sake of simplic- ity, the actual shape and the coiling are disregarded and each whorl is repre- sented as a section of a pyramid. The differences in these pyramids are obvi- ously in the apical segments, for the adult segments, 6, 7, and 8 of A, are identical with adult segments 3, 4, and 5 of B. However, segment 1 B is not comparable with 1 A but with 4 A. Inspection of tables of measurements, for example that of Fusulina illinois- ensis on page 118, shows little agreement between the dimensions of correspond- ing volutions of two shells having very unequal prolocula (prolocula designated by in table), but if the second or third, and succeeding volutions in the former be compared with first and succeeding volutions of the latter a very close cor- respondence exists. In principle a good case could be made out for tabulating the statistical measurements so that corresponding adult volutions are arranged side by side, but in practice this involves as- sumptions as to the normal adult size, and it appears wiser to tabulate the measurements as we have done and to make the proper allowances by inspec- tion. But it must be remembered that when specimens of a single species have distinctly unequal prolocula, statistical measurements for corresponding whorls will not agree. On the contrary, there will be systematic correspondence if we begin the comparison with post-neanic whorls of equal size. Tabulation of Measurements In the early stages of the present work, we were impressed with the need for fuller and more precise measure- ments of the types of new species. Ac- cordingly, the junior author worked out a compact form of tabulation which would permit direct comparison of each measurable feature in each volution. This device was subsequently adopted by Dunbar and Skinner in their study of the Permian fusulines of Texas, and is used in our specific descriptions. In these tables the specimens are numbered in order from left to right and the volu- tions are numbered from the top down- ward, the proloculum being designated SECTIONING 65 as zero. The features that are readily measured are : (1) length, (2) diameter, (3) wall thickness, (4) tunnel angle, and (5) number of septa (or chambers). SECTIONING The technique used in sectioning fusu- lines will vary with the purpose of the study, the equipment available, the abundance of material, the nature of preservation, and the economy of time and money required. If, for example, the sole aim is a quick age determina- tion in a region where the faunas are known, it may suffice to select a few specimens, grind them down to a pol- ished axial plane, and disregard all the rest of the collection. But if a fauna is to be critically studied and new spe- cies described, or if morphological fea- tures are to be investigated, more elab- orate technique is required. Preliminary Preparation Specimens preserved in marl, clay, or argillaceous limestone usually can be freed by simple washing or sieving. The matrix can be more effectively removed if the sample is first boiled for one to three hours in water to Avhich washing soda has been added. It is a great advantage to have abun- dant free specimens for study because they can be sorted into groups according to form and external appearance before individuals are selected for sectioning; the less common species are not so likely to be overlooked; and a more accurate estimate can be made of the relative abundance of different species in the fauna than is possible if the specimens are embedded in matrix. Even though embedded in solid mat- rix, specimens may in some instances be freed by one of the following meth- ods. (1) Where abundant material is available and the matrix is limestone, some of the specimens may break free if the rock is simply crushed to small pieces. A crusher that works by simple crushing action rather than by abrasion or grinding is necessary for success. This method works best for small and ventricose species, and is applicable only to certain types of stone. (2) The rock may be alternately heated and plunged into cold water until it crumbles into fragments. This method generally yields badly damaged specimens. (3) If the matrix is porous, the sample may be impregnated with molten sodium acetate which is then allowed to cool and crys- tallize. Crystallization causes vigorous rapid expansion of the salt which dis- integrates the matrix and thus frees the specimens. This technique requires im- mersion of the rock in a bath of sodium acetate that has been melted with the addition of about 5 drops of water for 50 cc. of solution and gently heated. Then, after the solution has impregnated the interstices, it is allowed to cool, but repeated melting and freezing is com- monly required. The solution should be kept covered to prevent decomposi- tion or absorption of water if air is moist. Cooling is very slow at room temperature but can be hastened by placing the covered container in a tray of cold water. Though time consuming, the method is surprisingly effective for releasing very delicate shells. 1 Methods 1 and especially 2 usually involve breaking a large percentage of the fusulines, and so are feasible only when material is abundant. Specimens that cannot be freed from a hard matrix by any practical method may be exposed in one of the following ways. (1) Chips of the rock may be spalled off by a glancing blow of the hammer and the new surfaces searched for partially exposed specimens. The search is facilitated if the chips are wet when examined under a low power of the binocular. When a specimen is thus discovered, more than half buried in the matrix, the chip can be broken down with a pair of rock pincers to a small piece enclosing the specimen, and a sec- tion is then made of the specimen with its enclosing matrix. If the fusuline is large and slender, it may be desirable to use the rock saw and cut out a narrow piece enclosing the fossil. This method may be applied, of course, to natural 1 This method was suggested by Mr. K. E. Lohman of the U. S. Geological Survey, who uses it to disinte- grate porous, diatom-bearing cherts. 66 PENNSYLVANIAN FUSULINIDAE exposures on weathered surfaces. (2) Another method, preferred by the jun- ior author, is to saw the f usuline-bearing rock into slices 3-5 mm. thick, etch these surfaces slightly with hydrochloric acid, and stain them with methylene blue or malachite green. The earthy matrix and chamber filling absorbs the stain, con- trasting sharply with the white shell material. These slices are then placed in a shallow tray, barely covered with water, and examined under a binocular to select specimens for development. This works well for small species, but if the shells are large, it results in the loss of a large percentage of shells because they are cut across in such ways that no complete section can be developed. It^commonly happens that subcylindri- cal shells lie more or less nearly parallel, and if care is taken to saw the rock in appropriate directions the wastage is re- duced to a minimum. If the specimens are hollow or the shell material and the matrix weak or friable, it may be necessary to harden them artificially before sectioning. This may be done by boiling them in Can- ada balsam or kollolith of the proper hardness, or by impregnating them with bakelite lacquer and allowing it to dry over night (longer if the specimen is more than 2 cm thick), and then cook- ing for 20-30 minutes at a temperature of 120° to 130° C. Impregnation by bakelite lacquer, in partial vacuum, fol- lowed by pressure when the specimen is submerged in the lacquer, will result in thorough induration. Selecting Specimens for Cutting When free specimens are available, it is desirable to classify them into groups according to form and external appear- ance before sectioning. Each form- group should then be subdivided into three or four parts, one to be used for making axial sections, one for sagittal sections, one to preserve for external features, and another for reserve. Each of these parts should be placed in a small vial and fully labeled with data giving (1) the station number, (2) a Letter designating the form-group rep- resented, and (3) an indication whether the part is to be used for axial or sagit- tal section or preservation. As an arbi- trary scheme, it may be desirable to give the letter A to the most ventricose form in any lot, B to the next, and so on to the most slender form. If enough form- groups are selected so that the individ- uals in each group are closely similar in shape and appearance, it is then pos- sible, after the sections are made, to be sure how each looked before sectioning. This provides the safest possible assur- ance that the axial and sagittal sections attributed to a single species are actu- ally conspecific. In case the specimens are rare, it may be desirable to photograph before sec- tioning those that will be made types. General Procedure After a specimen is selected for sec- tioning, one side (or one end) is ground away to the desired plane of the section. This surface is then mounted on a glass slide and the other side ground away until only a thin slice of the specimen remains. A coverslip is then placed over this slice and the slide is labeled. The choice of abrasive and cementing materials is discussed in the following paragraphs. Labeling As soon as a specimen is removed from its label and attached to a slide, the latter should receive a label that cannot be destroyed during the section- ing operation. This information should be etched on the back side and near one end of the slide with a diamond point or carborundum pencil. For this purpose it will suffice to give the station number of the collection and the group letter that has been assigned to this particular form-group from that collection (for ex- ample, "Sta. 28 (B)' r ). Although a good diamond point is sat- isfactory for writing on glass, equally convenient carborundum pencils and engravers chucks for holding them are SECTIONING 67 now available. Such pencils are avail- able in a size about 3 mm. thick and 25 mm. long, and in fine, medium, and coarse texture. The fine grade is pref- erable for delicate writing on slides. The carborundum pencils can be sharp- ened by rubbing on a silicon carbide whetstone or grinding wheel. It is important to write this prelimi- nary label on the back side of the slide (1) so that it will not be lost if the slide is abraded in the final stages of making the thin section, and (2) so that it will be available for subsequent reference after the final paper labels have been added to the slide. If in the course of time the final paper label should loosen from the slide the data cut into the glass will make it possible to restore the label. Polished Versus Thin Sections Although thin sections have been used almost exclusively in the preparation of reports on the Fusulinidae, some stu- dents have recently urged the general use of polished sections. Advantages of polished sections are : (1) they are much more easily and quickly made; (2) half the specimen is saved so that external as well as inter- nal features of one and the same speci- men are preserved; (3) in case the ma- trix is transparent, such internal fea- tures as septal folds, tunnel, and cho- mata can be seen in three dimensions and their form more readily appreciated than if represented only in a thin slice. Disadvantages are numerous. For ex- ample : ( 1 ) the microscopic wall struc- ture commonly is not visible in a polish- ed surface. Even with the latest types of vertical illuminators and epicondens- ers, the visibility of microstructure is far inferior to that in a thin section il- luminated by transmitted light. (2) It is rarely possible to make an acceptable photograph of even the gross internal features from a polished sur- face. (3) It is difficult to mount polished specimens permanently on glass slides. The usual cementing media will dry and crack and there is danger of loss of the specimen • or, if the mount is covered by a preservative paint to prevent such drying, the free surface of the specimen is obscured and one of the chief advant- ages of the polished section is sacrificed. (4) If the polished surface is cement- ed to a standard microscope slide, as is commonly done, the thickness of the glass prevents the critical use of stand- ard microscope objectives having a numerical aperture above about 0.20, and this limits observation with ordi- nary equipment to an approximate maximum of 50 to 100 diameters. (5) Inasmuch as the internal struct- ure of a shell appears somewhat differ- ent in polished and in thin sections, more than usual experience is required to make allowances for the differences if both kinds of sections are used indis- criminately. Obviously, the choice of polished or thin sections will be influenced by the purpose of any particular study. If the purpose is a quick identification of species in a known fauna for purposes of correlation, polished surfaces will suffice, and the polished specimens may be plac- ed in a capsule or small vial inside a larger one labeled for permanent safe- keeping, instead of being mounted on slides. But for critical study, or the descrip- tion and illustration of species, thin sections are much to be preferred. In cases where the shell substance is light and the internal matrix is dark and clear, polished surfaces may be used to< advantage as a supplement, but should never replace thin sections. Abrasive Powders, Laps, "Wheels, and Saws If the grinding is to be done by hand, the preliminary, rapid cutting may be accomplished by rubbing the specimen upon a file or upon a coarse or medium- textured silicon carbide whetstone which is kept wet during the cutting; or the specimen may be cut down by rubbing it upon a plate glass or plane metal lap covered with a sludge of moistened abrasive powder. The final grinding* and finishing are best done by using a sludge of very fine abrasive powder on a lap. For rapid cutting, coarse abrasives of textures from 120 to 220 may be used, but for the finishing, a grade of 600 to- 68 PENN8YLVANIAN FUSULINIDAE 820 is best. When changing from the coarse to fine abrasive powder great care is required to avoid contamination by the coarse abrasive, which tends to cling to the film of moisture on the specimen. The specimen should be scrubbed with a fine brush under running water and the lap thoroughly cleaned or, better still, a separate lap should be used for the fine abrasive. A single grain of coarse abrasive is likely to score the finished surface and seriously blemish the sec- tion. In order to avoid contamination, it is well to keep the working supply of each grade of abrasive in a can with a per- forated top like a pepper box from which it can be sifted upon the lap as needed. If mechanical grinding laps are avail- able, each lap should be used for a single grade of abrasive, and extreme care must be exercised to avoid contamina- tion of each by a coarser abrasive. A soft metal lap once contaminated may have to be resurfaced before it can be safely used. Accordingly, the laps should not be left uncovered when not in use, and should be protected from strong drafts of air. Coarse abrasive may be carried to the finer laps under the fingernails of the operator, or clinging to crevices in the specimen, if great care is not ob- served. If only one mechanical lap is available, the finishing should be done on a piece of plate glass with fine abrasive. Silicon carbide or aluminum oxide wheels are now available for grinding. Such wheels should have a resinoid bond, such as bakelite, and should be porous enough to permit water to lubri- cate the specimen and prevent gumming of the wheel by waste from the specimen and from the adhesive with which it is attached to the slide. Furthermore, the texture should not be coarser than 220. Cementing Materials After the desired surface is finished, it is fastened to a glass slide so the speci- men may be ground away to a thin slice. For this adhesive, Canada balsam is most widely used. It is a resin yielded by the white fir tree and is marketed in either a liquid or a solid form, the liquid form being a solution of balsam in xy- lene. If the liquid balsam is used, a little of it is placed on the glass slide and heated over an alcohol lamp until the solvent is evaporated so that the balsam will be hard when cooled. The specimen is im- bedded in the hot balsam (surfaced side down) and pressed firmly against the slide so that a very thin film of the ad- hesive remains between the specimen and the slide. The use of hard balsam has some ad- vantages. A small piece is placed on the slide and heated until it becomes fluid, and then the specimen is imbedded as described above. Liquid balsam may be hardened before using by heating a quantity of it slowly in a clean pan over a sand bath. Since the solvent (xylene) is highly inflammable, it is important to insure adequate ventilation about the bath while heating. As the volatile solvent is driven off, the balsam will become thicker and thicker and finally will harden at room temperature. It must not be cooked too long or it will become too brittle to hold specimens. During the cooking, a drop should be removed at occasional intervals and placed on a glass slide where it will spread and cool; then it may be placed under a binocular and examined by pressing a needle point into it. If the balsam yields easily without fracture, it needs further cooking, but if pieces spall off about the needle point, it is too brittle. This can be overcome by stir- ring in a small quantity of uncooked bal- sam before cooling. "When properly cooked for future use, the balsam should be hard and tough but not brittle when it is cold. When used to mount a specimen, a small bit of the balsam is placed on the glass slide and heated until it becomes fluid and the specimen is placed in the desired position. The final cooking to just the right consistency is then quickly accomplished. If the balsam is left too soft it will gum the grinding medium and will yield under the pressure of grinding and al- low the section to crack and spread; if over-cooked it will crumble when the section becomes thin, and the specimen will break away and be lost. Since the SECTIONING 69 correct amount of cooking can only be determined when the balsam is cool, it is good practice to sample it at intervals by removing a small quantity from the slide on the point of a needle, where it will quickly cool to form a tiny bead. It can be tested for brittleness by crush- ing between the thumbnail and the fore- finger. If it yields plastically it is too soft; if it crushes easily into powder it is too brittle ; but if it is both hard and tough it is just right. For the beginner the proper hardening of the balsam is the most important and most difficult step in the making of a thin section, but with experience satisfactory results can be had quickly and easily. After the specimen has been fastened to the slide and while the section is still thick, warnings commonly appear if the balsam is not properly cooked, and are easily detected when the section is being examined under the binocular. If the surface of the balsam picks up abrasive and becomes clouded, and if it shows stretching or flow at the margins, it is too soft. Grinding should then be halt- ed, the abrasive-impregnated surface film removed with a bit of cleansing tis- sue moistened in xylene, and the balsam reheated. But if radial cracks appear in the balsam, or its margins show evi- dence of crumbling away, it is too brit- tle. A new slide with fresh balsam should be prepared, the old slide heated, and the specimen floated to the new slide for remounting. By heeding these small warning signs, the experienced operator seldom loses a section. In mounting specimens for grinding, it is necessary to press them into place on the slide rather promptly at the moment the balsam is correctly cooked, and before it has cooled enough to inter- fere with close contact of the specimen and the slide. For this, it is convenient to use an electric hot plate with con- trolled temperature, but such expensive equipment is not necessary. If a hot plate is not available, it is well to lay the slide on a blotting paper, or some other poor conductor of heat, while pressing the specimen into place. For cementing specimens to glass slides kollolith has some advantages over balsam. It has a refractive index of 1.5354, according to the manufacturers, has somewhat greater strength than bal- sam as a cement, and is less affected by time and temperature when melted. It is supplied as a solid in foil tubes and is used just as hardened balsam. Bakelite is a poor substitute as a mounting medium because of its red color, which obscures detail and causes difficulty in photographing. In mounting specimens care must be exercised on four accounts. (1) The balsam must be kept clean and free from dust, abrasive, or lint, which may not only degrade the appearance but also interfere with the study and photo- graphy of the finished section. (2) The finished surface of the specimen must be pressed into close and even contact with the slide. If the film of balsam under the specimen is too thick, it will form a weak bond and the slide may de- velop a mosaic of minute fractures or may be lost during the final grinding. If the balsam is not uniform in thickness it will cause one side of the section to be ground thinner than the other, com- monly resulting in some loss of the thin- ner margin. (3) If the specimen is large, the slide should be evenly supported while it is being pressed into contact; otherwise the slide may be arched slight- ly and this will cause strains in the bal- sam after it is cool and after the pres- sure is released. (4) Gas bubbles be- tween the specimen and the slide must be avoided. Bubbles may form either (a) because the balsam is heated too fast and starts to boil, or (b) because the specimen is moist and the water, having a lower boiling point than balsam, bursts into steam when brought into contact with the hot balsam. It is quite impos- sible to mount a moist specimen prop- erly but if the specimen is thoroughly dry (warming over a radiator or hot plate is good insurance) and if the bal- sam is heated slowly, bubbles can be completely avoided. If some do appear, however, it is necessary to remove them from under the specimen before cutting it thin. This may be accomplished by pressing the specimen firmly down at one edge first and thus forcing the ex- cess balsam to flow out in one direction, carrying the bubbles with it. Or, the slide may be tilted while the balsam is still hot, and the specimen floated into a 70 PENNSYLVANIAN FUSULINIDAE new position free of bubbles. If it still cannot be freed of bubbles, it should be removed and remounted on a new slide. It is futile to attempt to cut a section thin if it has a bubble beneath it. The greatest care is required as the section approaches the desired thinness. A single grain of coarse abrasive or a minute fragment of loosened matrix may then plow a furrow across the section or rip it from the slide and shatter it to bits. Excessive pressure at this stage may cause the balsam to yield unless it is perfectly cooked. Furthermore, a momentary vacuum, produced as the slide is lifted from the wet lap, may loosen the section and allow it to be crushed. It is wise to use plenty of moist abrasive and to press lightly as the grinding approaches completion; a few flakes of soap added to the abrasive will serve as a lubricant, prevent gum- ming of the lap, and reduce the danger of suction pulling the section from its glass slide. Special difficulties are offered by spec- imens embedded in sandstone or sandy limestone in which sand grains insuffi- ciently secured by the matrix occasion- ally break free and are dragged across the slide. The experienced preparator depends largely on the sense of feel and hearing to detect such a loose grain, which causes a "gritting" sensation; and he ceases grinding immediately and thoroughly cleans both specimen and lap and starts again with fresh abrasive. With material of this sort two devices may be used to reduce the difficulty with loose sand grains. The first is to im- pregnate the first-finished surface with bakelite (as described on page 66) before cementing it to the slide. The second, best applied to large specimens, is to etch the first-finished surface slight- ly in dilute HC1 until the surface of the shell is reduced by 20 to 50 microns be- low the surrounding sandy matrix ; then, in the final grinding, the specimen will reach acceptable thinness while the ma- trix is still thick enough to hold its sand grains. The surface to be attached to a glass slide must, of course, be perfectly plane and free of beveled facets or abrasion marks; but it should not be highly pol- ished since it will then more easily break away from the slide during the final grinding. Covering the Section When the section is ground to the de- sired thinness it should be cleaned and dried. Then its surface should be clean- ed by rubbing quickly and lightly with a bit of cleansing tissue, moistened with xylene, in order to remove the film of abrasive that is certain to be embedded in the surface of the surrounding bal- sam. If this is not done before the coverslip is added the abrasive will spread through the balsam, produce a clouded or dirty-appearing mount, and more or less obscure the section. Care must be taken not to rub the section un- necessarily or to use too much xylene, because it is an active solvent of the bal- sam and may loosen the section from the slide. A cheap and convenient cleansing tissue is any of the cheap paper nap- kins that do not include a filler. Selection of suitable coverslips is im- portant. They should be of standard, No. 1 thickness (not more than 0.18 mm), because standard, dry objectives of moderate to high numerical aperture are corrected for covers 0.17 to 0.18 mm thick. Large, circular coverslips are to be preferred for the sake of permanence. If exposed to the air, balsam tends to lose its volatile solvents and in time be- comes hard and brittle. The coverslip largely protects it, but there is some loss around the edges unless it be sealed with a protective paint, such as gold size enamel. If, after some years, the balsam becomes too hard, it loses its adhesive quality and the coverslip, as well as the section, is likely to loosen and drop off, possibly carrying the section with it. Types and sections that are to be per- manently preserved should therefore be covered with care. A circular cover ex- poses the minimum drying margin per unit area and is therefore preferable to a square or rectangular one. A circular cover glass 20 mm across exposes exactly twice the circumference of one 10 mm in diameter, but it covers four times the area, and with proportional deterioration due to drying from the margins, should SECTIONING 71 last more than twice as long. The stand- ard circular coverglass, 22 mm across, is a convenient size for use on the stand- ard microscope slide, and it commonly leaves enough space around the margin to hold a ring of preservative paint. The coverslip may be mounted with pre-hardened balsam that will be firm as soon as cool, or it may be mounted with cold fluid balsam. The senior au- thor prefers the first method because the slide can be cleaned and labeled and put away at once. For this pur- pose, the balsam should be cooked so that it will be tough and just stiff enough to hold the coverslip firmly when cool. Af- ter the section is finished and cleaned, a small quantity of the pre-cooked balsam is placed upon it and a warmed coverslip is placed above the balsam. The whole is then gently heated over an alcohol lamp or a hot plate until the balsam softens and the slide settles down upon the specimen. Gentle pressure upon the cover with the point of a flexible needle will help to squeeze out the excess of balsam and seat the cover firmly in contact with the fossil, but since the bal- sam under the specimen will have been softened by the heat, care is required not to press too quickly or while the bal- sam is viscous, lest the section be shat- tered and spread apart. The junior author prefers to mount the coverslip on cold soft balsam. A bit of cold balsam is placed on the fin- ished section and a small square of blot- ting paper is laid over the slip as it is gently pressed down into position with the aid of a lead pencil rubber. The blotter will pick up the excess balsam and is removed at once. If the excess balsam is not thus removed and is al- lowed to dry about the edge of the cover- slip, surface tension will cause part of it to creep back under the cover, lifting it from the specimen ; at the same time, the fresh balsam will dissolve the hard bal- sam under the specimen and allow it to float from its position. After covering, the slide should be dried for a day or two in a warm place but at a tempera- ture not over 40°-45°C. When suffi- ciently dried, the slide should be care- fully cleaned and its final label added. Ringing the Coverslip Slides that are to be kept more than a few years should have the edges of the coverslips sealed by some protective lac- quer such as gold size enamel. This will inhibit drying of the balsam and prevent the loss of the coverslip and the section. This is best applied with a small, round, artist's brush of size 1 or 2. The most convenient device for ring- ing circular cover glasses is a small turn- table manufactured by Leitz and by Baker. The slide and its cover are cen- tered, with the concentric circles on the surface of the turntable as a guide; the slide is fastened in place with spring clips ; the turntable is given a spin ; and the lacquer is applied from the point of the brush as the specimen turns. Transferring or Repairing Sections Occasionally a glass slide gets broken without damage to the specimen itself; and it is then desirable to transfer the thin slice of fossil to a new slide. As a first step, the cover glass should be soak- ed in xylene until the balsam is dissolved and the cover and specimen are loosened. The latter may then be lifted by touch- ing it with the tip of a camel's hair brush moistened in xylene, and remount- ed in balsam on a new slide. Not uncommonly a specimen is divid- ed into two or more segments by frac- tures, and during the mounting or fin- ishing these may float apart in the hot balsam. If this happens after the sec- tion is thin, it is very difficult to crowd the pieces back together while they are floating in balsam. They may be re- paired, however, by the following tech- nique. (1) Dissolve the balsam away with xylene; (2) coat the center of a clean slide with a thin layer of dry gum tragacanth ; (3) transfer the pieces of the fossil one at a time with the tip of a camel's hair brush, as described above, and assemble them (dry) on the surface of the gum; (4) after the pieces are in place, touch each with the tip of a brush moistened with water to make the gum adhesive; (5) after allowing the pieces to dry in contact with the gum traga- canth, cover with cold liquid balsam and 72 PENNSYLVANIAN FUSULINIDAE add coverslip as directed above. The gum is not soluble in xylene and will keep the pieces from drifting apart af- ter they are covered by balsam. Clear Versus Frosted Slides It is sometimes recommended that bet- ter adherence of specimens to micro- scope slides can be obtained by grinding a fine-textured frosting on the top side of the glass before the specimen is mounted. This is said to produce a much firmer union between the slide and specimen and to prevent occasional losses of nearly completed sections. It is further claimed that the cement will eliminate the optical effects of the frost- ed surface. The first claim is obviously true, though a skilled preparator will find the cure more expensive than the disease. The second claim is definitely an error. As a result of frosting, three factors combine to produce a mottled appearance of the illumination that may seriously degrade the image at medium and high magnifications, especially for photomicrography. First, the cement may differ slightly in refractive index from that of the glass and fail to elimin- ate refractions. Second, many of the minute fractures are not penetrated by the cement. And third, microscopic areas of severe strain are associated with many of the incipient and visible frac- tures in the frosted zone and can pro- duce optical disturbance in critical work. Staining Methods The use of selective stains in the study of fusuline shell structures was first, em- ployed by the junior author and was dis- cussed at some length in the Journal of Paleontology (vol. 5, pp. 355-364, 1931). The continued use of stains has resulted in the following discussion on this topic. The staining methods used on some of the specimens figured in this report are not essentially different from those de- scribed in the earlier paper, but mention may be made of certain improvements and additions. In 1931 the use of methylene blue was not mentioned because no convenient fix- ing method had been discovered. Since that time it has been used successfully without any effort at fixation beyond the natural, mordanting properties of the object itself, because complete fixity in water is not very important in paleonto- logical work. Methylene blue is easy to apply and is highly selective wherever clean sur- faces are exposed. A mixture of grain alcohol and water is probably the most simple and efficacious solvent for the dye. The proportion of alcohol should amount to 10-30 per cent, and the pro- portion of the dye will vary greatly ac- cording to the requirements of the par- ticular specimen or type of work. For equal effects, thin sections ordinarily re- quire a heavier staining than polished faces, or, stated in another way, a given density of stain should appear about twice as great by lighting from above as it appears by transmitted light. The length of time the specimen is immersed in the staining bath will also be deter- mined by the particular requirements of each case and the susceptibility of the specimen to staining, but deep staining effects are often obtainable in easily dyed specimens almost instantly when strong dye solutions are used. In gen- eral, however, a clean-working stain ex- hibits its most sensitive and delicate selectivity when applied in dilute solu- tions for a great length of time. Methy- lene blue is clean working, and the solu- tion apparently requires no preservative when standing for long periods of use or in stock solutions. The principal change in regard to the application of malachite green is that for the most critical staining effects xylene is now used as a solvent. Holmes' recommendation to use xylene as a sol- vent for kaolinitic minerals was dis- puted 2 because several trials with xylene failed to bring success. The failure was probably caused by a too complete dry- ing of the specimens or failure to treat them for a sufficient length of time. The specimens apparently should not be dehydrated beyond normal drying at ordinary room atmosphere. In using xylene as a solvent when staining polished sections or specimens having one side planed in preparation 2 Henbest, L. G., op. cit. : p. 360. SECTIONING 73 for thin sectioning, the specimens are placed in as small a vial as possible and are covered with xylene and a small amount of powdered malachite green. The vial may then be stoppered and vigorously shaken to suspend tempor- arily the particles of dye in the liquid. The powder should then be allowed to settle over and between the specimens and remain without further disturbance. For rapid staining, the vial may be plac- ed above, but not in direct contact with a radiator for keeping it warm. Good staining effects may thereby be attained in one to three days. At ordinary tem- peratures this staining bath requires one to four weeks for deep staining. For critical work, however, a longer staining period is most likely to promote the most delicate and detailed coloring. After the stained face of a specimen is cemented to the slide and the section ground to the required thinness, it is sometimes worth while to stain the ex- posed face of the section by methylene blue or by malachite green dissolved in water alone. Alcohol must be avoided in staining completed thin sections be- cause of its degrading effect on Canada balsam and perhaps also on other resin- ous cements. The face of the section should be clean before staining. After staining, the surface should be cleared by gently wiping two or three times with very fine finishing abrasive and water under the finger tip. The original procedure recommended for using alizarine red (op. eit., p. 361) was to dissolve this dye in an aqueous solution of potassium hydroxide (KOH) or sodium hydroxide (NaOH). Diluted ammonium hydroxide (NH 4 OH) is now used, but no set formula is determined. About 1 part concentrated NH 4 OH added to 5-10 parts of water works very well as a solvent. Enough alizarine red is added to make a very dark purple solution and the specimens are boiled in this solution for 5 to 15 minutes. The specimens may then be washed for a few minutes in flowing water and the staining process is completed. This dye is especially recommended for emphasiz- ing apertures, pores, sutures, or other external structures of fossils which are filled with even a slightly earthy matrix. It will not work if the matrix is pure calcite. This staining method is more useful than any other we have tried for revealing hidden structures in external or weathered surfaces of fossils. It does not unselectively cover the entire weathered surface with heavy stain as do such stains as methylene blue and malachite green. In fossils that were embedded in a clayey matrix alizarine red selects pores, sutures, or other struc- tures that retain considerable amounts of earthy material, and deposits ' ' lakes ' ' or masses of dye on these areas. The advantages of using ammonia as a solvent are the greater ease with which it can be washed out of the pores of a specimen when staining is finished and the fact that any remaining ammonia will evaporate, thus leaving no residue of caustic alkali in the specimen. Heeger's method (op. cit., p. 362), which consists simply of acidifying a solution of potassium ferricyanide with hydrochloric acid and applying the re- sulting solution to a calcareous object, either with a medicine dropper or by im- mersion of the specimen, remains a very convenient dye for routine laboratory work. An application of the solution to an average unfinished fusulinid sec- tion will in less than a minute reveal internal structures that may have been obscure and kept the preparator in doubt as to location and orientation of the section. The "stain" forms a lake of dye which can be removed by rubbing the area but once with a finger. The only change of technique from that pre- viously published is that less care is needed in the proportions of the ingredi- ents than was originally supposed. A concentrated solution of the potassium ferricyanide diluted with an equal part of water and acidified barely enough to effervesce slowly on calcite will yield a very contrasty lake of dye if the matrix is not pure calcite. So far as known, this method is applicable only to calcare- ous fossils. Ethyl alcohol in a bath composed of soluble stains speeds the diffusion of the dye into fine pores and openings in the specimen. When using: selective stains as an aid 74 PENNSYLVANIAN FUSULINIDAE in resolving structures or textures for photographic purposes, it is highly im- portant to know the light absorption properties of the dye. Methylene blue has a maximum absorption range (with- in the visible spectrum) between 590 and 690 millimicrons, and malachite green a range between 570 and 640 millimi- crons. Accordingly, for maximum con- trast, an area stained by malachite green would photograph as black if illumi- nated only by orange-colored light, and areas stained by methylene blue would photograph black if illuminated by yel- low to medium red light. For obtaining photographs showing delicate gradations and maximum details of structure, a band of the spectrum lying partly in the zone of transmission and partly in the zone of absorption should be selected. SYSTEMATIC EEVIEW OF THE GENERA Four subfamilies and 55 genera of fusulines have been proposed. Various schemes of grouping and classifying these genera have been advanced by Staff and Wedekind (1910), Deprat (1913-15), Ozawa (1925), Dunbar and Condra (1927), Dunbar and Henbest (1930), Yabe (1933), Doutkevitch (1934), Dunbar and Skinner (1937), and others. The following arrangement seems to us to represent the most serv- iceable compromise of these many pro- posals. Our chief purpose here is to give a brief synopsis of the valid genera and critical notes on those of doubtful or negative validity. Order Foraminifera D 'Orbigny, 1826 Family Fusulinidae Moller, 1878 Foraminifera of medium to relatively large size; test fusiform, globular or subcylindrical (rarely nautiliform or discoidal or irregular) ; planispirally coiled and completely involute (except for terminal and aberrant genera such as Codonofusiella and Nipponitella), the axis commonly being the greatest dia- meter; surface divided by meridional furrows into numerous melon-like lobes; volutions subdivided internally into short meridional chambers by repeated inflections of the outer spiral wall to form septa; septa plane or folded; wall calcareous, very finely perforate, com- monly having a complex structure. Range, basal Pennsylvanian (possibly late Mississippian) to late Permian. This family includes the largest and most complexly organized Paleozoic Foraminifera, their shells ranging in length between 0.5 and 35.0 mm; very few are of microscopic dimensions and a few are relative giants, the average size, however, being that of grains of wheat or oats, which they commonly re- semble. Subfamily Fusulininae Rhumbler, 1895 (emend. Dunbar and Henbest, 1930) Fusulines of relatively small to me- dium size; spiral wall consisting of a thin protheca (commonly 10-15 and rarely as much as 20 microns thick) which in most genera is covered, both inside and out, by epitheca ; the pores in the mural wall are extremely fine capil- lary tubules, commonly invisible except where especially preserved or artificially colored; the septa are plane in small primitive genera (such as Staffella) but more or less folded in all the elongate and fusiform genera; a median tunnel is present, due to resorption of the septa along the middle of the shell, and cho- mata are present as ridges of secondary shell deposit alongside the tunnel ; sep- tal pores are present but there is no other form of aperture. Dimorphism is not uncommon and the microspheric shells possess an endothy- roid juvenarium, commonly coiled askew to the axis of the adult shell. So far as known, the microspheric and megalo- spheric generations differ little in size or external appearance. The more conservative genera, notably Staffella, are especially characteristic of, and largely confined to, the lower and middle Pennsylvanian (pre-Canyon — pre-Missourian) formations, but range from possibly late Mississippian to late Permian horizons. Genus Nummulostegina Schubert, 1907 Nummulostegina Schubert, Verh. k. k. geol. Reichsanstalt, Wien, vol. 5, p. 212, 1907. — Jahrb. k. k. geol. Reichsanstalt, vol. 58, p. 377, 1908. Genotype (designated by Cushman, 1928), Nummulostegina velebit ana Schu- bert. Small, nautiliform shells with the axis much shorter than equatorial diameter and the periphery rounded. [75] 76 PENNSYLVANIAN FUSULINIDAE The shell anatomy of the type species has not been critically studied or ade- quately described, and until this is done Nummulostegina cannot be referred to the Fusulinidae with certainty. Judg- ing solely by the external features il- lustrated by Schubert, it differs from Staff ella chiefly in having a shorter axis, being nautiliform instead of spheroidal. Possible synonyms are Fusulinella (part) of Staff, Deprat, and Colani; Staff ella (part) of authors; Orobias (part) of Galloway. Eange, ' ' Schwagerina dolomite " (presumably Sakmarian series) of Austria. This is the horizon of the type species, but shells of similar shape, pre- sumed to be congeneric, are common also in the Moscovian horizons of the U. S. S. R. and the Orient. Genus Staffella Ozawa, 1925 Staffella Ozawa, Tokyo Imp. Univ., Jour. Coll. Sci., vol. 45, art. 4, p. 24, and art. 6, p. 14, 1925 ("Fusulina sphaerica Moller" given as genotype); in Cush- man, Foraminifera, etc., p. 131, 1928 (gives Fusulina sphaerica Abich as "genoholotype"). — Galloway, Manual of Foraminifera, p. 397, 1933. — Dunbar, in Cushman, Foraminifera, etc., p. 131, 1933. — Thompson, Jour. Pal., vol. 9, p. 113, 1935. — Dunbar and Skinner, Texas Univ. Bull. 3701, p. 597, 1937 (also see footnote 13, p. 597). Fusulina (part) Abich, Acad. Imp. Sci., St. Petersbourg Mem., ser. 6, vol. 7, pp. 439 and 528, pi. 3, figs, 13 a, b, c, 1859. Fusulinella (part) Moller, Acad. Imp. Sci., St. Petersbourg Mem., ser. 7, vol. 25, no. 9, p. 114, 1878.— Staff, Neues Jahrb., Beilage-Band 27, p. 486, 1909.— Deprat, Mem. Serv. Geol. Indochine, vol. 11, fasc. 1, p. 38, 1913.— Colani, Mem. Serv. Geol. Indochine, vol. 11, fasc. 1, p. 131, 1924. 1 Ozawa cited as genotype "Fusulina sphaerica Moller". Dunbar called his attention to the fact that F. sphaerica was first described by Abich and not Moller, whereupon he replied under date of Jan. 16, 1929, "When I estab- lished the new genus Staffella, I selected at random a spheroidal species in the paper of Moller." The type figured by Abich was very poorly illustrated and may not be a foraminifer ; Thompson felt so certain that it is at least distinct from the form described under this name by Moller that he renamed the latter 8. mollerana. Whatever the nature of the original Fusulina sphaerica Abich, it is clear, both from Ozawa's original diagnosis and from his later specific declaration, that he was not acquainted with Abich's form and did not base his genus upon it. Instead, it is the shell illustrated by Moller in 1878 that served as the type of Staffella. Genotype, by original designation, Fusulina sphaerica Moller, 1878 1 (non Abich, 1859) = S. mollerana Thompson. Shell small, spherical, umbilici present in some species, chambers commonly numerous, septa plane, tunnel narrow, chomata massive and broad, volutions bi- laterally symmetrical ; spirotheca com- posed of tectum, diaphanotheca, and tec- tor ium. Range, late Mississippian (?) to late Permian. This genus may be a synonym of Nummulostegina Schubert. Genus Pisolina Lee, 1933 Pisolina Lee, Nat. Research Inst. Geology (Shanghai) Mem. no. 14, p. 19, 1933. — Dunbar and Skinner, Univ. of Texas Bull. 3701, p. 561, 1937. Genotype, by original designation, Pi- solina excessa Lee. This genus is not convincingly estab- lished, being based on a few sections of an inadequately described species. The genotype is spherical, about 4 mm in diameter, and has 7 or 8 volutions. Superficially it resembles Verbeekina but it lacks basal foramina and para- chomata and, on the contrary, has a me- dian tunnel and well-developed chomata. The wall is thin and consists of "tec- tum and ill-defined keriotheca, of which the alveolar structure is by no means clear." The proloculum is very large for a shell of this size. Range, Lower Permian of the Yangtze Gorge. From the meager description it ap- pears probable that this is a direct de- scendant of Staffella, differing from the latter only in a simplification of the wall through the loss of tectoria. Genus Ozawainella Thompson, 1935 Ozawainella Thompson, Jour. Paleontology, vol. 9, p. 114, 1935. — Dunbar and Skin- ner, Univ. of Texas Bull. 3701, p. 599, 1937. Ozaivaina Lee, Paleontologia Sinica ser. B, vol. 4, fasc. 1, p. 13, 1927. [Lee proposed the name Ozaivaina for lenticular fusulinids related to Staff- ella, if need arose in the future to sepa- rate the lenticular from the spherical forms. He did not designate a genotype. SYSTEMATIC REVIEW OF THE GENERA 77 Galloway (1933, p. 396) designated Nummulina antiquior Rouillier and Vasinsky as genotype of Ozawalna Lee and thereby placed the genus in abso- lute synonymy with Orobias, a, prior name with N. antiquior previously des- ignated as genotype.] Fusulinella (part) of Deprat and Colani. Staffella (part) of Ozawa, Lee, and Lee and Chen. Orobias of Galloway and Harlton, and of Galloway (not Eichwald). Genotype, by original designation, Fusulinella angulata Colani. Shell small, lenticular, with short axis and more or less sharply angular peri- phery. Spiral wall composed of thin tectum, and diaphanotheca covered by epitheca ; septa plane. Range, Pennsylvanian and Permian of North America and Eurasia. Genus Nankinella Lee, 1933 Nankinella Lee, Nat. Research Inst. Geology (Shanghai) Mem. no. 14, p. 14, 1933. Nanking ella Dunbar and Skinner, Univ. of Texas Bull. 3701, p. 560, 1937. (Spelling a typographical error for Nankinella.) Genotype, by original designation, Staffella discoides Lee. Very large, ventricosely lenticular with subacute to rounded periphery. Volutions and chambers numerous, closely coiled. Spiral wall thin, compos- ed of tectum and finely porous dia- phanotheca. Tectorium thin or absent. Chomata small but distinctly developed. Septa non-plicated. Tunnel narrow. Dimorphism present. Juvenarium of microspheric generation endothyroid. Range, Lower Permian of the Orient. Genus Leella Dunbar and Skinner, 1937 Leella Dunbar and Skinner, Texas Univ. Bull. 3701, p. 603, 1937. Genotype, by original designation, Leella bellula Dunbar and Skinner. Shells very small ; early volutions pre- cisely like Staffella but later ones elon- gating so that the adult shell has a thick- ly fusiform shape. Range, Upper Permian of Texas. Genus Fusulinella Moller, 1877 Fusulinella Moller, Neues Jahrb., 1877, p. 144 (preliminary introduction of genus) ; (part) Mem. Acad. Imp. Sci. St. Peters- bourg (7), vol. 25, no. 9, p. 101, 1878 (genus and species formally introduced and fully described). — Douville, Acad. Sci. Paris, Comptes Rendus, p. 258, 1906. — Ozawa, Tokyo Imp. Univ., Jour. Coll. Sci. vol. 45, art. 4, pp. 7 and 24, 1925 — Dunbar and Henbest, Am. Jour. Sci. (5), vol. 20, p. 357, 1930.— Gorsky, Atlas of Leading Forms of Fossil Faunas of U. S. S. R., vol. V, p. 36, 1939. Neo fusulinella (of authors. Not Neofusu- linella Deprat s. s., which may be a syno- nym of Schwagerina). — (part) Deprat, Mem. Serv. Geol. Indochine, vol. 2, fasc. 1, pp. 40-44, 1913 (not N. lantenoisi Deprat, the monotypical genotype of Neo fusulinella). — (part) Colani, Ibid., vol. 11, fasc. 1, pp. 101 and 144, 1924.— Lee, Paleontologia Sinica (Ser. B), vol. 4, fasc. 1, pp. 13 and 16, 1927.— Lee and Chen, Nat. Research Inst. Geology (Shanghai) Mem. no. 9, p. 118, 1930. Genotype (monotypical), Fusulinella bocki Moller. Shells small, fusiform; spiral wall thin, composed of tectum, diaphano- theca, and tectoria, but the tectum may be only locally recognizable. The epi- theca (tectoria) is commonly thicker than the diaphanotheca. Spiral wall very finely perforate, the pores being tub- ular and commonly invisible except when stained. Septa plane or only gent- ly folded toward the end (in advanced species the folding becomes stronger and rather deep in the last one or two whorls). The tunnel is narrow and the chomata are massive and broad at all stages of growth (except in the juvenari- um of microspheric shells). Dimorph- ism occurs, but microspheric shells are rare. There is little difference in size and external appearance between mega- lospheric and microspheric shells but the latter possess an endothyroid juvenari- um coiled askew to the axis of later whorls. Range, most common in, and charac- teristic of, the Lower Pennsylvanian, possibly ranging up into the Permian in the Pacific realm. Genus Eoschubertella Thompson, 1937 Eoschubertella Thompson, Jour. Paleontol- ogy, vol. 11, p. 123, 1937. Schubert ella Lee and Chen, Nat. Research Inst. Geology (Shanghai) no. 9, p. 109, 1930. Schubert ella (part) of authors, not Staff and Wedekind. 78 PENNSYLVANIAN FUSULINIDAE Genotype, by original designation, Schubertella lata Lee and Chen. Minute, thickly fusiform shells pre- sumed to differ from Schubertella chiefly in wall structure, the latter genus hav- ing a wall of two layers, without tec- toria, whereas Eo schubertella has a very thin wall composed largely of tectoria coating a very thin diaphanotheca and tectum. This genus was separated from Schu- bertella by Thompson, chiefly on the basis of Lee's description of the wall in species from the Huanglung limestone. These are of early Pennsylvanian (Mos- covian) age, whereas the types of Schu- bertella are from the early Permian (Sakmarian). Unfortunately, Lee's material was not well preserved and his description and illustrations leave much to be desired. The genotype species was based on microspheric shells, but associated spe- cies, believed to be congeneric, show both megalospheric and microspheric shells to occur. Lee believed the very thin wall to consist of tectum and tec- toria, but Thompson believes a thin dia- phanotheca also to be present. Until Oriental material can be critically re- studied, some uncertainty must exist whether Eo schubertella is distinct from Schubertella. If the wall consists of tectum and tec- toria only, as Lee inferred, then Eoschu- bertella differs from Fusiella chiefly in being more loosely coiled and less slender. Range, Pennsylvanian system, North America and Eurasia. Genus Schubertella Staff and Wedekind, 1910 Schubertella Staff and Wedekind, Geol. Inst. Bull. Upsala Univ., vol. 10, p. 121, 1910. — Thompson, Jour. Paleontology, vol. 11, pp. 118-123, 1937. ? Depratella Ozawa, Cushman Lab. Foram. Research Contr., vol. 4, pp. 9-10, 1928. (See Depratella, in discussion of invalid genera.) ? Eos chub ertella Thompson, Jour. Paleontol- ogy, vol. 11, p. 123, 1937. Genotype (monotypical), Schuber- tella transit oria Staff and Wedekind. Shell very small, 2 ventricosely fusi- form, of few loosely coiled volutions. Spiral wall composed of tectum and sup- posedly a comparatively thick diaphano- theca that does not show porous struct- ure. Septa nearly plane. Chomata well developed. The predominant form is microspher- ic, with an endothyroid juvenarium of 1 to 2 volutions coiled askew to the axis of later whorls. The megalospheric shells do not differ appreciably from the microspheric in size and external ap- pearance. Staff and Wedekind believed that the wall of their type species consisted of a single compact layer, but Thompson's study of supposedly topotype material indicates two layers as in the American species, S. kingi Dunbar and Skinner. Range, Permian, North America and Eurasia. Genus Fusiella Lee and Chen, 1930 Fusiella Lee and Chen, Nat. Research Inst. Geology (Shanghai) Mem. no. 9, pp. 107- 108, 1930. Profusulinella Rauser-Chernoussova, Trans. Polar Commission, no. 28, pp. 175 and 220, 1936. Genotype, by original designation, Fusiella typica Lee and Chen. Extremely small, fusiform shells hav- ing a very thin spiral wall formed of tectum and tectoria. The septa are nearly plane but slightly folded near the ends. Microspheric shells have an en- dothyroid juvenarium coiled askew to the axis of adult whorls, but megalo- spheric shells are bilaterally symmetri- cal. Microspheric shells appear to pre- dominate. The thin, three-layered wall is the dis- tinctive feature of this genus. The pro- theca is extremely thin, appearing as a dark film between two thicker layers of epitheca. The authors of the genus con- sider the middle layer to represent the tectum alone. The genotype species is tightly coiled and rather sharply point- ed and its chomata are small and nar- row. The genus Profusulinella was distin- guished from Fusulinella on the basis of its wall structure, which was said to consist of tectum and tectoria. Al- though Rauser-Chernoussova did not 2 Description based partly on Thompson's study (1937, p. 118). SYSTEMATIC REVIEW OF THE GENERA 79 mention Fusiella, it was based on pre- cisely the same character. The type of Profusulinella is a somewhat more thick- ly fusiform and more loosely coiled spe- cies than the type of Fusiella and its chomata are appreciably heavier, but it is doubtful whether either of these dif- ferences can be considered of generic value. The types of both genera show dimorphism and have endothyroid juve- naria in the microspheric generation; both are minute species; and they come from the Moscovian horizon. Wedekindellina differs in having a distinctly four-layered wall, with the diaphanotheca well developed, and in having much more massive epithecal deposits. Range, Huanglung limestone (Mosco- vian) of south China; Moscovian of the U. S. R. R. ; Lampasas (Big Saline) limestone of Texas. Genus Wedekindellina Dunbar and Henbest, 1933 Wedekindella Dunbar and Henbest, Am. Jour. Sci. (5), vol. 20, p. 357, 1930. (Name preoccupied by Schindewolf, 1928, for an ammonite.) Wedekindia Dunbar and Henbest, Ibid., vol. 21, p. 458, 1931. (Name also preoccupied by Schindewolf, 1925, for a cephalopod. This and the preceding name were orig- inally introduced in obscure locations and escaped notice of authors of zoo- logical indices.) — Skinner, Jour. Paleon- tology, vol. 5, p. 259, 1931. Wedekindellina Dunbar and Henbest, in Cushman, Foraminifera, etc., p. 134, 1933. Boultonia (part) Lee, Paleontologia Sinica, ser. B, vol. 4, fasc. 1, p. 11, 1927. Fusulinella (part) Henbest, Jour. Paleontol- ogy, vol. 2, p. 80, 1928. Fusulina (part) White, Univ. Texas Bull. 3211, p. 24, 1932. Genotype, by original designation, Fusulinella euthusepta Henbest. Small, fusiform to ellipsoidal. Very compactly coiled, chambers very numer- ous, and walls very thick for shell of such small size. Walls composed of pro- theca and thick epitheca. Chomata mas- sive, width moderate to broad. Axial zone between equator and poles com- monly filled with epitheca. Septa plane or but slightly and irregularly plicate in end zones. Tunnel narrow ; septal pores numerous and evenly spaced in geno- typical species. Proloculum very small. No microspheric generation so far de- scribed. Characteristic of middle Pennsyl- vanian of North America and Eurasia in association with Fusulina. Rarely found in the base of the Triticites zones in the upper Pennsylvanian in North America. Genus Boultonia Lee, 1927 Boultonia Lee, Paleontologia Sinica, ser. B, vol. 4, fasc. 1, p. 10, 1927. Genotype, by original designation, Boultonia willsi Lee. Minute, fusiform shells resembling Fusiella, but having a spiral wall of only two layers, tectum and diaphanotheca, and having deeply plicated septa. The types possessed an endothyroid juvenarium and probably represent the microspheric form; megalospheric form not known. Lee referred to this genus two species, B. willsi and B. rawi. The latter, occur- ring in the Penchi series, of Moscovian age, is quite different from the genotype and is here referred to the genus Wede- kindellina. Range, early Permian (Taiyuan series) of North China. Genus Yangchienia Lee, 1933 Yangchienia Lee, Nat. Research Inst. Geol- ogy (Shanghai) Mem. no. 14, 1933. — Dunbar and Skinner, Univ. of Texas Bull. 3701, p. 569, 1937. Genotype, by original designation, Yangchienia iniqua Lee. A very small, fusiform fusuline differ- ing from Schubertella only in the pos- session of very massive and broad cho- mata. This genus, based on only a few sec- tions of one species, is not securely estab- lished. In spite of the heavy chomata, these shells should probably be referred to Schubertella, which occurs in about the same stratigraphic position. Range, Lower Permian (Chihsia lime- stone) of China. 80 PENNSYLVANIAN FUSULINIDAE Genus Codonofusiella Dunbar and Skinner, 1937 Codonofusiella Dunbar and Skinner, Univ. of Texas Bull. 3701, pp. 606-607, 1937. Genotype, by original designation, Codonofusiella paradoxica Dunbar and Skinner. Exceedingly small, fusiform shells with a very minute proloculum and an endothyroid juvenarium of 1 to 2 volu- tions followed by 2 or 3 fusulinoid whorls. Approaching maturity, the outer whorl rapidly increases in length and height, producing a trumpet-like flaring terminus to the shell. The wall is extremely thin and ap- pears to consist of two layers, a thin tec- tum underlain by a thicker but less dense, homogeneous layer. The septa are very thin and are strongly folded, especially in the outer whorl and its flaring terminus, where the folds reach to the top of the septa. In the genotype there appears to be a tunnel, but cho- mata are lacking or very obscure, hence the tunnel is not clearly defined. Range, Permian (Capitan) of Texas and of British Columbia (Cache Creek). Genus Fusulina Fischer, 1829 Fusulina Fischer, Bull. Soc. Imp. Nat. Mos- cou, vol. 1, p. 330, 1829 (original intro- duction of genus) ; Oryctographie du Gouvernement de Moscou, p. 126, 1837 — Moller, Neues Jahrb., 1877, pp. 141-143, (redesignated F. cylindrica as the typi- cal form); Mem. Acad. Imp. Sci., St. Petersbourg, vol. 25, no. 9, pp. 45-54, 1878. — Schellwien, Paleontographica, Band 5, pp. 161-163, pi. 19, figs. 1 and 2, 1908 (photomicrographs of two of M61- ler's neotypes of Fusulina cylindrica Fischer). — Dunbar and Henbest, Am. Jour. Sci. (5), vol. 20, pp. 357-365, 1930. —Galloway, Manual' of Foraminifera, p. 401, 1933. — Dunbar, in Cushman, Fora- minifera, etc., p. 134, 1933. — Thompson, Am. Jour. Sci., vol. 32, pp. 287-291, 1936. —Henbest, Jour. Paleontology, vol. 11, pp. 221-222, 1937. — Dunbar and Skinner, Univ. of Texas Bull. 3701, pp. 562-563, 1937. — Gorsky, Atlas of Leading Forms of Fossil Faunas, vol. V, p. 38, 1939. Schellwienia Staff and Wedekind, Upsala Univ. Geol. Inst., Bull., vol. 10, p. 113, 1910. Name proposed to include Fusu- lina cylindrica Fischer, thus becoming an objective synonym of Fusulina. Hchellwienia of authors includes species of Triticites, Kchwagerina, Parafusulina, and Polydiexodina (?). Girtyina (of authors, not Girtyina Staff s. s., a synonym of Triticites q. v.) Lee, Pa- leontologia Sinica, ser. B, vol. 4, fasc. 1, pp. 22-40, 1927.— Lee and Chen, Nat. Re- search Inst. Geology (Shanghai) Mem. no. 9, p. 129, 1930. IBoultonia Lee, Paleontologia Sinica, ser. B, vol. 4, fasc. 1, p. 10, 1927 (possibly the microspheric stage of a species of Fusulina but tentatively listed as a valid genus). Beedeina Galloway, Manual of Foraminifera, p. 401, 1933 (genotype by original desig- nation, Fusulinella girtyi Dunbar and Condra, 1927). Genotype (monotypical), Fusulina cylindrica Fischer. Shells fusiform to ventricose and small to medium in size. The spiral wall consists of four layers, tectum, dia- phanotheca, and tectoria, the whole rare- ly exceeding 35 microns in thickness and the diaphanotheca rarely more than 20 microns. Septa deeply folded, even across the middle of the shell (less strongly folded in the juvenile stages of early species). Tunnel narrow to wide. Chomata gen- erally massive and fusulinelloid in the early stages of the older species, but nar- row and spreading high on the septa in more advanced species. The spiral wall is exceedingly finely perforate as in Fusulinella, but the tub- ular pores are coarser in the outer one or two whorls of the latest and most ad- vanced species. Septal pores are com- mon. Dimorphism occurs, as in Fusulinella, but the microspheric shells are very rare. Range, lower ( ? ) and middle Pennsyl- vanian ; Strawn or Des Moines series in America ; Moscovian series of Eurasia. Genus Quasifusulina Chen, 1934 Quasifusulina Chen, Paleontologia Sinica, ser. B, vol. 4, fasc. 2, p. 91, 1934. — Dun- bar and Skinner, Univ. of Texas Bull. 3701, p. 570, 1937.— Gorsky, Atlas of Leading Forms of Fossil Faunas of U. S. S. R., vol. 5, p. 39, 1939. Genotype, by original designation, Fusulina longissima Moller. Slender, subcylindrical, having a thin spiral wall and deeply folded septa but lacking chomata. The wall is commonly not more than 30 microns thick but rare- ly attains to 50 microns in the outer SYSTEMATIC REVIEW OF THE GENERA 81 whorl; it appears to consist of a single layer (diaphanotheca) having very fine tubular pores. Although a normal tec- torium is lacking, there is a broad, ir- regular belt on each side of the mid region in which the chambers are largely filled with epitheca. Chen supposed the lack of tectum and distinct alveoli to be a result of degener- ation from a schwagerinid ancestor, and Dunbar and Skinner placed this genus with some misgivings in the Schwager- ininae and near the genus Schwagerina. Since then Dunbar has had the oppor- tunity to visit the type locality of the genotype in the U. S. S. R., and to study its stratigraphic relations, with the re- sult that we now regard Quasifusulina as a specialized descendant of Fusulina and a member of the Fusulininae. It occurs low in the zone of Triticites and just above the range of Fusulina. It resembles Fusulina in the thinness of its wall and the depth of its septal folding, and is far too old to have descended from Schwagerina. The change from Fusulina involved the disappearance of tectum, tectoria, and chomata, and the development of localized axial filling. Chen included in this genus "Fusu- lina" tenuissima Schellwien from the Trogkofel limestone of the Carnic Alps. Subfamily Schwagerininae Dunbar and Henbest, 1930 Fusulines of medium to very large size ; fusiform to sub-cylindrical or sub- globular; spiral wall alveolar, consist- ing of tectum and keriotheca, the epi- theca being reduced and commonly lo- cal in occurrence or absent ; septa mod- erately to deeply plicated ; tunnel broad and slit-like; chomata prominent in the ancestral genus, Triticites, but obsolete in later genera or represented only in the early ontogeny; in the most special- ized genera new avenues of communica- tion between chambers appear in the form of cuniculi and supplementary tunnels. Dimorphism is present in some of the genera, at least, the microspheric genera- tion being rare and much larger than the megalospheric ; microspheric shells possess an endothyroid juvenarium coil- ed askew to the adult axis. A prolific stock, ranging through the Upper Pennsylvanian and the Permian. Genus Triticites Girty, 1904 Triticites Girty, Am. Jour. Sci. (4), vol. 17, p. 234, 1904.— Dunbar and Condra, Ne- braska Geol. Surv. (2), Bull. 2, pp. 53- 60, 1927 (1928).— Galloway, Manual of Foraminifera, p. 402, 1933. — Dunbar, in Cushman, Foraminifera, etc., p. 135, 1933. — Dunbar and Skinner, Univ. of Texas Bull. 3701, p. 613, 1937. Girtyina Staff, Neues Jahrb., Beilage-Band 27, pp. 490 and 506, 1909. (Genotype by original designation, "Girtyina ventri- eosa Meek" [and Hayden]. This form is a species of Triticites Girty, 1904, which Staff arbitrarily attempted to re- ject. Though Girtyina is a synonym of Triticites, Staff and others used the name in the sense of Fusulina s. s. See p. 89, also discussion under Fusulina girtyi in the description of species.) Grabauina Lee, Geol. Soc. China. Bull., vol. 3, no. 1, p. 51, 1924. Fusulina (part) of authors, 1878 to 1930. — Silvestri, Boll. Soc. Geol. Italiana, vol. 54, pp. 203-219, 1935. Schellwienia (part) of authors. ? Hemi fusulina Moller, Neues Jahrb., 1877, p. 144; Mem. Acad. Imp. Sci. St. Peters- bourg (7), vol. 25, no. 9, pp. 74-78, 1878. (Not recognizable, may be synonym of Schwagerina s. s. or juvenarium of Pseudoschwagerina. ) Genotype, by original designation, Miliolites secalica Say. Shells medium to large, typically fusi- form, but ranging from subcylindrical to subglobular. Spiral wall distinctly alveolar, consisting of tectum and kerio- theca (in some species a thin layer of epitheca persists as a tectorium on the outer surface of the wall). Septa only slightly to moderately folded across the middle of the shell, but more deeply folded near the poles (in the more ad- vanced species the folding becomes mod- erately strong even at the middle). Chomata are well developed and persist to maturity. Septal pores are commonly conspicuous in the outer whorls. Triticites differs from Schwagerina (Pseudo fusulina of authors) in (1) the less deep and regular septal folding and (2) the possession of conspicuous cho- mata. Triticites ranges through the upper Pennsylvanian and persists with declining numbers into the early Per- mian, where it overlaps on the range of Schwagerina. In this zone of overlap, 82 PENNSYLVANIAN FUSULINIDAE where a transition is made from Triti- cites to Schwagerina by the loss of cho- mata and the intensification of septal folding, some of the species are not easy to place, but otherwise a glance at an axial section is sufficient to distinguish these genera. Genus Schwagerina Moller, 1877 Schwagerina Moller, Neues Jahrb., 1877, p. 143. — Dunbar and Skinner, Jour. Paleon- tology, vol. 10, pp. 83-91, 1936; Texas Univ. Bull. 3701, p. 623, 1937.— Gorsky, Atlas of Leading Forms of Fossil Faunas of U. S. S. R., vol. 5, p. 41, 1939. [Not Schwagerina of most authors, which = Pseudoschwagerina or Para- schwagerina.'} Fusulina (part) of authors. ? Hemifusulina Moller, Neues Jahrb., 1877, p. 144; Mem. Acad. Imp. Sci. St. Peters- burg (7), vol. 25, no. 9, p. 76, 1878 (see also under Triticites). Pseudofusulina Dunbar and Skinner, Am. Jour. Sci. (5), vol. 22, p. 252, 1931 — Galloway, Manual of Foraminifera, p. 404, 1933. — Dunbar, in Cushman, Fora- minifera, etc., p. 136, 1933.— Chen, Pale- ontologia Sinica, ser. B, vol. 4, fasc. 2, p. 50, 1934. — Rauser-Chernoussova, Acad. Sci. U. S. S. R. Bull., pp. 573-584, 1936; Acad. Sci. U. S. S. R., Trans. Polar Commission, no. 28, p. 224, 1936.— Bel- jaev and Rauser-Chernoussova, Acad. Sci. U. S. S. R., Geol. Inst, vol. 7, pp. 169-196, 1938. Leeina Galloway, Manual of Foraminifera, p. 406, 1933. Nagatoella Thompson, Geol. Soc. Japan Jour., vol. 43, pp. 195-202, 1936. Schellwienia (part) of authors. Genotype, by original designation, Borelis princeps Ehrenberg. Fusiform to subcylindrical or sub- globular shells of medium to large size, having a distinctly alveolar spiral wall composed of tectum and keriotheca; whorls planispirally coiled and gradu- ally expanding; septa "regularly and very deeply folded so that the lower parts of opposed folds on adjacent septa meet to subdivide the meridional cham- bers into cell-like chamberlets. Median tunnel low and broad ; septal pores pres- ent in the outer whorls; chomata lack- ing or present only in a rudimentary condition in the early whorls of some of the oldest species. In various species of this genus a con- spicuous deposit of epitheca is laid down, largely filling the chambers in cer- tain parts of the shell. This filling may be localized in a narrow zone along the axis, or in a belt in each end zone some distance from the tunnel. Such filling assumes a distinctive pattern in many species but each pattern has developed independently in species obviously not closely related, and similar axial filling occurs also in other genera, notably Wedekindellina, Parafusulina, and Po- lydiexodina. It is therefore not a diag- nostic generic character. Range, especially characteristic of the Wolfcamp horizon in America and the Sakmarian of Eurasia, but ranging up into the middle Permian in both regions. Schwagerina has been the subject of unfortunate confusion. Moller defined it in 1877, designating Borelis princeps Ehrenberg as genotype, but he did not describe that species. A year later he applied the name Schwagerina princeps to a globular shell superficially resem- bling B. princeps but having a very dif- ferent interior. Moller 's 8. "princeps" of 1878 had a tightly coiled juvenarium followed by abrupt and rapid inflation, and this subsequently came to be re- garded as the diagnostic character of Schwagerina. Meanwhile, the real Bo- relis princeps was never restudied until the types were sectioned and described by Dunbar and Skinner in 1936. It was then discovered that expansion was gradual and the shell features were those for which Dunbar and Skinner had previously proposed the name Pseudo- fusulina. Schwagerina was then redi- agnosed in accordance with its genotype. Pseudofusulina was suppressed as a syn- onym, and the form so long mistaken for Schwagerina was described as a new genus Pseudoschwagerina. The true Schwagerina expands gradu- ally as does Triticites, from which it differs in its deep and regular septal folding and in the absence of chomata. Subgenus Rugofusulina (Rauser- Chernoussova) Rugofusulina Rauser-Chernoussova, Studies in Micropaleontology, Moscow Univ., vol. 1, fasc. 1, pp. 9-26, 1937. Genotype, by original designation, Fusulina prisca Ehrenberg emend. Moller. SYSTEMATIC REVIEW OF THE GENERA 83 Distinguished from Schwagerina s. s. because of the ''rugosity" of its spiral wall. Since the wall appears to undulate, regardless of the orientation of the sec- tion, it is evident that the inequalities are of the nature of dimples and mounds rather than rugae. In the older species, the entire wall is flexed, but in later species only the tectum is affected and the dimples are on a very small scale. The significance of this feature is not understood but it is clearly an original shell character, not a modification dur- ing fossilization, and it seems to charac- terize a group of related species in the U. S. S. R. and has been observed in forms from the Carnic Alps and from Texas, all of the same limited strati- graphic range. We tentatively regard this as a subgenus of Schwagerina. Range, lower Permian (Sakmarian). Genus Parafusulina Dunbar and Skinner, 1931 Parafusulina Dunbar and Skinner, Am. Jour. Sci. (5), vol. 22, p. 258, 1931.— Galloway, Manual of Foraminifera, p. 406, 1933. — Dunbar, in Cushman, Foraminifera, etc., p. 137, 1933.— Chen, Paleontologia Sin- ica, ser. B, vol. 4, fasc. 2, p. 80, 1934 — Dunbar and Skinner, Univ. of Texas Bull. 3701, p. 672, 1937. Fusulina (part) of authors. Schellwienia (part) of authors. Genotype, by original designation, Parafusulina wordensis Dunbar and Skinner. Shells of medium to extremely large size, and elongate fusiform to subcylin- drical shape. Spiral wall as in Schwag- erina. Septa deeply and regularly fold- ed, with the tips of opposed folds of adjacent septa meeting before reaching the floor of the volution, and joining each to each to form arch-like foramina. The repetition of these basal foramina under successive septa forms a series of spiral galleries, the cuniculi, running around the shell; the basal margins of the septa are joined along the sides of these cuniculi to form a series of wavy basal sutures running transverse to the axis of coiling. A single slit-like median tunnel is present and septal pores are abundant. Marked dimorphism occurs in some species, the microspheric shells being commonly twice as long as the megalo- spheric and much thicker. Microspheric shells have a minute endothyroid juve- narium coiled askew to the later whorls ; furthermore, they have no median tun- nel except in the earliest of the fusuli- noid whorls. Microspheric shells are rare. This genus was derived from Schwag- erina by progressive specialization of the septa, resulting in the formation of the cuniculi. Range, middle and upper Permian. Genus Polydiexodina Dunbar and Skinner, 1931 Polydiexodina Dunbar and Skinner, Am. Jour. Sci. (5), vol. 22, p. 263, 1931 — Galloway, Manual of Foraminifera, p. 406, 1933. — Dunbar, in Cushman, Fora- minifera, etc., p. 137, 1933. — Dunbar and Skinner, Univ. of Texas Bull. 3701, p. 693, 1937. Fusulina (part) of authors. Genotype, by original designation,. Polydiexodina capitanensis Dunbar and Skinner. Mostly large and very elongate fusu- lines, resembling Parafusulina, but dis- tinguished by the presence of a series of accessory tunnels paired on opposite sides of the median tunnel. Generally the whorls are low and tightly coiled, and considerable secondary shell mate- rial is deposited as an axial filling. The proloculum is commonly large, thin- walled, and irregular in shape. Marked dimorphism occurs here pre- cisely as in Parafusulina. Range, upper Permian of North America and Central Asia. Genus Pseudoschwagerina Dunbar and Skinner, 1936 Pseudoschwagerina Dunbar and Skinner, Jour. Paleontology, vol. 10, p. 89, 1936; Univ. of Texas Bull. 3701, p. 656, 1937.— Gorsky, Atlas of Leading Forms of Fos- sil Faunas of U. S. S. R., vol. V, p 43,. 1939. Schwagerina (part) of authors, not Moller r 1877. Genotype, by original designation, Schwagerina uddeni Beede and Kniker. 84 PENNSYLVANIAN FUSULINIDAE Thickly fusiform to subspherical fusu- lines in which the inner volutions are closely coiled as in Triticites, forming a compact juvenarium of .2 to 5 whorls, which is followed by a rapid change to the high, inflated volutions of the adult shell ; commonly the last whorl is less in- flated than the penultimate; the wall is alveolar as in Triticites, but the kerio- theca is commonly relatively thin; the septa are gently and irregularly folded and so widely spaced that opposed folds do not commonly touch ; the median tun- nel is low and slit-like; chomata are present in the juvenarium but rudiment- ary or lacking in the inflated whorls. The great height of the inflated whorls in some species is noteworthy, but the actual height varies with the size of the species; the diagnostic character is the abrupt change in the closeness of coil- ing, which leaves the juvenarium sharp- ly marked off from the outer whorls. The ontogeny clearly shows that this genus developed out of Triticites. Range, Wolfcamp and equivalent horizons in America and Sakmarian horizon in Eurasia. Subgenus Zellia (Kahler and Kahler), 1937 Pseudoschwagerina (Zellia) Kahler and Kahler, Paleontographica, Band 87, Abt. , A, Lief. 1, pp. 20-21, 1937. Genotype, by original designation, Pseudoschwagerina (Zellia) heritschi Kahler and Kahler. Distinguished from Pseudoschwag- erina s.s. by having a thicker wall and thicker septa and in the great abundance and prominence of the septal pores. The septa are said to have a distinct layer of epitheca on both front and back sides of the pyknotheca. Range, Schwagerinakalk (Sakmarian) of the Carnic Alps. Genus Paraschwagerina Dunbar and Skinner, 1936 Paraschwagerina Dunbar and Skinner, Jour. Paleontology, vol. 10, p. 89, 1936; Texas Univ. Bull. 3701, p. 666, 1937. Hchwagerina (part) of authors. Genotype, by original designation, Hchwagerina gigantea White. Differing from Pseudoschwagerina in that the whorls of the tightly coiled juvenarium are slender and elongate and the septa at all stages of growth are deeply and regularly folded as in Schwagerina s. s., and in that chomata are inconspicuous or lacking even in the juvenarium, and normally are complete- ly absent in the inflated whorls. The ontogeny clearly shows that this genus developed from Schwagerina s.s. from which it differs only in the abrupt inflation at the end of the juvenarium. Range, Wolfcamp and equivalent formations in America and Sakmarian horizon in Eurasia. Genus Paleofusulina Deprat, 1913 Paleofusulina Deprat, Acad. Sci. Paris Comptes Rendus, vol. 154, p. 1548, 1912; Mem. Serv. Geol. Indochine, vol. 2, fasc. 1, p. 36, 1913 (formally introduces genus and typical species, P. prisca). — Colani, Ibid., vol. 11, fasc. 1, pp. 24, 52, 79, and 133, 1924.— Likharev, Bull. Com. Geol. Leningrad, vol. 45, p. 59, 1926. Genotype (monotypical), Paleofusu- lina prisca Deprat. Test thickly fusiform; wall thin, con- sisting of a tectum and keriotheca, though the alveolar texture of the latter is commonly not discernible (Deprat fig- ured a distinct alveolar texture, but Colani later denied its existence; Lik- harev confirmed its presence, but stated that its texture is very fine, and that it is visible only in exceptional cases. Ac- cording to Likharev the wall is only 16-21 microns thick in the fifth volu- tion) ; septa strongly and regularly fluted, the septal folds being equally strong from top to bottom margin, so that in axial slices of the shell the sec- tions of the septa appear as pillar-like rods rather than loops; juvenarium bi- laterally symmetrical; septa perforated by a rather high and narrow median tunnel and, in the outer volutions, by abundant septal pores (fide Likharev). Chomata present, chiefly in the form of a secondary deposit coating the septa near the tunnel. The relations of this genus depend on its wall structure, which is still a sub- ject of some uncertainty. Its minute size, thin wall, and intense septal fluting suggest an alliance with Cbdonofusiella. SYSTEMATIC REVIEW OF THE GENERA 85 A superficial resemblance to Schwag- erina is seen in the shape and in the in- tense septal fluting, but if the wall of Paleofusulina is thin and non-alveolar the resemblance is probably an example of homeomorphy. The fact that the sep- tal folds are equally strong from base to top of each septum gives a distinctive appearance to the axial sections, where we see "pillars" instead of septal loops. Range, Permian. Deprat described the genus as occurring in the Mississip- pian, an obvious error later pointed out by Colani, who argues correctly that it should be Uralian or Permian. Likharev later described a second species from the Permian of the Caucasus. Genus Gallowaiinella Chen (in Dunbar and Skinner), 1937 Gallowaiinella Chen, in Dunbar and Skinner, Texas Univ. Bull. 3701, pp. 571-572, 1937. Gallowaiina Chen (not Ellis), Geol. Soc. China Bull., vol. 13, pp. 237-238, 1934 (homonym of Gallowayina Ellis, Am. Mus. Nat. Hist, Novitates no. 568, pp. 1-8, 1932, according to Article 35, Int. Rules Zool. Nomenclature.) Genotype, by original designation, Gallowaiina meitienensis Chen. Based on a single species of subcylin- drical form which differs from Schwag- erina only in wall structure, its spiro- theca being very thin (hardly exceeding 20 microns even in the outer whorls), and chiefly composed of a homogeneous clear layer coated both inside and out by a thin dark film. Of these dark films the outer is the more distinct and may be homologized with the tectum. The septa are regularly and deeply folded as in Schwagerina, the tunnel is slit-like, and there are no chomata. There is uncertainty as to the taxo- nomic position and value of this form. Its thin and nearly structureless wall suggests " degeneracy''. It does not have the distinct alveolar structure charac- teristic of the Schwagerininae, but its size, general organization and associa- tion suggest that it may be a special- ized or degenerate offshoot of this sub- family rather than a member of the Fu- sulininae. Range, Meitien limestone (middle or lower Permian) of China. Genus Nipponitella Hanzawa, 1938 Nipponitella Hanzawa, Imp. Acad. Tokyo Proc, vol. 14, no. 7, p. 256, 1938. Genotype, by original designation, Nipponitella explicata Hanzawa. An irregularly uncoiled fusuline ap- parently derived out of Triticites. It possesses a juvenarium of 2 or 3 nor- mally coiled, fusiform volutions, after which the shell grows out in rectilinear form as an irregularly undulating rib bon. The wall is alveolar and the early whorls have well-developed chomata and a median tunnel. In the uncoiled part of the shell the septa are deeply and closely folded. The only comparable fusuline is Co- donofusiella, which starts to uncoil at maturity; but there is probably no re- lationship here for Co donofusiella is a minute form with non-alveolar wall structure. Range, Permian (Maiya group) of Japan. Subfamily Verbeekininae Staff and Wedekind, 1910 Specialized fusulines of melon-shaped or subspherical form in which the septa are plane and (except in E overt eekina) do not have a tunnel but are perforated along the basal margin by a single row of round foramina. Parachomata are present in the later ontogeny of primi- tive forms and in all stages of more ad- vanced genera. The wall is normally alveolar, consist- ing of a thin tectum and a keriotheca of fine texture, but one specialized genus (Pseudodoliolina) has a thin, compact, and homogeneous wall. Dimorphism is common and the mi- crospheric shells have a juvenarium of endothyroid form coiled askew to the axis of later whorls. There is little dif- ference, however, in size and external appearance between the microspheric and megalospheric shells. Apparently this stock arose directly from Staff ella during Permian time, the genus E overt eekina being the connect- ing link. Range, Permian of the Orient and the Tethyan region. 86 PENNSYLVANIAN FUSULINIDAE Genus Eoverbeekina Lee, 1933 Eoverbeekina Lee, Mem. Nat. Research Inst. Geology (Shanghai), no. 14, p. 14, 1933. — Chen, Paleontologia Sinica, ser. B, vol. 4, fasc. 2, p. 103, 1934.— Dunbar and Skinner, Univ. of Texas Bull. 3701, p. 573, 1937. Genotype, by original designation, Eoverbeekina intermedia Lee. Subspherical shells of small size in which the inner whorls are nautiliform, gradually changing to spheroidal at ma- turity. The wall is thin, consisting of tectum and a finely alveolar keriotheca; the septa are plane and are perforated by a slit-like median tunnel and, in ad- dition, in the outer whorls, by numerous round basal foramina (stomata) on each side of the middle. Chomata are obso- lescent but rudimentary parachomata appear in the outer whorls. This genus differs from Verbeekina in smaller size, in possessing a median tunnel, in the rudimentary character of its parachomata, and in the fact that its early whorls are narrow instead of spheroidal. It forms an almost ideal link between Staff ella and Verbeekina. Range, lower Permian (Chihsia lime- stone of China). Genus Verbeekina Staff, 1909 Verbeekina Staff, Neues Jahrb., Beilage- Band 27, p. 476, 1909.— Ozawa, Imp. Univ. Tokyo, Jour. Coll. Sci., vol. 45, art. 4, p. 25, 1925; Ibid., vol. 45, art. 6, p. 48, 1925. — Dunbar and Condra, Ne- braska Geol. Surv. Bull. 2, 2nd ser., p. 74. 1927. — Dunbar, in Cushman, Fora- minifera, etc., p. 138, 1933.— Tan Sin Hok, Wetensch. Medeel. Mijnbouw Nederlandisch-Indie, no. 25, p. 57, 1933. — Thompson, Jour. Paleontology, vol. 10, p. 193, 1936. — Dunbar and Skinner, Univ. of Texas Bull. 3701, p. 573, 1937. Doliolina (part) of Schellwien. Schwagerina (part) of authors prior to 1909, and of Deprat, 1911-14. Genotype, (monotypical), Fusulina verbeeki Geinitz. Test spheroidal, consisting of numer- ous volutions; wall composed of tectum and thin keriotheca; septa plane, with- out a median tunnel, but with a regular row of round foramina along the basal margin ; parachomata lacking or rudi- mentary in the inner whorls but well developed in the outer ones. The proloculum is minute and is fol- lowed in the microspheric shells by a few obliquely coiled juvenile whorls. Closely allied to Doliolina, from which it differs in shape and in the fact that parachomata are developed later in the ontogeny. Range, Permian of the Orient and the Tethyan region. Genus Misellina Schenck and Thompson, 1940 Misellina Schenck and Thompson, Jour. Paleontology, vol. 14, pp. 584-589, 1940. Mbllerina Schellwien, Palaeontographica, vol. 44, p. 238, 1898 (name preoccupied). Doliolina Schellwien, Schrift. Phys.-Oekon. Gesell. Konigsberg, Jahrg. 43, p. 67, 1902; in Futterer, Durch Asien, vol. 3, p. 125, 1902.— Staff, Neues Jahrb. Beil- age-Band 27, p. 476, 1909. — Deprat, Mem. Serv. Geol. Indochine, vol. 1, fasc. 3, p. 42, 1912; vol. 4, fasc. 1, p. 27, 1915.— Yabe and Hanzawa, Imp. Acad. Japan Proc, vol. 8, no. 2, p. 41, 1932.— Gallo- way, Manual of Foraminifera, p. 408, 1933. — Dunbar, in Cushman, Foraminif- era, etc., p. 138, 1933. — Dunbar and Skin- ner, Univ. of Texas Bull. 3701, p. 574, 1937. Genotype, Doliolina ovalis Deprat. Test melon-shaped, being somewhat elongated and bluntly rounded at the ends; microspheric individuals possess- ing an endothyroid juvenarium but me- galospheric shells planispiral through- out; walls rather thin, consisting of a tectum and a finely alveolar keriotheca; septa plane, with a basal row of fora- mina but no median tunnel ; paracho- mata well developed at all stages of growth. Range, Permian of the Orient. Subgenus Brevaxina Schenck and Thompson, 1940. Brevaxina Schenck and Thompson, Jour. Paleontology, vol. 14, p. 587, 1940. Doliolina (part) of authors. Subgenotype, by original designation, Doliolina compressa Deprat. Differing from Misellina s.s. only in having a subspherical form with the axis the shortest diameter. Range, Permian of the Orient. SYSTEMATIC REVIEW OF THE GENERA 87 Genus Pseudodoliolina Yabe and Hanzawa, 1932 Pseudodoliolina Yabe and Hanzawa, Imp. Acad. Japan Proc, vol. 8, p. 40, 1932 — Galloway, Manual of Foraminifera, p. 410, 1933. — Dunbar, in Cushman, Fora- minifera, etc., p. 139, 1933. — Dunbar and Skinner, Univ. of Texas Bull. 3701, p. 575, 1937. Doliolina (part) of Deprat and Ozawa. Genotype, by original designation, Pseudodoliolina ozawai Yabe and Han- zawa. Differing from Misellina in wall struc- ture alone, the keriotheca being obsolete and the wall consisting of a single, thin layer, apparently the tectum. Range, Permian of the Orient. Subfamily Neoschwagerininae Dunbar and Condra, 1927 Specialized fusulines, mostly of large size and thickly fusiform to subglobular shape, in which the spiral wall is spe- cialized by the development of pendant lamellae called septula. There are usually numerous, closely coiled volutions; the septa are plane; there is no median tunnel but, instead, a row of rounded foramina (stomata) along the base of the septa ; paracho- mata are invariably present. The spiral wall consists of a tectum and finely alveolar keriotheca in the ancestral and more conservative genera, but the kerio- theca undergoes extensive specializations in this subfamily. The first specializa- tion took the form of local thickening of the keriotheca into septum-like pend- ants, the septula, which hung down into the chambers. In the most primitive genus (Cancellina), these septula formed a meridional series crossing the true septa at right angles; in the next genus (Neoschwagerina) a second set of septula appeared, paralleling the true septa and crossing the meridional sep- tula to form a grid of intersecting plates. In later genera the lower edges of these septula became solid instead of alveolar and eventually, in the most highly specialized genus (Lepidolina), the entire keriotheca was reduced to a thin, compact, and apparently homoge- neous layer from which hung the thin compact septula. The solidification of the septula be- gan at their free edge and progressed upward toward the spiral wall ; it also began late in the ontogeny and was gradually pushed back into the early whorls. Lee has proposed genera based on the stages of this progressive evolu- tion. Range, Permian of the Orient and the Tethyan region ; rare in British Colum- bia. Genus Cancellina Hayden, 1909 Cancellina Hayden, Rec. Geol. Surv. India, vol. 38, p. 249, 1909. — Ozawa, Imp. Univ. Tokyo Jour. Coll. Sci., vol. 45, art. 4, pp. 18, 26, 1925; in Cushman, Forami- nifera, etc., p. 138, 1928. — Galloway, Manual of Foraminifera, p. 410, 1933. — Dunbar, in Cushman, Foraminifera, etc., p. 139, 1933.— Dunbar and Skinner, Univ. of Texas Bull. 3701, p. 575, 1937. Genotype (selected by Ozawa, 1925 ) 7 Neoschwagerina primigenia Hayden. Like Neoschwagerina but with a single series of septula which run transverse to the axis and subdivide the longitudinal chambers into rectangular chamberlets. Range, Permian of Afghanistan and the Orient. Genus Neoschwagerina Yabe, 1903 Neoschwagerina Yabe, Jour. Geol. Soc. Tokyo, vol. 10, no. 113, p. 5, 1903; Imp. Univ. Tokyo Jour. Coll. Sci., vol. 21, art. 5, p. 3, 1906. — Deprat. Mem. Serv. Geol. Indochine, vol. 1, fasc. 3, pp. 6, 15, 1912; vol. 3, fasc. 1, p. 24, 1914.— Ozawa, Imp. Univ. Tokyo Jour. Coll. Sci., vol. 45, art. 4, pp. 18, 24. — Galloway, Manual of For- aminifera, p. 410, 1933. — Dunbar, in Cushman, Foraminifera, etc., p. 140, 1933. — Dunbar and Skinner, Univ. of Texas Bull. 3701, p. 576, 1937. Genotype, by original designation, Schwagerina craticidifera Schwager. Test large, thickly fusiform to sub- spherical, consisting of numerous, closely wound volutions ; wall thin, formed of tectum and keriotheca ; septa plane ; septula of two series well developed, one set alternating with the true septa and paralleling the axis, while the other set runs at right angles to the septa, the two sets of septula forming a rectangu- lar grid that hangs pendant from the wall ; septa perforated by a row of 88 PENNSYLVANIAN FUSULINIDAE rounded basal foramina (stomata) ; para- chomata well developed. This genus shows an advance over Cancellina in the addition of axial sep- tula. Range, Permian of the Orient and the Tethyan region; a single known Ameri- can species occurs in British Columbia. Genus Colania Lee, 1933 Colania Lee, Mem. Nat. Research Inst. Geol- ogy (Shanghai), no. 14, p. 20, 1933.— Dunbar and Skinner, Univ. of Texas Bull. 3701, p. 576, 1937. Genotype, by original designation, Co- lania kwangsiana Lee. Intermediate between Neoschwagerina and Yabeina, the inner whorls having exactly the character of those in the former genus, and the outer whorls fol- lowing the pattern in Yabeina. There is room for considerable doubt as to the usefulness of this generic dis- tinction. It is evident that Yabeina de- scended from Neoschwagerina, and it is to be expected that early species of the former would show in their ontogeny some recapitulation of this racial his- tory. Colania kwangsiana does so pre- cisely. It is, of course, an incompletely developed Yabeina and might be ad- mitted to that genus. The unique species is apparently rare since but a single figure was given to supplement the brief specific description of the genotype. We are inclined for the present to regard Colania as a synonym of Yabeina. Range, Permian of the Orient. Genus Yabeina Deprat, 1914 Yabeina Deprat, Mem. Serv. Geol. Indochine, vol. 3, fasc. 1, p. 30, 1914. — Ozawa, Imp. Univ. Tokyo Jour. Coll. Sci., vol. 45, art. 4, pp. 18, 26, 1925.— Galloway, Manual of Foraminifera, p. 411, 1933. — Dunbar, in Cushman, Foraminifera, etc., p. 140, 1933. — Dunbar and Skinner, Univ. of Texas Bull. 3701, p. 577, 1937. Genotype, by original designation, Neoschwagerina (Yabeina) inoueyi De- prat = Neoschwagerina globosa Yabe = Yabeina globosa (Yabe). Like Neoschwagerina except that the distal parts of the pendant septula are solid plates, the alveolar texture being lost here by a thickening and fusing of the lamellae. This genus is clearly a specialized de- scendant of Neoschwagerina from which it differs in the modification of the struc- ture of its wall pendants. There is also a tendency toward the introduction of a greater number of axial septula than in the parent genus, Neoschwagerina commonly having 1 to 3 septula be- tween each pair of true septa and Yabe- ina from 3 to 6. Range, upper Permian of the Orient. Genus Lepidolina Lee, 1933 Lepidolina Lee, Mem. Nat. Research Inst. Geology (Shanghai), no. 14, p. 21, 1933. — Dunbar and Skinner, Univ. of Texas Bull. 3701, p. 578, 1937. Genotype, by original designation, Neoschwagerina (Sumatrina) multisep- tata Deprat. _ Like Yabeina except that the fusion of the keriothecal lamellae is complete in both the wall and its pendants, the spirotheca consisting of a thin, homoge- neous layer and the septula being com- pact plates. While the general form is precisely that of Yabeina, the wall struc- ture is that of Sumatrina, We are uncertain of the validity of this genus because of discrepancies be- tween the observations of Deprat, Co- lani, and Lee on the structure of the type species. In the original descrip- tion Deprat indicated that the wall and septula both have an alveolar structure. Colani also discussed the species at length and stated (1924, p. 124) that the lamellae of the wall are long and thin, resembling somewhat those of Neo- schwagerina craticulifera. She con- cluded that the species belongs in Neo- schwagerina, not Sumatrina. Her illus- trations (1924, pi. 25, figs. 5, 6, 12) seem to confirm her observations. Lee, on the contrary, states that both wall and septula are compact as in Suma- trina and proposes the separation of the genus from Yabeina on this basis. Until Lee 's observations are confirmed or supported by adequate illustrations, Lepidolina must be considered a prob- able synonym of Yabeina or Neoschwag- erina. Range, Permian of the Orient. SYSTEMATIC REVIEW OF THE GENERA 89 Genus Sumatrina Volz, 1904 Sumatrina Volz, Geol. Pal. Abh. Koken (Jena), vol. 10, pt. 2, pp. 24, 98, 177, 1904. — Deprat, Mem. Serv. Geol. Indo- chine, vol. 1, fasc. 3, p. 56, 1912; vol. 3, fasc. 1, p. 34, 1914. — Ozawa, Imp. Univ. Tokyo Jour. Coll. Sci., vol. 45, art, 4, pp. 19, 26, 1925.— Galloway, Manual of Fora- minifera, p. 411, 1933. — Dunbar, in Cush- man, Foraminifera, etc., p. 140, 1933. — Lee, Mem. Nat. Research Inst. Geology (Shanghai), no. 14. p. 21, 1933.— Dun- bar and Skinner, Univ. of Texas Bull. 3701, p. 577, 1937. Genotype, by original designation, Sumatrina annae Volz. Elongate fusiform, consisting of sev- eral rather closely coiled volutions ; wall thin and compact, consisting of a single layer; septa unfluted; both axial and transverse septula abundant but short, and having the form of compact solid lamellae, thin near the outer wall but much thickened toward their free mar- gin. Three to six axial septula inter- vene between each pair of true septa. Sumatrina appears to be a descendant of some Neoschwagerina in which the alveolar texture of the wall and its pend- ants has been lost. It has been consid- ered to be a further specialization in the direction indicated by Yabeina. In- deed, Deprat considered Yabeina to be a direct connecting link between Neo- schwagerina and Sumatrina. It must be noted, however, that the known species of Sumatrina are rela- tively more slender than any of the species of Neoschwagerina or Yabeina. Furthermore, as Lee (1933, p. 21) has pointed out, the pendant septula are subequal jn length in Sumatrina and in the other genera appear as two or more series of unequal length in each meridi- onal chamber, the first-formed series be- ing longer than the next. Range, upper Permian of the Orient. Invalid or Questionable Genera and Generic Names In the preceding outline of the classi- fication of Fusulinidae, synonymies con- tain a number of generic names that are definitely or are apparently invalid. The reasons for rejecting some of the names so listed are too involved to describe in a concise outline of the accepted taxon- omy, but inasmuch as the reasons should be reviewed, they are given below. Girtyina Amidst the confusion of the principles of taxonomic nomenclature and the mis- understanding of North American fusu- lines by Staff, the history of his genus Girtyina is typical. This genus was pro- posed with " Girtyina ventricosa Meek' r cited as genotype. Meek and Hay den were authors of the species, not Meek alone. Staff evidently did not have in mind the species Fusulina cylindrica var. ventricosa Meek and Hayden as geno- type, but rather a form from the Brere- ton limestone of Illinois later identified by Meek and Worthen with the Meek and Hayden species. This form from the Brereton limestone long went by the double misnomer "Girtyina ventricosa" though it is now generally and properly known as Fusulina girtyi (Dunbar and Condra) (1927, pp. 61-65, and 76-78). The genotype species of "Girtyina" is clearly a species very closely related to Triticites secalicus (Say), the geno- type species of Triticites. Triticites was proposed five years prior to the intro- duction of "Girtyina". As used by Staff, Lee (1927), and others, Girtyina is a synonym of Fusulina Fischer s. s., Moller s. s., and authors since 1930, ex- cept Silvestri. The foregoing reasons for rejecting the name were originally set forth by Dunbar and Condra (1927, pp. 61-65, and 76-78) who revised the nomencla- ture to fit the International Code. Neofusulinella Deprat, 1913 N eofusulinella was introduced by De- prat under the supposition that Fusu- linella Moller, 1877, represents the spherical Fusulininae that we now call Staffella. In the preliminary introduc- tion of Neofusulinella, Deprat indicated that the species on which this new genus was based came from Bam-Na-Mat. In the formal introduction of the genus in 1913 (p. 40), Deprat described the spe- cies as Neofusulinella lantenoisi, n. sp., and stated that he had also found two additional species from other localities. In the description of these three species, 90 PENNSYLVANIAN FUSULINIDAE N. lantenoisi is the only one cited as having been found in Bam-Na-Mat, so it must be regarded as the genotype. As discussed in detail by Dunbar and Skin- ner (1937, pp. 564-567) this species must be regarded as the type species re- gardless of Galloway's designation (1933, p. 400) of X. praecursor Deprat as genotype. The validity of Neofusulinella there- fore depends on the character of X. lan- tenoisi Deprat. Deprat 's description and illustrations of this species are poor, but furnish significant information. In the description the measurements pre- sented for the thickness of the reseau alveola ire range from 11 microns in the first volution to 80 in the last two. This information indicates that the wall is keriothecal rather than fusulinellid. De- prat's figures (1913, pi. 7, figs. 24, 25) are crude drawings and show no details of wall structure. His figure 23, which is evidently a photomicrograph, gives almost indubitable evidence of kerio- thecal wall structure. Writers since Deprat 's time have ac- cepted Xeofusulinella as having a fusu- linellid wall structure and have classed it with the Fusulininae. In spite of the fact that Deprat thought that he was dealing with a fusulinellid, the species is evidently a schwagerinoid of some kind. Figure 23 (1913, pi. 7) shows an excentric axial section and is perhaps slightly oblique. What appear to be chomata are present in next to the last volution, but the poor quality of the picture does not make a definite iden- tification of the structure possible. With- out these data and well-centered sec- tions, the characteristics of this genus remain too uncertain to warrant its con- tinued recognition. If, as it appears, .V. lantenoisi is either a Triticites or a Schwagerina, these names have priority over Xeofusulinella, which is a further reason for rejecting the name, at least tentatively. Recentlv, Thompson and Foster (1937, pp. 130-132) have attacked this difficult question and have attempted to save the name on the basis of specimens which they regard as closely similar to those illustrated by Deprat. Two objections may be raised against this. The first is that their sections are not well oriented or centered and the illustrations do not resolve critical features of the wall structure. The second and more im- portant objection relates to what may be considered authentic topotypes. Though poorly informed on the geogra- phy involved, we are under the impres- sion that the source of Deprat 's type material was not precisely indicated. Under these circumstances it seems best to reject the name as unrecognizable. Depratella Ozawa (1928, p. 9) decided that De- prat had included more than one genus in XeofusulineUa and erected a new genus for one of the later species de- scribed by Deprat as Xeofusulinella gi- ro urii. Ozawa gave almost no specific information about the form and as De- prat's description and illustration of the species are very poor, we must agree with Colani (1924, p. 25) that the in- ternal structure is not determinable and the species is insufficiently described. The size of the shell and the disposition of the inner volutions resemble those in Schubertella, with which it is tentatively listed as a synonym. One of Deprat 's figures (1915, pi. 1, fig. 7) gives a slight suggestion of keriotheca in the next to the last volution. Owing to the evident lack of discrimination in the original study of the genotype, it not only seems impossible to decide what the shell structure is like, but one cannot elimi- nate the possibility that Depratella gi- ro udi (Deprat) represents the imma- ture stage of a microspheric schwagerine or fusulinellid. Under such circumstances the genus is to be regarded as unrecognizable. Genotype of Fusulina Fischer In 1829, G. Fischer de Waldheim an- nounced the discovery of a new genus and species of fossils from the Carbo- niferous limestone at Mjatschkowa but did not describe or illustrate the form until 1837. At the latter time, he not only gave a formal introduction of Fus- ulina cylindrica but described another species which he called Fusulina de- pressa. The descriptive nature of these SYSTEMATIC REVIEW OF THE GENERA 91 names makes it impossible to suppose that Fischer 's specimens of F. cylindrica could have been the species of Staffella and Ozawainella that abound at Mjatschkowa. The obvious likelihood is that Fischer's specimens were the cylin- drical Fusulina which are abundant at this locality. Fischer may unwittingly have included specimens of the small ventricose fusulinellid or the fusiform species of Triticites, both of which are relatively scarce. Even granting this technical possibility, the problem can- not be settled except by means of indu- bitably authentic types, which seem not to exist. The obvious or commonsense solution is to consider the most common cylindrical species at the designated type locality as typical. Fortunately, the problem was settled in this logical way by Moller (1877, p. 142) who stated that F. cylindrica must be re- garded as the typical form. In 1878 (p. 51) he reiterated this, by inference placing F. depressa in synonymy with F. cylindrica. Whether the last act of placing this species in synonymy with F. cylindrica was justified or not, it clearly indicated the disposition of Moller who made the first critical study and emen- dation of this important genus and spe- cies. Moller 's nomenclatorial designa- tions and specimens become authorita- tive as the first and formal emendation of the species as long as authentic types remain unknown. Though Moller 's studies were ad- vanced and discriminating for his time, Tie made an error in the illustrations of his topotypical specimens that intro- duced a serious misconception of the true nature of Fusulina cylindrica Fischer. He erroneously illustrated his topotypes with a spiral wall composed of a thick, clear, and coarsely porous protheca with no tectorium and with chomata. A further circumstance that led to un- suspecting acceptance of Moller 's illus- trations of Fusulina cylindrica was his description and illustration of a number of species now identified with Triticites and Schwagerina s. s. not only as be- longing to the genus Fusulina but as having similar wall structure. Though Schellwien (1908, pi. 13, figs. 1, 2) reillustrated two of Moller 's topo- types of Fusulina cylindrica by photo- micrographs which clearly demonstrate a spiral wall structure composed of dia- phanotheca and tectorium, he appar- ently did not recognize the significance of his discovery. Nineteen years later, Lee (1927, pp. 22-24, 32-39) discussed at length his observations on the nature of Fusulina cylindrica from the type lo- cality at Mjatschkowa and the meta- types of Moller that were refigured by Schellwien, but he too failed to recog- nize the significance of this observation. Lee (1927, p. 24) proposed to recognize three subgenera of Fusulina — Girtyina, Schellwienia, and Schwagerina. It may be noted in passing that Lee assigned Girtyina as the subgenus containing the type species of the genus, which is ob- viously contrary to nomenclatorial prac- tice ; and, worse yet, the genotype of Girtyina Staff (Fusulina ventricosa Meek and Hay den) is a species belong- ing to "Schellwienia". Schellwienia Staff and Wedekind in turn was pro- posed originally by its authors as a sub- genus of Fusulina with F. cylindrica Fischer as the typical species — an ob- viously impossible procedure. Further- more, the authors arbitrarily placed a prior generic name, Triticites Girty, in synonymy with Schellwienia. This cha- otic state of the nomenclature was partly rectified by Dunbar and Condra in 1927, who clearly demonstrated that the names Girtyina and Schellwienia were invalid, but they continued to recognize Fusu- lina as of Moller and authors but not of Fischer s. s. The confusion introduced by Moller regarding the nature of Fusulina cylin- drica was not corrected until Dunbar and Henbest (1930), in a study of topo- types of F. cylindrica in the Yale col- lections from Mjatschkowa, showed, as Schellwien and Lee had previously dis- covered, that the spiral wall of F. cylin- drica is fusulinellid and not schwager- inid as Moller had indicated. These authors reorganized the classification of the Fusulininae to fit the requirements of the international code. This revision is now generally ac- cepted, with Silvestri (1935) alone dis- 92 PENN8YLVANIAN FUSULINIDAE senting. Silvestri's arguments have al- ready been discussed at length by Thompson (1936) and by Dunbar and Skinner (1937, pp. 562-563 and footnote p. 563). No further comment is needed here except to say that Silvestri's dis- covery and argument do not accord with the determinations of the first critical emendation of Fischer's work by M61- ler, which must obviously be accepted as authentic and authoritative, which is probable unless Fischer's type speci- mens are discovered and prove to differ significantly from Moller's metatypes. The nature of Moller's metatypes was demonstrated by Schellwien. In addi- tion to Schellwien 's studies of Moller's metatypes, studies of separate collec- tions of" topotypes by Lee (1927, pp. 22-24, 32-39), Dunbar and Henbest (1930), Thompson (1936), Henbest (1937), and Dunbar and Skinner (1937, p. 563, footnote) are in complete ac- cord as to the nature of Fusulina cylin- drical There is a collection (U. S. N. M. 24281) of topotypes in the U. S. Na- tional Museum that was received in ex- change from Alexander Pavlow, June 6, 1890. This material is typical white porous coquinoid limestone that contains an abundance of fusulines and is very closely similar to the material collected by Pirsson in the Yale collection studied by Dunbar and Henbest (1930). A number of sections have been made of specimens from Pavlow 's collection and they not only confirm the discoveries of others listed above, but we have been able to resolve fine pores in the spiral wall of some specimens of Fusulina cylindrica. These pores are very fine and traverse the diaphanotheca and the thin epithecal veneer. The wall struc- ture of these topotypes resembles that of our species of Fusulina from the Lons- dale limestone very closely and is dis- tinguishable at a glance from a schwa- gerinid wall. ADDENDUM While this work was being set in page proof, M. L. Thompson proposed four new genera of fusulines ("New Genera of Pennsylvanian Fusulinids", Am. Jour. Sci., vol. 240, pp. 403-420, 1942). Of these Miller ella (genotype, M. marblensis Thompson) is distinguished from Ozawainella by its minute size, its extremely short axis, and especially by the evolute growth of its outer whorls. Pseudo staff ella (genotype, P. need- hami Thompson) was proposed to in- clude part of the species currently em- braced in Staff ella, the latter genus be- ing restricted accordingly. This seems premature to the authors until the geno- type of Staffella can be critically re- studied. Waeringella (genotype, W. spiveyi Thompson) is distinguished from Wede- kindellina chiefly by the structure of its spirotheca, which is alleged to have only two or three layers instead of four. After studying some of the genotype material kindly presented by Dr. Thompson, we are not convinced that the distinction is well founded. Dunbarinella (genotype, D. ervinen- sis Thompson) includes a tribe of fusi- form shells possibly transitional from Triticites to Schwagerina. DESCRIPTION OF SPECIES The type specimens are deposited in the U. S. National Museum. Duplicate collections are preserved at the Illinois State Geological Survey and at Peabody Museum of Natural History, Yale Uni- versity. Fusulinella iowensis Thompson Plate 3, figures 10-25 Girtyina ventricosa Morningstar. Ohio Geol. Survey, 4th ser., Bull. 25, 1922, p. 153, pi. 6, fig. 4. Upper Mercer limestone, Muskingum County, Ohio. Fusulinella iowensis Thompson. Iowa Univ. Studies in Nat. Hist, vol. 16, 1934, pp. 296-297, pi. 20, figs. 28-30; Jour. Paleon- tology, vol. 9, 1935, p. 293. Cherokee shale, 90 feet below Whitebreast coal, Davis County, Iowa. Material studied — The material in- cluded many sections from the Seville limestone in northwestern Illinois (sta- tions 580, G 3 and G 7 ) and also syn- types from Iowa. Description — A small, obese species having 8 or 9 volutions at maturity, with a length of about 2.8 mm and a diameter of 1.8 to 2.0 mm. The ends are bluntly rounded and the lateral slopes slightly concave or nearly flat until nearly full grown, but there is a tendency to ex- tend the axis into polar nubs in the last two volutions, as clearly indicated by Thompson (1934, pi. 20, fig. 29). In weathering, however, the polar nubs are commonly lost and the shells appear sub- spherical or very bluntly ended. Well-marked dimorphism has been observed, but the microspheric and megalospheric shells differ little in ex- ternal appearance. In the megalo- spheric shells the proloculum is sub- spherical and ranges between 40 and 130 microns in diameter, averaging about 85 microns in 7 specimens from Illinois. The equatorial expansion of the first two volutions is commonly a little less rapid than that of the others. The form ratio changes but little during growth and is commonly between 1.5 and 1.7 at maturity, although it may be as low as 1.3 in the immature whorls which lack the slight polar extensions. The protheca of the proloculum is 9 to 11 microns thick, increasing gradu- ally to about 15 microns in the penulti- mate whorl. The epitheca is very mas- sive and extensive, filling one-half to three-fourths of the chamber space in the equatorial region and forming very massive chomata and a thick outer tec- torium. The inner tectorium, on the contrary, is thin and locally absent. Faint traces of mural pores have been observed but in the majority of speci- mens the structure of the diaphanotheca is obscure, this layer appearing as a nearly clear space between the more opaque tectoria. The septa are rather numerous, in- creasing gradually to 35 or more in the outer whorls. They are nearly plane except near the poles, where slight folds develop, especially in the eighth and ninth whorls. Septal pores have not been observed. The tunnel is narrow, high, and well defined by the massive chomata. The tunnel angle ranges commonly between 10° and 16°, varying considerably and irregularly in successive volutions of a single shell, but with little tendency to a systematic change. The greatest vari- ation appears to be due to constriction of the tunnel in places by the heavy epithecal deposits. A single, very perfect microspheric shell (specimen 3) was found at station G 7 and is shown on pi. 3, figs. 14, 15, and 25. Its measurements are given in the tabulation below. In this shell the proloculum has a diameter of 56 mi- crons, and is followed by an endothy- roid juvenarium of about l 1 /^ volutions which lies coiled at right angles to the axis of later whorls. This is followed first by a rapid change in orientation and then by the adoption of the fusi- form shape. The chambers of the first [93] 94 PENNSYLVANIAN FUSULINIDAE Measurements of F. iowensis Thompson Volution Half length Radius vector Form ratio 12 3 4 12 3 4 12 3 4 1 2 3 4 5 6 7 8 9 0.042 0.028 0.08 0.09 0.06 0.16 0.17 0.13 0.13 0.24 0.26 0.21 0.23 0.37 0.39 0.34 0.40 0.54 0.54 0.46 0.51 0.74 0.71 0.64 0.62 0.94 0.97 0.79 0.72 1.44 1.04 0.90 1.43 1.10 0.042 0.035 0.028 0.07 0.06 0.08 0.05 0.11 0.10 0.13 0.10 0.18 0.15 0.17 0.15 0.26 0.22 0.26 0.23 0.39 0.31 0.34 0.30 0.51 0.43 0.46 0.40 0.66 0.56 0.59 0.50 0.83 0.71 0.71 0.62 0.89 0.77 l'l" l.h" 0.7" '.'.'. 1.4 1.7 1.0 1.3 1.3 1.7 1.2 1.5 1.4 1.7 1.3 1.7 1.3 1.7 1.3 1.7 1.4 1.6 1.3 1.5 1.4 1.7 1.3 1.4 1.7 1.4 1.5 1.6 1.4 Tunnel angle Thickness of protheca Septal count : 1 2 3 4 12 3 4 5 6 1 2 3 4 5 6 7 8 9 '.'.'.'.'. '.'.'.'.'. "l6° "l2° 13° 13° 11° 11° 16° 14° 13° 11° 15° 14° 12° 9° 16° 20° 10° 12° 16° 12° 14° 13° 16° ...'.'. .'.'..'.' o!oio ..... 0.010 0.010 0.010 0.015 0.012 0.012 0.015 0.015 0.015 0.020 0.020 9? 10 18 15 20 19 25 20 32 26 36 30 36 34? 43? Specimens 1-6 are shown on plate 3 as figures 18, 17, 14, 23, 21, and 20 respectively. volution were obviously subspherical and typically endothyroid in shape. As indicated in the table of measurements, the later whorls agree well in size and proportions with those of the megalo- spheric form. The microspheric shells are obviously very rare. Discussion. — This is the oldest and the most common Fusulinella found in Illi- nois and in the northern mid-Continent region. It shows little resemblance to the Bend species F. llanoensis Thomas, which has fewer volutions, is more loosely coiled, less obese, and has less massive epitheca. The closest resemblance is to F. cadyi Dunbar and Henbest, n. sp., which agrees in size and shape. The latter, however, differs in the form of its ju- venile whorls, in the excessive massive- ness of its chomata, and in its deeper septal folds. Resemblance to F. biconica Ozawa is marked but that species has a larger proloculum and more rapid expansion than F. iowensis. The endothyroid ju- venarium of one of our specimens and the excessive size of the chomata strongly resemble the characters on which Lee based the genus Yangchienia. His description indicates the lack of tectoria and, if this is accepted, his genus may be distinguishable from Fusuli- nella, otherwise the characters indi- cated might be considered specific rather than generic. His genotype, Y. iniqua Lee, is more slender and elliptical than the species before us. The ventricose shape of Fusulinella iowensis has in the past led to confu- sion of this species with Fusulina gir- tyi Dunbar and Condra (formerly known as Girtyina ventricosa) . On the basis of their supposed identity and the supposed restriction of these ventricose fusulines to the Herrin or Brereton limestone, it has been assumed that an extensive overlap of Carbondale strata onto the Caseyville existed in the DESCRIPTION OF SPECIES 95 vicinity of Rock Island. A care- ful study of the stratigraphic section and a critical examination of the fusu- lines and other fossils clearly shows, however, that no such overlap exists. 1 Thompson has described the same species of Fusulinella from the lower and upper Mercer limestones in the Potts- ville group of Ohio. Distribution. — Fusulinella iowensis Thompson is one of the most common and characteristic fossils of the Seville limestone of northwestern Illinois. This limestone, which crops out in several places between Rock Island and Fulton counties, is believed to be equivalent to the limestone 90 feet below the White- breast coal in the adjacent corner of Iowa, from which Thompson secured the types of F. iowensis. Our good collec- tions are from stations 580, G3 and G7. The species occurs also in the upper Mercer, and less commonly in the lower Mercer limestone. This places its occur- rence near the top of the Pottsville group in Ohio. Fusulinella iowensis var. stouti Thompson Plate 3, figures 7, 8 (?), and 9 Fusulinella iowensis var. stouti Thompson. Jour. Paleontology, vol. 10, p. 676, pi. 90, figs. 5-11, 1936. Lower and upper Mercer and Boggs limestones, Muskin- gum County, Ohio. Material studied. — This discussion is based on a single good axial section from the Seville limestone at station G7. A single axial section from the Bosky- dell ( ? ) marine zone at station 248 re- sembles this but is too poorly preserved to be identified with certainty. Description and discussion. — The fine section from station G7 indicates an elongate-fusiform species, very slightly inflated at the middle and bluntly rounded at the ends. This specimen had 7% volutions and attained a length of 3.0 mm and a diameter of 1.3 mm. The following measurements were taken : 1 Wanless, H. R., Geology and mineral resources of the Alexis quadrangle : Illinois Geol. Survey Bull. 57, pp. 63-64, 1929. Measurements of F. iowensis var. stouti Thompson Volu- Radius Tunnel tion Half length vector angle 0.043 0.043 1 0.086 0.071 2 0.18 0.11 3 0.30 0.17 22° 4 0.49 0.24 18° 5 0.79 0.33 20° 6 1.08 0.47 18° 7 1.41 0.60 23° The septa are nearly plane across the middle of the shell and gently folded toward the ends. In this specimen their course was not quite parallel to the slice and the section gives the first im- pression that septal folding is much stronger than it actually is. By careful observation, however, it is easy to dis- tinguish the true septal loops from oblique sections of septa which cross the slice without being folded. The cho- mata are relatively heavy and broad. In its shape and moderate septal fold- ing this shell resembles primitive species of Fusulina, and it apparently is in a transitional stage of its evolution, but we regard it as still within the limits of Fusulinella. Possibly the same species occurs in the Bosky dell ( ? ) marine zone at station 248, an isolated outcrop of calcareous conglomerate in Pope County, Illinois. Only a few specimens were found there and they are all badly preserved. The best one is illustrated in figure 8 of plate 3. So far as its characters can be made out it has approximately the same size and shape and same number of volu- tions as the shell described above. Our best sections fall well within the limits of variation illustrated by Thompson in the types from Ohio. Occurrence. — Seville limestone at sta- tion G7 and possibly from the Bosky- dell (?) marine zone at station 248. Also in the lower and upper Mercer and the Boggs limestones in Muskingum County, Ohio. 96 PENN8YLVANIAN FUSULINIDAE Fusulinella gephyrea Dunbar and Henbest, n. sp. Plate 3, figures 1-6 Material studied. — A few rare speci- mens (two good sections) from the Se- ville limestone at station 580. Description and discussion. — Associ- ated with Fusulinella iowensis Thomp- son in the Seville limestone at station 580 were found a few specimens of much more slender form. The best two of these were photographed and then sec- tioned, one axially and the other sagit- tally. These constitute the chief basis for the following description. The holotype (figs. 1-3 of pi. 3) is fusiform, moderately inflated at the middle and extended at the ends to sub- acute poles. The axis in this specimen is arcuate, but that of the associated paratype is straight. The holotype had a length of 2.0 mm and a diameter of €.9 mm and was formed of 6% volu- tions. Its measurements are as follows : Measurements of F. gephyrea Dunbar and Henbest Volu- Radius Tunnel tion Half length vector angle 0.03 0.03 1 0.05 0.07 2 0.10 0.097 3 0.21 0.16 14° 4 0.36 0.23 12° 5 0.61 0.33 15° 6 0.90 0.44 14° The first paratype (figs. 4-6 of pi. 3) was 3.0 mm long and 1.17 mm in di- ameter and had a little more than 7% volutions. Its septa number 13, 16, 20, 26, 29, 33, 37 in the first 7 volutions respectively. The early volutions are typically fusu- linelloid, having nearly plane septa and massive, broad chomata. Moreover, they are thickly fusiform and bluntly rounded at the poles. The ends be- come rapidly extended in the last one or two whorls and in this extension strong septal folds are developed. In the outer volution these folds extend almost to the middle of the shell, becoming weaker, of course, toward the middle. The rapid increase in septal folding in the outer whorls gives these shells a transitional character from Fusulinella toward Fusulina and the name gephyrea was given in allusion to this fact (Gr. gephyra, a bridge). More material is needed to demon- strate the relation of this slender form to F. iowensis Thompson. The latter also shows considerable septal folding in the extended polar nubs of the outer whorls, and some specimens which we would assign to that species are some- what more slender than the figured types and suggest a possible gradation between F. iowensis and F. gephyrea. Distribution. — This rare form has been found only in the Seville lime- stone where it is associated with F. iowensis Thompson. The types are from station 580 in Warren County, Illinois. Fusulinella cadyi Dunbar and Henbest, n. sp. Plate 4, figures 20-28 Material studied. — About 30 speci- mens from three localities (stations 498, 466 and A6) were collected. Ten thin sections were made from this material. Description. — A thickly fusiform spe- cies of 8 or 9 volutions, attaining a length of about 2.6 mm and a thickness of 1.5 mm. In the outer volutions the poles are extended and the lateral slopes appear concave. There is a striking re- semblance to F. iowensis Thompson, but this species is a little more slender, its form ratio being 1.7 to about 2.0. In our limited collections of this spe- cies all the axial sections show an irregu- lar or spiral juvenarium. One (pi. 4, fig. 28) is definitely microspheric, with a proloculum only 28 microns in diameter and an endothyroid juvenarium of about l 1 /^ volutions of spheroid chambers coiled at right angles to that of the later whorls. The other axial sections (pi. 4, figs. 22-25) have only slightly larger prolocula and the ^'"zi solution is oblique and appears as an irregularly coiled cluster of subspherical chambers. DESCRIPTION OF SPECIES Measurements of F. cadyi Dunbar and Henbest 97 Volution Half length Radius vector Form ratio 1 2 3 1 2 3 1 2 3 1 2 3 4 5 6 7 8 9 0'l2 0.21 0.29 0.43 0.59 0.79 1.06 1.30 6" ii 0.18 0.34 0.53 0.71 0.94 6i08 0.19 0.27 0.43 0.64 0.017 0.017 0.014 0.06 0.04 0.09 0.08 0.07 0.13 0.10 0.11 0.19 0.17 0.17 0.27 0.25 0.24 0.34 0.34 0.34 0.49 0.47 0.46 0.63 0.60 0.60 0.77 1A 1.3 1.6 1.8 1 1.5 2.0 1 1.5 2.1 1 1.7 2.0 1 1.6 2.0 1.6 1.7 7 5 8 8 Volution Tunnel angle Thickness of protheca Septal count 1 2 3 1 2 3 4 5 1 2 3 4 5 6 7 8 9 ::: ;;: ir 14° 12° 10° 10° 13° 14° 14° 16° 14° 12° 13° 12° 14° 15° 0^015 0'015 '.'.'.'.'. 0.015 0.015 0.015 12 18 12 ? 20 26 20 32 25 40 35 42 35 ipecimens 1-5 are shown on plate 4 as figures 24, 22, 28, 26, and 27, respectively. These may be similar to the specimen shown in figure 28, differing in appear- ance chiefly because the plane of coil- ing of the juvenarium is at a large angle to, instead of coincident with, that of the slice. On the contrary, the sagittal section (fig. 26, pi. 4) indicates perfect bilateral symmetry from the start ; its proloculum has a diameter of about 115 microns. The protheca is thin as in F. iowensis, but the epitheca is much heavier, the chomata appearing in axial sections as solid deposits occupying more than half the height of the volutions and reaching laterally about half way to the poles. Because of this heavy secondary deposit the true form of the septa is somewhat obscured, but apparently they are nearly plane across the center of the shell and considerably folded near the poles. In the last volution the folding reaches nearly to the middle. The septa are rather abundant and increase from about 12 in the first or second volution to 35 or 40 in the sev- enth. No septal pores have been ob- served. In specimen A12 from station 498, stained with methylene blue, faint mural pores may be detected in places. The tunnel is narrow and somewhat un- even, as it is in F. iowensis. Discussion. — This species most resem- bles F. iowensis from which it differs in being somewhat more slender, having larger polar extensions, much heavier chomata and, apparently, more strongly folded septa. Although nearly all of our sectioned specimens have a spiral juvenarium, there are too few of these to indicate certainly that this is a spe- cific character. 98 PENNSYLVANIAN FUSULINIDAE Distribution. — This species has been found only in a thin limestone bed that lies 20-25 feet above the Harrisburg No. 5 coal at stations 466 and A6 in Wil- liamson County and at station 498 in Randolph County. The name Absher limestone was applied to this bed by the junior author at station 466. At all three localities F. cadyi is asso- ciated with two extremely small species of Fusulina, F. lucasensis Thompson, and F. levicula Dunbar and Henbest, n. sp. These fusulines are most com- mon at station 498. F. cadyi is the youngest species of Fusulinella thus far known in the mid- Continent region and eastern United States, but the genus ranges upward with Fusulina in the U. S. S. R. as high as the top of the Moscovian. Wedekindellina euthysepta (Henbest) Plate 8, figures 1-23; plate 9, figures 1-4 Fusulinella euthusepta 2 Henbest, Jour. Pale- ontology, vol. 2, 1928, pp. 80-81, pi. 8, figs. 6-8, pi. 9, figs. 1, 2. Stonefort lime- stone, station 370, Williamson County, Illinois. Wedekindella euthysepta Dunbar and Hen- best, Am. Jour. Sci., vol. 20, pp. 357-364, 1930. (F. euthysepta Henbest desig- nated as type species of new genus.) Wedekindia euthysepta Dunbar and Henbest, Am. Jour. Sci., vol. 21, p. 458, 1931. (The name Wedekindella preoccupied in ob- scure footnote by Schindewolf for ceph- alopod. New name Wedekindia pro- posed.) Wedekindellina euthysepta Dunbar and Hen- best, in Cushman, Foraminifera, etc., Cushman Lab. Foram. Research, Spec. Pub. 4, p. 134, key plate 10, figs. 13-15, 1933. (Second name also preoccupied by generic name proposed in obscure footnote. Third new name proposed.) Wedekindellina euthysepta Thompson, Univ. Iowa Studies, vol. 16, pp. 282-285, pi. 20, figs. 1, 2, 7, 9, 12, 13, 17, 22, 24-27, 1934. Cherokee shale, 35 feet below White- breast coal, Lucas and Monroe counties, Iowa. Wedekindellina dunbari Thompson, Univ. Iowa Studies, vol. 16, pp. 285-287, pi. 20, figs. 3, 6, 15, 16, 20, 21, 1934. Cherokee shale, 35 feet below Whitebreast coal, Lucas and Monroe counties, Iowa. 2 Transcription from the Greek should have been euthy. The spelling was corrected to euthysepta by Dunbar and Henbest in 1930. Material studied. — Many specimens were collected from the Stonefort lime- stone and from a marine zone above Colchester No. 2 coal. More than 50 thin sections were made. Description. — This species develops 8 to lO^ volutions and attains a length of about 4.0 mm and a diameter of 1.0 mm, the form ratio being generally near 4.0. It is distinguished by its slender form, straight axis, and evenly tapering and neatly pointed ends. The meridi- onal furrows are generally nearly straight, paralleling the axis, and the antetheca is singularly free of septal folds. The proloculum is very small and commonly oval as indicated by the di- ameters measured in seven typical speci- mens, as follows : 0.040 mm, 0.042 by 0.047 mm, 0.052 by 0.062 mm, 0.048 mm, 0.076 mm, 0.045 mm, and 0.050 mm. The shell expands slowly and gradually and, although the axis of the first volu- tion is occasionally not precisely that of later whorls, we have seen no distinct endothyroid juvenarium. The slender fusiform shape is attained at an early stage and maintained thereafter, the form ratio increasing gradually from about 2 in the early volutions to about 4 at maturity. It is not feasible, how- ever, to divide the ontogeny into distinct stages. The protheca is very thin in the early whorls but thickens to about 15 microns in the mature part of the shell. The diaphanotheca commonly appears struc- tureless even where associated textular- ians show distinct structure, but by care- ful microscopy a porous structure can be determined (pi. 8, figs. 22 and 23). The junior author made a careful search for porosity at three different times and was able to demonstrate its presence only after assembling a highly corrected optical system. The dark lines appear- ing in the photomicrographs on plate 8 are evidently slender pores, and it is noteworthy that they pass through the tectoria as well as the diaphanotheca. The epitheca is strongly developed, appearing as tectoria on the spiral wall and as filling of the chambers in the axial region. The tectoria equal or ex- DESCRIPTION OF SPECIES Measurements of W. euthysepta (Henbest) 99 Volution Half length Radius vector Form ratio 12 3 4 12 3 4 12 3 4 1 2 3 4 5 6 7 8 9 10 0.028 0.028 0.029 0.07 0.06 0.057 0.23 0.16 0.13 0.37 0.29 0.27 0.53 0.40 0.43 0.71 0.60 0.64 1.01 0.74 0.81 1.30 1.10 1.16 1.71 1.44 1.43 2.14 1.71 1.85 2 14 0.028 0.035 0.017 0.020 0.04 0.057 0.035 0.04 0.06 0.09 0.05 0.06 0.10 0.13 0.08 0.08 0.14 0.17 0.11 0.12 0.19 0.23 0.17 0.16 0.24 0.31 0.19 0.22 0.32 0.40 0.24 0.29 0.41 0.50 0.33 0.36 0.50 0.60 0.41 0.46 0.53 l.Y' '.'.'.'.'. 1.7" ll3" 2.6 2.2 3.7 3.0 3.3 3.8 ..... 3.4 3.6 3.7 3.5 4.0 4.2 3.9 3.7 4.1 4.5 4.0 4.1 4.3 4.0 4.3 4.1 4.0 4.0 11 0.66 Tunnel angle Wall thickness Septal count 12 3 4 12 3 4 5 6 7 1 2 20° 13° .... 0.010 0.005 0.007 0.007 0.007 0.010 10 10 10 11 13 13 3 4 5 6 7 8 9 10 19° 15° 20° 20° 22° 17° 19° 20° 25° 19° 17° 19° 21° 21° 14° 19° 20° 20° 15° 16° 19° 19° 15° 17° 16° 20° 17° 0.015 0.015 0.017 0.015 0.015 0.020 0.020 0.015 0.015 0.025 0.025 0.020 0.030 0.020 0.020 0.035 0.025 0.020 0.025 14 14 15 19 16 16 20 21 18 20 22 22 24 24 22 • 25 27 25 26 ? 29 30 ? ? Specimens 1, 2, 4, and 5 are illustrated on plate 8 as figures 15, 12, 14, and 18, respectively; specimens 3, 6, and 7 are shown on plate 9 as figures 1, 4, and 3, respectively. Specimen 1 is the holotype. Half axial lengths are not given for specimen 2 because it is somewhat oblique and appears shorter and blunter than it should. ceed the diaphanotheca in thickness. The chomata are well developed and slope away from the tunnel to merge with the outer tectorium. The axial deposit com- monly fills completely the chambers along the axis from near the middle to the ends. The septa are entirely plane except near the poles where they are somewhat irregular or very feebly folded. Septal pores are abundant in the outer whorls as shown in plate 9, figure 2. These pores are 10 to 12 microns in diameter. One exceptionally well preserved speci- men (pi. 8, figs. 6 and 21) shows a con- centration of such pores in a single row along the base of the antetheca for a considerable distance across the middle of the shell but toward the ends the septal pores are normally distributed. The tunnel is narrow and rather high, appearing elliptical rather than slit-like in axial sections. The tunnel angle does not vary greatly during growth and is commonly between 19° and 25°. Discussion. — The axial section origi- nally figured by Henbest (1928, pi. 8, fig. 6) is here designated the holotype of this species ; the other specimens orig- inally figured are paratypes. Of the ten American species and vari- eties referred to this genus, W. euthy- septa is one of the largest, being slightly exceeded by W. ellipsoides, n. sp., and W. henbesti (Skinner). The types of the latter are illustrated on plate 9 to per- mit comparison with W. euthysepta. It may be noted that an adult specimen of W. henbesti with only 10 volutions 100 PENN8YLVANIAN FUSULINIDAE (pi. 9, fig. 8) exceeds in size a mature shell of W. euthysepta having 11 volu- tions (pi. 9, fig. 2). Furthermore, the axial filling is less extensive in W. hen- besti and the septa are distinctly folded in the end zone of the outer volutions. W. dunbari Thompson was distin- guished on the basis that it is smaller and differs in ontogeny from W. euthy- septa, but we cannot confirm these ob- servations. The types of W. dunbari had only about 8 volutions and agree well with submature specimens of W. euthysepta, having the same number of volutions. Thompson stated that the ratio of diameter to length decreases steadily in successive volutions of W. dunbari but in W. euthysepta decreases rapidly until the seventh whorl and then increases; but in view of the fact that Thompson's types had only 8 volutions there is no disagreement with corres- ponding volutions of W. henbesti. Neither W. excentrica (Roth and Skinner) or W. coloradoensis (Roth and Skinner) or their varieties are as slen- der or as acutely pointed as W. euthy- septa. W. ultimata Newell and Keroher is somewhat larger, relatively thicker, and blunter at the poles ; its proloculum is about twice as large, its septa show more folding in the end zone, and its axial filling is much less extensive than that of W. euthysepta. The other Amer- ican species are much smaller. Age and distribution. — Originally known only from the Stonefort lime- stone (stations 237, 250, 370, 371), this species has recently been found in a limestone outcropping south of Mur- physboro, Jackson County, Illinois (sta- tion Bl), which is probably near the same age as the Stonefort. This species is also abundant in the dark, highly carbonaceous marine zone above the Col- chester No. 2 coal at station E9, Madi- son County, at station 581, Greene County and station G2, Adams County. A single specimen was found in the Sea- horne limestone at station G5 and a fragment of another, doubtfully identi- fied, was found in presumably the same horizon at station B3. Since this species was originally described, examples have been found in Oklahoma, Kansas, Colo- rado, New Mexico and Iowa. It appar- ently ranges through the equivalent of two or three cyclothems in southeastern Kansas in the Cherokee group, accord- ing to collections recently studied by the junior author. W. euthysepta seems everywhere to be associated with fusulines of upper Tradewater and lower Carbondale age, and though possibly ranging through two or three cyclothems, it is probably a good indicator of that position. Rauser-Chernoussova (1935) has shown that in the Ural region the genus is restricted to the uppermost division of the Moscovian, a position somewhat higher than the chief zone of Wedekin- dellina in America. The recurrence of the genus in W. ultimata Newell and Keroher in the base of the Missouri series near Kansas City is, however, slightly younger than the top of the Moscovian. Newell and Keroher found that W. ultimata is more like the Mos- covian species W. uralica Doutkevitch and W. doutkevitchi in its stage of evo- lution than it is like W. euthysepta. Wedekindellina minuta (Henbest) Plate 10, figures 1-6 Fusulinella minuta Henbest, Jour. Paleon- tology, vol. 2, 1928, p. 81, pi. 8, figs. 2-5. Stonefort limestone, station 370, Wil- liamson County, Illinois. Material studied. — Only a few speci- mens were collected from three localities in the Stonefort limestone. Only one really good axial and two sagittal sec- tions were prepared. Specimens of this species are so rare that a broader sur- vey of the species cannot be undertaken at the present time. When originally described, the specimens were thought to be sufficiently distinct to require a special name even though only a few could be found. Description. — The shell is very minute and somewhat cylindrical, consisting of 5 to 6 volutions. The ends are blunt or truncated. The length of the holotype is 1.28 mm and diameter 0.32 mm; ac- cordingly, the form ratio is 1 :4.3. The proloculum varies in shape, and even though it is large in proportion to the size of the shell, in comparison with DESCRIPTION OF SPECIES 101 other fusulines it is minute. In three specimens, the sizes of prolocula are 0.036 by 0.047 mm, 0.04 by 0.05 mm, and 0.05 by 0.08 mm. The height of the tunnel is about two-fifths to one-half its width. The angular width is rather small. The protheca is thin. In the proloculum, the protheca is 0.003 to 0.006 mm thick and in the last whorl 0.008 to 0.012 mm. The diaphanotheca appears to be structureless even at high magnifications. The epitheca is much thicker than the protheca throughout the shell and is especially massive on the floor of the chambers. Its thickness in- creases toward the poles, but in this spe- cies the axial zone is not completely filled with this secondary deposit. In general, the epitheca is at least two to three times the thickness of the protheca. Probably less than one-half the total space enclosed by the shell was avail- able for sarcode space. Chomata are broad and have only a little of the levee- like appearance. The septa are not plicated. Their trend is oblique at the polar zones which may give a false ap- pearance of plication. The existence of septal pores is quite uncertain in the specimens at hand but it is likely that they do exist. The axial section of the holotype has a total length of 1.2 mm and a diameter of 0.32 mm. Its proloculum is elliptical in section and measures 36 by 47 mi- crons. It is illustrated on plate 10 as figures 1 and 4. It was measured as follows : to this species or may be a young indi- vidual of W. euthy septa (Henbest) is illustrated by figures 3 and 6 of the same plate. These are slides O and A respectively from station 370. They give the following measurements: Measurements of W. minuta (Henbest) (?) Radius vector Septal count Volu- tion Slide O Slide A Slide O Slide A 1 0.05 0.10 10 14 2 0.08 0.13 13 16 3 0.10 0.17 16 17 4 0.13 0.23 19 18 5 0.17 0.28 19 21 6 0.34 ? 21 Discussion — If the types of this spe- cies be adult it is distinguished by its minute size. It resembles the young of the associated W. euthysepta in many features, but is more slender, more nearly cylindrical, and has blunter ends. More material is needed to prove whether it is a valid species but we retain it ten- tatively until such is discovered. Age and distribution. — W. minuta has been found only in the Stonefort lime- stone in Saline and Williamson coun- ties where it is associated with W. euthy- septa, Fusulina novamexicana, Polytaxis sp.,Tetrataxis sp., Endothyra sp., Textu- laria sp., etc. Stations 250, 370, and 371. Measurements of the holotype of W. minuta (Henbest) Volu- Radius Form Tunnel tion vector Half length ratio angle 1 0.035 0.086 2.5 2 0.055 0.186 3.0 16° 3 0.08 0.30 3.8 22° 4 0.11 0.46 4.2 23° 5 0.15 0.64 4.3 19° The first paratype is a sagittal section with nearly 6 volutions, having a proloc- ulum 70 microns in diameter. It is illus- trated as figures 2 and 5 of plate 10. A second sagittal section which may belong Wedekindellina ellipsoides Dunbar and Henbest, n. sp. Plate 9, figures 9-14 Material studied. — This species is based on two specimens from a marine zone over Colchester No. 2 coal at sta- tion 581 in Greene County. After ex- ternal photographs were taken, the holo- type was cut to an axial section and the paratype to a sagittal section. Description. — The shells are short, thick, bluntly rounded at the ends, and evenly elliptical in axial profile. The holotype has a length of 4 mm and a diameter of about 2.3 mm, the form ratio at maturity being 1.7. The large 102 PENNSYLVANIAN FUSULINIDAE number of volutions is remarkable, the holotype having 14 and its paratype about 12i/ 2 . The proloculum is minute, having a diameter of 56 microns in one type and 84 microns in the other. The volutions increase gradually in height but are less tightly coiled than in other species of this genus. The elliptical form is at- tained in the earliest volutions and main- tained throughout growth. Moreover, there is little change in the form ratio after the fourth volution. The tunnel is about half as wide as high and extremely narrow, its angle measuring between 9° and 12°. The walls are thin, the protheca being about 8 microns thick in the proloculum of the paratype and 10 to 15 microns in the later whorls. The epitheca assumes the form of well denned tectoria, and of chomata, as well as a secondary filling of the chambers unequalled in extent in any other species of the genus. Only the chambers of the last one or two volu- tions are open to the ends and the inner whorls are partly open only near the middle of the shell. So massive is this deposit that it combines with the cho- mata, obscuring their form in the inner whorls. The holotype axial section (pi. 9, fig. 11) gives the following measurements: Measurements of W. ellipsoides Dunbar and Henbest Volu- Radius Form Tunnel tion Half length vector ratio angle 1 0.05 0.05 1.0 2 0.10 0.08 1.2 3 0.16 0.12 1.3 4 0.28 0.16 1.7 5 0.44 0.21 2.1 6 0.56 0.28 2.0 7 0.70 0.35 2.0 '9° 8 0.89 0.46 1.9 9 1.13 0.57 2.0 '9° 10 1.29 0.67 1.9 9° 11 1.46 0.80 1.8 11° 12 1.64 0.94 1.7 10° 13 1.88 1.08 1.7 12° 14 2.08 10° The paratype sagittal section (pi. 9, figs. 12 and 13) has the following septal count in the first 12 volutions respec- tively: 10, 15, 19, 21, 23, 25, 29, 34, 37?, 43?, 42, and 49. The septa are plane and nearly paral- lel to the axis. No definite evidence of septal pores was seen but this is hardly surprising as the thick epitheca would cover and fill them if present, except in the outer volution, and our single axial section does not clearly show the septa in this volution. Discussion. — The shell structure is in many respects like that of W. euthy septa (Henbest) and the generic relations are clear in spite of the unusual shape of this species. A comparison of these two species should leave no doubt of the validity of the genus Wedekindellina. The new species is distinguished by its thickly elliptical profile, its many vo- lutions, and its very heavy axial filling. Its nearest resemblance is seen in W. magna (Roth and Skinner) from the McCoy formation in Colorado, but that species is more slender, has fewer volu- tions, a wider tunnel, and its septa in- crease less rapidly in successive whorls. Age and distribution. — The two known specimens were found by Mr. T. A. Hen- dricks at station 581 in Greene County. The horizon is a marine zone of dark gray to black, calcareous shale above the Colchester No. 2 coal. Here it was asso- ciated with W. excentrica (Roth and Skinner) ? and a few species of Tetra- taxis, and Bigenerina or Climacammina. Wedekindellina excentrica (Roth and Skinner) ? Plate 7, figures 13, 14 Fusulinella euthy septa Henbest (part), Jour. Paleontology, vol. 2, 1928, plate 9, fig. 5 (not pi. 8, figs. 6-8, or pi. 9, figs. 1, 2). Stonefort limestone, station 370, Wil- liamson County, Illinois. ? Wedekindella excentrica Roth and Skinner, Jour. Paleontology, vol. 4, 19S0, pp. 340- 341, pi. 30, figs. 1-3. McCoy formation, near McCoy, Colorado. Discussion. — In our collection from station 581 there is a specimen (pi. 7, fig. 14) which we refer with some un- certainty to this western species. It has 12 volutions and was rather thickly fusi- form, its axial profile being elliptical DESCRIPTION OF SPECIES 103 and almost intermediate in form between that of W. euthy septa (Henbest) and that of W. ellipsoides Dunbar and Hen- best, n. sp. It was originally about 5 mm long and 1.7 mm in diameter, hav- ing a form ratio near 3.0. Although as- sociated with W. ellipsoides, it is much more slender than the types of that spe- cies and has much less axial filling. This specimen was found in a marine zone above the Colchester No. 2 coal at station 581 in Greene County, Illinois. A single cross-section, slightly excen- tric (pi. 7, fig. 13) from the Stonefort limestone at station 250 in Saline Coun- ty, Illinois, may represent the same species. It has more than 12 volutions but much lighter axial filling than W. ellipsoides. Other doubtfully identified specimens were found at stations 371 and E9. Fusulina lucasensis Thompson Plate 4, figures 1-lla, 29, 30 Fusulina lucasensis Thompson, Iowa Univ. Studies, vol. 16, no. 4, p. 309, pi. 22, figs. 2, 9, 12, 17, 19, 1934. Upper Cherokee shale, in a limestone 10 feet below the Mystic coal, Lucas County, Iowa. Material studied. — Collections include a dozen cotypes from Iowa ; a few speci- mens from the Absher limestone at sta- tion 466 and A6 ; numerous specimens from station 498, probably Absher lime- stone ; and a single good specimen from the Brereton limestone at station 528. About 20 sections were made. Description. — An extremely minute fusiform species. The type collection includes shells of 6 or 7 volutions, the latter attaining a length of about 3.0 mm and a thickness of 1.25 mm ; but the majorhy of shells have only 5 or 6 whorls and are little over 2 mm long and 1 mm thick. The lateral slopes are con- vex and the axial profile subelliptical. The form changes only slightly during growth, the form ratio being 1.2 to 1.8 in the second whorl and 2.0 to 2.4 at maturity. The proloculum is commonly between 40 and 80 microns in diameter and is subspherical. The shell is tightly coiled and its spiral wall is very thin, ranging from about 10 microns in the second to 25 or 30 microns in the fifth whorl. In very thin sections it can be seen to con- sist of a thin protheca covered with epi- theca, the outer tectorium being dis- tinctly thicker than the inner. The septa are numerous for a shell of such minute size, increasing generally from about 10 in the first whorl to 25 or 30 in the outer whorls. They are thin (not thick as stated by Thompson) and are deeply and regularly folded so that in axial sections the septal loops appear numerous and high. The tunnel angle ranges commonly between 20° and 30° with no very definite systematic change during growth. The chomata are well defined but narrow ridges. Septal pores are present but easily overlooked. Discussion. — This is the smallest spe- cies of Fusulina recognized in Illinois and one of the smallest ever described. The identity of the species in Illinois was at first overlooked because Thomp- son's illustrations were on a larger scale than those of associated species and its minute size was not appreciated. A col- lection of numerous syntypes presented to the senior author by Mr. Thompson enabled us to make direct comparison with the Illinois material. Two of these syntypes are illustrated on plate 4 and appear in the table of measurements given above. Distribution. — In Iowa this species is only known 10 feet below the Mystic coal in a limestone believed to be equiva- lent to the St. David limestone of west- ern Illinois. In its type locality no other species of fusulines were found associated. In Illinois the species was found in three localities in the Absher limestone (stations 498, 466, and A6), and at one locality (station 528) in the Brereton limestone. At all three locali- ties in the Absher horizon it is associ- ated with Fusulinella cadyi Dunbar and Henbest, n. sp., and Fusulina levicula Dunbar and Henbest, n. sp. 104 PENNSYLVANIAN FUSULINIDAE Measurements of F. lucasensis Thompson Volution Half length Radius vector Form ratio 12 3 4 12 3 4 12 3 4 1 2 3 4 5 6 0.029 0.036 0.039 0.03 0.07 0.07 0.07 0.10 0.13 0.16 0.15 0.19 0.27 0.37 0.31 0.31 0.50 0.60 0.47 0.46 0.73 0.87 0.70 0.71 1.0(?) 1.01 1.04 0.03 0.03 0.039 0.03 0.07 0.05 0.07 0.07 0.11 0.09 0.12 0.12 0.15 0.16 0.17 0.18 0.23 0.24 0.26 0.26 0.33 0.37 0.36 0.39 0.46(?) 0.46 0.53 i!6" '.'.'.'.'. 1.0" ....'. 1.2 1.8 1.2 1.6 1.8 2.3 1.8 1.8 2.1 2.5 1.9 1.8 2.2 2.4 2.0 1.8 2.2 2.0 Tunnel angle Wall thickness Septal count 12 3 4 12 3 4 5 6 7 1 2 '.'.'.'.'. "25° ....'. ..... 0.011 0.007 0.011 10 11 10 14 13 15 3 4 5 6 28° 20° 17° 22° 24° 19° 21° 27° 34° 23° 19° 27° 27° 25° 0.020 0.017 0.018 0.022 0.026 0.017 0.020 0.017 0.026 0.030 16 18 20 19 24 22 26 26? Specimens 1-6 are illustrated on plate 4 as figures 5, 4, 29, 30, 7, and 8, respectively. Fusulina levicula Dunbar and Henbest, n. sp. Plate 4, figures 12-19 Material studied. — Collections in- cluded about a score of specimens from three localities (stations 498, 466, and A6) ; about a dozen sections were made. Description. — A minute species of rather thickly fusiform shape. Our best specimens, from station 498, were washed free of matrix and are mostly imma- ture. The largest of these has 6 volu- tions and a length of 2.8 mm and a di- ameter of 1.4 mm; but we have three sections showing 8 or 9 volutions and indicating a shell about 5.0 mm long and 2.0 mm in diameter. The form ratio changes but little during growth and is commonly near 2.0, ranging be- tween 1.8 and 2.6 in the measured types. The proloculum is of medium size and the whorls expand with a gradual ac- celeration. The wall is of moderate thickness, the protheca being very thin in the first volution and increasing rather gradually to a maximum of about 20 microns in the penultimate whorl. In the first 3 or 4 volutions the septa are almost plane but in the remaining whorls they are rather strongly folded even to the middle. The tunnel angle varies irregularly between 15° and 20°, or rarely a little more. Chomata are well developed but rather narrow. Sep- tal pores are abundant in the end zones of the outer 2 or 3 volutions. Discussion. — This species is distin- guished by its small size and its on- togeny, the first 3 or 4 whorls being typically fusulinelloid with plane septa and broad chomata, whereas the later whorls are typically fusulinoid. It is larger and much thicker than the asso- ciated F. lucasensis Thompson. It agrees closely with F. pumila Thompson in size and proportions and may prove to be identical with that species. Thompson did not mention the fusulinelloid charac- ter of the early volutions and his sec- DESCRIPTION OF SPECIES Measurements of F. levicula Dunbar and Henbest 105 Volution Half length Radius vector Form ratio 12 3 4 12 3 4 12 3 4 2 3 4 5 6 7 0.070 0.21 0.23 0.10 0.27 0.34 0.37 0.21 0.47 0.50 0.61 0.36 0.69 0.77 0.94 0.50 0.91 1.15 1.35 0.67 1.43 1.85 0.90 1 . 30 0.064 0.042 0.070 0.10 0.11 0.07 0.13 0.16 0.14 0.11 0.21 0.25 0.24 0.17 0.31 0.41 0.36 0.25 0.44 0.61 0.53 0.34 0.60 0.80 0.66 0.47 . 64 2!i" 2!6'" ia" 2~0 " 2.1 2.6 1.9 2.2 2.0 2.5 2.1 2.2 1.8 2.6 2.0 2.0 1.8 2.5 1.9 1.8 2.6 1.9 2.0 8 1.71 0.81 2.0 9 2 . 72 Tunnel angle Wall thickness Septal count 12 3 4 1 2 5 1 2 3 4 5 6 22° '.'.'.'.'. '.'.'.'.'. "l7° 18° 17° 16° 20° 19° 15° 23° 16° o!o2i '.'.'.'.'. 0.028 0.042 0.025 . 030 12 19 24 26 30 7 16° . 035 8 19° 0.017 Specimens 1-5 are illustrated on plate 4 as figures 15, 16, 19, 14, and 17, respectively. tions do not distinctly show it ; however, this character is seen best in thick axial sections or slices tangential to the pro- loculum and may be overlooked in well- centered thin sections. The two axial sections figured by Thompson appear much shorter and blunter than our form, but if the poles be restored the resem- blance is close, as suggested by the pro- portions measured by Thompson. The septa appear to be less intensely folded in the Iowa form. Distribution. — This species has been found only in a thin limestone bed that lies 20-25 feet above the Harrisburg No. 5 coal in Saline and eastern Williamson counties at stations 466 and A6 and in a limestone of apparently similar age at station 498, Randolph County, Illi- nois, where it is most common. This limestone above coal No. 5, identified as the Absher limestone by the junior au- thor, lies within the upper 90 feet of the Carbondale group. F. levicula is associated with Fusulin- ella cadyi n. sp. and Fusulina lucasensis Thompson. Fusulina spissiplicata Dunbar and Henbest, n. sp. Plate 7, figures 1-12 Material studied. — This species is based upon about a score of specimens, of which eight were sectioned, from a single locality (station E9) in a thin limestone overlying the Colchester No. 2 coal. Description. — A very small, evenly fusiform species with gently convex lat- eral slopes and neatly pointed poles, having 7 or 8 volutions and attaining a length of about 4 mm and a diameter of 1.0 to 1.25 mm. All but one of our sectioned specimens are typically megalospheric, with pro- locula ranging between 80 and 100 mi- 106 PENNSYLVANIAN FUSULINIDAE Measurements of F. spissiplicata Dunbar and Henbest Volution Half length Radius vector Form ratio 12 3 4 12 3 4 12 3 4 1 2 3 4 5 6 7 8 0.05 0.042 0.016 0.11 0.13 0.16 0.05 0.21 0.18 0.29 0.09 0.33 0.46 0.46 0.16 0.46 0.67 0.69 0.30 0.80 1.07 1.06 0.47 1.19 1.44 1.44 0.63 2.01 1.08 0.05 0.042 0.016 0.08 0.07 0.07 0.04 0.12 0.11 0.11 0.07 0.17 0.16 0.16 0.10 0.24 0.22 0.24 0.16 0.33 ,0.29 0.32 0.21 0.45 0.40 0.44 0.31 0.54 0.57 0.46 0.60 1*2" l'.7" 2^2" i!2" 1.7 1.6 2.6 1.2 1.9 2.8 2.8 1.6 1.9 3.0 2.9 1.8 2.4 3.6 3.1 2.2 2.6 3.6 3.2 2.0 3.7 2.3 Tunnel angle Wall thickness Septal count 12 3 4 1 2 3 4 5 1 2 3 4 5 18° 18° 16° 20° 16° 17° 15° 21° 17° 22° 17° 20° 22° 23° 0.012 0.008 0.020 0.015 0.020 0.010 0.020 0.018 0.020 0.025 0.020 10 19 20 23 26 6 7 24° 24° 31° 32° 25° 29° 27° 0.020 0.030 0.030 0.030 0.020 Specimens 1-5 are illustrated on plate 7 as figures i, 5, 8, 12, and 6, respectively. crons in diameter, but a single shell (pi. 7, fig. 12), is typically microspheric, having a proloculum of irregular shape, 30 by 42 microns in diameter, followed by a full volution of minute spheroidal chambers coiled at right angles to the ensuing fusiform whorls. This is speci- men number 4 in our table of measure- ments. In the megalospheric shells the whorls are bilaterally symmetrical and rather low, increasing with some acceleration in the outer volutions. The antetheca in- creases in height to the poles and the form ratio increases gradually, from about 1.6 or 1.7 in the second to 2.5 or even 3.0 or more in the last. Speci- men 2 (pi. 7, fig. 5) appears to be ab- normally long on the end measured (left). The wall is rather thin, the diaphano- theca attaining a maximum of about 10 microns in thickness in the outer whorls and the tectoria adding; a somewhat greater deposit to give the entire wall a thickness of 20 to 30 microns. In two specimens, fine mural pores may be de- tected in the diaphanotheca. Septa and chomata show a marked ontogenetic change, best seen in thick sections such as figure 4 of plate 5. The first 3 or 4 volutions are typically fusu- linellid, with nearly plane septa and broad, heavy, ridge-like chomata. Sep- tal folds begin to appear in the ends of the next volution and spread to the cen- ter of the shell in the last two whorls. Meanwhile, the chomata become narrow and spread as a thickening upon the septa near the tunnel. The tunnel is of moderate width, the tunnel angle ranging generally between 15° and 25° but rising in some individ- uals to 30° or 32° in the outer whorls. Septal pores are present in the end zones of the outer whorls but are easily overlooked because of the strong septal folding. DESCRIPTION OF SPECIES 107 Discussion. — The largest of the whole specimens, illustrated in figure 2 of plate 7, was sectioned and is illustrated in axial section as figures 3 and 4. The section was purposely left thick to show the character of the septa. This makes it appear different from the thinner sec- tions which are more open. Both ex- ternal appearance and statistical meas- urements indicate, however, that the shells figured are conspecific, with the possible exception of the one in figure 5 which is somewhat larger and relatively longer than the rest. It, like the others, shows marked fusulinellid characters in its early whorls. The microspheric individual is par- ticularly interesting. Unfortunately, both poles have suffered abrasion so that, before sectioning, the shell ap- peared thickly elliptical and was mis- taken for W edekindellina ellipsoidalis ; but the shape of all the preserved whorls indicates a shell of elongate-fusiform proportions. The identity of this speci- men is, of course, not quite certain, but if allowance be made for its small pro- loculum, and if the measurements of volutions 4 to 8 be compared with those of volutions 3 to 7, respectively, in the other shells, the agreement is close. More- over, it is associated with numerous megalospheric specimens of this species and with no other fusulines to which it could reasonably be referred. The ontogeny resembles that of F. leei Skinner and F. pumila Thompson, indi- cating a primitive stage of development for the genus, but F. spissiplicata is much smaller and more delicate than either of these genera at all stages of growth. The name (L., spissus, dense, com- pact) refers to the densely crowded sep- tal folds. Distribution. — This species is common in the thin carbonaceous and pyritifer- ous limestone above the Colchester No. 2 coal at station E9 in Madison County, Illinois. Here it is associated with W edekindellina euthy septa (Henbest) and W. excentrica Roth and Skinner ( ?). Fusulina pumila Thompson Plate 5, figures 9-21 Fusulina pumila Thompson, Iowa Univ. Studies, vol. 16, no. 4, p. 313, pi. 22, figs. 6, 8, 10, 11, 1934. Material studied. — Numerous speci- mens were collected from two localities (stations B3 and 452) in southwestern Illinois, and numerous poorly preserved specimens from a single locality (station Fl) in northwestern Illinois. Ten slides were prepared. Description. — A small, ventricose spe- cies of 8 to 9 volutions, attaining an average length of about 4.0 mm and a thickness of 2.0 mm. The poles tend to be slightly extended and neatly pointed, the lateral slopes being slightly concave, at least on one side. The form ratio is near 2.0 and shows little change during growth after the third volution. The proloculum is commonly between 100 and 120 microns in diameter and is subspherical. The first 3 or 4 volutions are fusulinelloid, with nearly plane septa and relatively broad, massive cho- mata; but plications begin in or near the fourth whorl and in the fifth reach to the middle of the shell. Thereafter the folding is rather strong, reaching nearly to the top of the septa, and op- posed folds meet near the base. The tunnel is narrow, its angle varying some- what irregularly between 15° and 20° (rarely more), with no definite or sys- tematic change during growth. Through- out all volutions the chomata are mas- sive and wider than the tunnel, a feat- ure that will aid in distinguishing this from later species of similar shape and larger size. Commonly the chomata are half to three-fourths the height of the free chambers and further constrict the chambers by, extending high on the septa. The septa are numerous and rather closely spaced, increasing from about 10 in the first volution to more than 30 in the sixth. Septal pores occur in the end zones of the outer whorls but are not conspicuous. 108 PENNSYLVANIAN FUSULINIDAE Measurements of F. pumila Thompson Volution Half length Radius vector Form ratio 12 3 4 12 3 4 12 3 4 1 2 3 4 5 6 7 8 9 0.055 0.04 0.06 0.12 0.10 0.15 0.22 0.24 0.29 0.35 0.37 0.44 0.50 0.52 0.59 0.69 0.74 0.75 0.83 0.97 1.16 1.00 1.24 1.22 1.44 1.38 1.44 1.80 2.14 0.055 0.04 0.06 0.08 0.08 0.12 0.12 0.13 0.17 0.15 0.19 0.19 0.24 0.23 0.26 0.27 0.37 0.31 0.38 0.40 0.54 0.44 0.52 0.54 0.69 0.59 0.69 0.73 ..... 0.74 0.93 0.94 1.15 1.8" 1.2" JL2" '.'.".'.[ 1.8 1.8 1.7 2.0 1.9 1.8 2.1 2.0 2.1 1.8 2.3 1.9 2.0 1.8 2.6 2.0 2.3 1.7 2.4 2.0 1.9 2.0 2.2 Tunnel angle Wall thickness Septal count 12 3 4 1 2 5 6 7 1 2 3 4 5 6 7 "l8° "l4° '.'.'.'.'. '.'.'.'.'. 17° 14° 15° 21° 17° 18° 19° 21° 23° 16° 16° 16° 22° 15° 15° 26° 18° 15° '.'.'.'.'. 0^025 .'.'.'.'.. '.'.'.'.'. ? '..'.'.'. 0.031 ..'.'.'. ..'..'. 0.042 . 038 11 11 9 15 19 17 19 26 19 22 27 24 35 29 31? 40? 33 8 0.050 Specimens 1-3 and 5-7 are illustrated on plate 5 as figures 15, 12, 13, 18, 17, and 19, respectively. The diaphanotheca is well defined and thin, the tectoria being darker in color and thicker. Mural pores are indicated but are generally very obscure. No microscopic shells have been ob- served. The whole specimen shown as figure 10 has a length of 3.8 mm and a diam- eter of 1.9 mm; that of figure 11. has a length of 4.5 mm and a diameter of 2.2. The latter specimen was sectioned after photographing and its axial slice is shown as figure 12. The sagittal sec- tion, figure 18, indicates a diameter of 2.1 mm at 7 volutions, and that of figure 19 indicates a diameter of 1.5 mm at the end of the sixth whorl. Discussion. — This species may prove to be identical with Fusulina meeki var. tregoensis Roth and Skinner, which was described from the Cherokee shale in Kansas. That shell has a similar shape, massive chomata, narrow tunnel, and deeply folded septa. The brief original description accompanied by a single axial section is inadequate to settle the matter, but if its shells have 8 to 8% volutions at a length of 2.2 and a diam- eter of 1.5 mm, the Kansas variety must be smaller at all stages of growth than F. pumila. F. distensa Roth and Skin- ner, from the McCoy formation of Colo- rado, is also similar to the form be- fore us, but it expands more rapidly, is larger at maturity and at each corres- ponding volution, and it has a wider tunnel, narrower chomata, and more nu- merous septa. F. leei Skinner is much more slender, has a wider tunnel, somewhat narrower chomata and less deeply folded septa. F. euryteines Thompson is also closely similar but is relatively longer and more slender, tends to have extended poles and concave slopes, has a wider tunnel and less massive chomata. DESCRIPTION OF SPECIES 109 Distribution. — The types of this spe- cies were from a zone 35 feet below the "Whitebreast coal in Iowa and were as- sociated with W edekindellina and Fus- ulina leei. In Illinois it has been found in only a few localities and without asso- ciated fusulines except at station B3 where two specimens were found, iden- tified as F. cf. leei. These are the ones described on page 111. It occurs rather abundantly, though disseminated, in a limestone near the village of Wine Hill, Randolph County (station B3). This limestone resembles the Seahorne in lith- ology as well as in the nature of the underlying fireclay. A few specimens have been found in the Seahorne at sta- tion 452. Poorly preserved, more or less pyritized specimens are sparsely scat- tered through the same limestone at sta- tion Fl where the stratigraphic rela- tions are well exposed (see the section at station E9). Fusulines are also very rare in the Seahorne limestone at sta- tion G5. The junior author has searched for fusulines in a number of other ex- cellent outcrops of the Seahorne lime- stone but has found specimens at only the localities mentioned. Fusulina leei Skinner Plate 5, figures 1-8; plate 6, figures 1-10 Fusulina leei Skinner. Jour. Paleontology, vol. 5, pp. 257-258, pi. 30, figs. 4 and 6, 1931. Cherokee shale, just over Blue- jacket sandstone member, near Pryor, Oklahoma. ? Fusulina leei Thompson. Iowa Univ. Studies, vol. 16, no. 4 (new ser., no. 284), pp. 301-303, pi. 21, figs. 3, 7, 10, 18, 1934. Cherokee shale, 35 feet below the White- breast coal, Lucas and Monroe counties, Iowa. Material studied. — Numerous speci- mens were collected from the Curlew horizon at stations 234, 235, and 464 in Saline County. Syntypes from Okla- homa and specimens from Iowa were also studied. About 50 sections were made. Description. — Species small, elongate- fusiform, tapering to rather acute ends. Adult shells commonly have about 7 vo- lutions and attain a length of approxi- mately 5.0 mm and a diameter of 1.5 mm; the observed range is from 5 to 83/3 volutions. As suggested by figure 1 of plate 5, the growth is somewhat ir- regular and the shape commonly asym- metrical. The proloculum is small and normally spherical, the average diameter being about 90 microns with extremes rang- ing from 70 to 130 microns. No micro- spheric individuals have been observed. The volutions expand gradually and slowly, the shell being rather closely coiled. The wall is moderately thin, the pro- theca being of normal thickness for a Fusulina of this size, but the epitheca is abnormally thin for this low strati- graphic position. The outer tectorium, deposited on the floor of each volution, is thickest, but the inner tectorium, coating the septa and the ceiling of each volution, is notably thin. The septa are moderately numerous and increase somewhat regularly in suc- cessive volutions. In the first three vo- lutions they are plane; in the next two they develop folds, and in the outer whorls they are deeply but somewhat irregularly folded except near the tun- nel where the folds are slight. Septal pores are present in the end zones of the outer whorls but are not conspicu- ous. The tunnel is wide for this genus and is notable for the way it broadens in the last whorl; although the tunnel angle is normally about 30° in the sixth volu- tion, three of our specimens have a tunnel angle of 35°, 37°, and 40°, re- spectively, in the outer whorl. In the adult stage of F. leei, as in most species of Fusulina having strongly folded septa, the chomata are less like levees than they are in Fusulinella, be- cause the deposit extends up the sides of the septa adjacent to the tunnel and makes only a narrow and uneven ridge on the floor of the volution. In the ju- venile whorls, however, the chomata are relatively broad and heavy, this com- bination of plane septa and heavy cho- mata marking the first 3 volutions as a distinctly fusulinellid stage. 110 PENNSYLVANIAN FUSULINIDAE Measurements of F. leei Skinner Volution Half length Radius vector Form ratio 12 3 4 12 3 4 12 3 4 1 2 3 4 5 6 7 0.06 0.057 0.13 0.13 0.16 0.26 0.26 0.29 0.24 43 0.57 0.43 0.46 0.63 0.89 0.79 0.69 1.20 1.27 1.15 1.08 1.66 1.86 1.71 1.44 2 . 26 2 . 43 0.06 0.05 0.057 0.07 0.07 0.09 0.08 0.12 0.12 0.14 0.14 0.19 0.19 0.21 0.21 0.27 0.29 0.31 0.30 0.40 0.41 0.44 0.43 0.56 0.59 0.60 0.59 0.75 0.77 0.79 0.81 i'.k" '.'.'.'.'. i'a" 2.Q~ 2.1 2.1 2.0 1.7 2.2 3.0 2.0 2.1 2.3 3.0 2.4 2.3 3.0 3.0 2.6 1.9 2.9 3.1 2.7 1.8 3.0 3.0 Tunnel angle Wall thickness Septal count 12 3 4 12 3 4 5 6 7 1 2 3 4 5 6 7 22° 22° 16° 23° 19° 27° 21° 23° 23° 22° 22° 29° 22° 22° 25° 32° 30° 27° 30° 27° 28° 35° '.'.'.'.'. '.'.'.:'. 0^020 0'025 0.021 0.030 0.030 0.030 0.020 0.034 0.035 0.025 0.028 0.035 14 9 11 15 12 16 17 18 18 21 19 20 23 22 27 24 30 29 27 36 31 Specimens 1, 3, 5 and 6 are illustrated on plate 5 as figures 3, 6, 4, and 8, respectively ; specimens 2 and 7 are shown on plate 6 as figures 1 and 8, respectively. Discussion. — The low stratigraphic position of this species harmonizes with its ontogeny. The first 3 or 4 volutions, with their plane septa and broad, levee- like chomata, represent the Fusulinella stage. The change from this to the Fusulina stage is gradual and takes place in about 2 volutions through the development of septal folds first near the ends, and their subsequent spread toward the equator. Curiously, the tunnel is relatively wide in the first 2 volutions, its angle then dropping to a minimum in the third or fourth and thereafter increasing again. This species clearly represents an early stage in the development of the genus Fusulina. More than a third of the volutions are typically fusulinelloid and the inset of the septal folding and reduction of the chomata are so gradual that less than half the shell is in the typical Fusulina stage. Furthermore, the septal folds are rather primitive in that they are not deep enough for much fusion between opposed folds and they are somewhat irregularly and distantly placed. The external form of the shell also is generalized. It is not intended to infer that this species represents the first Fusulina, but that it has not pro- ceeded far in the evolution of that genus. We were fortunate in having access to the types of this species which are preserved in the U. S. National Museum, and to a group of topotypes presented to the senior author by Mr. Skinner. The types are here refigured to permit easy comparison with the Illinois shells, and statistical measurements are like- wise introduced in our table of measure- ments. Fusulina leei is easy to distinguish from most of the described species by the combination of several distinctive characters such as small size, wide tun- nel, degree of septal plication, and onto- genetic development. In comparison with Fusulina rockymontana Roth and Skin- ner, the distinction is not so easy to DESCRIPTION OF SPECIES 111 make. F. leei is more slender and less ellipsoidal ; has more pointed ends ; has a smaller proloculum and more volutions in the Fusulinella stage; has thinner walls, the epitheea being considerably thinner; the chomata are narrower; the shell is more closely coiled, the rate of spiral expansion being less; and the septa may be less deeply folded. Each of these discriminations is slight, but it appears that the combination of all the differences points to a different identity. Distribution. — Fusulina leei is locally abundant in the Curlew limestone of Sa- line and Gallatin counties, Illinois. At the type locality of the Curlew lime- stone, which is at Indian Hill, south of DeKoven, Kentucky, no specimens were found during a brief search. The speci- mens herein described came from sta- tions 234, 235, and 464 in Saline County, Illinois. Fusulina leei Skinner (1931, p. 257) was described originally from a marl overlying the Bluejacket sandstone in sec. 7, T. 21 N., R. 18 E., northeastern Oklahoma. Similar but not precisely identical forms identified by Thompson (1934) as F. leei and F. kayi Thomp- son, n. sp., were found by him in a lime- stone about 35 feet below the White- breast coal, Cherokee group, in Lucas and Monroe counties, Iowa. Fusulina cf. F. leei Skinner Plate 6, figures 12, 13 Description and discussion. — From station B3 we have two good axial sec- tions of a species closely similar to F. leei but larger and possibly more ad- vanced. One of these shows 8V2 an( i the other 9 full volutions. The prolocu- lum of the first has a diameter of 115 microns and that of the second is slightly elongated along the axis and measures 142 by 158 microns. The dimensions and proportions of the inner seven volutions fall within the limits of variation of the typical speci- mens of F. leei, but the eighth and ninth volutions make these adult shells appre- ciably larger than F. leei. The tunnel angle in the first specimen measures 17°, 17°, 23°, 20°, 24°, 32° Measurements of F. cf. F. leei Skinner Radius Half length vector Form ratio Volu- tion 1 2 1 2 1 2 0.057 0.079 0.057 0.071 1 0.13 0.17 0.079 0.116 1.6 1*5 2 0.21 0.31 0.14 0.18 1.5 1.8 3 0.43 0.50 0.22 0.26 2.0 2.0 4 0.66 0.71 0.31 0.37 2.1 1.9 5 1.16 1.01 0.45 0.51 2.6 2.0 6 1 . 60 1.41 0.61 0.68 2.6 2.1 7 2 . 04 1 . 85 0.96 0.90 2.0 2.1 8 2.55 2.37 1.04 1.13 2.4 2.1 9 3.16 .... 1.19 .... 2.6 and 39°, respectively, in the second to eighth volutions ; in the second specimen the corresponding measurements are 24°, 20°, 18°, 20°, 20°, 22°, and 22°. The first falls well within the limits of vari- ation of F. leei but the second is ab- normally narrow in the outer volutions. In wall thickness and other characters there is also close agreement with F. leei. In short, these specimens agree closely with F. leei except for the fact that they include nearly two more volutions and attain a correspondingly larger size. It is worthy of note that they are from a distinct horizon probably considerably above the known range of typical F. leei and that they occur with abundant F. pumila Thompson, whereas the latter species has not been found with typical F. leei and vice versa. This would sug- gest that the two specimens from station B3 represent a variety of F. leei, some- what younger, and appreciably larger than the typical form. Occurrence. — Only two specimens were found in the Seahorne(?) lime- stone at station B3 in Randolph County. Fusulina sp. A Plate 6, figure 11 Fusulinella, n. sp. Henbest, Jour. Paleontol- ogy, vol. 2, p. 79, pi. X, figs. 2 and 4, 1928. Stonefort limestone, station 237, Saline County, Illinois (not station 337 as originally stated). 112 PENNSYLVANIA^ FUSULINIDAE Description and discussion. — A single axial section (pi. 6, fig. 11) from the Stonefort limestone at station 237 re- sembles F. leei in shape but is slightly larger, has slighter chomata, somewhat deeper and more crowded septal folds, and a very much thinner spiral wall. The proloculum has a diameter of 126 microns. The shell almost agrees with F. leei in rate of expansion and in its form ratio, but at 7 volutions is appre- ciably larger, measuring 6.4 mm long and 2.8 mm thick. Its spiral wall scarely exceeds 20 microns in thickness in any of the whorls. The diaphanotheca ap- pears clear and structureless and is some- what thinner than the tectoria. The tunnel angle is about 20° and varied but little during growth. A second shell externally similar to this was found at the same locality but was destroyed in sectioning, and later search for additional specimens at that locality was fruitless. This is probably a descendant of F. leei and appears to represent a distinct variety or species, but with only one sec- tion for study we refrain from giving it a name. We cannot accept Thompson's identification of this specimen (1934, p. 311) with F. euryteines Thompson; it is larger and less ventricose than that species at all stages of growth. Distribution. — The single specimen was found in the Stonefort limestone at station 237 in Saline County, Illinois. Fusulina knighti Dunbar and Henbest, n. sp. Plate 6, figures 14-21 Material studied. — Several hundred free specimens were collected and more than a score of thin sections were made. Description. — A small, elongate-fusi- form species with rather sharply pointed ends, commonly having 5^ to 6 volu- tions and ranging from 5 to 5.5 mm in length and 1.5 to 1.8 mm in diameter. The prolocula are commonly between 100 and 150 microns in diameter and are subspherical. The shells are tightly coiled, the equatorial expansion being slow and gradual. The spiral wall is commonly not more than 35 microns Measurements of F. knighti Dunbar and Henbest Volution Half length Radius vector Form ratio 1 2 3 4 1 2 3 4 1 2 3 4 0.054 0.07 0.050 0.046 0.054 0.07 0.046 0.046 1 0.16 0.24 0.16 0.10 0.116 0.13 0.09 0.086 2 0.31 0.57 0.36 0.21 0.18 0.21 0.16 0.13 1.7 2.7 2.2 1.6 3 0.67 1.00 0.60 0.37 0.27 0.31 0.24 0.21 2.5 3.0 2.6 1.8 4 1.16 1 . 50 . 94 0.71 0.41 0.49 0.37 0.31 2.8 3.0 2.6 2.3 5 1.85 2.40 1.50 1.23 0.60 0.67 0.53 0.45 3.0 3.6 3.0 3.0 6 2.43 ' 1.83 0.79 0.69 3.0 2.7 Tunnel angle Wall thickness Septal count 1 2 3 4 1 2 3 4 5 6 7 8 1 10 9 10 10 2 19° 23° 18° 16 16 16 15 3 21° 33° 20° 22° 0.025 20 20 16 18 4 25° 44° 27° 26° 0.025 0.035 22 20 20 24 5 33° 41° 29° 24° 0.045 . 030 0.035 24 27 26 28 6 36° . 050 ? 30 26 33 7 . 040 ? 29 Specimei s 1-3 and 5-7 are illustrated on p] ate 6 as figures 17, 18, 16 , 20, 19 and 21 , respectively. DESCRIPTION OF SPECIES 113 thick, the inner tectorium being relative- ly thin and the outer tectorium thick. In specimen 1 of the table of measure- ments the wall is locally thicker due to an abnormal thickness of such epitheca. The septa are deeply fluted and in axial sections the septal loops are crowded even to the middle of the shell. Septal pores are abundant. The tunnel is of moderate width, the tunnel angle increasing generally from about 20° in the second whorl to 30°-40° in the fifth. Chomata are very narrow and, in axial sections, commonly are not easily dis- tinguished from the associated septal loops. Discussion. — This species resembles F. lucasensis Thompson in its small size, its deeply folded septa, and its very nar- row chomata; but it is a larger shell at all stages of growth. For example, its prolocula are commonly between 100 and 150 microns in diameter and those of F. lucasensis generally between 40 and 80; it attains a length of 5 to 5.5 mm in the fifth volution and F. lucasensis has a corresponding length of less than 2.0 mm. Moreover, it is more slender than Thompson's species, its form ratio at maturity being about 3 instead of 2. It is also similar to F. kayi Thompson, but that species is somewhat smaller and relatively thicker, and its chomata are thicker and its septa less deeply folded in the middle part of the shell than in F. knighti. Fusulina leei Skinner is similar in size and external appearance, but appears quite different in axial sections, because in F. leei the chomata are stronger and the septal loops less crowded near the middle of the shell. The differences are such, however, that F. leei, being the older, may be directly ancestral to F. knighti, the evolution from one to the other having involved a reduction of the chomata and an increase in the depth of septal folding across the middle of the shell. Fusulina inconspicua Girty is also similar but is distinctly more subcylin- drical, having bluntly rounded instead of acute poles. In addition, its septal folds are not so deep across the middle of the shell as are those of F. knighti. Distribution. — This species occurs in abundance in collections made by J. Brookes Knight in the Upper Fort Scott limestone at his locality 45 (y 2 mile north of Olive Street road at juncture with Spoede road) in the city of St. Louis, Missouri. There it is associated with abundant specimens of F. girtyi and F. Illinois ensis. Two specimens were found in the Bankston Fork limestone near Bunkum, Illinois (station Kd8), where they were associated with F. girtyi and F. Illinois ensis. Fusulina novamexicana Needham Plate 10, figures 7-17 Fusulinella meeki Dunbar and Condra (part). Nebraska Geol. Surv. Bull. 2, 2nd ser., p. 78, pi. 2, figs. 12, 13, and 14?, 1927. Millsap Lake limestone in the Strawn group of Texas. Not the type specimens from Rich Hill, Missouri. Fusulinella (Girtyina) aff. ventricosa Hen- best. Jour. Paleontology, vol. II, p. 76, pi. 10, figs. 5 and 7, and probably also figs, la and 3, 1928. Stonefort lime- stone, station 370, Williamson County, Illinois. Fusulina novamexicana Needham, New Mex. School of Mines Bull. 14, p. 23, pi. 2, figs. 11-15, 1937. Material studied. — Numerous speci- mens from three localities in the Stone- fort limestone (stations 250, 370, and 371), also the types of the species from New Mexico ; abundant specimens from Texas, a few from Oklahoma, and one good section from station Bl in Illinois. Eight sections from Illinois. Description. — A thickly fusiform spe- cies of about 8 volutions, attaining a length of about 6 mm and a diameter of about 3 mm. The average size is some- what smaller, being about 4.8 mm in length and 2.6 mm in diameter for our Illinois specimens. The poles are com- monly blunt and unsymmetrically de- veloped, as suggested by the figures on plate 10. The lateral slopes are nearly flat or slightly concave, especially in the last two volutions which tend to be dis- proportionately extended at the poles. The proloculum is large for this genus, but there is an exceptional variation among specimens, the diameter ranging from 120 to 240 microns. The average, 114 PENNSYLVANIAN FUSULINIDAE Measurements of P. novamexicana Needham Volution Half length Radius vector Form ratio 12 3 4 12 3 4 12 3 4 1 2 3 4 5 6 7 8 0.085 0.085 0.085 0.28 0.21 0.31 0.27 0.50 0.37 0.46 0.44 0.70 0.59 0.64 0.71 0.88 0.90 0.83 0.89 1.15 1.20 1.22 1.19 1.75 1.58 1.58 1.58 2.50 2.00 2.14 2.28 3.18 2.28+ ..... 0.085 0.085 0.085 0.15 0.17 0.15 0.14 0.25 0.27 0.26 0.23 0.36 0.41 0.40 0.37 0.52 0.58 0.56 0.51 0.70 0.76 0.76 0.69 0.96 1.04 0.97 0.89 1.02 1.27 1.27 1.14 1.55 i'.s" i.2 - 2.6" 1.9" 2.0 1.3 1.7 1.9 1.9 1.4 1.6 1.9 1.7 1.5 1.4 1.7 1.6 1.5 1.6 1.7 1.8 1.5 1.6 1.7 2.4 1.5 1.6 2.0 Tunnel angle Wall thickness Septal count - 12 3 4 12 3 4 5 6 7 1 18° 0.020 0.020 0.020 10 11 2 3 4 18° 17° 21° 15° 16° 21° 16° 13° 0.030 0.030 0.040 . 035 . 040 20 22 22 22 23 26 29 37 32 5 6 7 8 15° 14° 15° 14° 14° 14° 13° 12° 17° 15° 13° 16° 19° 17° 0.050 0.040 0.050 0.045 0.050 0.045 0.050 0.040 28 42 37 37 47 43 45 51 42 54 Specimens 1-6 are illustrated on plate 10 as figures 8, 10, 12, 15, 13, and 14, respectively. Specimen 7 is on slide Y2 from station 371. The tabulated measurements for specimen 1, here designated the holotype of the species, were deducted from Needham's illustration (1937, pi, 2, fig. 13). They are introduced here to permit better comparison with the Illinois shells. however, is about 160 microns and, in spite of variations in size of the prolo- culum, the early whorls of all specimens observed are fusulinoid and coiled in harmony with the rest. There is no reason to regard any of the specimens before us as microspheric. The wall of the proloculum is exceptionally thick, measuring in four specimens 17, 20, 21, and 30 microns, respectively. On the contrary, the protheca of the spiral wall is not thick, commonly measuring be- tween 8 and 11 microns in the early whorls and attaining to only 12 to 17 microns in the later ones. The tectoria are moderately thick, however, and the entire wall commonly has a thickness of 40 to 50 microns in the middle part of the outer whorls. The whorls expand gradually and the form ratio changes but little after the second or third volution. The septa are numerous, increasing from about 10 in the first whorl to 45 or more in the last. They are strongly folded across the center of the shell as well as near the poles, opposed folds meeting to subdivide the lower part of the chambers into regular cell-like chamberlets, as well shown in figure 11 of plate 10. The tunnel is narrow and commonly irregular in its course, deviating appre- ciably from the equatorial plane. The tunnel angle is usually 18° to 21° in the first 2 volutions and then decreases slightly, being about 15° in the outer whorls. The chomata take the form chiefly of a thickening of the septa at the edges of the tunnel, rising high on the septa but forming only a narrow and ill-defined ridge on the floor of the volution. Septal pores are present in the end zones of the DESCRIPTION OF SPECIES 115 outer whorls but because of the strong septal folding are not conspicuous in thin sections. Station Bl, in the Stonefort (?) lime- stone, yielded a single axial section of this species along with W edekindellina euthy septa (Henbest). This specimen (pi. 10, fig. 7) is somewhat smaller than the types, having only 7 volutions, but the proportions of these agree closely with corresponding whorls in the speci- mens from the unquestioned Stonefort limestone. The radius vector of this specimen measures 0.16, 0.24, 0.37, 0.53, 0.70, 0.90, and 1.13 mm in successive volutions and the corresponding half length is 0.21, 0.36, 0.64, 0.93, 1.16, 1.71, and 2.07 mm. Discussion. — This species resembles F. euryteines Thompson but it is larger and much more ventricose. It is more likely to be confused with F. girtyi Dunbar and Condra which has about the same size and shape but occurs considerably higher in the section. The latter is a little shorter, its form ratio being com- monly 1.3 to 1.5 at maturity whereas that of F. novamexicana ranges upward from 1.5 to more than 2.0. There is also a slight but characteristic difference in shape, F. girtyi having more regular and neatly pointed polar extremities. As a result of its regular lateral slopes and acute poles, F. girtyi appears lozenge- shaped in axial profile, especially in the first several volutions, whereas F . nova- mexicana is more bluntly rounded at the ends. Distribution. — The wide distribution of this species in association with W ede- kindellina euthy septa (Henbest) is re- markable. In Illinois it has been found only in the Stonefort limestone. A col- lection from the Spaniard Creek lime- stone member of the Savanna formation at Muskogee, Oklahoma, was submitted to the senior author of this report by Norman D. Newell. The same form was mistakenly identified by Dunbar and Condra (1927, p. 80) as Fusulinella meeki (=Fusulina euryteines Thomp- son) in collections from the Kickapoo limestone in the lower part of the Strawn group of central Texas. There, as in Illinois, it is associated with W ede- kindellina euthy septa. It was described by Needham from the same association in the lower Magdalena limestone of New Mexico. It is rare at most outcrops in Illinois, the best collecting being at station 371. Other sources are stations 250, 370, and Bl. Fusulina girtyi (Dunbar and Condra) Plate 11, figures 1-17; plate 12, figures 2-8, 10-11 Fusulina ventricosa Meek and Worthen (not Fusulina cylindrica var. ventricosa Meek and Hayden, 1858). Geol. Survey of Illinois, vol. 5, p. 560, pi. 24, figs. 8a, 8b, 1873.— Meek, Am. Jour. Sci., 3rd ser., vol. 7, p. 484, 1874, Herrin lime- stone, Fulton and Peoria counties, Illi- nois. Girtyina ventricosa Staff. Paleontographica, vol. 59, 1912, pt. 3, pp. 164-165, pi. 18, figs. 2, 5, 7.— Cady, Illinois Geol. Sur- vey, Rept. of Investigations, No. 2, pp. 8-9, text fig. 2, 1925, Herrin limestone, Saline and Williamson counties, Illinois. Fusulinella girtyi Dunbar and Condra. Ne- braska Geol. Survey, 2nd ser. Bull. 2, pp. 76-78, pi. 2, figs. 1-4 (not fig. 5), 1927, Herrin limestone, Fulton and Peoria counties, Illinois; Fort Scott limestone, Mystic, Iowa, and Oswego, Kansas. Fusulinella (Girtyina) aff. ventricosa Hen- best. Jour. Paleontology, vol. 2, 1928, p. 83, pi. 9, figs. 3, 4, 6 (not pi. 10, figs. 1-7). Herrin limestone, station 377, Saline County, Illinois. Beedeina girtyi Galloway. Manual of For- aminifera, p. 401, pi. 36, fig. 17, 1933. Fusulina girtyi Thompson. Iowa Univ. Studies, vol. 16, no. 4, pp. 314-16, pi. 22, figs. 1, 5, 7, 20, 1934. Limestone 18 feet above the Mystic coal, Appanoose and Monroe counties, Iowa. Material studied. — Abundant material from many localities was studied and many sections were made. Description. — A medium-sized, gib- bous species attaining a length of 4.6 to 5.0 mm and a thickness of 2.8 to 3.0 mm. Weathered shells commonly appear al- most spherical, but well-preserved indi- viduals normally possess short, subacute polar extremities and present a thickly fusiform profile as in figures 5-9 of plate 11. The whorls are closely coiled and al- most uniform in height from equator to poles. As a result, the ratio of length 116 PENNSYLVANIAN FUSULINIDAE to thickness changes but little during growth and the number of whorls is ex- ceptional for shells of such small size, commonly amounting to 9 or 10 and rarely 11 at maturity. The proloculum is of medium size, ranging from about 140 to 170 microns in diameter. The spiral wall is very thin, the protheca scarcely exceeding 12 mi- crons in thickness. Epithecal deposits are strongly developed, however, in a zone on each side of the tunnel. In part, these take the form of chomata, but for the most part the deposit lines all walls of the chambers, greatly thickening the septa as well as the roof and floor. This deposit may even reach the extent of sol- idly filling the chambers for some dis- tance on each side of the tunnel. Such deposits are best shown in sagittal sec- tions that are slightly oblique, as figures 16 and 17 of plate 11. A well-centered sagittal section like figure 15 of the same plate shows the pendant septa above the tunnel to be greatly thickened in this way. The diaphanotheca normally ap- pears clearer than the epitheca and structureless when properly illuminated, but very thin sections of well-preserved specimens commonly show evidence of porosity, at least locally, in the outer whorls. The septa are rather closely spaced and very numerous, increasing steadily from 15 or less in the first volution to 55 or 60 in the last. They are deeply and strongly folded, even across the middle of the shell. Septal pores are abundant in the end zones of the outer whorls. The tunnel is exceptionally narrow and, as it widened but little while the shell grew, the tunnel angle commonly decreases with growth, measuring 15° to 20° in the early whorls but generally less than 15° in the adult volutions. Measurements of F. girtyi (Dunbar and Condra) Volution Half length Radius vector Form ratio 12 3 4 12 3 4 12 3 4 1 2 3 4 5 6 7 8 9 0.090 0.095 0.09 0.26 0.20 0.21 0.43 0.47 0.31 0.37 0.67 0.71 0.49 0.60 0.93 0.91 0.70 0.83 1.22 1.10 0.86 1.08 1.58 1.39 1.16 1.36 2.00 1.58 1.49 1.70 2.44 1.86 1.81 2.14 2.24 0.070 0.09 0.10 0.11 0.13 0.16 0.18 0.29 0.31 0.24 0.26 0.43 0.43 0.35 0.38 0.57 0.57 0.50 0.53 0.76 0.74 0.65 0.71 1.01 0.94 0.83 0.91 1.30 1.16 1.05 1.15 1.44 1.39 ? 1.39 ? 1.2 2.0 1 1.5 1 1.6 1 1.5 1 1.4 1 1.4 1 1.3 1 1.3 2 1.1 2 1.4 4 1.6 4 1.5 3 1.5 4 1.5 4 1.4 ... 1.5 Tunnel angle Wall thickness Septal count 12 3 4 12 3 4 5 6 7 1 2 20° 16° ..... . 025 . 030 . 030 13 15 13 20 20 17 3 4 16° 22° 15° 16° 18° 14° 0.030 0.030 0.035 24 28 28 31 34 33 5 6 7 8 9 11° 15° 12° 11° 9° 16° 14° 9° 13° 16° 15° 13° 13° 14° 13° . 040 0.040 0.040 0.040 36 40? 37? 42 45? 40? 44 53 54 56 55 59? Specimen 1 is the holotype (here designated), shown as figure 9 on plate 11 away to a polished axial surface. Specimen 2 is shown as figure 4 on plate 12. on plate 11 as figures 14,13,17,10, and 15, respectively. one side has been ground Specimens 3-7 are shown DESCRIPTION OF SPECIES 117 Discussion. — Fusulina girtyi and its associates, F. illinoisensis Dunbar and Henbest, n. sp., and F. haworthi (Beede), constitute the most important fusuline assemblage in Illinois and serve as a guide to the Brereton lime- stone. Since this is one of the more ex- tensive and persistent limestones in the Pennsylvanian rocks of the State, and the underlying Herrin (No. 6) coal is likewise widely persistent and economi- cally important, these beds have been extensively used for mapping and for structural studies in the southern Illi- nois coal fields. The history of the nomenclature of F. girtyi is unfortunately involved. The species was recognized during the first geological survey of Illinois and figured by Meek and Worthen in 1873 but was erroneously identified as F. ventricosa Meek and Hayden, a much larger species now referred to Triticites. Specimens were later secured from Illinois by Schellwien who accepted Meek and Worthen 's identification. These were later studied by Staff (1912) who pro- posed a new genus, Girtyina, which he intended for the Illinois species. But in designating as genotype Fusulina ventricosa Meek and Hayden, he actu- ally made his generic name a synonym of Triticites and left the Illinois species without a valid name. It was described as Fusulinella girtyi by Dunbar and Condra in 1927 and later was transferred to Fusulina by Dunbar and Henbest. In 1933 Gallo- way used this species as the type of his genus Beedeina, which we regard as a straight synonym of Fusulina. The cir- cumstances leading to the rejection of the name Girtyina ventricosa have been set forth by Dunbar and Condra (1927, pp. 61 and 76) and are reviewed on page 89. The distinguishing characters of F. girtyi are its very obese form, nearly flat lateral slopes, and acutely pointed poles, its large number of closely coiled volutions, its deep septal folds and its narrow tunnel. Because of the shape and the acute poles the whorls appear lozenge-shaped rather than elliptical in axial sections. This is particularly true of the inner whorls and not quite true of the outer ones, which are commonly more extended at the ends. It most closely resembles F. nova- mexicana Needham which occurs in a lower stratigraphic horizon. That spe- cies has larger and blunter polar ex- tremities and commonly shows distinctly concave lateral slopes. F. illinoisensis is apparently closely allied and may be only a more elongate variety of this species with which it is commonly associated. It is longer and more slender than F. girtyi and com- monly shows a middle inflation, distinctly concave lateral slopes, and extended poles. Its tunnel is also wider than that of F. girtyi. Distribution. — Fusulina girtyi can be found in practically all outcrops of the Brereton (Herrin) limestone though sparsely distributed at some localities. Free specimens are available in abund- ance at station B9, and in moderate numbers at station 464a, and locally in Fulton County in clay partings in the limestone. Inasmuch as specimens were found at 24, or about one-third, of the stations listed in this report, the reader is referred to the Catalogue of Collect- ing Localities (end of report) for details of distribution. Fusulina girtyi is pres- ent also in the Bankston Fork limestone of Saline and Williamson counties, but is very scarce at most localities. It is present in a limestone identified by Wel- ler as the St. David at station W232 in Greene County. Further investigation is needed to determine whether it appears in the Hanover limestone and whether it is common in the St. David. Our ob- servations thus far indicate that it does not occur below the Hanover and does not range above the Bankston Fork lime- stone. According to collections submitted by various field parties of the U. S. Geolog- ical Survey, this species is abundant in the Lower and sparse in the Upper Fort Scott limestone of Kansas. 118 PENNSYLVANIAN FUSUL1NIDAE Fusulina illinoisensis Dunbar and Henbest, n. sp. Plate 11, figures 18-30; plate 12, figure 9; plate 13, figures 1-12 Material studied. — Study was based on hundreds of haphazard sections and weathered exposures, and on many free specimens (especially from stations B9 and 464a). More than a score of axial sections were carefully cut for critical study and measurement. Description. — Similar to F. girtyi but more slender and elongate. The middle is inflated, the poles extended, and the lateral slopes distinctly concave. The average length of 7 measured specimens is 4.6 mm and the diameter 2.3, but fully grown shells having about 8 volutions attain a length of about 5 mm and a diameter of 2.5 mm, the form ratio be- ing near 2 in this species as compared with 1.4 to 1.7 in F. girtyi (occasional shells are still larger and have as many as 9 volutions). The adult proportions are attained at an early stage and the changes during growth are small and irregular. The prolocula range in diameter from about 120 to 240 microns. The spiral wall is very thin, as in F. girtyi, and epithecal deposits are similarly disposed but lighter than in that species. Thus, instead of forming heavy chomata in the form of levee-like ridges on the floor of the volutions, the deposit is laid down on the septa and roof as well as the floor, constricting or even filling the cham- bers for a short distance on each side of the tunnel (pi. 11, fig. 30 and pi. 13, fig. 4), and even thickening the septa where they hang pendant above the tun- nel (pi. 11, fig. 25). The septa are rather closely spaced and are regularly and strongly fluted Measurements of F. illinoisensis Dunbar and Henbest Volution Half length Radius vector Form ratio 1 2 3 4 1 2 3 4 1 2 3 4 0.055 0.070 0.11 0.078 0.055 0.065 0.11 0.078 1 0.20 0.14 0.23 0.19 0.09 0.11 0.18 0.12 2.2 1.3 1.3 1.6 2 0.30 0.33 0.46 0.33 0.16 0.17 0.31 0.18 2.0 1.9 1.5 1.8 3 0.60 0.56 0.71 0.51 0.27 0.27 0.46 0.26 2.2 2.1 1.5 2.0 4 0.85 0.73 1.16 0.79 0.38 0.41 0.63 0.34 2.2 1.8 1.8 2.3 5 1.10 1.21 1.60 1.11 0.60 0.59 0.81 0.47 1.8 2.0 2.0 2.4 6 1.50 1.60 2.35 1.43 0.83 0.79 1.08 0.61 1.8 2.0 2.1 2.3 7 2.00 ? 3.0 + 1.85 1.05 0.99 1.31 0.86 1.9 ? ? 2.1 8 2.50 ? 2.43 ? 1.11 ? 2.2 9 ? 1.34 ? Tunnel angle Wall thickness Septal count 1 2 3 4 1 2 3 4 5 6 7 8 1 22° 0.020 15 14 12 15 2 18° 24° 16° 18° 0.030 0.030 0.025 23? 19 22 23 3 19° 25° 15° 17° 0.040 0.035 0.035 0.025 28 26 26 27 4 22° 24° 15° 20° 0.035 0.030 34 32 30? 30 5 21° 28° 16° 20° 0.050 0.045 0.025 39 39 39 38 6 17° 20° 20° 18° 0.040 0.050 0.040 0.025 40 41 34 7 18° 18° 20° 0.040 0.045 0.035 ? 44 44 8 25° ? ? 9. . . . 0.040 Specimens 1-3 and 5-7 are illustrated on plate 11 as figures 27, 28, 30, mens 4 and 8 are illustrated on plate 13 as figures 4 and 3. 25, and 26, respectively; speci- DESCRIPTION OF SPECIES 119 with high, narrow folds. Strong septal plication began at an early stage of growth and the fusulinelloid stage if rec- ognizable at all is restricted to the first volution in shells with large prolocula or the first two in those with small pro- locula. The tunnel is generally wider than that of F. girtyi, averaging between 20° and 25° instead of 15°, but the ranges in the two species overlap considerably. In this species, as in F. girtyi, the tun- nel angle is widest in the early volutions. Discussion. — F. illinoisensis is nearly intermediate between F. girtyi (Dunbar and Condra) and F. haworthi (Beede) in external form as well as internal structure. In form F. girtyi is very strongly and rather evenly ventricose, with short, acute poles; F. illinoisensis is more slender, has an inflated middle and extended poles so that the lateral slopes are concave; F. haworthi is still more slender and more evenly fusiform, lacking the inflation of the middle. In- ternally F. girtyi is somewhat more closely coiled, having a greater number of volutions at a given diameter, and its epithecal deposits are heavier than in either of the others; in F. haworthi the epithecal deposits are more definitely concentrated at the margins of the tun- nel. These three forms occur together in the Brereton limestone and apparently are genetically related. In a locality such as station B9, where thousands of specimens can be freed from a calcare- ous shale, the majority can be separated on shape alone into the three forms here recognized. Yet individual vari- ation is great enough so that the three groups overlap in form and perhaps one-fourth of the specimens appear to be transitional. Whether the three groups are specific or varietal is problematical. It seems unlikely that these variations are merely individual because in some parts of the State not all forms are present and, moreover, neither form is restricted to any particu- lar lithology so far as the junior au- thor's somewhat limited observations in- dicate. At certain localities, but not everywhere, in Randolph County, F. illi- noisensis occurs almost alone. In Ful- ton County F. girtyi locally dominates. We recognize these three closely allied forms as distinct species rather than varieties chiefly for the advantage of simplicity in nomenclature. Occasional specimens, as figures 4 and 5 of plate 13, have the general form of F. illinoisensis but show abnormally massive epithecal deposits near the tun- nel. They resemble F. girtyi in this respect as well as in the close coiling of their inner whorls. In axial sections the inner whorls have a false appearance of being fusulinelloid because of the fact that a thin slice of the epithecal filling resembles a plain septum ; actually the septa are more strongly folded than they appear to be in this region. Distribution. — This is probably the most common fusuline in the Brereton limestone, and it is also common in the Bankston Fork limestone, but has not been found in higher beds. It is present in one collection from the St. David limestone of Greene County and another from the same horizon in Fulton County. From the Piasa limestone at station Kd5 we have a single axial section of a specimen identified as F. cf. illinoisensis but it is much larger than the normal limits of this species, having 9 volutions and attaining a length of 6.6 mm and a diameter of 2.8 mm. This is the form originally described by Dunbar and Condra from the Pawnee limestone in Kansas as Fusulinella meekivar. robusta. That name, however, must be rejected as a homonym of F. robusta Meek and Hayden. Fusulina haworthi (Beede) 1916 emend. Dunbar and Henbest Plate 12, figure 1; plate 14, figures 1-18 Girtyina haworthi Beede. Indiana Univ. Studies, vol. 3, no. 29, p. 14, March. (Not Fusulinella haworthi of Dunbar and Condra, Nebraska Geol. Survey, 2nd ser., Bull., 2, p. 82, pi. 2, figs. 6-11.) Lower Fort Scott limestone, Fort Scott, Kansas. Fusulina haworthi White. Univ. of Texas, Bull. 3211, p. 26, pi. 1, figs. 4-6, 1932. Upper Millsap Lake formation, Palo Pinto County, Texas. 120 PENN8YLVANIAN FUSULINIDAE Fusulina stookeyi Thompson. Iowa Univ. Studies Nat. Hist., vol. 16, no. 4, p. 316, pi. 22, figs. 3, 15, 16, 21, 1934. (The specimen in pi. 22, fig. 15, one of the syntypes, is here designated as the lecto- holotype of F. stookeyi Thompson, and the one in pi. 22, fig. 21, is here desig- nated as the first lectoparatype.) Shale, 18 feet above the Mystic coal, Appanoose and Monroe counties, Iowa. Material studied. — Abundant material was collected at several localities in the Herrin limestone and numerous sections were made. Topotype material from Fort Scott, Kansas, is included in the description. Description (based on topotypes). — A fusiform species of 7 to 8 volutions, com- monly attaining a length of 6 or 7 mm and a thickness of 2.3 mm. The holotype was said to have a length of 7.8 mm and a thickness of 2.65 mm and it pre- sumably had about 8 volutions. The middle of the shell is broadly convex but not inflated and the lateral slopes are nearly flat or gently convex, taper- ing to subacute poles. The shape changes but little during growth, the form ratio being near 1.5 in the first volution and increasing to near 2.5 at maturity. The proloculum is moderately large, the average diameter being near 150 microns with extremes as small as 130 and as large as 190 microns. The whorls expand gradually and moderately rap- idly and the wall is thin, the protheca reaching a maximum thickness of 15 to 20 microns in the outer volutions and the epitheca being slightly thinner. The fine tubular mural pores are clearly visi- ble locally in the outer whorls and are further emphasized by staining (see Henbest, 1937, pi. 34, figs. 1-4, and this report pi. 14, figs. 16-18). The septa are strongly folded, from pole to equator in all volutions, as clear- ly seen in a thick section like figure 15 of plate 14, or in tangential sections like figure 10. The tunnel is of moderate width and height, its angle varying somewhat irregularly within the limits of 20° and 30°, with no systematic Measurements of F. hawoethi (Beede) Volution Half length Radius vector Form ratio 12 3 4 12 3 4 12 3 4 1 2 3 4 5 6 7 0.10 0.073 0.077 0.25 0.25 0.17 0.18 0.47 0.45 0.33 0.38 0.70 0.83 0.60 0.64 1 25 1.37 0.89 1.10 1.51 1.67 1.33 1.60 2.20 2.17 1.84 2.08 2.98 2.74 2.63 2.85 0.10 0.073 0.077 0.13 0.16 0.13 0.13 0.20 0.23 0.24 0.23 0.31 0.36 0.31 0.36 0.44 0.51 0.46 0.55 0.60 0.70 0.71 0.89 0.82 0.93 0.92 1.05 1.09 1.15 1.15 1.27 2.0 ' I.q" 1.3 ' 1a" 2.3 2.0 1.4 1.6 2.7 2.3 1.9 1.8 2.3 2.7 1.9 2.0 2.5 2.4 1.9 1.8 2.7 2.3 2.0 2.0 2.7 2.4 2.3 2.2 Tunnel angle Wall thickness Septal count 12 3 4 12 3 4 5 6 7 8 1 . 025 . 020 11 13 7 11 2 3 4 5 6 22° 21° 25° 27° 23° 15° 25° 28° 26° 15° 28° 27° 21° 27° .... . 025 . 025 . 025 . 040 . 040 . 030 . 050 . 040 0.055 0.045 . 030 . 045 . 040 16 20 16 19 19 24 21 23 24 30 24 26 23 41 30 29 26 31 34 7 0.025 38? 33 Specimen 1 is the holotype (measurements taken from Beede) and the half diameter rather than the radius vector is recorded for this specimen; specimens 2-8 are illustrated on plate 14 as figures 7, 6, 8, 11, 12, 13, and 14, respectively. DESCRIPTION OF SPECIES 121 change in successive whorls. The cho- mata are narrow and slight, taking the form of a thickening of the septa ad- jacent to the tunnel rather than of a levee-like ridge on the floor of the volu- tion. This is well seen in sagittal sec- tions like those of figures 12 and 13 of plate 14, which cut the chomata. It con- trasts strongly with the heavy deposits of F. girtyi (cf. figure 11 of plate 11). Septal pores are abundant in the end zones of the last 2 or 3 whorls. Discussion. — This species was describ- ed briefly without illustrations by Beede, who evidently planned but never pub- lished a fuller description. Repeated attempts failed to locate the types. Dr. Beede wrote us on January 4, 1931, that they were left with his collections in the Bureau of Economic Geology at Austin, Texas, but searches there did not locate them. Meanwhile the species could not be recognized from Beede 's description. Fortunately, however, he gave a definite type locality in the Lower Fort Scott limestone at Fort Scott, Kansas, and he also gave length and thickness for each volution in one of his types which we hereby designate the holotype. This makes it possible to interpret the spe- cies with reasonable certainty from topotype material. We are much in- debted to Raymond C. Moore and R. G. Moss for a collection made at the type locality for study. Although two or three species of fusulines occur at this horizon in southeastern Kansas, this one alone tallies closely with the detailed measurements given by Beede. Moreover, this is the dominant form in the collection from the type locality of F. haworthi. Our description is based on this topotype material from the Lower Fort Scott limestone in a cut of the Frisco Railroad at Fort Scott, Kan- sas, but the species is not uncommon in Illinois and we have illustrated several specimens from both states for compari- son. In the table of measurements we have adapted Beede 's measurements to our scheme as specimen 1 in order to facili- tate comparison. The half length is accurately secured by dividing his meas- urements for the length, but by taking half of his measurements of the diameter in place of the radius vector we have in- troduced a slight systematic error, for in shells that expand as rapidly as these the radius vector is appreciably more than half a diameter. If the proper cor- rection could be made for this, Beede 's type would probably agree very closely with our specimens in radius vectors. This correction would also reduce slight- ly the form ratio for Beede 's specimen and bring it closely into harmony with that of ours. F. haworthi is closely allied to F. girtyi and F. illinoisensis, both of which occur with it in the Brereton limestone in Illinois ; their relations are discussed on page 119. F. haworthi is more slender and considerably larger than F. girtyi and has fewer and less tightly coiled volutions. Its size and shape approach closer to F. illinoisensis but it is more evenly fusiform, lacking the inflation at the center and the polar extensions. Al- so its wall is thinner and the epithecal deposits lighter than in either F. girtyi or F. illinoisensis. Distribution. — Fusulina haworthi was originally described from the Lower Fort Scott limestone of Kansas. Though apparently abundant in the Lower Fort Scott limestone, F. haworthi is relatively rare in Illinois. This species, or speci- mens questionably referred to it, has been found at six localities in the Brere- ton limestone in association with F. gir- tyi and F. illinoisensis, and at one sta- tion (W232) in Greene County probably from the St. David limestone. Our best collections came from the Brereton lime- stone at station B9 in Monroe County. Fusulina cf. F. haworthi (Beede) Plate 14, figures 19 and 20 Occasional specimens are found in the Brereton limestone which differ from F. haworthi chiefly in being smaller and more slender. Whether they repre- sent a distinct variety or individual ab- normality we have insufficient data to determine. The specimen shown as figure 19 of plate 14 is from station 464A in Saline County and that shown as figure 20 is 122 PENNSYLVANIAN FUSULINIDAE from station 528 in Greene County, Illi- nois. A specimen similar to the last was found in the Cutler limestone at station Kd6. FUSULINA ACME Dunbar and Henbest, n. sp. Plate 15, figures 1-18; plate 16, figure 14 Fusulinella haworthi Dunbar and Condra (non Fusulina haworthi Beede). Ne- braska Geol. Surv. Bull. 2, 2nd ser., pp. 82-84, pi. II, figs. 6-11, 1927. Shales at the base of the Lonsdale limestone at Sparland, Illinois. Material studied. — Abundant speci- mens were collected at several localities in the Lonsdale and Piasa limestones, and more than 50 sections were pre- pared. Description. — A rather thickly fusi- form species of 7 to 8 volutions, attain- ing a length of about 7.5 mm and a di- ameter of 2.4 mm, the ratio of length to thickness being about 3 to 1 at maturity. The majority of specimens are somewhat smaller and have only 6 or 7 volutions. The ends are rather bluntly rounded and the middle part gently convex but not inflated. The septal furrows com- monly deviate more or less from a me- ridional course. The proloculum is of moderate size, commonly between 150 and 180 microns in diameter. No distinctly microspheric individuals have been observed. The spiral and septal walls are thin. The protheca generally equals or slight- ly exceeds the thickness of the tectoria except in the first few whorls and near the tunnel. There is no appreciable axial filling. The spiral wall is abun- dantly perforate, but the simple tubular pores are so fine that they can commonly be seen only in places under the best il- lumination, or in stained specimens. The septa are intensely and regularly folded, the tips of opposed folds meeting as in Schuiagerina s. s. Accordingly the septal loops are closely crowded through- out all axial sections, and in places one series of loops is superposed on another (pi. 15, fig. 15). This last peculiarity appears only where the septa incline strongly forward and the backwardly- directed folds of one septum rest upon the tips of the opposed folds of the pre- vious septum so that a vertical slice cuts both sets of folds. Although the septal folding is almost as highly specialized as that of Parafusulina, careful search has failed to reveal any cuniculi. Instead, and contrary to the condition in Parafu- sulina, the tips of forwardly-directed folds are complete and rest on the floor of the volution. Septal pores are abun- dant in the outer volutions. The tunnel begins with a moderate angular width of near 20° but widens gradually to 30°-35° in the adult whorls. The chomata are distinguishable in the first 4 or 5 volutions, both as a ridge- like deposit at each side of the tunnel and as a thickening of the septa adjacent to the tunnel ; but they are commonly al- most obsolete in the outer whorls, being smaller than in any other species of Fusulina in our faunas. In the first, and in some specimens in the second, vo- lutions, however, typical fusulinellid chomata occur. Discussion. — This species is closely similar to F. megista Thompson and F. mysticensis Thompson and in many re- spects is intermediate in form. F. me- gista is larger and relatively thicker, and has more distinct secondary axial filling. Also, its proloculum is some- what larger and it has a distinctly thicker spiral wall than that of F. acme. F. mysticensis is larger and more slender at maturity; its inner whorls are fusi- form and, up to 5 or 6 volutions, the young shells closely resemble F. acme, but its later whorls elongate much more rapidly and it takes on a subcylindrical form whereas F. acme maintains its pro- portions and fusiform shape. It is pos- sible that our species is only a geograph- ic variety of F. mysticensis, but in any event, we have vast numbers of free specimens for study from Illinois and the overwhelming majority of these fit closely the form we have described as F. acme, while only a few agree closely with the Iowan species. Distribution. — Fusulina acme and F. eximia Thompson are probably the DESCRIPTION OF SPECIES Measurements of F. acme Dunbar and Henbest 123 Volution Half length Radius vector Form ratio 1 2 3 4 1 2 3 4 1 2 3 4 0.085 0.085 0.086 0.086 0.086 1 0.17 0.21 0.21 0.24 0.11 o.io 0.13 0.i3 1.5 2.i 1.6 1.9 2 0.35 0.44 0.31 0.46 0.16 0.17 0.20 0.20 2.1 2.6 1.5 2.3 3 0.64 0.90 0.74 0.79 0.23 0.27 0.31 0.32 2.7 3.3 2.4 2.5 4 0.93 1.44 1.16 1.22 0.33 0.41 0.47 0.48 2.8 3.5 2.5 2.5 5 1.44 2.14 1.72 1,71 0.46 0.62 0.67 0.68 3.1 3.4 2.5 2.5 6 2.01 2.85 3.00 3.01 0.65 0.85 0.88 0.89 3.1 3.4 3.3 3.4 7 2.86 3.70? 3.74 0.86 1.06 1.14 3.3 3.5 8 1.10 Tunnel angle Wall thickness Septal count 1 2 3 4 1 2 3 4 5 6 7 1 0.012 11 2 20° 0.020 0.025 0.025 19 3 18° 25° 21° 0.020 0.030 0.030 23 4 19° 26° 38° 0.025 0.030 0.035 27 34? 28 5 25° 31° 35° 0.045 0.040 0.040 31 35 29 6 26° 37°? 31° 0.045 0.065 0.045 0.060 37 40 32 7 32° 36°? 0.050 0.025 0.025 0.055 ? 46? 39? 8 31° 0.030 Specimens 1-6 are illustrated on plate 15 as figures 8, 11, slide C from station 545. 7, 13, and 14, respectively. Specimen 7 is youngest species of Fusulina yet known, at least from this country. In the Piasa limestone, F. acme is associated with F. megista, F. mysticensis, and F. eximia. It is more prominent in the Lonsdale wherein it is associated with F. lonsdal- ensis n. sp., F. megista and, rarely, F. mysticensis. So far, the Triticites zone has not been found to overlap the range of this or any other species of Fusulina. Excellent collecting localities in the Lonsdale limestone may be found at stations 545, 547, and H2, where free specimens are abundant in a gray limy clay that locally contains nodules of limestone. The best collecting locality in the Piasa limestone is at station F5 where free specimens are available. The species occurs also in the Piasa limestone at station Kd5. Fusulina eximia Thompson Plate 17, figures 1-11; plate 23, figures 19, 20 Fusulina eximia Thompson. Iowa Univ. Studies, vol. 16, 1934, pp. 323-325, pi. 23, figs. 7-10. [We hereby designate as holotype the axial section shown as fig- ure 8 by Thompson.] Upper Des Moines series, 80 ft. above Mystic coal, Appa- noose County, Iowa. Material studied. — Syntypes from Iowa and numerous specimens from the Piasa limestone at station F5 and a few from the Lonsdale limestone at station 545. About a score of sections were pre- pared. Description. — Thompson 's detailed description leaves little to add. The shells are long and very slender, com- monly having a crooked or arcuate axis. The large shells have 7 to 8V2 volutions 124 PENNSYLVANIAN FUSULINIDAE and attain a length of 7 to 9 mm. and a diameter of 1.7 to about 2 mm. The first 3 or 4 whorls are fusiform and have acutely pointed poles. The form ratio of these inner whorls varies con- siderably among the specimens studied, being less than 2.5 in the second whorl in some specimens and nearly 4.0 in others. In all shells the form ratio increases steadily in the outer whorls, mounting from 3.5 to more than 5.0 at maturity. Meanwhile, the ends tend to fill out and the shell becomes more subcylindrical in the outer whorls. The proloculum is of medium size, generally between 100 and 180 microns in diameter. The equatorial expansion is slow and gradual and the whorls ap- pear low and tightly coiled. The spiro- theca is thin, commonly not over 30 microns, even in the outer whorls. The epitheca is relatively thick in the first 3 or 4 whorls but in the outer ones is equaled or exceeded by the protheca. The septa are rather crowded, increas- ing in number from about 15 in the first volution to 35 to 40 in the seventh. They are deeply and regularly folded, but in axial sections the loops commonly ap- pear more irregular than they otherwise should, because the septa are commonly irregular in their course and do not fol- low closely the plane of the slice. The chomata are very slender throughout and the tunnel is low and slit-like, and moderately wide, the tunnel angle in- creasing from near 20° in the third to 40° or 50° in the seventh (rarely more or less). Septal pores are common in the end zones of the outer whorls. Discussion. — This is the most slender species of Fusulina now known in Illi- nois. It superficially resembles Triti- cites ohioensis, but is easily distinguish- ed by its wall structure, its deep septal folding, and other internal features. The closest relationship is with F. lonsdalen- sis Dunbar and Henbest, which has ap- Measurements of F. eximia Thompson Volution Half length Radius vector Form ratio 1 2 3 4 1 2 3 4 1 2 3 4 ' 0.07 . 042 . 068 0.093 0.07 0.042 0.068 0.093 1 0.33 0.23 0.12 0.23 0.14 0.06 0.09 0.14 2.3 3.8 1.3 1.6 2 0.64 0.49 0.29 0.40 0.20 0.13 0.16 0.18 3.2 3.7 1.8 2.2 3 1.08 0.76 0.47 0.77 0.27 0.19 0.22 0.26 4.0 4.0 3.1 3.0 4 1.58 1.16 0.93 1.00 0.39 0.29 0.31 0.34 4.0 4.0 3.0 3.0 5 2.15 1 . 85 1 . 44 1.37 0.51 0.43 0.44 0.46 4.2 4.3 3.2 3.0 6 2.87 3.00 2.01 1.88 0.69 0.58 0.60 0.58 4.1 5.1 3.3 3.2 7 3.87 4.00 2.58 2.93 0.86 0.74 0.76 0.77 4.5 5.4 3.4 3.8 8 3 65 0.97 0.93 3.9 Tunnel angle Wall thickness Septal count 1 2 3 4 1 2 3 4 5 1 16° 0.020 15 2 25° 12° 0.025 17 3 17° 19° 23° 17° 0.025 0.025 21 4 19° 28° 25° 20° 0.030 0.025 0.025 24 5 20° 30° 25° 21° 0.035 0.030 0.035 0.030 27 6 25° 45° 32° 26° 0.040 0.030 0.040 31 7 38° 54° 42° 32° 0.035 0.050 0.035 36 Specii nens 1-3 and 5 are illustrated on p late 17 as figures G, 7, 8, and 5, respectively. Specimen 4 is slide Ml from station F5. DESCRIPTION OF SPECIES 125 proximately the same size and shape but is normally a little thicker at the middle. In F. eximia the equatorial expansion is very slow and gradual throughout, whereas in F. lonsdalensis it is accelerat- ed after the first 3 or 4 volutions; also, in the former the septal folds are deep and closely crowded even at the middle of the outer whorls, whereas in F. lons- dalensis they are broader and lower across the middle of the outer whorls. Distribution. — The types were secured from a calcareous zone about 80 feet above the Mystic coal in Appanoose County, Iowa, the highest zone in that state known to bear the genus Fusulina s. s. In Illinois the species occurs in most abundance and in typical form in the Piasa limestone at station F5. It is present also in the Cutler limestone at station Kdl. A few specimens were identified also from the Lonsdale lime- stone at station 545. Fusulina lonsdalensis Dunbar and Henbest, n. sp. Plate 16, figures 1-13, 15-21 Material studied. — Numerous speci- mens were collected from the Lonsdale limestone at stations 545, 547, and H2 ; more than 50 slides were prepared. Description. — An elongate-fusiform species of 6 or 7 volutions attaining, at 6 volutions, a length of 6.0 to 6.6 mm (rarely less) and a diameter of 1.4 to 1.7 mm. The proloculum is of medium size, having a diameter in 5 typical specimens of 140, 160, 170, 170, and 190 microns, respectively. The first 3 or 4 volutions are tightly coiled as in F. eximia but the expansion is gradually accelerated in the outer whorls. The spiral wall is thin as in F. eximia. The septa are rather numerous, in- creasing from about 20 in the second Measurements of F. lonsdalensis Dunbar and Henbest Volution Half length Radius vector Form ratio 1 2 3 4 1 2 3 4 1 2 3 4 0.086 .... 0.06 0.086 .... 1 0.17 0.22 0.24 0.18 0.10 0.14 0.09 0.10 1.6 2.7 2 0.35 0.49 0.37 0.35 0.16 0.18 0.17 0.17 2.7 2.2 3 0.74 0.80 0.68 0.62 0.24 0.28 0.28 0.27 3.0 2.8 2.4 2.3 4 1.30 1 . 44 1 . 42 1.23 0.36 0.41 0.41 0.44 3.6 3.5 3.5 2.8 5 2.14 2.43 2.09 2.14 0.50 0.59 0.59 0.62 4.3 4.1 2.5 3.4 6 3.29 3.15 2.50 3.10 0.67 0.80 0.71 0.83 4.9 3 7 3.5 3.7 7 ? ? Tunnel angle Wall thickness Septal count 1 2 3 1 2 3 4 5 6 7 1 0.015 0.025 12 16 13 2 31° 22° 0.025 0.025 0.030 21 22 20 3 39° 21° 27° 0.020 0.025 0.025 0.030 27 28 25 4 47° 27° 33° 0.035 0.045 . 030 29 32 29 5 49° 42° 58° . 035 . 040 . 025 0,030 35 32 31 6 ? 46° 0.025 0.045 0.040 41? 38 34 7 ? ? ? Specimens 1-6 are illustrated on plate 16 as figures 8, 2 from station 545. 7, 12 and 13, respectively. Specimen 7 is slide 126 PENN8YLVANIAN FUSULINIDAE whorl to 35 or 40 in the sixth. They are deeply and regularly folded, but the folds are not quite so deep or so crowded as they are in F. eximia. Septal pores are present in the outer whorls. The tunnel shows considerable variation in width in different specimens but in- creases during growth, the tunnel angle being commonly between 20° and 30° in the second whorl and 45° to 60° in the sixth. Chomata are very slender. Discussion. — This is a slender species very closely resembling F. eximia, from which it differs in several minor but con- stant characters. As indicated by a comparison of figures 4 on plates 16 and 17, there is a slight difference in shape, F. lonsdalensis being relatively thicker in the middle and elongate-fusiform rather than subcylindrical. This is to be correlated with a difference in style of growth, for in F. eximia the equato- rial expansion is slow and gradual throughout, whereas in F. lonsdalensis there is a moderate acceleration in the rate of expansion in the last 2 or 3 whorls. In axial sections the septal loops ap- pear broader and less crowded in the last 2 or 3 whorls of F. lonsdalensis than they do in F. eximia. F. acme is also closely allied to F. lonsdalensis but is shorter and thicker. Distribution. — This species occurs in some abundance in the Lonsdale lime- stone, especially in Peoria and Marshall counties (sta. 545, 547, and H2), where it is associated with the much more common F. acme and with rare speci- mens of F. eximia. Fusulina megista Thompson Plate 17, figures 12-20 Fusulina megista Thompson. Iowa Univ. Studies Nat. Hist, vol. 16, pp. 320-323, pi. 23, figs. 4-6, 1934. Upper Des Moines shale, 50 feet above the Mystic coal, Appanoose County, Iowa. Material studied. — Scattered speci- mens were collected from several locali- ties in the Cutler and Piasa limestones and one in the Lonsdale limestone. About a score of sections were made. Cotypes are from Iowa. Description. — This large species is thickly fusiform, with blunt ends and a subelliptical axial profile. It attains 8 to 9 volutions and at the mature stage measures about 8.0 mm long and 3.5 mm thick. The shape changes but little dur- ing growth, the ratio of length to thick- ness being near 2.5 in the third and fourth volutions and 2.7 to 2.9 in the outer whorls. The proloculum is large for this genus, commonly near 200 microns in diameter, is nearly spherical, and has an exceptionally thick wall. The first 3 to 3~jA volutions are rather low and closely coiled, but succeeding whorls expand more rapidly. The septa are numerous and intensely folded. There are as many as 15 to 25 in the first volution and 45 to 50 more in the outer whorls. The septal folds are narrow and high throughout the length of the shell and so strong that those of one septum meet the next, dividing the lower part of each meridional chamber into cell-like cham- berlets. Thus, in axial sections the sep- tal loops are high, narrow, and abundant throughout all the whorls. The tunnel is narrow and somewhat irregular in width and in its course. The tunnel angle commonly measures be- tween 15° and 20°, but shows no sys- tematic change and is inclined to de- crease slightly in the mature whorls. Cho- mata appear as well-defined ridges bor- dering the tunnel and thickening the edges of the septa beside it in the first 3 or 4 volutions but in the outer whorls take the form of thickenings of the septa for a short distance from the tunnel. There is also more or less secondary thickening of the tectoria along the axial zone. Such axial filling is irregularly distributed, however, and not equally developed in all shells. The spirotheca is moderately thick for this genus. The protheca increases gradually from about 15 microns in the second volution to 30 in the adult whorls, but the tectoria vary much in thickness in different parts of the shell. The entire wall commonly appears to be 40 to 50 microns thick in the sixth to eighth whorls but is thinner in the last volution. DESCRIPTION OF SPECIES Measurements of F. megista Thompson 127 Volution Half length Radius vector Form ratio 1 2 3 4 1 2 3 4 1 2 3 4 0.10 0.10 0.11 0.10 0.10 0.10 0.11 0.086 1 0.31 0.31 0.40 0.18 0.16 0.17 0.17 0.14 2 0.50 0.56 0.61 0.26 0.24 0.24 0.29 0.20 3 0.97 0.86 0.94 0.71 0.34 0.33 0.39 0.30 2.9 2 6 2 4 2 4 4 1.33 1.23 1.41 1.16 0.51 0.47 0.57 0.44 2.6 2 6 2 5 2 6 5 1.86 1.71 1.86 1.58 0.67 0.60 0.79 0.67 6 2.57 2.43 2.58 2.72 0.89 0.91 1.06 0.91 7 3.14 3.15 .... 3.30 1.17 1.17 1.24 1.16 2.7 2 7 2 8 8 4.00 3.86+ .... 4.14 1.44 1.43 .... 1.44 2.8 2 9 9 1.71 1.58 .... Tunnel angle Wall thickness Septal count 1 2 3 4 1 2 3 4 5 6 7 1 23 15 2 21° 14° 0.028 30 23 27 3 21° 14° 13° 18° 0.028 41 26 30 4 22° 17° 20° 22° 0.043 44 32 35 5 20° 15° 17° 19° . 022 0.050 47 39 45 6 16° 19° 20° 20° 0.025 0.043 0.036 47 45 46 7 17° 19° 19° 56 48 49 8 0.043 47 Specimens 1-5 are illustrated on plate 17 as figures 19, 18, 16, 15, and 20, respectively. Specimen i Thompson's paratype sagittal section and specimen 7 is our slide 11 from the Piasa limestone at station F5. Discussion. — This is one of the rare species in Illinois and our redescription is based largely upon syntypes from Iowa presented by Mr. Thompson. On plate 17 we figure four of these syntypes along with five specimens from Illinois. None of the latter is quite as large as the Iowa specimens but the two axial sections agree very closely with corres- ponding volutions of the syntypes and appear to represent slightly immature individuals. The whole specimens fig- ured are little more than half grown. This species is distinguished by its robust size, its evenly elliptical profile, its nearly constant form ratio through- out growth, its secondary chamber fill- ing, and the thickness of the wall of its proloculum. Distribution. — A few specimens were found in the Piasa limestone at station F5 in Jersey County; they are much more common in the same limestone at station Kd4 in Greene County and at Kd5 in Macoupin County. This species is also common in the Cutler limestone at stations Kd7, Kd9, and KdlO in St. Clair County. It is very rare in the Lonsdale limestone at station 545. Fusulina mysticensis Thompson Plate 18, figures 1-3 Fusulina mysticensis Thompson. Iowa Univ. Studies, vol. 16, pp. 319-320, pi. 23, figs. 1-3, 1934. Upper Des Moines shale, 50 feet above the Mystic coal, Appanoose County, Iowa. Material studied. — A few sections from the Lonsdale and a few from the Piasa limestone; also syntypes from Iowa. Original description. — "Shell large, elongate, fusiform to sub-cylindrical, 128 PENNSYLVANIAN FUSULINIDAE Measurements of F. mysticensis Thompson Volution Half length Radius vector Form ratio 1 2 3 4 1 2 3 4 1 2 3 4 0.092 . 085 . 079 0.086 0.092 0.085 0.079 0.086 1 0.35 0.28 0.36 0.24 0.14 0.14 0.14 0.14 2.5 2.0 2.6 1.7 2 0.46 0.50 0.56 0.50 0.21 0.21 0.23 0.22 2.2 2.4 2.4 2.3 3 0.79 0.79 0.84 0.79 0.30 0.31 0.31 0.34 2.6 2.5 2.7 2.3 4 1.20 1 . 23 1 . 43 1.36 0.43 0.45 0.49 0.50 2.8 2.7 3.0 2.7 5 1.76 1.65 2.14 1.64 0.60 . 62 . 67 0.71 2.9 2.7 3.2 2.3 6 2.65 2.34 3.05 2.71 0.83 0.83 0.86 0.96 3.2 2.8 3.5 2.8 7 3.14 3.45 4.30 3.60? 1.01 1.07 1.23 1.21 3.1 3.2 3.5 3.0 8 4.20 4.50 .... 1.23 1.30 1.33 3.4 3.4 9 1.40 1 . 50 Tunnel angle Wall thickness 1 2 3 4 1 2 3 4 1 16° 19° 0.020 0.020 2 17° 20° 18° 16° 0.025 0.020 0.025 3 18° 18° 22° 18° 0.030 0.030 0.030 4 19° 19° 21° 24° 0.035 0.035 0.040 0.035 5 25° 22° 25° 27° 0.040 0.050 0.035 0.040 6 23° 21° 31° 27° 0.040 0.040 0.050 0.040 7 25° 22° 50° 40° 0.040 0.035 0.040 8 47° 23° 46° 0.060 0.060 9 0.035 Specimens 1 and 2 are cotypes from Iowa. 2, 3, and 1, respectively. Specimens 1, md 4 are illustrated on plate 18 figures with bluntly pointed poles. In profile representatives of this species are vari- able, but sub-cylindrical forms with very bluntly pointed poles are the more common. Mature forms consist of 8% to 9 volutions and they are 8.5 to 10.2 mm in length and 2.6 to 3.0 mm in width. The form ratio of mature specimens is 1 :4 to 1 :3, with an average closer to the larger ratio. The average form ratio of 14 specimens is 1 :2.5 for the third volution, 1 :2.7 for the fourth, 1 :3.0 for the fifth, 1 :3.3 for the sixth, and 1 :3.2 for the seventh. The shell is fusiform in the inner six volutions and the poles are sharply pointed, but in the outer volutions the poles become very bluntly rounded and the lateral slopes are very gentle. "The septa are thin. The tectoria are very thin near the poles but they ap- pear to be relatively thick near the tun- nel ; this increase in thickness near the tunnel is due to the addition of material probably from the chomata. The dia- phanotheca is less dense than the tec- toria in the upper part of the septa but in the lower part of the septa it appears more dense and is not distinguishable from the tectoria. The external furrows are essentially straight. The septa are very narrowly and highly fluted through- out the length of the shell, but in the mid-portion of the shell the fluting is slightly broader than it is near the poles. The septal count varies considerably for different individuals. The average sep- tal count for 7 sagittal sections is 23 for the second volution, 28 for the third volution, 30 for the fourth volution, 35 for the fifth volution, 39 for the sixth volution, and 43 for the seventh volu- tion. The variations for these different volutions are 18 to 28, 25 to 31, 29 to 33, 31 to 37, 35 to 45, and 40 to 53, re- spectively. DESCRIPTION OF SPECIES 129 "The proloculum is sub-spherical and is 130 to 175 microns in diameter. The inner two volutions are very tightly coiled about the proloculum, in the third volution the coiling is somewhat less tight and beyond the third volution the chambers become noticeably higher. "The spirotheca is of medium thick- ness for the genus. The tectoria are thin, they are of about equal thicknesses, and they are composed of rather dense calcite. In the seventh volution, beyond the limits of the chomata, they are about 5 microns thick. The diaphanotheca is of translucent calcite and it is about 18.7 microns thick in the seventh volution near the tunnel. "The tunnel is one-third to one-half the height of the chamber and about one- fifth as high as wide in the seventh vo- lution. The tunnel angle is 21 to 32 degrees in the seventh volution, with an average of about 26 degrees. The cho- mata are in the form of very asym- metrical ridges in the inner five volu- tions, but in the outer volutions the de- posits are rather irregular and they cover the upper part of the spirotheca and the septa with rapidly decreasing thicknesses for about one-fourth the dis- tance from the tunnel to the poles." Discussion. — This is a rare species in Illinois and we have therefore quoted Thompson's description. Plate 18, figure 2 shows one of the syntypes presented to the senior author by Mr. Thompson. Figures 1 and 3 show the same species from the Lonsdale and the Piasa lime- stones respectively. Our table of meas- urements includes the same three speci- mens. This is one of the largest described species of the genus Fusulina s. s. It is much longer and more nearly cylindrical than F. megista and has a wider tunnel angle, though, as Thompson observes, these species are closely allied and occur together and in association with occa- sional shells more or less intermediate in shape between his types. One of our specimens (PI. 18, fig. 3) somewhat exceeds the maximum size indicated in the original description. It is possible that F. mysticensis is only a large, elon- gate variety of F. megista rather than a distinct species. F. acme is also closely similar but appreciably smaller, rela- tively shorter, and more elliptical in axial profile. Moreover, its walls are thinner, chiefly because of the lesser de- velopment of epitheca. Distribution. — This species was de- scribed from a limestone in the upper Des Moines shales about 50 feet above the Mystic coal in Appanoose County, Iowa. In Illinois it appears to be rep- resented rarely in the Lonsdale lime- stone at station 545 (see pi. 18, fig. 1) and also rarely, but perhaps more typ- ically, in the Piasa limestone at station F5. Fusulina piasaensis Dunbar and Henbest, n. sp. Plate 18, figures 4-9 Material studied. — Not more than a score of specimens were collected from stations F5 and Kdl ; 6 sections were made. Description. — A long, subcylindrical species of 8 or 9 volutions, attaining at 8 whorls a length of 8.0 to 11.0 mm and a diameter of 2.0 to 2.5 mm. In the early whorls the ends taper to slender and acute poles, but in the last 2 or 3 whorls the ends fill out and become bluntly rounded. The proloculum is of medium size, measuring in our types between 120 and 160 microns in diameter. The whorls are rather closely coiled and the in- crease in height is very gradual. The form ratio and the axial profile change progressively during the first 5 or 6 vo- lutions, the inner ones being fusiform, with nearly flat lateral slopes converg- ing to acute ends and with a form ratio of 2.0 to 3.0, whereas the ratio rises to 4.0 or more at maturity and the form is nearly cylindrical. The wall is relatively thin on account of the deficiency of the tectoria, which are thinner than the protheca in most parts of the shell. The septa are numerous, increasing gradually from about 15 in the first whorl to 40 or more in the last. Septal folds are strong and regular from pole to equator as in F. mysticensis and F. acme. Septal pores are abundant in the 130 PENNSYLVANIAN FUSULINIDAE Measurements of F. piasaensis Dunbar and Henbest Volution Half length Radius vector Form ratio 1 2 3 1 2 3 1 2 3 1 2 3 4 5 6 7 8 0.071 .... 0.071 0.21 .... 0.27 0.36 0.64 0.51 0.64 1.16 0.79 . 87 1 . 72 1 . 37 1.27 2.60 2.00 2.15 3.58 2.75 3.15 4.50 3.57 4.15 5.40 0.071 0.078 0.064 0.11 0.12 0.10 0.15 0.21 0.16 0.21 0.29 0.22 0.31 0.41 0.33 0.44 0.59 0.48 0.61 0.80 0.69 0.79 1.01 0.87 1.01 1.24 1.07 i!9 '.'.'. 2.1 2.4 2.9 3.2 3.0 4.0 3.6 2.8 4.2 4.1 2.9 4.4 4.2 3.5 4.4 4.0 3.7 4.4 4.1 4.1 4.3 Tunnel angle Wall thickness Septal count - 1 2 3 1 2 3 4 5 1 2 3 4 5 6 7 8 14° ... 26° 15° ... 23° 19° 21° 23° 24° 25° 26° 22° 27° 25° 45° 31° 35° 27° 48° 32° 34° 63° 6.050 '.'.'.'.'. '.'.'.'.'. 0.040 0.030 0.045 0.035 0.070 '.'.'.'.'. 6!050 15 13 23 19 29 22 36 30 38 33 43 37 ? 40 ? Specimens 1-5 are illustrated on plate 18 as figures 6, 7, 5, 8, and 9, respectively. end zones of the outer whorls and are relatively coarse. The tunnel is wide, its angle increas- ing with rapid acceleration in the last 2 volutions and reaching an extreme of more than 60°. The chomata are nar- row but somewhat better developed than in F. mysticensis. Discussion. — This is not the most abundant but is probably the most char- acteristic species in the Piasa limestone from which it is named. It resembles F. mysticensis and was at first identified therewith, but comparison with cotypes of that species and with Thompson's description and illustrations indicates consistent differences from this Piasa form. The Illinois species is distinctly more slender and has a larger form ratio. It also has a wider tunnel, espe- cially in the outer whorls, and its poles are more acute, the axial profile of the early whorls being acutely fusiform in this species and subelliptical in F. mys- ticensis. F. piasaensis also resembles F. acme but attains a length almost twice as great and has a much larger form ratio and a wider tunnel. In size and shape it is almost intermediate between F. mysticensis and F. eximia. The latter is smaller and more slender. Distribution. — F. piasaensis is mod- erately common in the Piasa limestone. Our best collections are from station F5, the type locality of this formation, in Jersey County, Illinois. It occurs also in the Cutler limestone at station Kdl. Triticites ohioensis Thompson Plate 19, figures 1-22; plate 20, figures 20-24 Fusulina secalica Condit, Ohio Geol. Surv., 4th ser., Bull. 17, pp. 44, 88. Cambridge limestone, eastern Ohio. Triticites ohioensis Thompson, Jour. Pale- ontology, vol. 10, p. 680, pi. 91, figs. 1-3, 1936. Brush Creek and Cambridge lime- stones, Gallia County, Ohio. DESCRIPTION OF SPECIES 131 Material studied. — Abundant speci- mens were collected from a few localities in the Livingston limestone in Edgar and Christian Counties, Illinois. More than a score of sections were prepared. Description. — A slender, cigar-shaped species of about 8 volutions attaining a length of about 9.0 mm and a diameter of 2.0 mm. The proloculum is small, commonly between 80 and 100 microns in diame- ter, and subspherical. No microspheric individuals have been found. The volu- tions are rather closely coiled but the wall is thin and septal folds weak so that in axial section the whorls do not appear crowded. The ends are elon- gated with rapid acceleration and the form ratio increases markedly after the third volution, commonly being between 4.0 mm and 4.5 mm at maturity. The spiral wall is thin for this genus, measuring 15 to 25 microns in thick- ness in the inner whorls and 35 to 55 in the fifth and sixth, reaching a maxi- mum of about 65 microns near the equa- tor in the penultimate whorl. It con- sists of a thin tectum and a well denned keriotheca in the outer whorls where the alveolar structure is conspicuous in good thin sections, as indicated in figures 21 and 22 of plate 19; but in the first 3 volutions the structure of the keriothecal layer is very obscure and there is con- siderable epithecal deposition. The septa are only moderately numer- ous and relatively simple. Septal fold- ing appears only in the polar zones of the first 2 or 3 volutions and gradually spreads toward the middle in the outer whorls. Except near the ends, however, the folds are low and weak, even in the adult volutions. In axial sections, there- fore, there is a net of septal loops along the axis increasing in width to the ends of the last whorl, but septal folds are few and low across the middle half of the shell. In the sections figured the septa cross the slice at occasional inter- vals on each side of the tunnel, not so much because of folding as because their course is not quite parallel to the slice, the actual loops being almost con- fined to the axial region and the end zones. Septal pores are abundant in the end zones of the last 3 or 4 volutions. The tunnel is low and broad, the tun- nel angle increasing from about 25° in the third whorl to near 60° in the sev- enth. The chomata are relatively broad and heavy and fusulinellid in form in the first 2 or 3 volutions and thereafter become narrower but persist into the last volution as typical levee-like ridges beside the tunnel. Discussion. — The primitive character of this species is indicated by several ontogenetic features. The first 2 or 3 vo- lutions are fusulinellid in wall structure, in the form of the chomata, and in the simplicity of the septa. If juvenile specimens alone were examined they would almost certainly be referred to Fusulinella, though they are somewhat more elongate than the typical form of that genus. The wall of these early whorls is not alveolar, and if originally porous probably had fine tubular pores which have since been obscured by the epitheca. As Thompson has observed, it is one of a group of primitive, slender, thin- walled species commonly identified as Triticites irregularis (Staff). While representing about the same stage of development as the typical form of that species, T. ohioensis may be distin- guished by its more regular growth,, more cylindrical form, slightly thicker wall, and coarser alveoli. Both T. osag- ensis Newell and T. neglectus Newell are somewhat more advanced in their evo- lution and have stronger septal fluting. Distribution. — T. ohioensis was de- scribed from the Brush Creek and Cam- bridge limestones, both of which are near the base of the Conemaugh group, in Gallia County, Ohio. In Illinois it is abundant at station 286 in Edgar County in the Livingston limestone, a supposed equivalent of the La Salle limestone of La Salle County. Although the Livingston limestone is well devel- oped in Edgar and Clark Counties, es- pecially near the town of Marshall, Trit- icites is rare except locally. The species occurs at station 490 in Christian County in what appears to be the same limestone, but there the fusulines are.- 132 PENNSYLVANIAN FUSULINIDAE Measurements of T. ohioensis Thompson Volution Half length Radius vector Form ratio 1 2 3 4 1 2 3 4 1 2 3 4 0.05 0.043 0.05 0.047 0.05 0.045 0.05 0.04 1 0.17 0.10 0.12 0.13 0.08? 0.08 0.12 2.1 1.0 2 0.30 0.21 0.23 0.27 0.12 0.12 0.18 0.10 2.5 1.8 1.3 2.7 3 0.47 0.40 0.39 0.54 0.20 0.19 0.26 0.16 2.4 2.1 1.5 3.4 4 0.87 0.86 0.81 0.77 0.31 0.28 0.40 0.25 2.8 3.1 2.0 3.1 5 1.80 1.57 1.43 1.57 0.47 0.41 0.58 0.40 3.8 3.8 2.5 3.9 6 2.95 2.46 2.43 2.36 0.65 0.61 0.80 0.60 4.5 4.0 3.0 3.9 7 4.30 3.46 3.78 3.00 ? 0.80 ? 0.82 4.3 3.6 8 ? 1.05 Tunnel angle Wall thickness Septal count 1 2 3 4 1 2 3 4 5 6 7 8 1 0.015 9 10 11 2 0.025 15 17 15 18 3 25°? 26° 25° 0.015 0.025 0.020 17 21 19 19 4 32° 40° 44° 22° 0.020 0.035 0.040 20 23 22 24 5 58° 50° 55° 30° 0.035 0.040 0.050 0.045 23 ? 22 23 6 55° 60° 56° 38° 0.035 0.050 0.055 0.035 25 ? 22 26 7 59° 58° ? 40° 0.045 0.065 0.065 22 8 ? 47° 30 9 ? Specimens 1 to 8 are illustrated on plate 1& as figures 10, 11, 13, 12, 20, 14, 15, and 18, respectively. encrusted with algae and are poorly preserved. It is less common in the Omega limestone at stations W10 and Wll, in Effingham County. In the mid-Continent region the stage of evolution closest to that of T. ohioen- sis is found in the Kansas City group in the lower part of the Missouri series. Triticites venustus Dunbar and Henbest, n. sp. Plate 20, figures 5-19 Material studied. — Abundant material was collected from three localities in the Omega limestone in Effingham County, numerous specimens from the Livings- ton limestone at station 490 in Christian County, and a few poorly preserved specimens from the Calhoun limestone at station 329 in Lawrence County. More than a score of sections were pre- pared. Description. — A small elongate-fusi- form species of about 7 volutions at- taining a maximum length of about 6 mm and a diameter of about 1.8 mm. The lateral slopes are convex and the ends rather bluntly rounded. The proloculum is small, commonly between 80 and 100 microns in diameter. The early whorls are thin-walled and rather closely coiled but the outer ones increase gradually in height. The wall attains a maximum thickness of only 60-75 microns but shows exceptionally well the keriothecal structure in the outer whorls, where the alveoli have a diameter of about 10 microns and the intervening lamellae a thickness of 6 or 7 microns. The septa are folded somewhat irregu- larly in the end zones but the folds die out toward the middle of the shell where the septa are nearly plane. The tunnel is rather wide, the tunnel anole increas- DESCRIPTION OF SPECIES Measurements of T. venustus Dunbar and Henbest 133 Volution Half length Radius vector Form ratio 1 2 3 4 1 2 3 4 1 2 3 4 0.046 0.050 0.043 0.050 0.046 0.050 0.043 0.050 1 0.10 0.14 0.13 0.21 0.07 0.08 0.09 0.10 1.4 1.7 1.4 2.i 2 0.20 0.29 0.29 0.43 0.11 0.12 0.14 0.16 1.8 2.8 2.0 2.6 3 0.36 0.50 0.50 0.69 0.16 0.17 0.19 0.23 2.2 2.6 2.6 3.0 4 0.61 0.79 0.93 1.16 0.23 0.25 0.29 0.41 2.6 3.1 3.2 2.8 5 0.96 1.07 1.44 1.72 0.36 0.36 0.46 0.50 2.6 3.0 3.1 3.4 6 1.58 1.57 2.43 9 0.51 0.50 0.71 0.73 3.1 3.1 3.4 7 ? ? ? ? 0.71 0.96 Tunnel angle Wall thickness Septal count 1 2 3 4 1 2 3 4 5 6 1 0.015 0.015 12 12 2 20° 32° 0.020 0.020 0.025 16 16 3 33° 25° 32° 32° 0.030 0.030 0.025 0.025 18 20 4 34° 25° 27° 35° 0.030 0.030 0.030 22 23 5 37° 34° 26° 42° 0.050 0.045 0.045 0.045 23 24 6 41° 41° 32° 48° 0.055 0.060 0.065 0.055 24 27? 7 52° 42° 0.075 24 8 26 9 28? Specimens 1-3 and 6 are illustrated on plate 20 as figures 7, 5, 6, and 8, respectively. ing from 25° or more in the third volu- tion to about 50° in the seventh. The chomata are comparatively narrow but well denned ridges. Figure 6 of plate 20 gives a false impression of very mas- sive chomata because in several of the volutions the septa lie in the plane of the slice for a distance on each side of the tunnel where they are essentially plane. The true size of the chomata may be seen in all but the penultimate volution on the right side above. Sep- tal pores are abundant in the end zones of the last 2 or 3 volutions. Discussion. — This species most closely resembles T. secalicus var. oryziformis Newell from the lower part of the Doug- las group in the Virgil series of Kansas ; but it differs therefrom in being smaller and more delicate at all stages of growth. Although both have comparable pro- locula, T. venustus averages about as large in the seventh volution as the Kan- sas form does at 5% volutions. They agree well, however, in shape and in form ratio, but the septal folding ap- pears to be slightly more advanced in T. venustus. The coarseness of the alveoli in the keriotheca of the latter, and the clarity with which the structure may be seen appear to be distinctive features but are possibly due in some degree to the exceptional preservation of the Illi- nois shells. A cotype of T. secalicus var. oryziformis is introduced as figure 4 on plate 20 for comparison. Distribution. — The above description is based chiefly on material from the Omega limestone at stations 504, W10, Wll, and W13, in Effingham County. The species is sparsely represented at station 329 in Lawrence County in the probable equivalent of the Calhoun lime- stone. There, however, the specimens are small, partially pyritized, and badly pre- served. They lack one or two volutions of 134 PENN8YLVANIAN FUSULINIDAE Measurements of T. mediocris Dunbar and Henbest Volution Half length Radius vector Form ratio 1 2 3 1 2 3 1 2 3 0.054 0.036 0.067 0.054 0.036 0.067 1 0.17 0.086 0.16 0.10 0.071 0.13 1.7 l.i 1.2 2 0.34 0.20 0.34 0.20 0.13 0.20 1.7 1.5 1.7 3 0.63 0.41 0.61 0.34 0.21 0.29 1.8 1.9 2.1 4 1.17 0.66 0.86 0.57 0.30 0.43 2.0 2.2 2.0 5 1.52 0.96 1.34 0.83 0.43 0.66 1.7 2.2 2.0 6 2.25 1.40 2.00 1.1? 0.66 0.90 2.0? 2.1 2.2 7 2.93 2.00 0.93 2.1 8 1.33 2.0 + Tunnel angle Wall thickness Septal count - 1 2 3 1 2 3 4 5 6 7 1 _ 12 10 10 11 2 17° 12° 0.040 19 19 15 16 3 27° 25° 16° 0.040 0.035 22 23 19 18 4 28° 23° 22° 0.030 0.050 26 27 22? 20 5 28° 23° 26° 0.080 0.045 0.080 27 27 23 24 6 32° 23° 31° 0.080 29 28 ? 26 7 39° 31° ? ? ? Specimens 1-3 and 4 and 5 are illustrated on plate 21, figures 5, 4, 3, 7, and 8, respectively. being as large as the specimens from sta- tion 504 but agree well if corresponding volutions be measured. Probably the specimens at station 329 failed to reach normal mature size because of inhospita- ble environment. The species also occurs in the Livingston limestone at station 490 in Christian County where it is asso- ciated with T. ohioensis. Triticites mediocris Dunbar and Henbest, n. sp. Plate 21, figures 2-5, 7, 8, 16 Material studied. — Abundant speci- mens were collected from the Greenup limestone at station H9 ; more than a score of sections were prepared. Description. — This is a fusiform spe- cies of 6 to 8 volutions attaining at 6 volutions a length of 4 to 5 mm and a thickness of about 2.0 mm. Most of the axial sections appear elongate-elliptical, the lateral slopes being gently convex and the ends broadly rounded. The four measured types show the normal range of variation in proportions. Commonly the shape and the form ratio change but little during growth, but the more elon- gate shells attain somewhat more slender adult proportions by gradual increase in form ratio. In the majority of shells the adult form ratio is about 2.0. The proloculum is small, ranging from about 75 to 100 microns in diame- ter. The spiral wall is moderate in thickness, increasing from 20 to 25 mi- crons in the second whorl to 70 or 80 microns in the outer volutions. The outer surface of the wall is commonly formed of epitheca near the middle of the shell, especially in the inner volu- tions. The septa are moderately numerous, increasing from about 10 in the first vo- lution to near 30 in the last. They are only slightly folded, except near the ends. The tunnel is of moderate width and the tunnel angle tends to increase from near 25° in the third volution to DESCRIPTION OF SPECIES 135 between 30° and 40° in the last. It is commonly about half the height of the volution. The chomata are well denned but of moderate size. Septal pores are present but their distribution is ob- scured by the dark matrix that occupies the outer volutions of most of the shells studied. Discussion. — This species resembles both T. secalicus (Say) and T. cullo- mensis Dunbar and Condra of the mid- Continent region, but after direct com- parison with the types and many dupli- cate specimens of both those species, we are convinced that it is distinct from each. Our species is shorter and rela- tively thicker than T. secalicus, its outer volutions are a little higher, and its tun- nel angle is somewhat narrower. Be- cause the resemblance to T. cullomensis is so close, we introduce sections of four syntypes of the latter for comparison (pi. 23, figs. 13-16). T. cullomensis nor- mally attains a larger size and has dis- tinctly thicker walls and somewhat less deeply folded septa. It may be added that T. cullomensis represents a conser- vative, average-shaped type of Triticites and that species of this tribe are difficult to distinguish. In the original descrip- tion too much latitude was given and the description was not sufficiently critical. One of the specimens originally figured by Dunbar and Condra is here refigured and should be considered the holo- type. The other three specimens (figs. 13-15) are from the same original lot. The species should be restricted to this type of shell. In this connection it may be noted that specimens from the Ames limestone at Pittsburgh, Pennsylvania, presented by Dr. William Darrah (pi. 23, figs. 17 and 18) agree fully and precisely with the typical T. cullomensis. The Illinois species may be closely related- but is probably of slightly different age. Distribution. — Abundant in the Greenup limestone at station H9 in Cumberland County, where it is associ- ated with its variety angustus n. var. and with T. callosus n. sp. Triticites mediocris var. angustus Dunbar and Henbest, n. var. Plate 21, figures 1, 6, 9-14. Material studied. — Abundant speci- mens were collected from two localities, H9 and W15, in the Greenup Milestone, and more than a score of sections were prepared. Description. — Although the majority of the shells at station H9 agree closely with the types of T. mediocris, about a third of those sectioned are decidedly more slender at all stages of growth, at- taining a form ratio of approximately 3.0 at maturity. As indicated by figures 1, 9, and 12 of plate 21, these tend to taper to rather narrow ends. Figure 11 shows a slightly oblique section in which the ends appear a little more bluntly rounded. Except for the differences in propor- tion, these shells agree closely with typi- cal T. mediocris and, indeed, the speci- Measurements of T. mediocris var. angustus Dunbar and Henbest Volution Half length Radius vector Form ratio 12 3 4 12 3 4 12 3 4 1 2 3 4 5 6 7 0.05 .... 0.050 0.057 0.21 .... 0.18 0.12 0.44 0.41 0.36 0.31 0.70 0.73 0.57 0.57 1.19 1.27 0.93 0.96 2.01 1.78 1.37 1.45 ? 2.86 2.01 3.50 ? 4.29 0.05 .... 0.050 0.043 0.09 .... 0.09 0.079 0.14 0.15 0.14 0.14 0.23 0.27 0.23 0.24 0.39 0.42 0.41 0.39 0.60 0.65 0.50 0.59 0.91 0.71 0.89 0.96 .... 1.3 2.3 ... 2.0 2.0 3.1 2.7 2.5 2.2 3.0 2.7 2.4 2.3 3.0 3.0 2.2 2.4 3.3 2.7 2.7 2.4 3.1 2.8 3.9 ? Specimens 2 and 3 are illustrated on plate 21 as figures 12 and 11, respectively. 136 PENNSYLVANIAN FUSULINIDAE mens shown by figures 6 and 11 are somewhat transitional in shape. For these reasons we consider the slender shells only a variety of T. mediocris and name it angustus because of its slender form. Adult shells have about 7 volu- tions and attain a diameter of 2.1 to 2.2 mm and a length of 5.5 to about 7.0 mm. The specimen shown by figure 9 is exceptional in having a proloculum much larger than any of the other shells in this suite. This variety resembles T. secalicus very closely in size, shape, and proportions, but its septal folding is more advanced, rather high, narrow septal loops appear- ing more abundantly than they do in T. secalicus, especially in the outer whorls. Furthermore, the tunnel angle of T. secalicus is considerably wider. Occurrence. — Found in abundance at two localities, H9 and W15, in the Greenup limestone. At the former it occurs with T. mediocris s. s. and T. callosus n. sp., but at station W15 only this variety was found. Triticites cullomensis Dunbar and Condra Plate 23, figures 13-18 Triticites cullomensis Dunbar and Condra, 1927. Nebraska Geological Survey, 2d ser., Bull. 2, pp. 93-95, pi. 5, figs. 5-10. Shawnee group, eastern Kansas and Nebraska. (Emendation of species appears in discussion of T. mediocris, n. sp., p. 135 above.) Triticites callosus Dunbar and Henbest, n. sp. Plate 21, figure 15; plate 22, figures 1-11 Material studied. — Numerous speci- mens were collected from a single lo- cality, station H9, in the Greenup lime- stone. Thirteen sections were prepared. Description. — This is the largest fusu- line known in Illinois. It is a thickly fusiform species of 8 or 9 volutions at- taining a length of 8 to 10 mm and a diameter of about 4 mm. The shell is thickest at the middle but not inflated, the lateral slopes tapering with slight convexity to neatly rounded ends. The inner whorls are relatively very short, having a form ratio of 1.1 to 2.1 but the ratio increases gradually to 2.0 to 3.0 at maturity. The proportions vary considerably among the specimens stu- died, the holotype having a form ratio not over 1.5 until the seventh volution when it rises to 2.4, whereas the other measured types have a form ratio near 2.0 in the immature whorls. The proloculum shows an exceptional range of size, from a diameter near 100 microns to about 300 microns; but the early whorls are bilaterally symmetrical and typically fusulinoid in all the speci- mens sectioned and none can be consid- ered truly microspheric. The whorls in- crease rather rapidly in height. The combination of rapid expansion and great variation in size of proloculum leads to apparently great discrepancies in the tabulated measurements; but in fact the early volutions in shells hav- ing small prolocula represent an early ontogenetic stage omitted from shells having much larger prolocula. Thus in our tabulation volutions 3 and later of specimens 3 and 4 should be compared with volutions 2 and following in speci- mens 1 and 2. The spirotheca is exceptionally thick, commonly measuring more than 50 mi- crons in the third volution and 100 to 125 microns in the sixth and seventh. The alveoli of the keriotheca are coarse and conspicuous, the individual alveoli having a maximum diameter of about 16 microns and the intervening lamellae a thickness of 6 to 8 microns. The kerio- theca is the dominant layer of the wall but an appreciable epithecal film covers the tectum thereby lining the floor of each chamber.. The septa are numerous, increasing gradually in successive volutions from 12 or 15 in the first to 35 or 40 in the seventh and eighth. In the first 2 or 3 volutions they are nearly plane, but folds begin to appear near the ends and gradually spread to the middle of the shell in the outer whorls. In the end zones, where the septa converge, op- posed folds touch, but across the middle of the shell the septa are more widely spaced and the folds are weak. DESCRIPTION OF SPECIES Measurements of T. callosus Dunbar and Henbest 137 Volution Half length Radius vector Form ratio 1 2 3 4 1 2 3 4 1 2 3 4 0.13 .... 0.065 0.13 0.100 0.065 1.0 1 0.21 6.39 20 0.26 0.185 0.10 2.i 2.0 2 0.50 0.64 .... 0.34 0.46 0.30 0.17 1.1 2.1 2.0 3 0.93 1.04 0.50 60 0.69 0.47 0.31 0.29 1.3 + 2.2 1.6 2.1 4 1.37 1.46 0.90 0.84 0.96 0.67 0.46 0.43 1.4 + 2.2 2.1 1.9 5 1.95 1.90 1.19 1 43 1.30 0.91 0.67 0.63 1.5 2.1 1.8 2.3 6 3.05 3.05 1.71 2.07 1.64 1.24 0.91 0.94 1.3— 2.4 1.9 2.2 7 4.7 + 4.43 2.43 2.71 1.96 1.60 1.30 1.30 2.4 + 2.8 1.9 2.1 8 3.25 3 43 1.96 1.64 2.0 Tunnel angle Wall thickness Septal count 1 2 3 4 1 2 3 4 5 6 7 1 15°? 14° 15° 13° 23° 15°? . 19° 12° 0.065 0.080 0.080 0. 045 0.055 0'055 12 20 22 23? 2 3 0.040 26 4 24° 21° 18° 0.065 0.070 0.045 31 29 24 5 26° 23° 23° 0.130 0.070 0.085 0.065 33 30 29 6 32° 30° 20° 0.130 0.105 0.105 0.085 40 32 34 7 ? 34° 31° 0.130 0.100 0.090 0.120 37 33? 35 8 41° 0.100 42? ? ? 9 ? Specimens 1-7 are illustrated on plate 22 as figures 5, 2, 4, 3, 7, 8, and 6, respectively. The chomata are typically fusulinel- loid in the first 3 or 4 volutions, being broad and massive, and although rela- tively narrower in the outer whorls are strongly developed even for this genus. Septal pores are abundant in the end zones of the outer whorls. Discussion — T. callosus belongs to the group of T. ventricosus (Meek and Hay- den) which it resembles closely in its shape, large size, and number of volu- tions, but it differs in several respects, notably in having a slightly thicker wall and heavier, more widely spread epithe- cal deposit. Also its septa are some- what more irregularly folded and in ax- ial sections it shows a more extensive net of septal loops in the axial and end zones. The thick wall and heavy epithecal deposit remind one of T. plummeri Dun- bar and Condra, but that species is shorter and more nearly spherical and has a smaller proloculum, more volu- tions, and more strongly folded septa. Distribution. — This species is known from a single isolated outcrop in Cum- berland County, station H9. The gen- eral stratigraphic relations indicate clearly that this limestone is near the top of the Pennsylvanian section in Illi- nois, and it has been inferred on the basis of general field relations that this may be the Omega limestone, but the fusulines would indicate that it is not only younger than the Omega but is sep- arated from it by a considerable inter- val or a great hiatus. The fusuline species found in the Omega limestone are closely allied to those which occur in the Kansas City group of the mid-Continent region, and represent the same primitive stage of 138 PENNSYLVANIAN FUSULINIDAE Measurements of T. tubgidus Dunbar and Henbest Volution Half length Radius vector Form ratio 1 2 3 4 1 2 3 4 1 2 3 4 0.050 0.071 0.045 0.049 0.050 0.071 0.044 0.048 1.0 1.0 1.0 1.0 1 0.14 0.15 0.10 0.143 0.09 0.116 0.08 0.086 1.5 1.3 1.8 1.6 2 0.30 0.25 0.19 0.26 0.16 0.17 0.13 0.14 1.8 1.4 1.4 1.8 3 0.47 0.39 0.33 0.46 0.26 0.27 0.21 0.22 1.8 1.4 1.5 2.0 4 0.66 0.63 0.60 0.71 0.38 0.39 0.31 0.30 1.7 1.6 1.9 2.3 5 1.16 1.06 0.96 1.11 0.56 0.57 0.47 0.44 2.0 1.8 2.0 2.5 6 1.57 1 . 50 1 . 53 1.57 0.78 0.80 0.68 0.64 2.0 1.8 2.2 2.4 7 2.35 2.17 2.28 1.08 1.10 0.96 0.90 2.1 2.1 2.3 Tunnel angle Wall thickness Septa] count 1 2 3 4 1 2 3 4 5 1 0.015 0.020 11 2 23° 17° 21° 22° 0.025 0.020 19 3 21° 20° 20° 22° 0.040 22 4 22° 20° 22° 0.050 0.035 0.025 25 5 21° 22° 23° 27° 0.060 0.060 0.045 0.040 33 6 22° 23° 24° 30° 0.110 0.060 0.065 0.060 33 7 21° 20° 28° 0.075 0.080 Specimens 1 to 5 are illustrated on plate 23 as figures 11, 10, 8, 9, and 12. evolution of the genus Triticites. T. cal- losus, on the contrary, appears to be one of the group of T. ventricosus which first appears in the Wabaunsee group of the mid-Continent region. A high stratigraphic position is indicated not only by its great size, but also by its exceptionally thick wall and its enor- mous prolocula. Since the fusuline fauna of the Livingston and Omega limestones can hardly be younger than the Lansing stage of Kansas, and the fusulines of station H9 can hardly be older than Wabaunsee, the interval be- tween the Omega limestone and the limestone of H9 in central Illinois would be represented by some 500 feet of strata in Kansas, comprising the Douglas and Shawnee groups. Triticites turgidus Dunbar and Henbest, n. sp. Plate 23, figures 6-12 Material studied. — Abundant speci- mens were collected from two localities in Effingham County. Seven sections were made. Description. — A small, thickly fusi- form species of about 7 volutions, at- taining at that stage of growth a length of 4.5 to 4.7 mm and a thickness of 1.8 to 2.2 mm. Axial sections are rather evenly elliptical, with gently convex lateral slopes and rounded poles. The shape and proportions vary but little after the first volution, the form ratio being between 1.5 and 2.0 in the third whorl and between 2.1 and 2.5 in the outer whorls. The proloculum is rather small, meas- uring between 90 and 150 microns in diameter in our sections, and the whorls begin rather closely coiled but expand with gradual acceleration to maturity. The spiral wall is only 20 to 25 microns thick in the inner whorls but increases to 60 or 80 (rarely 100) microns in the outer volutions. The alveolar texture of the keriotheca is conspicuous. The floor of the volutions is covered locally by epitheca. DESCRIPTION OF SPECIES 139 The septa are rather numerous for a shell of this size, increasing in number in successive volutions as shown in the table below. They are moderately strongly folded for this genus, septal loops appearing even near the middle of the shell in places where the section lies close to a septum. Septal pores are plentiful in the third and succeeding whorls. The tunnel is rather narrow and is exceptional in that it widens so slowly that the tunnel angle scarcely increases with growth, being about 20° in the third volution and commonly not more in the seventh. Its height is about two* fifths the height of the volution. The chomata are well defined, but generally rather narrow and of moderate height. Discussion. — This species resembles T. skinneri Thompson of the Ames lime- stone of Ohio, but direct comparison with the types of that species, kindly loaned by Dr. Arthur K. Miller, shows clear distinctions. The Ohio shell is somewhat smaller in corresponding vo- lutions; its early volutions are more slender and more closely coiled and have wider chomata than does our species, and its poles are somewhat more acute. T. beedei Dunbar and Skinner is much larger and differs constantly in shape, having a thicker mid-region and more acutely pointed ends. Our species more closely resembles T. cullomensis Dunbar and Condra, with which it agrees closely in shape and proportions. However, that shell attains a considerably larger size, has an appreciably thicker wall, a wider tunnel, and somewhat less deeply folded septa. The resemblance to T. mediocris is so close that the differences are difficult to state even though direct comparison shows that they are distinct. The form ratio is almost precisely the same in these species, and the number of volu- tions is identical, but if we compare shells starting with equal prolocula, that of T. mediocris is appreciably the larger at all stages of growth. Furthermore, T. mediocris tends to have a slightly dif- ferent shape, the axial sections being more broadly rounded than in T. tur- gidus n. sp. Also the wall is appreci- ably thicker in T. mediocris where, for example, it is normally about 80 mi- crons in the fifth whorl, and in T. tur- gidus n. sp. not more than 60 microns. An apparent exception to the last state- ment appears in the tabulated measure- ments of specimen no. 2 of T. mediocris, but in that specimen the proloculum is very small and the dimensions of each volution must be compared with those of one earlier in normal shells. The two species occur in distinct horizons, and in different fusuline assemblages. Occurrence. — Abundant in the Shum- way limestone at stations W12 and W14 in Effingham County, Illinois, where it is associated with T. pauper. Triticites pauper Dunbar and Henbest, n. sp. Plate 23, figures 1-5 Material studied. — Abundant speci- mens were collected from two localities in Effingham County. Five sections were made. Description. — A small, slender species of about 6 volutions, attaining a length of 4 to 4.5 mm and a thickness of 1 to 1.2 mm. The shell is narrowly fusiform with sharply pointed poles. It is not appreciably inflated at the middle but is commonly somewhat irregular in its growth. The proloculum is very small, com- monly between 75 and 100 microns in diameter, and the volutions are low, and the wall exceptionally thin for this genus. The first volution is short and subglobular but the form ratio increases steadily with growth, rising from about 2.0 in the second to near 4.0 in the sixth volution. Keriothecal structure is clearly shown in the spiral wall, which attains a thick- ness of only about 30 microns in the third volution and 45 to 55 microns in the sixth. The septa are rather slightly and irregularly folded ; septal pores are abundant in the last volution and com- monly inconspicuous, if present, in ear- lier whorls. The number of septa in- creases in successive whorls from near 10 in the first to about 25 in the last. Chomata are narrow and slight. The 140 PENNSYLVANIAN FUSULINIDAE Measurements of T. paupeb Dunbar and Henbest Volution Half length Radius vector Form ratio 1 2 3 1 2 3 4 1 2 3 ? 0.04 0.036 ? 0.04 0.036 0.049 1 0.10 0.07 0.072 0.07 0.06 ? 0.074 1.4 1.2 ? 2 0.21 0.16 0.21 0.11 0.10 0.10 0.119 2.0 1.6 2.1 3 0.37 0.33 0.36 0.15 0.16 0.16 0.185 2.5 2.0 2.2 4 0.73 0.57 0.60 0.23 0.23 0.22 0.286 3.2 2.5 2.7 5 1.45 ? 1.01 0.34 0.36 0.34 0.430 4.2 ? 3.0 6 2.14 1.95 1.85 0.49 0.52 0.57 0.58? 4.4 3.8 3.3 Tunnel angle Wall thickness Septal count 1 2 3 1 2 3 4 4 1 0.015 11 2 15° 24° 14 3 23° ? 0.025 0.020 19 4 25° 29° 0.030 0.030 0.030 0.025 21 5 30° 46° 0.035 0.035 0.035 0.030 23 6 34° 43° 0.055 0.045 0.045 25? Specimens 1 to 4 are illustrated on plate 23 as figures 5, 2, 3, and 4, respectively. tunnel is broad and low, the tunnel angle increasing with growth but, as in- dicated in the table, showing consider- able irregularity. Discussion. — This species falls in the group of Triticites irregularis (Staff) as indicated by its slender form, small size, slight septal folding, and thin wall. It is much smaller than the typical T. irregularis and is closest to T. neoras- kensis Thompson, from which it differs in having appreciably more septal fold- ing and thinner walls. The form of the septa would suggest that it is somewhat more advanced and therefore younger than T. neoraskensis Thompson. It is distinctly smaller and more slender than T. ohioensis Thompson. Occurrence. — This species has been found rather abundantly at two locali- ties, stations W12 and W14, in the Shumway limestone in Effingham County. In both it is associated with. T. turgidus and no other fusulines. CHECK LIST OF GENERA AND SPECIES A check list of the genera and species of the fusulines was first presented in 1937 in the University of Texas Bulletin 3701, pages 700-714, by Dunbar and Skinner. It included 52 generic and 457 specific names. The present list brings that one up to date and includes 55 generic and 675 specific names. Of the genera 38 appear to be valid (though 5 of these are of questionable value) and 17 are either homonyms or otherwise invalid. The names of invalid genera are italicized and in the list of species erroneous generic identifications are also italicized. In the specific list 19 synonyms are indicated by italics and 13 nomina nuda are noted, and many have been re- ferred to the correct genus according to present interpretations ; but no attempt has been made to verify the validity of all the species. The chief purposes of the list are to furnish a quick reference to original description and to enable the student to avoid an invalid duplication of names. By noting the author and date of the generic or specific name and referring to the bibliography, a complete citation can be obtained. Only the origi- nal descriptions or new naming of genera and species are indicated. Genera and Type Species Beedeina Galloway, 1933 (=Fusulina) ; Fu- sulinella girtyi Dunbar and Condra Boultonia Lee, 1927; B. willsi Lee Brevaxina Schenck and Thompson, 1940 (subgenus); Doliolina compressa De- prat Cancellina Hayden, 1910; Neoschwagerina primigena Hayden Codonofusiella Dunbar and Skinner, 1937; C. paradoxica Dunbar and Skinner Colania Lee, 1933; C. kwangsiana Lee Depratella Ozawa, 1928 (= Schubertella) ; Neofusulinella giraudi Deprat Doliolina Schellwien (=Misellina), 1902; Schwagerina lepida Schwager Eoschubertella Thompson, 1937; Schuber- tella lata Lee and Chen Eoverbeekina Lee, 1933; E. intermedia Lee Fusiella Lee and Chen, 1930; F. typica Lee and Chen Fusulina Fischer, 1829; F. cylindrica Fischer Fusulinella Moller, 1877; F. bocki Moller Gallowaiina Chen, 1934 ( = Gallowainella) ; G. meitienensis Chen Gallowainella Chen, in Dunbar and Skinner, 1937; Gallowaiina meitienensis Chen Girtyina Staff, 1909 (= Triticites) ; Fusu- lina ventricosa Meek and Hayden Grabauina Lee, 1924 (— Triticites); G. disca Lee Hemifusulina Moller, 1877 (not recogniz- able) ; H. bocki Moller Leella Dunbar and Skinner, 1937; L. bellula Dunbar and Skinner Leeina Galloway, 1933 ( = Schwagerina) ; Fusulina vulgaris var. fusiformis Schell- wien Lepidolina Lee, 1933; Neoschwagerina multi- septata Deprat Misellina Schenck and Thompson, 1940; Schwagerina lepida Schwager Mollerina Schellwien, 1898 (=Misellina) ; Schwagerina lepida Schwager Nagatoella Thompson, 1936 ( = Schwager- ina) ; Triticites ellipsoidalis var. orientis Ozawa Nankinella Lee, 1933; N. orbicularis Lee Neofusulinella Deprat, 1912 (=? Fusulin- ella) ; N. lantenoisi Deprat Neoschwagerina Yabe, 1903; Schwagerina craticulifera Schwager Nipponitella Hanzawa, 1938; N. explicata Hanzawa Nummulostegina Schubert, 1907; N. vele- bitana Schubert Orobias Eichwald, 1860 (probably not a fu- suline) ; Nummulina antiquior Rouillier and Vosinsky Ozawaina Lee, 1927 (= Orobias); N. anti- quior Rouillier and Vosinsky Ozawainella Thompson, 1935; Fusulinella an- gulata Colani Paleofusulina Deprat, 1912; P. prisca Deprat Parafusulina Dunbar and Skinner, 1931; P. wordensis Dunbar and Skinner Paraschwagerina Dunbar and Skinner, 1936; Schwagerina gigantea White Pisolina Lee, 1933; P. excessa Lee Polydiexodina Dunbar and Skinner, 1931; P. capitanensis Dunbar and Skinner Profusulinella Rauser-Chernoussova, Bel- jaev and Reitlinger, 1936 (= Fusiella); P. pararhomboides Rauser-Chernoussova, Beljaev and Reitlinger Pseudodoliolina Yabe and Hanzawa, 1932; P. ozawai Yabe and Hanzawa Pseudo fusulina Dunbar and Skinner, 1931 (= Schwagerina) ; P. huecoensis Dun- bar and Skinner Pseudoschwagerina Dunbar and Skinner, 1936; Schwagerina uddeni Beede and Kniker [141] 142 PENN8YLVANIAN FUSULINIDAE Quasifusulina Chen, 1934; Fusulina longis- sima Moller Rugofusulina Rauser-Chernoussova, 1937 (subgenus); F. prisca Ehrenberg [emend Moller] Schellwienia Staff and Wedekind, 1910 ( = Fusulina) ; Fusulina cylindrica Fischer Schubertella Staff and Wedekind, 1910; S. transitoria Staff and Wedekind Schwagerina Moller, 1877; Borelis princeps Ehrenberg Sphaerulina Lee, 1933; S. crassispira Lee Staffella Ozawa, 1925; S. moellerana Thomp- son = Fusulina sphaerica Moller (non Abich) Sumatrina Volz, 1904; S. annae Volz Triticites Girty, 1904; Miliolites secalicus Say Verbeekina Staff, 1909; Fusulina verbeeki Geinitz Wedekindella Dunbar and Henbest, 1930 ( = Wedekindellina) ; Fusulinella euthy- septa Henbest Wedekindia Dunbar and Henbest, 1931 (= Wedekindellina) ; F. euthysepta Henbest Wedekindellina Dunbar and Henbest, in Cushman, 1933; F. euthysepta Henbest Yabeina Deprat, 1914; Neoschwagerina in- ouyei Deprat = Y. globosa Yabe Yangchienia Lee, 1933; Y. iniqua Lee Zellia Kahler and Kahler, 1937 (subgenus); Pseudoschwagerina (Zellia) heritschi heritschi Kahler and Kahler Species acme Dunbar and Henbest, Fusulina, 1942 acuminata Thompson, Fusulinella, 1936 acuminata Dunbar and Skinner, Paraschwa- gerina, 1937 acuta Lee, Schellwienia, 1927 = Schwagerina acutus Dunbar and Condra, Triticites, 1928 aequabilis Lange, Schellwienia, 1925 (not recognizable) aequalis Schellwein, Fusulina molleri var., 1908 = ? Schwagerina aequalis Kahler and Kahler, Pseudoschwa- gerina, 1937 aganoensis Huzimoto, Pseudofusulina, 1936 = Schwagerina akasakensis Deprat, Fusulina japonica var., 1914 = ? Parafusulina akasakensis Thompson, Verbeekina, 1936 aktjubensis, Rauser-Chernoussova, Rugofu- sulina, 1937 aliciae Deprat, Doliolina, 1912 aljutovica Rauser-Chernoussova, Profusulin- ella, 1938 == Fusiella alpina Schellwien, Fusulina, 1898 == Schwa- gerina alternans Schellwien, Fusulina, 1911 = Schwagerina ambigua Deprat, Fusulina, 1913 = Schwa- gerina amedaei Deprat, Schwagerina, 1915 = Pseudoschwagerina ameradaensis Harlton, Endothyra, 1927 = ? Ozawainella anderssoni, Schellwien, Fusulina, 1908 = Schwagerina angulata Colani, Fusulinella, 1924 = Oza- wainella angustus Dunbar and Henbest, Triticites mediocris var., 1942 annae Volz, Sumatrina, 1904 annamitica Deprat, Fusulina, 1913 = ? Schwagerina annulifera Rauser-Chernoussova, Triticites irregularis var., 1938 antiqua Schellwien, Fusulina alpina var., 1898 = Schwagerina antiquior Rouillier and Vosinsky, Nummu- lina, 1849 (not a fusuline) area Lee, Fusulina longissima var., 1923 = Quasifusulina arctica Schellwien, Fusulina, 1908 = ? Triti- cites ardmorensis Harlton, Nummulostegina, 1927 = Ozawainella arenacea Lange, Fusulinella, 1925 = ? Staff- ella artiensis Schellwien, Fusulina prisca var., 1908 = Schwagerina atokensis Thompson, Staffella, 1935 attenuata Dunbar and Skinner, Parafusu- lina bosei var., 1937 auriculla Hanzawa, Nipponitella, 1938 baituganensis Rauser-Chernoussova, Pseudo- fusulina, 1938 = Schwagerina bakeri Dunbar and Skinner, Parafusulina, 1937 bassleri Galloway and Harlton, Orobias, 1928 = Ozawainella beedei Dunbar and Skinner, Pseudoschwa- gerina, 1937 beedei Dunbar and Condra, Triticites, 1928 bellula Dunbar and Skinner, Leella, 1937 bellula Dunbar and Skinner, Schwagerina, 1937 = S. thompsoni Needham bellus Chen, Triticites, 1934 berryi Jones (in Berry), Fusulina, 1933 = Schwagerina biconica Hayasaka, Fusulinella, 1924 bicornis Chen, Pseudofusulina, 1934 = Schwagerina biumbonata Galloway and Harlton, Orobias, 1928 = Ozawainella bocki Moller, Fusulina, 1878 bocki Moller, Hemifusulina, 1878 bocki Moller, Fusulinella, 1878 bosei Dunbar and Skinner, Parafusulina, 1937 borealis Rauser-Chernoussova, Beljaev and Reitlinger, Pseudofusulina, 1936 = Schwagerina bradyi Moller, Fusulinella, 1878 = Nummu- lostegina brevicula Schwager, Fusulina, 1883 = Schwagerina brevis Lee, Girtyina quasicylindrica var., 1927 = Fusulina brevis Chen, Pseudofusulina chihsiaensis var. 1934 = Schwagerina brevis, Rauser-Chernoussova, Beljaev and Reitlinger, Triticites petschoricus var.. 1936 buxtorfi, Lange, Neoschwagerina, 1925 CHECK LIST OF GENERA AND SPECIES 143 cadyi Dunbar and Henbest, Fusulinella, 1942 californica Staff, Fusulina extensa var., 1912 = Parafusulina callosus Dunbar and Henbest, Triticites, 1942 cambodgiensis Gubler, Pseudo fusulina, 1936 = Schwagerina capitanensis Dunbar and Skinner, Polydiex- odina, 1931 carinthiaca Stache, Fusulina, 1874 (nomen nudum) carmani Thompson, Fusulinella, 1936 carnica Gortani, Fusulina, 1909 carniolica Kahler and Kahler, Pseudoschwa- gerina, 1937 cayeuxi Deprat, Fusulina, 1913 = ? Parafu- sulina centralis Say, Miliolites, 1823 = Triticites centralis Staff [non Say], Fusulina, 1912 = Triticites secalicus cervicalis Lee, Schellwienia, 1927 = Schwa- gerina chamchitensis Colani, Fusulina, 1924 = Schwagerina chaoi Lee, N eofusulinella, 1927 = Fusulin- ella chaputi Ciry, Staffella, 1938 chekiangensis Chen, Parafusulina, 1934 cheni Thompson and Foster, Eoverbeekina, 1937 chihsiaensis Chen, Pseudo fusulina, 1934 = Schwagerina chihsiaensis Lee, Schellwienia, 1931 = ? Parafusulina chinensis Ozawa, Fusulina prisca var., 1923 = ? Triticites chinensis Chen, Triticites regularis var., 1934 chitralensis Reed, Fusulina (Schellwienia) molleri var., 1924 = ? Parafusulina chuanshanensis Lee and Chen, Neofusulin- ella, 1930 = Fusulinella chui Chen, Triticites, 1934 cicer Stache, Fusulina, 187.4 (nomen nudum) ciceroidea Rauser-Chernoussova, Beljaev and Reitlinger, Schwagerina, 1936 = Pseudo- schwagerina ciscoensis Harlton, Staffella, 1928 = ? Oza- wainella colaniae Ozawa, Neoschwagerina, 1927 colanii Lee and Chen, N eofusulinella, 1930 = Fusulinella colanii Kahler and Kahler, Pseudofusulina (Zellia) heritschi var., 1937 coloradoensis Roth and Skinner, Wedekin- della, 1930 = Wedekindellina columbiana Dawson, Loftusia, 1879 = Neo- schwagerina communis Schellwien, Fusulina alpina var., 1898 = Schwagerina compacta Lee, Schellwienia longissima var., 1927 = Quasifusulina compactus White, Triticites, 1932 = Schwa- gerina complicata Schellwien, Fusulina, 1898 = ? Parafusulina compressa Deprat, Doliolina, 1915 = Brevax- ina compressa Ozawa, Fusulinella, 1927 compressa Rauser-Chernoussova, Staffella, 1938 confinii Kahler and Kahler, Pseudoschwa- gerina, 1937 confusa Lee and Chen, Staffella, 1930 consobrinus Galloway and Ryniker (in White), Triticites, 1932 constricta Chen, Parafusulina, 1934 constricta Deprat, Fusulina japonica var., 1914 = ? Parafusulina contracta Schellwien, Fusulina, 1909 = Tri- ticites convoluta Lee and Chen, N eofusulinella parva var., 1930 = Fusulinella convoluta Meyer, Schellwienia, 1914=? Schwagerina crassa Deprat, Fusulina, 1913 = Schwagerina crassa Moller, Fusulinella, 1880 = Staffella crassiseptata Deprat, Fusulina, 1915 = Schwagerina crassiseptata Silvestri, Fusulina uralica var., 1934 (nomen nudum) crassispira Lee, Sphaerulina, 1933 crassitectoria Dunbar and Skinner, Schwa- gerina, 1937 craticulifera Schwager, Schwagerina, 1883 = Neoschwagerina cuchilloensis Needham, Triticites, 1937 cullomensis Dunbar and Condra, Triticites, 1928 cushmani Chen, Pseudofusulina, 1934 = Schwagerina *cylindrica Chen, Boultonia, 1934 cylindrica Fischer, Fusulina, 1829 dagmarae Doutkevitch, Staffella, 1934 dakotensis Thompson, Fusulinella, 1936 delawarensis Dunbar and Skinner, Ozawain- ella, 1937 delicatus Chen, Triticites, 1934 deliciasensis Dunbar and Skinner, Parafu- sulina, 1936 densimedius Chen, Triticites, 1934 deprati Beede and Kniker, Fusulina, 1924 = Schwagerina prisca Deprat = Fusuli- nella prisca (Deprat) deprati Yabe, Verbeekina, 1924 deprati Ozawa, Schellwienia, 1925 = Schwa- gerina douvillei Deprat depressa Fischer, Fusulina, 1829 devexa Rauser-Chernoussova, Rugofusulina, 1937 diabloensis Dunbar and Skinner, Parafusu- lina, 1937 diminutiva Thompson, Fusulinella, 1936 disca Lee, Graoauina, 1924 = Triticites discoides Lee, Staffella, 1931 = Nankinella distenta Roth and Skinner, Fusulina, 1930 diversiformis Dunbar and Skinner, Schwa- gerina, 1937 donetziana Lee, Schwagerina ?, 1937 dongvanensis Colani, Fusulina, 1924 = Schwagerina doutkevitchi Rauser-Chernoussova and Bel- jaev, Wedekindellina, 1935 (nomen nu- dum) douvillei Colani, Fusulina, 1924 = Schwager- ina douvillei Deprat, Schwagerina, 1912 = Ver- beekina douvillei Gubler, Doliolina, 1936 =? Pseudo- doliolina douvillei Ozawa, Neoschwagerina, 1925 144 PENNSYLVANIAN FUSULINIDAE dunbari Gubler, Doliolina, 1936 = Pseudo- doliolina dunbari Thompson, Wedekindellina, 1934 = W. euthysepta dunbari Needham, Parafusulina, 1937 = P. rothi Dunbar and Skinner dussaulti Deprat, Fusulina, 1912 = Parafu- sulina elatior Kahler and Kahler, Pseudoschwa- gerina (Zellia) heritschi var., 1937 elegans Harlton, Endothyra, 1927 = ? Oza- wainella elegans Stache, Fusulina, 1874 (nomen nu- dum) elfina Thompson, Wedekindellina, 1934 — W. euthysepta ellipsoidalis Chen, Pseudo fusulina tscherny- schewi var., 1934 = Schwagerina ellipsoidalis Schwager, Doliolina lepida var., 1883 =? Pseudodoliolina ellipsoidalis Staff, Fusulina, 1912 ( not recognizable) ellipsoidalis Rauser-Chernoussova, Schwa- gerina, 1938 = Pseudoschwagerina ellipsoides Lee and Chen, Neofusulinella chuanshanensis var., 1930 = Fusulinella ellipsoides Dunbar and Henbest, Wedekindel- 'iriii 1942 elliptica Lee, Triticites, 1937 elongata Deprat, Neofusulinella, 1915 = Fu# sulinella elongata Shumard, Fusulina, 1858 (not recognizable) elongata Gubler, Neoschwagerina, 1936 elongata Rauser - Chernoussova, Profusu- linella aljutovica var., 1938 = Fusiella emaciata Beede, Fusulina, 1916 = Schwa- gerina erucaria Schwager, Fusulina, 1887 = Schwa- gerina euryteines Thompson, Fusulina, 1934 euthysepta Henbest, Fusulinella, 1928 = Wedekindellina evoluta Chen, Gallowaiina meitienensis var., 1934 = Gallowainella excentrica Roth and Skinner, Wedekindia, 1930 = Wedekindellina excessa Lee, Pisolina, 1933 exigua Schellwien, Fusulina vulgaris var., 1909 = Schwagerina exigua Staff, Fusulina, 1912 = Triticites ne- brascensis Thompson exilis Chen, Schwagerina fusulinoides var., 1934 = Pseudoschwagerina exilis Schwager, Fusulina, 1883 = ? Schwa- gerina eximia Thompson, Fusulina, 1934 expansa Lee, Schellwienia, 1927 = Schwa- gerina expansa Hanzawa, Nipponitella, 1938 explicata Hanzawa, Nipponitella, 1938 extensa Staff, Fusulina, 1912 (nomen nu- dum) extensa Kahler and Kahler, Pseudoschwa- gerina, 1937 fava Lee and Chen, Girtyina, 1930 = Fusu- lina fittsi Thompson, Fusulinella, 1935 fluxa Lee and Chen, Neofusulinella, 1930 = Fusulinella forakerensis Skinner, Fusulina. 1931 = Schwagerina formosa Harlton, Staff ella. 1928 = ? Oza- wainella forojuliensis Gortani, Fusulina, 1909 fosteri, Thompson and Miller, Schwagerina, 1935 = Paraschwagerina fountaini Dunbar and Skinner, Staffella, 1937 fountaini Dunbar and Skinner, Parafusulina, 1937 fragilis Chen, Pseudofusulina chihsiaensis var. 1934 — Schwagerina fragilis Colani, Fusulina, 1924 = Schwa- gerina fragilis Rauser-Chernoussova, Pseudofusu- lina lutugini var., 1935 = Schwagerina fragilis Dunbar and Skinner, Leella, 1937 fragilis Schellwien, Fusulina alpina var., 1898 = Schwagerina franklinensis Dunbar and Skinner, Schwa- gerina, 1937 fresnalensis Needham. Triticites, 1937 furnishi Thompson, Fusulinella, 1936 fusiformis Chen, Pseudofusulina tscherny- schewi var., 1934 = Schwagerina fusiformis Krotow, Schwagerina, 1898 = Pseudoschwagerina fusiformis Schellwien, Fusulina vulgaris var., 1909 = Schwagerina fusulinoides Schellwien, Schwagerina, 1898 =Pseudoschwagerina gallowayi Chen, Pseudofusulina, 1934 = Schwagerina gallowayi Skinner, Schubertella, 1931 = Eo- schubertella gallowayi Needham, Triticites, 1937 gemmellaroi Silvestri, Sumatrina, 1933 gephyrea Dunbar and Henbest, Fusulinella, 1942 gerontica Dunbar and Skinner, Pseudo- schwagerina, 1937 gigantea Deprat, Fusulina, 1913 = ? Parafu- sulina gigantea Gubler, Neoschwagerina mega- sphaerica var., 1935 gigantea White, Schwagerina, 1932 = Para- schwagerina gigas Mansuy, Fusulinella, 1912 = ? Nankin- ella giraudi Deprat, Neofusulinella, 1915 = Schubertella girtyi Dunbar and Condra, Fusulinella, 1928 = Fusulina globosa Deprat, Fusulina, 1912 = Schwa- gerina globosa Huzimoto, Pseudofusulina tscherny- schewi var., 1936 = Schwagerina globosa Schellwien, Fusulina vulgaris var., 1909 = Schwagerina globosa Stache, Fusulina, 1874 (nomen nu- dum) globosa Yabe, Neoschwagerina, 1906 = Yabeina globularis Gubler, Pseudofusulina, 1936 = Schwagerina glomerosa Schwager, Schwagerina princeps var., 1883 = Pseudoschwagerina CHECK LIST OF GENERA AND SPECIES 145 grabaui Thompson and Foster, Verbeekina, 1937 gracilis Chen, Parafusulina, 1934 gracilis Meek, Fusulina, 1864 = Schwager- ina gracilis Ozawa, Schellwienia, 1927 = ? Co- donofusiella gracilitatis Dunbar and Skinner, Schwager- ina, 1937 graciosa Lee, Triticites, 1937 grandis Deprat, Neoschwagerina craticuli- fera var., 1912 granum-avenae Roemer, Fusulina, 1880 = Schwagerina granum-oryzae Doutkevitch, Fusiella, 1934 gregaria Lee, Schellwienia, 1931 = ? Schwa- gerina guadalupensis Needham, Polydiexodina, 1937 = P. shumardi Dunbar and Skinner guatemalaensis Dunbar, Parafusulina, 1939 giimbeli Stache, Fusulina, 1874 (nomen nu- dum) giimbeli Dunbar and Skinner, Schwagerina, 1937 hartvillensis Roth and Skinner, Fusulina, 1930 hawkinsi Dunbar and Skinner, Schwagerina, 1937 haworthi Beede, Fusulina, 1916 hayasakai Lee, Schellwienia japonica var., 1927 = ? Parafusulina hayasakai Ozawa, Neoschwagerina, 1922 = Neoschwagerina multiseptata Deprat haydeni Doutkevitch, Neoschwagerina cra- ticulifera var., 1934 haydeni Ozawa, Schellwienia, 1925 = Schwa- gerina haymanaensis Ciry, Staffella, 1938 heimi Thompson and Foster, Verbeekina, 1937 henbesti, Skinner, Wedekindia, 1931 = Wede- kindellina heritschi Kahler and Kahler, Pseudoschwa- gerina (Zellia), 1937 heritschi Kahler and Kahler, Pseudoschwa- gerina (Zellia) heritschi var., 1937 hessensis Dunbar and Skinner, Schwager- ina, 1937 hoeferi Stache, Fusulina, 1874 (nomen nudum) hollingsworthi Thompson, Staffella, 1935 huanglienhsiaensis Chen, Triticites, 1934 huecoensis Dunbar and Skinner, Pseudofu- sulina, 1931 = Schwagerina huecoensis Dunbar and Skinner, Ozawain- ella, 1937 hutienensis Chen, Pseudo fusulina, 1934 = Schwagerina hyperborea Salter, Fusulina, 1855 = Schwa- gerina illinoisensis Dunbar and Henbest, Fusulina, 1942 imlayi Dunbar, Parafusulina, 1939 implicata Schellwien, Fusulina moelleri var., 1908 = ? Schwagerina incisa Schellwien, Fusulina, 1898 = Schwa- gerina inconspicua Girty, Fusulina, 1915 infecta Vissarionova, Pseudofusulina ver- neuili var., 1937 = Schwagerina inflata Colani, Fusulinella, 1924 = ? Nankin- ella inflata Doutkevitch, Fusulinella uralica var., 1934 = Wedekindellina (homonym) inflatus Galloway and Ryniker (in White), Triticites ventricosus var., 1932 iniqua Lee, Yangchienia, 1933 inouyei, Deprat, Yabeina, 1914 = Y. globosa Yabe intermedia Lee, Eoverbeekina, 1933 intermedia Rauser-Chernoussova, Beljaev and Reitlinger, Pseudofusulina, 1936 = Schwagerina iowensis Thompson, Fusulinella, 1934 irregularis Staff, Fusulina centralis var., 1912 = Triticites irregularis (Staff) irumensis Huzimoto, Fusulinella, 1936 itoi Ozawa, Fusulinella, 1925 ivanovi Doutkevitch, Staffella, 1934 = Oza- wainella japonica Huzimoto, Sumatrina, 1936 japonica Giimbel, Fusulina, 1874 = Parafu- sulina jarillaensis Needham, Schwagerina emaciata var., 1937 jaroslavkensis Vissarionova, Pseudofusulina, 1937 = Schwagerina jemezensis Needham, Triticites, 1937 jigulensis Rauser-Chernoussova, Triticites, 1938 kaerimizensis Ozawa, Schellwienia, 1925 = Parafusulina kagaharensis Huzimoto, Triticites, 1936 kagomoriensis Huzimoto, Pseudofusulina, 1936 = Schwagerina kaizensis Huzimoto, Yabeina, 1936 kansasensis Beede and Kniker, Schwagerina, 1924 = Paraschwagerina kargalensis Rauser-Chernoussova, Rugofu- sulina, 1937 katoi Ozawa, Neoschwagerina, 1927 = Yabe- ina kattaensis Schwager, Fusulina, 1885 = Parafusulina kawanoboriensis Huzimoto, Triticites, 1937 kayi Thompson, Fusulina, 1934 kelleyensis Needham, Triticites, 1937 keytei Roth and Skinner, Staffella, 1930 kiangsuensis Chen, Pseudofusulina, 1934 = Schwagerina kingi Dunbar and Skinner, Schubertella, 1937 kingorum Dunbar and Skinner, Parafusu- lina, 1936 kiuyaoshanensis Chen, Triticites, 1934 knighti Dunbar and Skinner, Schwagerina, 1937 knighti Dunbar and Henbest, Fusulina, 1942 kobayashii Thompson, Nagatoella, 1936 = Schwagerina konnoi Ozawa, Fusulinella, 1925 koschmanni Skinner, Triticites, 1931 kozui Deprat, Fusulina, 1914 = Schwagerina kraffti Schellwien, Fusulina, 1908 = Schwa- gerina krotowi Schellwien, Fusulina, 1908 = Schwagerina kuanshanensis Chen, Triticites, 1934 kueichihensis Chen, Orobias, 1934 = Oza- wainella 146 PENNSYLVANIAN FUSULINIDAE kwangsiana Lee, Colania, 1933 labyrinthiformis Ehrenberg, Borelis, 1854 = ? Staffella lacunosa Dunbar and Skinner, Staffella, 1937 laevis Schellwien, Fusulinella, 1898 = Staff- ella lanceolata Lee and Chen, Girtyina, 1930 = Fusulina lantenoisi Deprat, Fusulina, 1912 = Schwa- gerina lantenoisi Deprat, Neofusulinella, 1913 laosensis Deprat, Fusulina, 1913 = ? Schwa- gerina lata Lee and Chen, Schubertella, 1930 = Eo- schubertella latioralis Rauser-Chernoussova, Rugofusu- lina, 1937 laxa Lee, Schellwienia nathorsti var., 1927 = ? Schwagerina laxissima Dunbar and Skinner, Schwager- ina, 1937 leei Doutkevitch, Staffella, 1934 leei Skinner, Fusulina, 1931 lepida Deprat, Fusulina, 1914 = Schwager- ina lepida Schwager, Schwagerina, 1883 =? Pseudodoliolina lettensis Schubert, Doliolina lepida var., 1914 = Pseudodoliolina levicula Dunbar and Henbest, Fusulina, 1942 levidensis Lee, Schellwienia verneuili var., 1927 = ? Schwagerina librovitchi Doutkevitch, Fusulinella, 1934 linearis Dunbar and Skinner, Schwagerina, 1937 lineata Dunbar and Skinner, Parafusulina, 1937 liuchowensis Chen., Triticites, 1934 llanoensis Thomas, Fusulina, 1931 = Fusu- linella locbyi Lorenthey, Fusulinella, 1899 longa Doutkevitch, Fusulinella uralica var., 1934 = Wedekindellina longa Rauser-Chernoussova, Pseudo fusulina stabilis var., 1938 = Schwagerina. longissima Deprat, Sumatrina, 1914 longissima Moller, Fusulina, 1878 = Quasi- fusulina longissimoidea Beede, Fusulina, 1916 == Schwagerina lonsdalensis Dunbar and Henbest, Fusulina, 1942 lucasensis Thompson, Fusulina, 1934 lungtanensis Chen, Parafusulina, 1934 lutugini Staff, Fusulina, 1908 = Schwager- ina maccoyensis Thompson, Staffella keytei var., 1935 magna Lee and Chen, Schubertella, 1930 magna Roth and Skinner, Wedekindia ex- centrica var., 1930 = Wedekindellina magnae sphaerae Colani, Schwagerina prin- ceps var., 1924 = Pseudoschwagerina magnini Deprat, Fusulina, 1913 = Schwa- gerina major Deprat, Doliolina, 1914 = Pseudodo- liolina maleyi Dunbar and Skinner, Parafusulina, 1937 mansuyi Deprat, Fusulina, 1912 = Schwa- gerina maoshanensis Chen, Pseudo fusulina, 1934 = Schwagerina margaritae Deprat, Neoschwagerina, 1913 margheritii Deprat, Fusulina, 1912 = Schwagerina mathildae Doutkevitch, Staffella, 1934 = Ozawainella media Kahler and Kahler, Pseudoschwa- gerina (Zellia) heritschi var., 1937 medialis Staff, Fusulina secalis var., 1912 = Triticites mediocris Dunbar and Henbest, Triticites, 1940 meeki Moller, Fusulina ventricosa var., 1879 = Triticites meeki Dunbar and Condra, Fusulinella, 1928 = Fusulina euryteines Thompson megaspherica Deprat, Neoschwagerina, 1913 megista Thompson, Fusulina, 1934 meitienensis Chen, Gallowaiina, 1934 = Gal- lowainella melonica Dunbar and Skinner, Schubertella, 1937 merangienensis Thompson, Pseudoschwa- gerina, 1936 milleri Thompson, Triticites, 1936 = Tritic- ites cullomensis Dunbar and Condra minima Deprat, Neofusulinella, 1915 = Fus- ulinella minima Lange, Doliolina, 1925 = Misellina minima Schellwien, Fusulina, 1908 minoensis Deprat, Neoschwagerina craticu- lifera var., 1914 minor Chen, Verbeekina, 1934 minor Lee, Schellwienia vulgaris var., 1927 = Schwagerina minoris Lee, Fusulina elongata var., 1923 = ? Parafusulina minuta Henbest, Fusulinella, 1928 = Wede- kindellina minuta Lee, Schellwienia simplex var., 1927 = Triticites minutissima Roth and Skinner, Fusulina, 1930 mira Kahler and Kahler, Pseudoschwagerina (Zellia) heritschi var., 1937 mirabilis Galloway and Ryniker (in White), Fusulina, 1932 (nomen nudum) moderata Rauser-Chernoussova, Rugofusu- lina, 1937 moellerana Thompson, Staffella, 1935 moelleri Schellwien, Fusulina, 1908 = ? Schwagerina molengraaffl Schubert, Fusulina, 1915 =? Schwagerina molleri Ozawa, Staffella, 1925 montipara Ehrenberg, Alveolina, 1854 = Schwagerina moorei Dunbar and Condra, Triticites, 1928 morsei Needham, Pseudoschwagerina, 1937 multicircumvoluta Deprat, Neoschwagerina craticulifera var., 1912 multiseptata Deprat, Neoschwagerina, 1912 = Lepidolina CHECK LIST OF GENERA AND SPECIES 147 multiseptata Schellwien, Fusulina, 1898 = ? Schwagerina muongthensis Deprat, Fusulina, 1915 = Pseudoschwagerina mutabilis Chen, Pseudo fusulina, 1934 = Schwagerina mysticensis Thompson, Fusulina, 1934 nana Likharev, Palaeofusulina, 1926 nebraskensis Thompson, Triticites, 1934 (re- placing invalid "Fusulina exigua" Schellwien and Staff) neglectus Newell, Triticites, 1934 nelsoni Dunbar and Skinner, Schwagerina, 1937 neoschwagerinoides Deprat, Doliolina, 1913 == Cancellina nipponica Ozawa, Cancellina, 1927 nitida Kahler and Kahler, Pseudoschwa- gerina, 1937 nobilis Lee, Schellwienia, 1927 = Schwa- gerina noinskyi Rauser-Chernoussova, Triticites, 1938 novamexicana Needham, Fusulina, 1937 nunosei Hanzawa, Pseudoschwagerina (Zel- lia), 1939 nux Schellwien, Fusulina krotowi var., 1908 = Schwagerina obesa Beede, Fusulina, 1916 = Triticites obesa Lee, Schellwienia, 1927 (nomen nu- dum) oblonga Ozawa, Schellwienia, 1925 = ? Schwagerina obscura Lee and Chen, Schubertella, 1930 = Eoschubertella obsoleta Schellwien, Fusulina, 1908 =Tri- ticites obtusa Lee, Schellwienia verneuili var., 1927 = ? Parafusulina ohioensis Thompson, Triticites, 1936 oklahomaensis Galloway and Harlton, Orobias, 1928 = Ozawainella okuboensis Ozawa, Schellwienia subobsoleta var., 1927 = Parafusulina oliviformis Thompson, Fusulinella, 1935 ominensis Ozawa, Schellwienia, 1925 = ? Triticites orbicularia Lee, Nankinella, 1935 orbicularis Gregorio, Schwagerina ver- beeki var., 1930 orbulinopsis Gregorio, Schwagerina ver- beeki var., 1930 (not recognizable) ordinatus Chen, Triticites, 1934 orientale Huzimoto, Pseudoschwagerina, 1937 orientis Ozawa, Schellwienia ellipsoidalis var., 1925 = Schwagerina orientis Ozawa oryziformis Newell, Triticites secalicus var., 1935 osagensis Newell, Triticites, 1935 otakiensis Huzimoto, Pseudodoliolina, 1936 otukai Huzimoto, Pseudofusulina, 1936 = Schwagerina ovalis Deprat, Doliolina, 1915 = Misellina ovata Rauser-Chernoussova, Profusulinella, 1938 = Fusulinella ovoideus Chen, Triticites, 1934 ozawai Iisaka, Schellwienia, 1932 = ? Para- fusulina ozawai Lee and Chen, Staffella, 1930 ozawai Yabe and Hanzawa, Pseudodoliolina, 1932 padangensis Lange, Nummulostegina, 1925 padangensis Lange, Schellwienia, 1925 = Schwagerina pailensis Waagen, Fusulina, 1887 = ? Para- fusulina paleophacus Ehrenberg, Borelis, 1854 = ? Staffella pamirensis Doutkevitch, Doliolina termieri var., 1934 = Misellina pankouensis Lee, Girtyina, 1927 = Fusulina paraarcticus Rauser-Chernoussova, Tritic- ites, 1938 paradoxa Lee and Chen, Fusiella, 1930 paradoxa Doutkevitch, Staffella, 1934 paradoxica Dunbar and Skinner, Codonofusi- ella, 1937 parajaponica Beljaev, Pseudofusulina, 1938 = ? Schwagerina paramolleri Rauser-Chernoussova, Pseudo- fusulina, 1938 = ? Schwagerina paraprisca Chen, Pseudofusulina, 1934 = Schwagerina pararegularis Chen, Triticites, 1934 pararhomboides Rauser-Chernoussova, Bel- jaev and Reitlinger, Profusulinella, 1936 = Fusulinella parasphaeroidea Lee and Chen, Staffella, 1930 paraverneuili Vissarionova, Pseudofusulina, 1937 = Schwagerina parumvoluta Deprat, Fusulina, 1913 =? Schwagerina parva Colani, Neoschwagerina, 1924 parva Lange, Nummulostegina ?, 1925 parva Lee and Chen, Neo fusulinella, 193Q = Fusulinella parva Beljaev and Rauser-Chernoussova, Pseudo fusulinella uralica var., 1938 = Schwagerina parvicostata Deprat, Doliolina, 1915 = Mis- ellina parvula Schellwien, Fusulina prisca var., 1908 = Schwagerina parvus Chen, Triticites, 1934 pattoni Needham, Fusulina, 1937 pauciseptata Rauser-Chernoussova, Schu- bertella, 1938 pauciseptata Rauser-Chernoussova, Beljaev and Reitlinger, Fusulina bocki var., 1936 pauper Dunbar and Henbest, Triticites, 1942 pavlovi Rauser-Chernoussova, Schwagerina, 1938 = Pseudoschwagerina perforata Roth and Skinner, Wedekindia coloradoensis var., 1930 = Wedekindel- lina persica Kahler, Polydiexodina, 1933 peruana Meyer, Schellwienia, 1914 = ? Fus- ulinella pesuliensis Ozawa and Tobler, Sumatrina, 1929 petschoricus Rauser-Chernoussova, Beljaev and Reitlinger, Triticites, 1936 phairayensis Colani, Neo fusulinella, 1924 = Schubertella phaselus Lee, Schellwienia longissima var.„ 1927 = Quasifusulina 148 PENN8YLVANIAN FUSULINIDAE philipsoni Schellwien, Fusulina = Schwa- gerina vulgaris pinguis Dunbar and Skinner, Triticites, 1937 piasaensis Dunbar and Henbest, Fusulina, 1942 plana Lange, Schubertella, 1925 plattensis Thompson, Fusulina, 1936 plicata Lee, Schellwienia, 1927 = Parafusu- lina plicatulus Merchant and Keroher, Triticites, 1939 plummeri Dunbar and Condra, Triticites, 1928 powwowensis Dunbar and Skinner, Tritic- ites, 1937 praecursor Deprat, Neofusulinella, 1913 = ? Fusulinella praesimplex Lee, Neofusulinella, 1927 = Fusulinella preobrajenskyi Doutkevitch, Staffella, 1934 primaeva Skinner, Fusiella, 1931 primarius Merchant and Keroher, Triticites secalicus var., 1939 primigena Hayden, Neoschwagerina, 1909 = Cancellina primigenius Rauser-Chernoussova, Beljaev and Reitlinger, Triticites, 1936 princeps Ehrenberg, Borelis, 1842 (1854) = Schwagerina princeps Moller, Schwagerina, 1878 = Pseu- doschwagerina prisca Ehrenberg emend. Moller, Fusulina, 1878 = Schwagerina prisca Deprat, Paleofusulina, 1913 prisca Deprat, Schwagerina, 1912 = Schu- bertella or Fusulinella priscoidea Rauser-Chernoussova, Profusu- linella, 1938 = Fusulinella problematica Thompson, Fusulina ?, 1934 prolifica Thompson, Fusulinella, 1935 prolongada Berry, Fusulina, 1933 = Schwa- gerina propinqua Deprat, Fusulina, 1914 = Schwa- gerina protensa Thompson, Fusulinella velmae var., 1936 pseudoarcticus Rauser-Chernoussova, Tri- ticites, 1938 pseudobocki Lee and Chen, Neofusulinella, 1930 = Fusulinella pseudobrevicula Deprat, Fusulina, 1913 = Schwagerina pseudochihsiaensis Chen, Pseudo fusulina, 1934 = Schwagerina pseudoexilis Chen, Pseudo fusulina, 1934 = Schwagerina pseudolepida Deprat, Doliolina, 1912 = Pseu- dodoliolina pseudoobscura Chen, Schubertella, 1934 = Eoschubertella pseudoprisca Colani, Fusulina, 1924 = Paleo- fusulina prisca Deprat pseudoregularis Dunbar and Skinner, Schwagerina giimbeli var., 1937 pseudosimplex Chen, Triticites, 1934 pseudosphaeroidea Doutkevitch, Staffella, 1934 pseudostruvei Rauser - Chernoussova, Bel- jaev and Reitlinger, Staffella, 1936 pseudo-verbeeki Deprat, Schwagerina, 1913 = Verbeekina pulchella Rauser-Chernoussova, Rugofusu- lina, 1937 pulchra Kahler and Kahler, Pseudoschwag- erina, 1937 pulchra Rauser-Chernoussova and Beljaev, Fusulinella, 1936 pulla Lange, Schellwienia, 1925 = Schwag- erina pumila Thompson, Fusulina, 1934 pursatensis Gubler, Pseudo fusulina ambigua var., 1936 = Schwagerina pusilla Colani, Neofusulinella praecursor var., 1924 = Fusulinella pusilla Schellwien, Fusulina, 1898 = Schwag- erina pygmaeus Dunbar and Condra, Triticites cullomensis var., 1928 = T. pygmaeus quadrata Deprat, Fusulinella, 1913 = Staf- fella quasicylindrica Lee, Girtyina, 1927 = Fusu- lina radiata Brady, Involutina, 1869 = Ozawain- ella rawi Lee, Boultonia, 1927 = Wedekindellina referta Dunbar and Skinner, Parafusulina maleyi var., 1937 = Parafusulina delicia- sensis regularis Chen, Pseudo fusulina chihsiaensis, 1934 = Schwagerina regularis Chen, Schubertella, 1934 regularis Schellwien, Fusulina, 1898 = Schwagerina rhodesi Needham, Triticites, 1937 rhombica Stache, Fusulina, 1874 (nomen nudum) rhomboides Lee and Chen, Neofusulinella, 1930 = Fusulinella richthofeni Schwager, Fusulina, 1883 =? Schwagerina robusta Chen, Pseudofusulina, 1934 = Schwagerina robusta Dunbar and Condra, Fusulinella meeki var., 1928 = Fusulina [homonym] robusta Meek, Fusulina, 1864 = Pseudo- schwagerina robusta Silvestri, Fusulina uralica var., 1935 = Schwagerina robusta Rauser-Chernoussova, Beljaev and Reitlinger, Profusulinella parva var., 1936 = Fusulinella robustata Chen, Triticites chui var., 1934 rockymontana Roth and Skinner, Fusulina, 1930 rossica Schellwien, Fusulina alpina var., 1908 = ? Triticites rothi Dunbar and Skinner, Parafusulina, 1936 rothi Skinner, Triticites, 1931 rotkyana Stache, Fusulina, 1874 (nomen nudum) rotunda Deprat, Neoschwagerina craticuli- fera var., 1914 rotundata Dunbar and Skinner, Polydiexo- dina ?, 1937 rouxi Deprat, Fusulina, 1913 = Triticites rutschi Thompson, Schwagerina, 1936 = Triticites CHECK LIST OF GENERA AND SPECIES 149 ruzencevi Rauser-Chernoussova, Rugofusu- lina, 1937 sacramentoensis Needham, Triticites ventri- cosus var., 1937 samariea Rauser-Chernoussova, Triticites secalicus var., 1938 samenkiangensis Chen, Triticites, 1934 santyuensis Huzimoto, Pseudofusulina, 1936 === Schwagerina sapperi Staff, Fusulina verneuili var., 1912 = Paraf usulina satoi Ozawa, Schellwienia, 1925 = Schwag- erina satoi Huzimoto, Triticites, 1937 schellwieni Deprat, Doliolina, 1913 = Can- cellina schellwieni Staff, Girtyina, 1912 = ? Fusu- lina girtyi schellwieni Vissarionova, Pseudofusulina, 1937 = Schwagerina schuberti Lange, Nummulostegina, 1925 schuberti Lange, Schellwienia, 1925 = Schwagerina schucherti Dunbar and Skinner, Parafusu- lina, 1937 schwageriniformis Rauser - Chernoussova, Triticites, 1938 schwageriniformis Rauser- Chernoussova, Beljaev and Reitlinger, Pseudofusulina, 1936 = Schwagerina schwagerinoides Deprat, Neofusulinella, 1913 = Fusulinella secalicus Say, Miliolites, 1833 = Triticites secalicus Staff, Fusulina, 1912 = Triticites ventricosus Meek sellardsi Dunbar and Skinner, Parafusulina, 1937 serotina Thompson, Fusulinella, 1936 serrata Rauser-Chernoussova, Rugofusulina, 1937 setum Dunbar and Skinner, Schwagerina, 1937 shiraiwensis Ozawa, Yaoeina, 1925 = Lepido- lina multiseptata Deprat shumardi Dunbar and Skinner, Polydiexo- dina, 1931 similis Galloway and White (in White), Fusulina meeki var., 1932 simplex Lange, Schubertella, 1925 simplex Ozawa, Neoschwagerina, 1927 simplex Schellwien, Fusulina, 1908 = Triti- cites simplicata Lee, Wedekindellina ?, 1937 sinensis Chen, Triticites, 1934 skinneri Thompson, Triticites, 1936 skinneri Dunbar, Parafusulina, 1939 socorrensis Needham, Fusulina, 1937 sokensis Rauser-Chernoussova, Pseudofusu- lina, 1938 = Schwagerina solida Colani, Fusulina, 1924 = Schwagerina solida Schellwien, Fusulina verneuili var., 1908 = Schwagerina sonoraensis Dunbar, Parafusulina, 1939 speciosa Lee, Schellwienia richthofeni var., 1927 = ? Parafusulina sphaera Ozawa, Verbeekina verbeeki var., 1925 = V. sphaera Ozawa snhaerica Abich, Fusulina, 1858 = Staffella sphaerica Beljaev, Pseudofusulina uralica var., 1938 = Schwagerina sphaeroidea Ehrenberg, Melonia (Borelis), 1842 = Staffella sphaeroidea Rauser-Chernoussova, Pseudo- fusulina krotowi var., 1938 = ? Schwag- erina spissiplicata Dunbar and Henbest, Fusulina, 1942 splendens Dunbar and Skinner, Parafusu- lina, 1937 stabilis Rauser-Chernoussova, Pseudofusu- lina, 1938 = Schwagerina staffi Lange, Neoschwagerina, 1925 staffi Ozawa, Schellwienia, 1925 = ? Schwag- erina stookei Thompson, Fusulina, 1934 stouti Thompson, Fusulinella iowensis var., 1936 stricta Deprat, Neoschwagerina anna var., 1912 = Sumatrina struvii Moller, Fusulinella, 1880 = Staffella stuckenbergi Rauser - Chernoussova, Triti- cites, 1938 subcylindrica Deprat, Fusulina, 1913 = ? Schwagerina subextensa Chen, Parafusulina, 1934 submucronata Thompson, Triticites, 1936 subnathorsti Lee, Schellwienia, 1927 = ? Schwagerina subobsoleta Ozawa, Schellwienia, 1925 = Triticites subrhomboides Chen, Triticites, 1934 subrhomboides Lee and Chen, Neofusulinella, 1930 = Fusulinella subtilis Schellwien, Fusulina, 1908 = ? Schwagerina subventricosus Dunbar and Skinner, Triti- cites, 1937 suessi Stache, Fusulina, 1874 (nomen nudum) sumatrensis Lange, Neoschwagerina, 1925 sumatrinaeformis Gubler, Neoschwagerina, 1936 suzukii Ozawa, Schellwienia, 1925 = ? Triti- cites tanoensis Huzimoto, Pseudofusulina, 1936 = Schwagerina taosensis Needham, Fusulina, 1937 tastubensis Vissarionova, Pseudofusulina, 1937 = Schwagerina tchengkiangensis Deprat, Fusulina, 1912 = Schwagerina tchussovensis Rauser-Chernoussova, Pseudo- fusulina, 1935 = Schwagerina teilhardti Lee, Girtyina, 1927 = Fusulina tenuis Chen, Pseudofusulina, 1934 = Schwag- erina tenuis Deprat, Neoschwagerina craticulifera var., 1912 tenuis Lee, Schellwienia longissima var., 1928 = Quasifusulina tenuis Merchant and Keroher, Triticites, 1929 tenuissima Schellwien, Fusulina, 1898 = ? Quasifusulina tenuithecus Chen, Triticites, 1934 terebra Lange, Fusulinella, 1925 = Ozawain- ella 150 PENN8YLVANIAN FUSULINIDAE termieri Deprat, Doliolina, 1915 = Misellina texana Harlton, Staff ella, 1928 = ? Nura- mulostegina texana Dunbar and Skinner, Pseudoschwag- erina, 1937 thompsoni Needham, Schwagerina, 1937 tietzei Stache, Fusulina, 1874 (nomen nudum) tingi Lee, Orobias, 1937 = Ozawainella tinvenkiangi Lee, Schwagerina, 1927 = ? Paraschwagerina tobleri Lange, Neoschwagerina, 1925 tobleri Thompson, Yangchienia, 1935 tomlinsoni Galloway and White (in White), Fusulina, 1932 (nomen nudum) transita Rauser-Chernoussova, Rugofusulina serrata var., 1937 transitoria Staff and Wedekind, Schuber- tella, 1910 tregoensis Roth and Skinner, Fusulina meeki var., 1930 triangula Rauser-Chernoussova, Beljaev and Reitlinger, Fusulina, 1936 trisulcata Thompson, Fusulinella, 1935 truncata Ozawa, Schellwienia japonica var., 1927 = ? Parafusulina truncatus Chen, Triticites, 1934 tschernyschewi Schellwien, Fusulina, 1908 = Schwagerina tudai Huzimoto, Fusulinella, 1936 tumida Likharev, Schwagerina. 1937 = Pseudoschwagerina tumidus Skinner, Triticites, 1931 turbida Kahler and Kahler, Pseudoschwag- erina, 1937 turgidus Dunbar and Henbest, Triticites, 1942 turki Skinner, Fusulina, 1931 = Schwagerina typica Lee and Chen, Fusiella, 1930 uddeni Beede and Kniker, Schwagerina, 1924 = Pseudoschwagerina uddeni Dunbar and Skinner, Triticites, 1937 ultima Dunbar and Skinner, Pseudoschwag- erina texana var., 1937 ultimata Newell and Keroher, Wedekindel- lina, 1937 umbilicata Colani, Fusulinella, 1924 = Staf- fella umboniplicatus Rauser-Chernoussova and Beljaev (in Rauser-Chern.) Triticites, 1938 undulata Chen, Parafusulina, 1934 uniformis Thompson, Wedekindellina, 1934 uralica Doutkevitch, Fusulinella. 1934 = Wedekindellina uralica Krotow, Fusulina, 1888 = Schwag- erina usvae Doutkevitch, Fusulinella, 1932 valens Rauser-Chernoussova, Rugofusulina serrata var., 1937 valida Lee, Schellwienia, 1927 == Schwag- erina fusiformis variata Lee, Fusulina, 1923 = Schwagerina velebitana Schubert, Nummulostegina, 1908 velmae Thompson, Fusulinella velmae var., 1936 ventricosa Meek and Hayden, Fusulina cyl- indrica var. = Triticites ventricosus venustus Dunbar and Henbest, Triticites, 1942 verbeeki Geinitz, Fusulina, 1876=Verbeekina verneuili Moller, Fusulina, 1878 = Schwag- erina vetusta Schellwien, Fusulina alpina var., 1908 = ? Triticites victorioensis Dunbar and Skinner, Triticites, 1937 volgensis Rauser-Chernoussova, Triticites, 1938 volzi Staff, Verbeekina verbeeki var., 1909 vulgaris Schellwien, Fusulina, 1909 = Schwagerina waageni Schwager, Fusulinella, 1887 = Ozawainella or Nankinella wanneri Schubert, Fusulina, 1915 == Schwag- erina watanabei Ozawa, Schellwienia vulgaris var., 1923 (emend. Lee, 1927)= Schwagerina weberi Schubert, Fusulina, 1915 = ? Schwag- erina wellsi Needham, Triticites, 1937 whitei Rauser-Chernoussova, Beljaev and Reitlinger, Triticites, 1936 willsi Lee, Boultonia, 1927 wongwenhaoi Lee, Schwagerina, 1927 = Pseudoschwagerina wordensis Dunbar and Skinner, Parafusu- lina, 1931 yabei Staff, Schwagerina, 1909 = P a r a - schwagerina yangchenensis Lee, Schubertella, 1924 (no- men nudum) yarkhunensis Reed, Fusulina (Schellwienia) verneuili var., 1924 = Parafusulina yobarensis Ozawa, Schellwienia, 1925 = ? Triticites yobarensis Ozawa, Staffella, 1925 zidoensis Huzimoto, Fusulinella bocki var.. 1938 BIBLIOGEAPHY OF THE FUSULINIDAE The following bibliography may be considered reasonably exhaustive to and including the year 1939. In addition to works dealing with shell anatomy and classification, works are included that deal with the strati- graphic and geographic distribution and the ecology of the fusulinids. Mere in- clusion of fusulinid names in faunal lists or incidental mention of occurrences have not been considered a reason for in- clusion. Abich, H., 1858. Vergleichende geologische Grundziige der kaukasischen, arme- nischen und nordpersischen Gebirge: Acad. Imp. Sci. St. Petersbourg Mem. (6), vol. 7, pp. 439 and 528, pi. 3, fig. 13. Altpeter. 0. 1913. Beitrage zur Anatomie und Physiologie von Alveolina: Neues Jahrb., Beilage-Band 36, pp. 82-112, pis. 6-7. Beede, J. W., 1916. New species of fossils from the Pennsylvanian and Permian rocks of Kansas and Oklahoma: Indiana Univ. Studies, vol. 3, no. 29, pp. 5-15. Beede, J. W. and Kniker, H. T., 1924. Spe- cies of the genus Schwagerina and their stratigraphic significance: Univ. Texas Bull. 2433, pp. 1-96, pis. 1-9. [Brings together all known species of Pseudo- schwagerina.] Beljaev, G. M. (see Rauser-Chernoussova) Berry, W., 1931. Distribution of the Fusu- linidae: Pan-Am. Geologist, vol. 56, pp. 181-187. , 1933. Fusulina from Peru and Bolivia: Pan-Am. Geologist, vol. 59, pp. 269-272, pi. 22. Brady, H. B., 1875. On some fossil Foramini- fera from the West-Coast district, Suma- tra: Geol. Mag. (2), vol. 2, pp. 532-539, pis. 13-14. , 1876. A monograph of Carboni- ferous and Permian Foraminifera (-the genus Fusulina excepted). Paleont. Soc. London, vol. 30, pp. 1-166, pis. 1-12. [Some of the species classed with En- dothyra are fusulines.] , 1876a. Notes on a group of Rus- sian Fusulinae: Ann. Mag. Nat. History (4), vol. 18, pp. 414-422, pi. 18. [First to note resemblance of Orobias to fusu- lines.] Brazhnikova, N., 1937. Schwagerina ex gr. princeps Ehrenberg in the dolomites of the Artemovsk region: Acad. Sci. Ukrai- nian S. S. R., Jour. Geol., vol. 3, issue 2, pp. 46-61, 6 pis. [Ukrainian with Rus- sian and English summary.] Cady, G. H., 1924. Structure of parts of northeastern Williamson and western Saline counties: Illinois Geol. Survey, Rept. of Investigations, no. 2, pp. 8-9. [Description and two figures of Girtyina ventricosa = Fusulina girtyi (Dunbar and Condra).] Carpenter, W. B., 1862. Introduction to the study of Foraminifera: Roy. Society, London, pi. 12, figs. 24-29. Chapman, F., 1902. The Foraminifera: Longmans, Green and Co., London and New York, 354 pp., 14 pis., 42 text figs. Chapman, F., and Parr, W. J., 1936. A classification of the Foraminifera: Royal Soc. Victoria, Proc. (n. s.), vol. 49, pt. 1, pp. 139-151. , 1937. On the discovery of fusu- linid Foraminifera in the upper Paleo- zoic of Northwest Australia: with a note on a new bivalve: Victoria Natural- ist, vol. 53, pp. 175-179, pi. 16. Chen, S., 1934. Fusulinidae of the Huang- lung and Maping limestones, Kwangsi: Nat. Research Inst. Geology (Shanghai) Mem. no. 14, pp. 33-54, pis. 6-8. , 1934a. Fusulinidae of South China, Part I: Paleontologia Sinica, ser. B, vol. 4, fasc. 2, pp. 1-185, pis. 1-16. [Chiefly a description of species.] , 1934b. A new species of Fusu- linidae from the Meitien limestone: Geol. Soc. China Bull., vol. 13, No. 2, pp. 237-242, pi. 1. [Describes a new genus, Gallowaiina (homonym of Galloway- ina).'] Ciry, Raymond, 1938 [1939]. Sur quelques Fusulinides Nouveaux du Permian de Turquie. Bull. Sci. de Bourgogne, vol. 8, pp. 53-60, pi. 1. Colani, M., 1924. Nouvelles contributions a l'etude des Fusulinides de TExtreme- Orient: Serv. Geol. de l'lndochine Mem., vol. 11, fasc. 1, pp. 1-191, pis. 1-29. [A detailed restudy and revision of the Fusulinidae in Indo-China.] 151 152 PENN8YLVANIAN FUSULINIDAE Culver, H. E., 1922. Note on the occurrence of Fusulinas in the Pennsylvanian rocks of Illinois: Illinois Acad. Sci. Trans., vol. 15, pp. 421-425. Cushman, J. A., 1928. The Foraminifera, their classification and economic use: Cushman Lab. Foram. Research, Spec. Pub. no. 1 (Sharon, Mass.). [Contains chapter on Fusulinidae by Y. Ozawa in addition to matters of general interest.] , 1933. The Foraminifera, etc. (2nd ed.): Cushman Lab. Foram. Re- search, Spec. Pub. no. 4 (with an il- lustrated key, Spec. Pub. no. 5). [Fam- ily Fusulinidae by C. O. Dunbar, pp. 126- 140, pis. 10-12.] Dawson, G. M., 1879. On a new species of Loftusia from British Columbia: Geol. Soc. London Quart. Jour., vol. 35, pp. 69- 75, pi. 6, figs. 1-7. [Describes the new species Neoschwagerina (= "Loftusia") columbiana.] Deecke, W., 1914. Uber Foraminif eren : Neues Jahrb., pp. 21-43. Deprat, J., 1912. Etude des Fusulinides de Chine et d'Indo-chine et classification des calcaires a fusulines, Pt. I: Serv. Geol. de l'lndochine Mem., vol. 1, fasc. 3, pp. 1-76, pis. 1-9, text figs. 1-30. [Very important general discussion of shell structure and classification of the fusu- lines, followed by a description of num- erous species; also an account of the faunal zones of the "Carboniferous" of Indo-China.] , 1912a. Sur deux genres nouveaux de Fusulinides de l'Asie orientale, in- teressants au point de vue phylogeni- que: Acad. Sci. Paris Comptes rendus, vol. 154, pp. 1548-1550. [Preliminary introduction of the genera Paleofusulina and Neofusulinella.] , 1913. Etude des Fusulinides de Chine et d'Indochine et classification des calcaires a fusulines, Pt. II, Les Fusulinides des calcaires carboniferiens et permiens du Tonkin, du Laos et du Nord-Annam: Ibid., vol. 2, fasc. 1, pp. 1-74, pis. 1-10, text figs. 1-25. [Further discussion of structure and of classifi- cation, and description of numerous species.] , 1914. Etude des Fusulinides du Japon, de Chine et d'Indochine, Pt. Ill, Etude comparative des Fusulinides d'Akasaka (Japon) et des Fusulinides de Chine et d'Indochine: Ibid., vol. 3, fasc. 1, pp. 1-45, pis. 1-8, text figs. 1-8. [Chiefly devoted to description of species; de- scribes the new subgenus Yabeina.] , 1915. Etudes des Fusulinides de Chine et d'Indochine, Pt. IV, Les Fusu- linides des calcaires carboniferiens et permiens du Tonkin, du Laos et du Nord-Annam: Ibid., vol. 4, fasc. 1, pp. 1-30, pis. 1-3, text figs. 1-11. [Chiefly a description of species. In summary, gives a catalogue of all the species of the fusulines of the world, 88 in num- ber, which he regards as valid, and cites original references for each.] D'Orbigny, A., 1845. in Murchison, deVer- neuil, and Keyserling, G£ologie de la Russie d'Europe et des montagnes de l'Oural, Vol. II, Paleontologie, pp. 16 and 382, pi. 1, figs. 1 a-d. , 1934. Some new species of Fusulinidae from the Upper and Middle Carboniferous of Verkhne-Chussovskye Gorodki on the Chussovaya River (west- ern slope of the Middle Ural) : Pet. Prosp. and Geol. Inst. Pub. (A), no. 36, pp. 1-98, pis. 1-6. [Describes ten new species and two varieties and rede- scribes four old ones from the Mosco- vian and (?) lower Uralian.] -, 1934a. Sur la stratigraphie du Carbonif^re Moyen de l'Oural: Oil Geol. Inst. Mem., vol. 55, pp. 1-41. [Rede- scribes twelve species of Fusulinidae.] , 1934b. Permian fauna of fusu- linids found in the sections of Kara-su and Kuberganda in East Pamir, in Doutkevitch, G. A., Geology of Pamir Acad. Sci. U. S. S. R., vol. 7, pp. 53-104, pis. 1-3. [Good diagrams of the generic structures and new classifications.] -, 1937. Sur l'importance de la microfaune pour la correlation du Per- mien de la partie meridionale de l'URSS: Int. Geol. Congress, XVII Ses- sion, Abstracts of Papers, pp. 95-96. Doutkevitch, G. A., 1932. Geological in- vestigations in the eastern part of the Tchussovskoi oil-bearing region: Oil Geol. Inst. Trans., vol. 30 (in Russian). [Includes considerable discussion of the stratigraphie relations of the fusulines in this area in the central western Urals.] Douville, H., 1906. Sur la structure du test dans les fusulines: Acad. Sci. Paris Comptes rendus, vol. 143, pp. 258-261. [First correct explanation of fusulinid wall structure.] , 1906a. Les calcaires a fusulines de l'lndochine: Soc. Geol. France Bull. (4), vol. 6, pp. 576-587, pis. 17-18. Douville, H., 1934. Les Fusulinides de la Tunisie, II, Le Permien marin de l'extreme-Sud Tunisie: Serv. Carte Geol. Tunisie Mem. (n. s.), no. 1, pp. 75-90. BIBLIOGRAPHY 153 Dunbar, Carl O., 1930. Identification of Fusulinidae from the Big Lake Oil Com- pany Well 1-C, in Sellards, Bybee, and Hemphill, Producing horizons in the Big Lake oil field, Reagan County, Texas: Univ. Texas Bull. 3001, p. 154. , 1932. Neoschwagerina in the Permian faunas of British Columbia: Royal Soc. Canada Trans., vol. 26, pp. 45-49, pi. 1. 1933. Fusulinids of the Big Lake oil field, Reagan County, Texas: Univ. Texas Bull. 3201, pp. 69-74, pi. 6. , 1933a. Stratigraphic signifi- cance of the fusulinids of the lower Pro- ductus limestone of the Salt Range: Geol. Survey India Records, vol. 66, pp. 405-413, pi. 22. ■, 1933b. Fusulinidae: in Cush- man, J. A., Foraminifera, etc. 2d ed., pp. 126-140, pis. 10-12. , 1937. Zonation and correlation of the late Paleozoic on the basis of Fusu- linidae (Abstract) : Internat. Geol. Con- gress, XVII Session, Abstracts of papers, p. 84. , 1939. Permian fusulines from Central America: Jour. Paleontology, vol. 13, pp. 344-348, pis. 35, 36. , 1939. Permian fusulines from Sonora: Geol. Soc. America Bull., vol. 50, pp. 1745-1760, 4 pis. - — •, 1940. Fusulinidae: in Cushman, J. A. Foraminifera, etc. 3rd ed., pp. 132-156, pis. 10-12 and 44 of the illus- trated key. , (See also Longwell, C. R., and Dunbar, C. O., 1936.) Dunbar, C. O., and Condra, G. E., 1927 [1928]. The Fusulinidae of the Penn- sylvanian system in Nebraska: Nebraska Geol. Surv. (2), Bull. 2, pp. 1-135, pis. 1-15, text figs. 1-13. Dunbar, C. O. and Henbest, L. G., 1930. The fusulinid genera Fusulina, Fusulinella, and Wedekindella: Am. Jour. Sci. (5), vol. 20, pp. 357-364. , 1931. Wedekindia, a new fusu- linid name: Am. Jour. Sci. (5), vol. 21, p. 458. , 1933. Wedekindellina, new name: in Cushman, J. A., Foraminifera, 2d ed., p. 134. , 1934. Comparative anatomy and evolutionary trends of the Pennsylva- nian Fusulinidae (abstract) : Geol. Soc. America Proc. for 1933, pp. 352-353. , 1938. Pennsylvanian Fusulini- dae of Illinois (abstract) : Geol. Soc. America Proc. for 1937, p. 320. Dunbar, C. O., and Skinner, J. W., 1931. New fusulinid genera from the Permian of west Texas: Am. Jour. Sci. (5), vol, 22, pp. 252-268. , 1936. Schwagerina versus Pseu- doschwagerina and Paraschwagerina: Jour. Paleontology, vol. 10, pp. 83-91. , 1937. The geology of Texas; Part 2, Permian Fusulinidae of Texas: Univ. Texas Bull. 3701, pp. 517-825, pis. 42-81, text figs. 89-97. Dunbar, C. O., Skinner, J. W., and King, R. E., 1936. Dimorphism in Permian fusulines: Univ. Texas Bull. 3501, pp. 173-190, pis. 1-3, text fig. 30. Dyhrenfurth, G., 1909. Die Fusulinen von Darwas (Schellwien's Monographie der Fusulinen, Pt. II): Palaeontographica, vol. 56, pp. 137-176, pis. 13-16, 10 text figs. Ehrenberg, C. G., 1842. (Discussion with- out title:) Berichte d. Kais. Preuss. Akad. Wiss., Berlin, pp. 273-275. [Orig- inal description of Borelis princeps, the named genotype of Schwagerina.'] — : , 1854. Mikrogeologie, pi. 37, X, C, 1-6. [Original illustrations of Bore- lis princeps and Alveolina montipara.] Eichwald, E., 1860. Lethaea Rossica, vol. 1, 2nd part and Atlas. [Original de- scription of genus Ore-bias.] Enderle, J., 1901. Uber eine anthracolith- ische Fauna von Balia Maden in Klein- asien: Beitr. Palaontologie u. Geol. Oesterr.-Ungarns u. des Orients, vol. 13, pp. 43-109. Elias, M. K., 1937. Depth of deposition of the Big Blue (late Paleozoic) sediments in Kansas: Geol. Soc. America Bull., vol. 48, pp. 403-432. [Position of fusu- linids in cyclothem described.] Fischer de Waldheim, G., 1829. Sur les cephalopodes fossiles de Moscou at de ses environs, en montrant des objets en nature: Soc. Imp. Nat. Moscou, Bull. 1, pp. 330-331. [Introduction of the name Fusulina.] , 1837. Oryctographie du Gouv- ernement de Moscou, pp. 126-127, pi. 13, figs. 1-11. [Original description of Fus- ulina cylindrica and F. depressa.] Fliegel, G., 1898. Die Verbreitung des ma- rinen Obercarbon in Sud und Ost-asien: Deutsche geol. Gesell. Zeitschr., vol. 50, pp. 385-408, pi. 14. 154 PENNSYLVANIAN FUSULINIDAE Fromaget, J., 1931. L'Anthracolithique en Indochine apr£s la regression moscovi- enne, ses transgressions et sa strati- graphie: Serv. Geol. Indochine Bull., vol. 19, fasc. 2, pp. 7-44. [Discusses zonation on basis of fusulines.] , 1934. Note de la classification du Fusulinides permiens: Soc. Geol. France Bull. (5), vol. 4, pp. 385-388. Fujimoto, H. (See Huzimoto, H.) Galloway, J. J., 1933. A manual of Fora- minifera: Principia Press, Blooming- ton, Indiana, pp. 388-411, pis. 36-38. Galloway, J. J., and Harlton, B. H., 1928. Some Pennsylvanian Foraminifera of Oklahoma, with special reference to the genus Orobias: Jour. Paleontology, vol. 2, pp. 338-357. Galloway, J. J. and Ryniker, C., 1930. Foraminifera from the Atoka formation of Oklahoma: Oklahoma Geol. Survey Circ. 21, pp. 1-36, pis. 1-5. Galloway, J. J., and Spock, L. E., 1933. Pennsylvanian Foraminifera from Mon- golia: Am. Mus. Novitates no. 658, pp. 1-6, pi. 1. Geinitz, H. B., 1876. Zur Geologie von Sumatra's Westkiiste: Palaeontograph- ica, vol. 22, p. 399-404. Girty, G. H., 1904. Triticites, a new genus of Carboniferous Foraminifera: Am. Jour. Sci. (4), vol. 17, pp. 234-240. , 1908. The Guadalupian fauna: U. S. Geol. Survey Prof. Paper 58, pp. 56-67, pis. 5, 17, 22, 27. , 1911. On some new genera and species of Pennsylvanian fossils from the Wewoka formation of Oklahoma: N. Y. Acad. Sci. Annals, vol. 21, pp. 119-156. , 1914. On the names of Ameri- can Fusulinas: Jour. Geol., vol. 22, pp. 237-242. — , 1915. Fauna of the Wewoka formation of Oklahoma: U. S. Geol. Survey Bull. 544, pp. 15-16, pi. 1. Gorsky, I. I., 1939. Atlas of the Leading Forms of the Fossil Faunas of the U. S. S. R., vol. V, pp. 30-48, pis, I-V. Gortani, M., 1903. Fossili rinvenuti in un primo Saggio del Calcare a Fusuline di Forni Avoltri (Alta Carnia occidentale). Riv. italiana Paleontologia, vol. IX, pp. 35-50, pis. 3, 4. , 1906. Contribuzioni alio Studio del Paleozoico Carnico. I. La Fauna Permo-Carbonifera del Col Mezzodi presso Forni Avoltri. Paleontogr. ital- ica, vol. XII, pp. 1-84, pis. 1-3. , 1909. Sui Metodi di Determina- zione della Fusuline. Atti. Soc. tosc. Sci. Nat. Proc.-verb., vol. 18, pp. 15-17. Gottsche, C, 1884. Uber japanisches Car- bon: Deutsche geol. Gesell., Zeitschr., vol. 36, p. 653. Gregorio, Antonio de, 1930. Sul Permiano di Sicilia: Annales Geol. et Paleontol- ogie Livr. 52, pp. 1-70, pis. 1-21. [Pages 49-50 and Plate 20, figs. 12-31, are de- voted to fusulines.] Gubler, J., 1934. La valeur stratigraphique des Fusulinides du Permien: Acad. Sci. Paris Comptes rendus, vol. 198, pp. 381- 383. , 1934a. Structure et secretion du test des Fusulinides: Annales de Protistologie, vol. 4, pp. 1-24, text figs. 1-15, Paul Lechevalier, Paris. [Proposes theory that keriotheca is a prismatic structure.] , 1934b. A propos de la classifica- tion du Permien a Fusulindes: Soc. geol. France Bull., vol. 4, fasc. 4-5, pp. 443-448, pi. 1. , 1934c. A propos de Doliolina neoschwagerinoides Deprat: Soc. geol. France Comptes rendus, fasc. 16, pp. 252-254. , 1935 [1936]. Les Fusulinides du Permien de l'lndochine, leur struc- ture et leur classification: Soc. geol. France Mem. (n. s.), vol. 11, fasc. 4, pp. 1-173, pis. 1-8. [Revises the classifi- cation and presents in greater detail his ideas on shell structure.] GiiMBEL, W., 1874. Ausland [a newspaper], p. 479. [Introduces the name Fusulina japonica.} Hanzawa, S., 1933. On a Neoschwagerina- limestone from Okinawa-jima, the Riu- kiu (Loochoo) Islands: Japanese Jour. Geology and Geography, vol. 10, nos. 3-4, pp. 107-110, pi. 7. , 1937. Stratigraphical distribu- tion of the fusulinid Foraminifera from south Manchuria and Japan: Internal. Geol. Congress, XVII Session, Abstracts of papers, p. 86. , 1938. An aberrant type of the Fusulinidae from the Kitakami Moun- tainland, northeastern Japan: Imp. Acad. Tokyo Proc, vol. 14, pp. 255-259, figs. 1-16. [Describes the peculiar new genus Nipponitella and three new spe- cies.] BIBLIOGRAPHY 155 , 1938b. Stratigraphical distribu- tion of the genera Pseudoschwagerina and Paras chwagerina in Japan with de- scriptions of two new species of Pseudo- schwagerina from the Kitakami moun- tainland, northeastern Japan, Japanese Jour. Geol. and Geogr. vol. XVI, pp. 65- 73, pi. IV. Harlton, B. H., 1927. Some Pennsylvanian Foraminifera of the Glenn formation of southern Oklahoma: Jour. Paleontol- ogy, vol. 1, pp. 15-27, pis. 1-5. , 1928. Pennsylvanian Foramin- ifera of Oklahoma and Texas: Jour. Paleontology, vol. 1, pp. 305-311. (See also Galloway, J. J., and Harlton, B. H., 1928). Hayasaka, I., 1922. The limestone of Omi- Mura, Province of Echigo: Japanese Jour. Geology and Geography, vol. 1, pp. 1-7. , 1924. On the fauna of the An- thracolithic limestone of Omi-Mura in the western part of Echigo: Tohoku Imp. Univ., Sci. Rept. (2, Geology), vol. 8, pp. 1-83, pis. 1-7. Hayden, H. H., 1909. Fusulinidae from Afghanistan: Geol. Survey India Rec- ords, vol. 38, pp. 230-256, pis. 17-22. Henbest, L. G., 1928. Fusulinellas from the Stonefort limestone member of the Tradewater formation: Jour. Paleon- tology, vol. 2, pp. 70-85. , 1934. A new term for the youthful stage of foraminiferal shells: Science (n. s.), vol. 79, pp. 363-364. , 1934a. Keriothecal wall struc- ture in Fusulina; its significance and resolution by selective stains (ab- stract) : Geol. Soc. America Proc. for 1933, p. 353. , 1937. Keriothecal wall struc- ture in Fusulina and its influence on fusuline classification: Jour. Paleontol- ogy, vol. 11, pp. 212-230, pis. 34-35. , 1938. Notes on the ranges of Fusulinidae in the Cisco group (re- stricted) of the Brazos River region, north-central Texas: in W. Lee, C. O. Nickell, J. S. Williams, and L. G. Hen- best, Stratigraphic and paleontologic studies of the Pennsylvanian and Per- mian rocks in north-central Texas: Univ. Texas Bull. 3801, pp. 237-247, chart (pi. 11). (See also Dunbar, C. O., and Henbest, L. G., 1930, 1934, 1938). Heritsch, F., 1934. Die oberpermische Fauna von Zazar und Vrzdenec in den Savefalten: Serv. geol. Yougoslavie. Bull., vol. 3, pp. 6-61, 2 pis. Hok, Tan Sin, 1933. Notiz uber das Basal- skelett von Verbeekina: Dienst van den Mijnbouw in Nederlandsch-Indie, We- tensch. Meded., no. 25, pp. 57-65, 1 pi. Huzimoto, H., 1936. Stratigraphical and pa- leontological studies of the Titibu sys- tem of the Kwanto-Mountainland, Pt. 2, Paleontology: Tokyo Bunrika Daigaku, Sci. Repts., sec. 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Fusulinas from the Ping- ting Basin, northeast Shansi: Ibid., vol. 3, pp. 15-16. , 1927. Fusulinidae of North China: Paleontologia Sinica (B), vol. 4, fasc. 1, pp. 1-123, pis. 1-24. [Extensive monograph. First to rediscover the true character of Fusulina. Introduces genus Boultonia.] , 1931. Distribution of the domi- nant types of the fusulinoid Forami- nifera in the Chinese seas: Geol. Soc. China Bull., vol. 10 (Grabau Anniver- sary vol.), pp. 273-290, 1 pi. [Defines 9 faunal zones on basis of fusulinids.] , 1933. Taxonomic criteria of Fusulinidae, with notes on seven new Permian genera: Nat. Research Inst. Geol. (Shanghai), Mem., vol. 14, pp. 1-32, 5 pis. , 1937. Foraminifera from the Donetz Basin and their stratigraphical significance: Geol. Soc. China Bull. (V. K. Ting Memorial volume), vol. 16, pp. 57-107, pis. 1-2. Lee, J. S., Chen, S., and Chu, S., 1930. Huanglung limestone and its fauna: Nat. Research Inst. Geol. (Shanghai)^ Mem., vol. 9, pp. 85-144, pis. 1-15. 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Monographic der Fusu- linen, Teil III, Die Fusulinen (Schell- wienien) Nordamerikas: Palaeontog- raphica. vol. 59, pp. 157-192, pis. 15-20, text figs. 1-17. [Identification of Amer- ican species badly confused.] Staff, H. von, and Wedekind, R., 1910. Die Oberkarbone Foraminiferensapropelit Spitzbergens: Geol. Inst. Upsala Bull., vol. 10, pp. 81-123, pis. 2-4. [Proposes a new scheme of classification.] Suess, E., 1870. iiber das Vorkommen von Fusulinen in den Alpen: K. K. geol. Reichs. Wien Verh. vol. 24, pp. 4-5. Tan Sin Hok. (See Hok). Thomas, N. L., 1931. New early fusulinids from Texas: Univ. Texas Bull. 3101, pp. 27-33, pi. 1. Thompson, M. L., 1934. The fusulinids of the Des Moines series of Iowa: Iowa Univ. Studies in Nat. Hist., vol. 16, pp. 277-332, pis. 20-23. , 1935. The fusulinid genus Staff ella in America: Jour. Paleon- tology, vol. 9, pp. 111-120, pi. 13. , 1935a. The fusulinids of the Atoka and Boggy formations of Okla- homa: Jour. Paleontology, vol. 9, pp. 291-306, pi. 26. 1935b. The fusulinid genus Yangchienia Lee: Eclogae geol. Helve- tiae, vol. 28, pp. 511-517, pi. 17. 1936. Fusulinids from the Black Hills and adjacent areas in Wyo- ming: Jour. Paleontology, vol. 10, pp. 95-113, pis. 13-16. , 1936a. The fusulinid genus Verbeekina: Jour. Paleontology, vol. 10, pp. 193-201, pi. 24. , 1936b. The genotype of Fusu- lina s. a.: Am. Jour. Sci. (5), vol. 32, pp. 287-291. , 1936c. Lower Permian fusu- linids from Sumatra: Jour. Paleontol- ogy, vol. 10, pp. 587-592, figs. 1-13. , 1936d. Nagatoella, a new genus of Permian fusulinids: Geol. Soc. Japan Jour., vol. 43, pp. 195-202, pi. 12. , 1936e. Pennsylvanian fusuli- nids from Ohio: Jour. Paleontology, vol. 10, pp. 673-683, pis. 90, 91. , 1937. Fusulinids of the sub- family Schubertellinae: Jour. Paleon- tology, vol. 11, pp. 118-125, pi. 22. Thompson, M. L., and Foster, C. L., 1937. Fusulinids from the Middle Permian of Szechuan, China: Jour. Paleontology, vol. 11, pp. 126-144, pis. 23-25. Thompson, M. L., and Miller, A. K., 1935. Schwagerina from the western edge of the Red Basin, China: Jour. Paleontol- ogy, vol. 9, pp. 647-652, pi. 79. Thompson, M. L., and Scott, H. W., 1941. Fusulinids from the type section of the Lower Pennsylvanian quadrant forma- tion: Jour. Paleo., vol. 15, pp. 349-353, pi. 48. Ting, V. K., and Grabau, A. W., 1933. The Carboniferous of China and its bearing on the classification of the Mississip- pian and Pennsylvanian: Internat. Geol. Congress, XVI Session, Repts., vol. 1, pp. 555-571, pi. 1, [Gives stratigraphic ranges of fusulinids.] , 1933a. The Permian of China and its bearing on Permian classifica- tion: Internat. Geol. Congress, XVI Session, Repts., vol. 1, pp. 663-678. [Gives stratigraphic ranges of fusu- linids.] Tschernyschew, T., 1889. Uber eine Samm- lung aus dem Carbon der Umgegend von Vladivostok: Com. Geol. St. Peters- bourg, Bull., VII, pp. 353-359. Verbeek, D. M., and Fennema, R., 1896. De- scription geologique de Java et Madoura, Amsterdam, vol. 2, p. 1134 et seq. Verneuil, E. de, 1846. On the Fusulina in the coal formation of Ohio: Am. Jour. Sci. (2), vol. 2, p. 293. Volz, W., 1904. Zur Geologie von Sumatra, Anhang II, Einige neue Foraminiferen und Korallen sowie Hydrokorallen aus dem Oberkarbon Sumatras: Geol. Pa- laeont. Abh. Koken (Jena), vol. 10, pp. 177-194, text figs. 26-45. [Original use of several terms applied by German writers to shell structures. Original description of the genus Sumatrina.] Warthin, A. S. Jr., 1930. Micropaleontology of the Wetumka, Wewoka, and Holden- ville formations: Oklahoma Geol. Sur vey Bull. 53, pp. 1-94, pis. 1-7. BIBLIOGRAPHY 161 Westheimer, J. M., 1931. Classification of Fusulinids: Micropaleontology Bull., vol. 3, no. 1, pp. 7-9. Wheeler, H. E., 1933. Fusulinids of the McCloud and Nosoni formations of north California (abstract) : Geol. Soc. Ameri- ca Bull., vol. 44, p. 218. White, C. A., 1877. Paleontology: U. S. Geol. Survey West of 100th Meridian, vol. 4, p. 98. White, M. P., 1932. Some Texas Fusulin- idae: Univ. Texas Bull. 3211, pp. 1-105, pis. 1-10. , 1936. Some fusulinid problems: Jour. Paleontology, vol. 10, pp. 123-133, pis. 18-20. Wittenburg, P. von, 1908. Neue Beitrage zur Geologie und Palaontologie der Wer- fener Schichten Sudtirols, mit Beruck- sichtigung der Schichten von Vladivos- tok :Centralbl. Mineralogie, pp. 67-89. ■, 1909. Geologische Studien an der ostasiatische Kuste im Golfe Peter des Grossen: Neues Jahrb., Beilage- Band 27, pp. 509-540, pis. 9-17. Yabe, H., 1899. On Fusulina japonica Schwager from Tomuro, Province of Schimotsuke: Geol. Soc. Tokyo Jour., vol. 6. , 1902. Materials for a knowledge of the anthracolitic fauna in Japan: Geol. Soc. Tokyo Jour., vol. 9, No. 104, pp. 1-5. ,1902. On the genus Schwagerina : Geol. Soc. Tokyo Jour. vol. 9, pp. 283- 286 [in Japanese]. , 1903. On a Fusulina limestone with Helicoprion in Japan: Geol. Soc. Tokyo Jour., vol. 10, No. 113, pp. 1-13, pi. 2. , 1906. A contribution to the genus Fusulina, with notes on a Fusu- lina limestone from Korea: Imp. Univ. Tokyo Coll. Sci. Jour., vol. 21, pp. 1-36, pis. 1-3. — , 1910. Strukturproblem der Fu- sulinenschale: Beitr. Geol. Palaontolo- gie Oesterr.-Ungarns, u. des Orients, vol. 23, pp. 273-282. Yabe, H., and Hanzawa, S., 1931. Paleozoic and Mesozoic Foraminifera [of Nether- lands East Indies] : Leidsche Geol. Meded., Deel 5 [Feestbundel K. Martin] pp. 23-34. ■ , 1932. Tentative classification of the Foraminifera of the Fusulinidae: Imp. Acad. Tokyo Proa, vol. 8, pp. 40-43. Yabe, H., and Hayasaka, I., 1920. Paleon- tology of Southern China, in Geographi- cal Research in China (Tokyo Geog. Soc. vol. 3). COLLECTING LOCALITIES Our studied collections came from 75 localities and represent at least 13 hori- zons. They were mostly gathered over a period of years incidental to other field work and the collecting of larger fossils, hence several series of numbering are used and none is complete. But since the numbers correspond with field note- books preserved in the Survey files we have retained them instead of assigning a single new series. In the following catalogue each locali- ty is indicated precisely so that others interested may return to the same sta- tions. The complete fusuline fauna ob- tained at each station is given in italics. An asterisk ( # )preceding fossil names indicates that identification has been made from haphazard sections, from weathered surfaces, etc., without the aid of critical measurement of thin sections. Where this method of identification was used, the peculiar characteristics of the species are considered adequate to make the identification reasonably accurate. The sections given for stations Bl, B3, B9, E9, G3, G7, and G9 were described by Clayton Ball under the direct super- vision of the junior author. Description of the stratigraphic succession at most localities is not given because the source is either a single thin bed or an unmis- takably recognizable zone. At several localities the stratigraphic relations are either so critical or complicated that a description of the sedimentary sequence is necessary for identifying the source. Sta. 223, 7/16/25.— Bankston Fork Lime- stone, Williamson County (Harrisburg quadrangle). NE. i/4, SE. 14, NE. %, sec. 24, T. 9 S., R. 4 E. Outcrop beside road. Lime- stone about 3 feet thick lies approximately 1 foot below a 12-inch coal bed. Fusulina girtyi, F. illinoisensis ?. Sta. 229, 7/11/25.— Herrin Limestone, Williamson County (Harrisburg quadrangle). SW.14, NE. %, SE. i/4, Sec. 22, T. 9 S., R. 4 E. Limestone caprock of Herrin No. 6 coal, at local strip mine. *Fusulina girtyi, F. cf. F. haworthi f, F. illinoisensis ?. Sta. 231, 7/14/25.— Herrin Limestone, Williamson County (Harrisburg quad- rangle). SE. 14, SW. %, SE. %, sec. 25, T. 9 S., R. 4 E. Limestone caprock of Herrin No. 6 coal at local strip mine which extends into adjacent part of sec. 36 on the south. *Fusulina girtyi, F. illinoisensis. Sta. 232, 7/14/25.— Bankston Fork Lime- stone, Saline County (Harrisburg quad- rangle). NW. i/4, SE. i/4, NW. 1/4, sec. 19, T. 9 S., R. 5 E. Type locality for this lime- stone member. Outcrop in ravine near ele- vation 425 feet. Fusulina illinoisensis, F. girtyi. Sta. 233, 7/20/25.— Bankston Fork Lime- stone, Saline County (Harrisburg quad- rangle). Near center SE. 14, SE. %, sec. 25, T. 9 S., R. 5 E. and in adjoining area in sec. 36 on the south. *Fusulina girtyi ?, F. illi- noisensis. (Fusulines rare.) Sta. 234, 7/29/25.— Curlew Limestone, Sa- line County (Harrisburg quadrangle). In creek bed along west side of SW. %, NW. i/t, NW. i/4, sec. 27, T. 10 S., R. 6 E. Fusulina leei (locally abundant), F. sp. Sta. 235, 7/30/25.— Curlew Limestone, Sa- line County (Harrisburg quadrangle). SE. 14, SW. 1/4, SW. %, sec. 22, T. 10 S., R. 6 E. Fusulina leei (locally abundant). Sta. 237, 7/30/25.— Stonefort Limestone, Saline County (Harrisburg quadrangle). Near center W. y 2 , NE. %, NW. 14, sec. 22, T. 10 S., R. 6 E. Outcrop in old road near elevation 380. Fusulina sp. A, Wedekindel- lina euthysepta ?. Sta. 244, 8/8/25.— Bankston Fork Lime- stone, Saline County (Harrisburg quad- rangle). About 150 feet southwest of cen- ter, sec. 24, T. 9 S., R. 5 E. *Fusulina girtyi, F. illinoisensis. Sta. 248, 8/15/25.— Boskydell (?) marine zone, Pope County (Harrisburg quadrangle). Near center SW. 14, NE. %, NE. 14, sec. 4, T. 11 S., R. 6 E. Fossils from a 4-inch bed of calcareous conglomeratic sandstone crop- ping out in stream bed. Area of outcrop very small. Generally covered by wash. Fusulinella iowensis var. stouti (?) (rare and poorly preserved). Sta. 250, 8/ ? / 25.— Stonefort Limestone, Saline County (Harrisburg quadrangle). Near or south of center of S. V 2 , NW. i/4, NW. 1/4, sec. 29, T. 10 S., R. 6 E. In west side of small, northward sloping ravine at elevation approximately 440 feet. Fossils rare. Wedekindellina euthysepta, W. excen- trica (?), W. minuta, and Fusulina nova- mexicana. 162 COLLECTING LOCALITIES 163 Sta. 286, 7/8/26.— Livingston Limestone, Edgar County. Near center, S. V2, SE. 1 / 4, NE. %, sec. 10, T. 14 N., R. 11 W. At water- falls and in small quarry, north of rural Roman Catholic church. Fusulines are abundant in calcareous clay zones 2 to 4 feet beneath top of the 10-foot limestone bed. Triticites ohioensis. Sta. 329, 8/6/26.— Calhoun Limestone, Lawrence County (Sumner quadrangle). SW. %, SW. V4, SW. y 4 , sec. 29, T. 3 N., R. 13 W. 3.6 miles south and 1.6 miles west of Sumner. Limestone caprock of coal in local strip mine. Preservation poor. Triti- cites venustus (rare). Sta. 330, 8/6/26. — Calhoun Limestone, Richland County (Sumner quadrangle). Local coal strippings along west side SE. i/4, NE. 14, sec. 11, T. 2 N., R. 14 W. Along creek. Limestone caprock of coal. Triti- cites venustus (rare). Sta. 370, 9/3/26. — Stonefort Limestone, Williamson County (Harrisburg quadrangle). NE. 14, SE. %, SE. i/4, sec. 34, T. 10 S., R. 4 E. Outcrop in hillside ravine at approxi- mate elevation 550 feet. Limestone thin, more or less shaly. Good locality for Stone- fort fusulines. Wedekindellina euthysepta, W. minuta. Fusulina novamexicana. Sta. 371, 9/3/26.— Stonefort Limestone, Williamson County (Harrisburg quad- rangle). Near center NE. %, SE. %, sec. 25, T. 10 S., R. 4 E. In vicinity of local drift mine, north edge of Stonefort village. Type locality of Stonefort limestone. Wedekin- dellina euthysepta, W. minuta, W. excen- tricd ?, Fusulina novamexicana. Sta. 377, 9/5/26.— Herrin Limestone, Sa- line County (Harrisburg quadrangle). Sec. 31, T. 9 S., R. 6 E. In old electric railway cut at Ledford. Fusulina illinoisensis, F. girtyi. Sta. 388, 9/8/26. — Herrin Limestone, Gal- latin County (Shawneetown quadrangle). Near center, E. side, NE. %, NW. 14, SE %, sec. 21, T. 10 S., R. 9 E. At abandoned drift mine about 200 feet southeast of road fork and at elevation 50 feet below top of hill. Collection from limestone above coal. Fusulina girtyi, F. illinoisensis. Sta. 452, 11/7/26. — Seahorne Limestone, Fulton County (Vermont quadrangle). Cen- ter SW. %, NW. %, sec. 27, T. 4 N., R. 2 E. West bank of small stream flowing northeast about 300 feet above mouth. Outcrop small. Fusulines rare. Fusulina pumila. Sta. 464, 6/13/27.— Curlew Limestone, Sa- line County (Harrisburg quadrangle). NE. 14, SW. 14, SW. 14, NW. 14, sec. 27, T. 10 S., R. 6 E. Outcrop in field west of road. Cur- lew limestone contains many siliceous sponge spicules here. Fusulina leei. Sta. 464a, 1927. — Herrin Limestone, Saline County (Harrisburg quadrangle). Near center, W. side, sec. 30, T. 9 S., R. 5 E. In the Illinois Central R. R. cut. Collected from various parts of the limestone. Fusu- lina illinoisensis, F. girtyi, F. aff. F. ha- worthi. Sta. 466, 7/5/27.— Absher Limestone/Will- iamson County (Marion quadrangle). SW. %, SW. %, NW. Vi, sec. 3, T. 10 S., R. 4 E. Small inconspicuous outcrop on north side of westward sloping ravine about 200 feet west of barn. Fusulina levicula, F. lucasen- sis, Fusulinella cadyi. Sta. 490, 1927. — Livingston (?) Limestone, Christian County. SE. 14, NE. 14, sec. 28, T. 12 N., R. 1 W. Triticites ohioensis, T. Venustus. Sta. 495, 8/17/27— Brereton Limestone, Randolph County (Baldwin quadrangle). SW. %, NE. 1/4, SW. 14, sec. 9, T. 5 S., R. 6 W. Northeast of road. Extensive outcrop in stream bed. Good collecting locality for fusulines. Fusulina illinoisensis. Sta. 498, 8/17/27.— Absher (?) Limestone, Randolph County (Baldwin quadrangle). Center S. %, SW. 14, NE. 14, sec. 9, T. 5 S., R. 6 W. At small waterfalls over limestone below junction of two small streams. Free specimens in clay lenses of limestone. The stratigraphic evidence that this limestone is equivalent to the true Absher limestone at station 466 is not entirely secure but approximate equivalence is generally ac- cepted. Best locality at which to collect this fauna. Fusulina lucasensis, F. levicula, Fusulinella cadyi. Sta. 504, 12/14/36.— Omega Limestone, Effingham County. NE. 14, sec. 18 T. 6 N., R. 5 E. Collected by G. H. Cady. Triticites venustus. Sta. 520, 8/27/27.— Herrin Limestone, Perry County (Coulterville quadrangle). NW. i/4, SW. i/4, NE. 14, sec. 16, T. 6 S., R. 4 W. In stream bed at bend in Pipestone Creek. Fusulines abundant. Fusulina gir- tyi, F. illinoisensis. Sta. 528, 9/7/27. — Brereton Limestone, Greene County (Roodhouse quadrangle). SW. 14, NE. 14, NE. 14, sec. 30, T. 11 N., R. 10 W. Outcrop in Little Bear Creek. Col- lected by L. G. Henbest, G. H. Cady, I. R. Van Pelt, and T. A. Hendricks. Fusulina girtyi, F. illinoisensis, F. lucasensis, and F. cfr. F. haworthi. Sta. 533, 9/9/27. — Brereton Limestone, Morgan County (Winchester quadrangle). At local mines in southwest corner of sec. 30, T. 13 N., R. 10 W. *Fusulina girtyi, F. illinoisensis. 164 PENNSYLVANIAN FUSULINIDAE Sta. 539, 9/11/27. Brereton Limestone, Fulton County (Havana quadrangle). SW. 1,4, SW. 1/4, SE. 14, sec. 19, T. 6 N., R. 3 E. Outcrop in ravine about 500 feet north of road. *Fusulina girtyi, F. Illinois ensis. Sta. 545, 9/12/27. — Lonsdale Limestone, Peoria County (Peoria quadrangle). NE. i/4, NW. 14, SE. 14, sec. 7, T. 8 N., R. 7 E. About i/4 mile east of J. B. Armstrong's house, in ravine at falls over Lonsdale lime- stone. Fusulines exceptionally abundant in gray marl about 1 foot beneath brink of falls. Specimens exceptionally well pre- served. L. G. Henbest and G. H. Cady, col- lectors. Fusulina acme, F. lonsdalensis, F. megista, F. mysticensis, F. eximia. Sta. 546, 9/12/27. — Brereton Limestone, Peoria County (Peoria quadrangle). NE. 1/4, NE. i/4, SW. 1/4, sec. 11, T. 8 N., R. 7 E. About 100 feet north of road between two houses and beside hillside ravine. Level about 10 feet above road. Collected by L. G. Henbest and G. H. Cady. Fusulina girtyi, F. illinois ensis. Sta. 547, 9/13/27. — Lonsdale Limestone, Marshall County. West of center, SE. %, sec. 16, T. 12 N., R. 9 E. At small waterfalls over Lonsdale limestone west of road in Gimlet Creek. Fusulina acme, F. lonsdalen- sis. Sta. 580, 9/21/28.— Seville Limestone, War- ren County (Monmouth quadrangle). Near C. S. 1/2, NE. i/4, NW. 14, sec. 15, T. 11 N., R. 2 W. At low bluff formed by Seville lime- stone; south side of stream; about 1,500 feet north of road. Limestone about 9 feet thick. C. O. Dunbar, L. G. Henbest, G. H. Cady, col- lectors. Fusulinella iowensis. F. gephyrea. Sta. 581, 9/ ? /28. — Oak Grove Limestone, Greene County (Roodhouse quadrangle). NE. %, NE. 14, sec. 22, T. 12 N., R. 11 W. At mouth of tributary gully from west. Col- lected by T. A. Hendricks. Wedekindellina ellipsoides, W. excentrica (?),W. euthy septa. Sta. 582, 10/28/27.— Brereton Limestone, Pulton County (Glasford quadrangle). East of Brereton, type locality of Brereton lime- stone in vicinity of station G9. Collected by G. H. Cady. Fusulina girtyi, F. illinoisensis (rare). Sta. 583, 1927. — Brereton Limestone, Ful- ton County. SW. %, SE. %, NE. 14, sec. 19, T. 6 N., R. 3 E. Collected by J. M. Weller. Fusulina girtyi (abundant), F. illinoisensis. Sta. A2, 8/2/29.— Herrin Limestone, Perry County (Pinckneyville quadrangle). Near center, sec. 1, T. 5 S., R. 3 W. V 2 mile south- southwest from tipple of Pyramid Strip Mine. Fusuline collections derived from harder layers of the caprock of the Herrin (No. 6) coal. * Fusulina girtyi, F. illinois- ensis. Sta. A3, 8/2/29.— Herrin Limestone, Will- iamson County (West Frankfort quad- rangle). SW. i/4, SW. i/4, SE. i/4, sec. 6, T. 9 S., R. 3 E. Blocks of the limestone cap- rock of the Herrin No. 6 coal about 6 feet thick in the Stroud strip mine % mile south of Spillertown and Vs mile east of concrete highway. Fusulina girtyi, F. illinoisensis, F. haworthi (?). Sta. A4, 8/2/29.— Herrin Limestone, Will- iamson County (West Frankfort quad- rangle). Near center NE. %, NW. i/4, sec. 7,. T. 9 S., R. 3 E. In strip mine west of con- crete highway. About 14 mile southwest from station A3 above, but same horizon.. Fusulina girtyi, F. illinoisensis, F. haworthi (?). Sta. A6, 8/3/29.— Absher Limestone, Will- iamson County (Herrin quadrangle). Near NW. cor. sec. 5, T. 9 S., R. 1 E. Abandoned strip mine, Harrisburg (No. 5) coal. Fossils collected from loose blocks of the limestone- caprock of the coal. The limestone lies close above the coal with but little shale interven- ing. Fusulinella cadyi, Fusulina levicula, F. lucasensis. Sta. A9, 8/3/29. — Herrin Limestone, Jack- son County (Murphysboro quadrangle). Near- center sec. 18, T. 7 S., R. 1 W., due west of Elkville on spoil banks of Truax-Traer Mine- No. 1 (Black Servant). The Herrin lime- stone observed in the cuts varies in position from 1 to 8 feet above the coal. Fusulina- girtyi, F. illinoisensis (?). Sta. B1, 8/5/29.— Stonefort (?) Limestone, Jackson County (Murphysboro quadrangle). Near SW. cor. NE. 14, SE. %, sec. 9, T. $ S., R. 2 W. Near boundary between Alto Pass and Murphysboro quadrangles. In bed. of stream flowing north-northwest through east half of Section 9. Thickness Ft. In. 7. Shale, soft 4? 6. Coal 12-15 5. Shale, with underclay at top 3 4. Sandstone, with plant impressions 4 3. Shale, variegated, with coal stringer 6 2. Limestone, gray, fossili- ferous (marine), upper part reddish, nodular and concretionary. Con- tains a few fusulines . . 1 3 : 1. Shale, black, more or less fissile 10 , The limestone lies about 30 feet above the Murphysboro (No. 2) coal. Wedekindellina euthysepta, Fusulina novamexicana. Sta. B3, 8/5/29. — Seahorne (?) Limestone,.. Randolph County (Campbell Hill quad- rangle). Near center N. y 2 , SW. 14, SE. %,. sec. 5, T. 7 S., R. 5 W. About % mile south of Wine Hill Village. Limestone forms- waterfalls. COLLECTING LOCALITIES 165 Thickness Ft. In. '8. Siliceous residue of leached limestone, finely porous; bears impres- sions of Marginifera and other marine fossils 1(?) 7. (Covered) +5-10 (?) .. •6. Shale 2 5. (Covered) 3 4. Limestone, nodular, dense, hard, gray, weathers t o reddish- brown or variegated col- or, contains numerous Fusulina pumila 2 6 3. Fireclay '. .. 6 2. Underclay, variegated reddish, yellowish, and bluish; soft 4 1. Shale, green +8 Fusulina pumila, F. cfr. F. leei (two speci- mens), Wedekindellina euthysepta (?). Sta. B9, 8/6/29. — Herrin Limestone, Mon- roe County (Waterloo quadrangle). NW. 1 /4, NE. 14, sec. 3, T. 2 S., R. 10 W. Outcrop in creek bed short distance upstream from local mine. West of Mobile and Ohio Ry. tracks. South of road. Thickness Ft. In. 6. Glacial drift 5. Limestone, light brown, dense, apparently non- fossiliferous 10 4. Underclay 12 3. Herrin limestone (upper part), calcareous clay shale containing no- dules of limestone, abundantly fossiliferous 6 2. Herrin limestone (lower part), indurated, upper part nodular; remain- der more or less platy, gray to light gray, weathers to light ochre; fossiliferous 4 1. Coal, Herrin (No. 6). Reported to be 3 to 5 feet thick in mine. Blue band absent or unknown to local resident 3-5 Collection B9 derived only from bed 3 and upper part of bed 2. Great care taken to ■avoid possible contamination with material from bed 5. B9 is the source of the most prolific and varied fusuline fauna that we Tiave yet found representing the Herrin- TBrereton horizon. Free specimens abun- dantly available. Fusulina girtyi, F. illinois- ensis, F. haworthi. Sta. E9, 8/12/29.— Oak Grove Limestone, Madison County (Alton quadrangle). SW. %, NE. iyi, NW. %, sec. 15, T. 5 N., R. 9 W. Outcrop south bank of East Fork Creek near l)end, 6 or 7 feet above Seahorne limestone. About 200-300 yards above bridge near "brick plant. Thickness Ft. In. 11. Siltstone, shaly +2 10. Oak Grove limestone and marl (according to H. R. Wanless and G. H. Cady), marine, earthy, carbonaceous, dark gray to black, pyritic, more or less nodular, richly fossiliferous with highly varied fauna of fusu- lines; source of E9 col- lection 4 9. Shale, b.ack, fissile, nig- gerhead concretions in lower part 1 7 8. Coal, Colchester No. 2 (according to H. R. W. and G. H. C.) 29-32 7. Underclay 2 7 6. Seahorne limestone, im- pure, nodular, pyritifer- ous; source of Fl col- lection. Fossils rare.. 0(?)-30 5. Siltstone. flinty, leach- ed fireclay 1 4. Coal streak %-% 3. Fireclay 3 2. Fireclay or ironstone ferruginous, thin band 1. Fireclay +1 The fossils in collection E9 were derived only from horizon 10. Wedekindellina eu- thysepta, W. sp., W. excentrica (?) (rare), Fusulina sp., F. spissiplicata. Sta. F1, 8/12/29. — Seahorne Limestone, Madison County (Alton quadrangle). Same location as station E9 above but collection derived from bed 6. Specimens scarce. Some pyritized in part. Fusulina pumila. Sta. F4, 8/12/29.— Piasa Limestone, Jer- sey County (Brighton quadrangle). Near cen. W. y 2 , NW. &, NE. %, sec. 23, T. 7 N., R. 10 W. North of Little Piasa Creek. Fusulina eximia, F. piasaensis. Sta. F5, 8/12/29. — Piasa Limestone, Jersey County (Brighton, quadrang'e). Near the middle E. %, NE. 14, sec. 25, T. 8 N., R. 10 W. At Piasa Falls on Piasa Creek. Collec- tion derived both from the indurated lime- stone and from the calcareous marl imme- diately underlying the limestone. Fusu- lines abundant in both. Free specimens available in the marl. Collected by G. H. Cady. Later revisited by L. G. Henbest and Clayton Ball. Fusulina eximia, F. mysticen- sis, F. piasaensis. Sta. G2, 8/13/29.— Oak Grove Limestone, Adams County. Near SW. cor. sec. 12, T. 1 N., R. 5 W. Low bluff north side of creek, about 300 yards below highway bridge. Collected by L. G. Henbest, G. H. Cady, and Clayton Ball. Wedekindellina euthysepta (common), Fusulina sp. (small, crushed, poorly preserved). 166 PENNSYLVANIAN FUSULINIDAE Sta. G3, 8/14/29.— Seville and Seahorne limestones, Mercer County (Edgington quad- rangle). Near cen. S. %, SE. 14, NE. 14, sec. 24, T. 15 N., R. 4 W. In ravine at base of small waterfalls, 10 to 20 feet below Sea- horne limestone. North of this locality a litter of limestone blocks covers the ground in places but it is uncertain whether these are glacial erratics or float possibly derived from the Seahorne limestone; consequently, no specimens of these blocks were collected. The section at G3 is imperfectly exposed, but a careful study on two different occas- ions indicated the following succession: Thickness Ft. In. 10. Soil and glacial drift 9. Sandstone + 5(?) 8. Seahorne 1 i m e s t o ne, light gray, more or less dense, sparingly fossili- ferous, Stigmaria and root impressions in the top, Fusulina pumila (rare), Wedekindellina euthy septa (a single specimen). Source of collection G5 2(?) ... .. 7. (Claystone ? poorly ex- posed) (Coal ? poorly exposed) 4(?) ... .. 6. Covered interval (less than 10 feet) +6 5. Sandstone +4 4. Covered interval 4 3. Seville limestone, dark to brownish black, car- bonaceous, dense, con- tains numerous Fusu- linella iowensis. Source of collection G3 ±11 2. Covered interval 1(?) 1. Rock Island No. 1 coal. 5(?) The interval between the Seville and the Seahorne limestones appears to be about 18 feet. Collected by L. G. Henbest and G. H. Cady, and later by C. O. Dunbar, L. G. Hen- best, and G. H. Cady. Sta. G5, 8/14/29. — Seahorne Limestone, Mercer County (Edgington quadrangle). Same location as G3 above. See horizon 8 in stratigraphic section for position and fauna. Sta. G7, 8/14/29.— Seville Limestone, Ful- ton County (Vermont quadrangle). SW. %, NE. %, sec. 23, T. 6 N, R. 1 E. At railroad cut and low bluff formed by the Seville limestone on the north side of Spoon River, northwest of Seville Station. The position of the horizon from which collection G7 came is indicated in the following sec- tion: Thickness Ft. In. 11. Seahorne limestone, thin, irregularly bedded, variegated, barren of fusulines 6 ±: 10. Claystone 1(?) 9. Coal streak 8. Underclay, grading into shale below ±3 7. Shale ±3 6. Seville limestone, thin- bedded, dark gray, weathers to light gray, fossiliferous; Fusulinel- la iowensis, F. iowensis var. stouti, F. gephy- rea. Source of collec- tion G7 6 5. Shale 1 6(?> 4. Rock Island (No. 1) coal, at outcrop in road, coal contains a sand- stone parting 2 S- 3. Underclay, Stigmaria (1] to 2 feet thick) j 2. Shale grading into the \ 8 underclay above | 1. Sandstone, earthy, ir- regularly bedded to mas- sive, top exposed, bears plant impressions +5 Sta. G9, 8/15/29. — Brereton Limestone, Fulton County (Glasford quadrangle). N.. y 2 , SE. 14, NW. 14, sec. 1, T. 7 N, R. 4 E. Outcrop about 20 feet above creek bed; north side, middle branch of Copperas Creek just west of bridge. The section follows: Thickness. Ft. In. 6. Sandstone, thin-bedded, impure 1 5. Shale, olive-drab to gray with small earthy con- cretions. Lower foot calcareous and fossili- ferous 6 4. Limestone, dark gray, relatively pure, fossili- ferous 2 3. Shale, olive-drab, calcar- eous, bearing concre- tions and lenses of lime- stone 2 2. Coal, with blue band, dirty, no black shale above coal at this locali- ty. Locally the lime- stone lies directly on the coal 4 2" 1. Underclay +1 ..... Type region of the Brereton limestone. Beds 3, 4, and lower part of 5 compose the- Brereton here. Collection derived from same horizons. Fusulina girtyi. COLLECTING LOCALITIES 167 Sta. H2, 8/15/29. — Lonsdale Limestone, Peoria County (Glasford quadrangle). SW. 14, NW. %, sec. 28, T. 8 N., R. 5 E. Outcrop in creek bed of southward flowing stream, about V 8 mile north of road. Fusulines ex- ceptionally abundant in marl lenses near base of limestone. Many of the free speci- mens abraded or slightly crushed. Fusulina lonsdalensis, F. acme, F. sp. Sta. H8, 1938.— Lower Fort Scott Lime- stone, Fort Scott, Bourbon County, Kansas. From railway cut at Fort Scott. Collected by R. C. Moore and R. G. Moss. Fusulina haivorthi, F. girtyi. Sta. H9, 8/?/29. — Greenup Limestone, Cumberland County. Small limestone quarry in the SE. corner, NE. 14, sec. 17, T. 10 N., R. 8 E. Quarry filled with water but speci- mens collected from waste heap. Most speci- mens encrusted with algal and protozoan growths. Collected by L. G. Henbest and L, E. Workman. Triticites callosus, T. me- diocris, T. mediocris var. angustus. Sta. Kd1, 8/20/39.— Cutler Limestone, St. Clair County (French Village quadrangle). Near Bunkum, south center sec. 18, T. 2 N., R. 8 W. Large block of brownish-white lime- stone about 3 feet thick in drift, along with many other blocks of the same lithology — probably nearly in place. Collected by G. H. Cady. Fusulina eximia, F. piasaensis. Sta. Kd2, 8/20/39.— Brereton Limestone, St. Clair County (French Village quad- rangle). Near Bunkum, NW. *4, SW. %, sec. 18, T. 2 N., R. 8 W. In ravine parallel to road. Just above No. 6 coal. Collected by G. H. Cady. Fusulina girtyi. Sta. Kd3, 8/26/39— Bankston Fork Lime- stone, St. Clair County (French Village quadrangle). Sec. 18, T. 2 N., R. 8 W., in ravine east of Bunkum. Only 2 to 3 feet above the caprock of No. 6 coal and below a "fresh-water" limestone. Loose blocks of the Cutler limestone lie still higher. Col- lected by G. H. Cady. Fusulina girtyi (?), F. knighti (?) Sta. Kd4, 8/23/39.— Piasa (?) Limestone, Greene County. Sec. 27, T. 11 N., R. 10 W., along Rubicon Creek, 1 mile north of Green- field. Collected by G. H. Cady. Fusulina megista. Sta. Kd5, 8/22/39.— Piasa Limestone, Ma- coupin County (Greenfield quadrangle). Sec. 17, T. 12 N., R. 9 W., near Scottsville. Col- lected by G. H. Cady. Fusulina megista, F. acme, F. cfr. F. illinoisensis. Sta. Kd6, 8/26/39.— Cutler (?) Limestone, St. Clair County (French Village quad- rangle). West side, sec. 17, T. 2 N., R. 8 W., in ravine. Same bed as Sta. Kdl. Col- lected by G. H. Cady. Fusulina acme, F. megista ( ?) F. cf. F. haworthi. Sta. Kd7, 8/26/39.— Cutler Limestone, St. Clair County (Belleville quadrangle). Sec. 21, T. 1 N., R. 8 W„ in Belleville, in quarry 3 blocks W. and % mi. N. of the city square. This is the upper limestone in the quarry. Collected by G. H. Cady. Fusulina megista. Sta. Kd8, 2/23/40.— Bankston Fork Lime- stone, St. Clair County (French Village quadrangle). Sec. 18, T. 2 N., R. 8 W. at Bunkum. Collected by G. H. Cady. Fusu- lina girtyi, F. illinoisensis, F. knighti. Sta. Kd9, 2/24/40.— Cutler Limestone (upper part), St. Clair County (Belleville quadrangle). Sec. 21, T. 1 N., R. 6 W. Quarry in Belleville. Same as Sta. Kd7. Fusulina megista. Sta. Kd10, 2/23/40.— Cutler Limestone, St. Clair County. NE. 14, sec. 33, T. 1 S., R. 7 W., about 100 yards north of bridge on highway No. 110, on Silver Creek, near Free- burg. Collected by J. N. Payne and G. H. Cady. Fusulina megista. Sta. T9, 9/20/28.— Brereton Lime-stone, Fulton County. NE. %, SE. %, SW. %, sec. 19, T. 6 N., R. 3 E. In type region of the Brereton limestone. Fusulina illinoisensis, F. girtyi. Sta. W10, 1/2/38.— Omega Limestone, Effingham County. NE. %, sec. 18, T. 6 N., R. 5 E. Collection furnished by H. R. Wan- less and others. Triticites venustus, T. ohioensis. Sta. W11, 1/2/38.— Omega Limestone, Ef- fingham County. NW. %, SE. %, SE. V± f sec. 11, T. 6 N., R. 4 E. At small waterfalls west of road. Furnished by H. R. Wanless and others. Triticites venustus, T. ohioensis. Sta. W12, 1/2/38.— Shumway Limestone, Effingham County. SE. %, SE. 14, SW. 14, sec. 26, T. 9 N., R. 5 E. Below slate at bridge over Shoal Creek east of Shumway. Collection furnished by H. R. Wanless and others. Triticites pauper, T. turgidus. Sta. W13, 1/2/38.— Omega Limestone, Ef- fingham County. Sec. 26, T. 6 N., R. 4 E. Collection furnished by H. R. Wanless and others. Triticites venustus. Sta. W14, 1/2/38.— Shumway Limestone, Effingham County. SW. V±, sec, 13, T. 6 N., R. 5 E. "Just east of ford in road 200 yards." Collection furnished by H. R. Wanless and others. Triticites pauper, T. turgidus. Sta. W15. — Greenup Limestone, Cumber- land County. NW. 14, sec. 10, T. 9 N., R. 9 E. Ravine west side of Embarrass River and north of U. S. Highway No. 40. Col- lected by J. M. Weller. Triticites mediocris var. angustus. Sta. W232. — St. David Limestone, Greene County. North center, sec. 30, T. 11 N., R. 10 W. Collected by J. Marvin Weller. Fusu- lina girtyi, F. illinoisensis, F. haworthi. !' L A T E S AND EXPLANATIONS PLATE 1 Shell Structure Fig. 1. Part of an axial section (X 125) of Fusulinella llanoensis Thomas, from the Bend limestone in the bluffs of Llano River, Mason County, Texas. Y.P.M. 15274. The tunnel passed just to the right of this area. Note the 4 layers of the wall (i, inner tectorium; d, diaphanotheca; t, tec- tum; o, outer tectorium); also the laminated structure of the cho- mata (c). 2. Part of excentric section (X 125) of Fusulinella iowensis Thompson from the Seville limestone at station G7 in Fulton County, Illinois (Slide Y 7). The section shows the antetheca (an) of the last volu- tion. Note that the wall is thin and homogeneous in these last few chambers where no epitheca has formed. In the whorl below, the diaphanotheca (d) is coated by epitheca (e). 3. Part of sagittal section (X 125) of Schwagerina crass it ectoria Dunbar and Skinner from the Leonard formation near Gaptank, Glass Mts., Texas. Y.P.M. 14941. The direction of coiling is from left to right. Compare the alveoli (a) in the keriotheca (k) with the septal pores (sp) in the septa. Note how the keriotheca bends down at the right and passes into a thinner, dense pyknotheca (p) that comprises the bulk of each septum. The tectum (t) can be traced along the outer surface of the wall and down the front side of the septa. 4. 6. Parts of an excentric section (X 125 and X 100 respectively) of Triticites ventricosus (Meek and Hayden) from the Hughes Creek shale at the base of the Council Grove Group of the Big Blue Series at Eiss Hill in southern Nebraska (Y. P. M. 11098). The pyknotheca (p) ap- pears lighter than the epitheca (e). One of the chambers is nearly filled by the latter which is the edge of one of the chomata. The coiling is from right to left in both pictures and the tectum (t) can be followed along the surface of the keriotheca (k) and down the front of each septum. 5. Part of a sagittal section (X 117) of Pseudoschwagerina cfr. P. uddeni Beede, from Bolivia. Collection of Dr. R. Kozlowski. The coiling is from left to right. Note how the keriotheca (k) bends in and thins as it passes into the pyknotheca (p) of the septum. The tectum (t) can be followed as a dark line down the front side of each septum. The alveoli (a) of the keriotheca are smaller than the septal pores (sp) in the septa. [170] Illinois State Geological Survey Bulletin 67, Plate 1 Illinois State Geological Survey Bulletin 67, Plate 2 PLATE 2 Shell Structure Pig. 1. Tunnel (t) and chomata (c) in Triticites meeki Moller. The spiral wall and septa are mostly broken away. Note that the chomata are thickened near the septa (X 9 ) . 2. Antetheca in Fusulina acme, n. sp., from the Lonsdale limestone at station 545, showing deep but irregular septal folds (X 10). 3, 4. Schwagerina diversiformis Dunbar and Skinner, front and end view, showing perfect antetheca with deep and regular septal folds (X 8 + ). Hueco limestone, Franklin Mountains, Texas. 5, 6. Pseudoschwagerina sp., front and end views, showing antetheca that lacks septal folds. From Permian beds in Karkartka Valley, Tian- schan Mts., China. Y. P. M. 13125 (X 6). 7. Slice of a partly crushed specimen of Parafusulina guatemalaensis Dunbar (X 82) in which the wall is cut in both transverse and tangential directions. Middle Permian near Purula, Guatemala. 8. Tangential slice of the spiral wall of Parafusulina guatemalaensis Dunbar (X 82), showing the perforate structure of both keriotheca (k) and tectum (t). The diagram at the right indicates the position of the section. From Permian beds at Purula, Guatemala. 9. Bit of axial section of Triticites plummeri Dunbar and Condra (X 250), showing the structure of the keriotheca (k) and of the edge of the overlying chomata (c). Station 628, slide A2 of the Wallace Lee collection from the Wayland shale member of the Graham formation, Cisco Group, north central Texas (Henbest, 1937, pi. 34, fig. 13). 10. Portion of an axial section of Triticites ventricosus (Meek and Hayden) (X 82), showing the laminated structure of the chomata (c). From the Hughes Creek shale at Eiss Hill, Nebraska. Y. P. M. 11098. 11. Bit of a slightly excentric sagittal section of the same species from the Naco limestone 1 mile northwest of Cave Creek P. O. Ariz. (X 82). The slice follows the chomata. Note how successive laminae of this secondary deposit have been deposited on the floor of tne volution, lapping part way up the sides of the septa. Y. P. M. 13905. 173 PLATE 3 Fusulinella gephyrea Dunbar and Henbest, n. sp p. 96 Fig. 1. Holotype, external view (X 10) with weathered surface showing strong septal folds in the end zones. From the Seville limestone at station 580 in Warren County, Illinois. 2. Axial section (X 10) of the same specimen. 3. Same unsectioned specimen photographed under water (about X 8). 4. Another specimen (X 5.5) from the same locality. 5,6. Sagittal section (X 10 and X 25) of specimen shown as figure 4. Fusulinella iowensis var. stouti Thompson p. 95 7,9. Axial section (X 10 and X 25) from the Seville limestone at station G7 in Fulton County, Illinois (Slide Y 1). Fusulinella iowensis var. stouti Thompson (?) p. 95 8. Axial section (X 10) of a specimen from the Boskydell (?) zone at sta- tion 248 in Pope County, Illinois (Slide 1). All specimens from this locality are badly preserved. Fusulinella iowensis Thompson p. 93 10-13. Four specimens (X 5) showing external view. All are from the Seville limestone. Figures 10 and 12 are from station 580 in Warren County; figure 11 is from either station G7 in Fulton County or G3 in Mercer County; and fig. 13 is from station G7 in Fulton County, Illinois. 14,15. Axial section ( X 10 and X 25) of a microspheric shell from the Seville limestone at station G7 in Fulton County (Slide Y 3). The center is shown in greater enlargement in figure 25. 16,24. Axial section (X 10 and X50) from the Seville limestone at station 580 in Warren County, Illinois (Slide 6). 17,18. Axial sections (X 10) from station G7 in Fulton County, Illinois (Slides Y 2 and Y 1). 19-21. Three sagittal sections (X 10) from station 580 in Warren County, Illi- nois. (Slides 8, 17, and 2). 22. Polished axial surface (X 25). (Station number lost). 23. Incomplete axial section (X 30) from station 580 in Warren County, Illinois. (Slide 28). 25. Great enlargement (X 90) of the center of the section shown in figures 14 and 15. The juvenarium of 15 chambers forming about 1% volu- tions is coiled in the plane of the slice. 1174] Illinois State Geological Survey Bulletin 67, Plate 3 Illinois State Geological Survey Bulletin 67, Plate 4 PLATE 4 Fusulina lucasensis Thompson p. 103 Figs. 1-3. Two specimens (X 2 and X 10) from the Absher (?) limestone at station 498 in Randolph County, Illinois. 4. Axial section (X 10) from the same locality (Slide F 2). 5,6. Axial section (X 10 and X 25) from the same locality (Slide D 2). 7.9. Sagittal section (X 10 and X 25) from the same locality (Slide D 1). 8.10. Sagittal section (X 10 and X 25) of another specimen from the same locality (Slide D 3). 11, 11a. Axial section (X 10 and X 25) of a specimen from the Herrin-Brereton limestone at station 528 in Greene County (Slide C 7). 29,30. Axial sections (X 10) of two cotypes from a limestone 10 feet below the Mystic coal, S. W. %, N. E. %, Sec. 16, T. 72 N., R. 22 W., Lucas County, Iowa. Y. P. M. 14684 Fusulina levicula Dunbar and Henbest, n. sp p. 104 12,13. Cotypes (X 5) showing various stages of growth. From the Absher (?) limestone at station 498 in Randolph County, Illinois (Slide A 1). 14-16. Axial sections (X 10) of 3 cotypes from the same locality (Slides Y 5, Y 1, and Y 4). No. 14 is the lower left specimen in figure 12 and No. 15 is the specimen shown as figure 13. No. 16 is the largest specimen observed. 17,18. Sagittal section (X 10 and X 25) from the same locality (Slide A 2). 19. Axial section (X 10) of another specimen from station A6 in Williamson County (Slide 3). Fusulinella cadyi Dunbar and Henbest, n. sp p. 96 20,24, 25. Holotype, external view (X 5) and axial section (X 10 and X 25), from the Absher (?) limestone at station 498 in Randolph County (Slide Y 3). 21-23. A paratype, external view (X 10) and axial section of the same (X 10 and X 25), from the same locality (Slide Y 1). 26. Sagittal section (X 10) of a paratype from the same locality (Slide B 3). 27. Sagittal section (X 10) from the Absher limestone at station A6 in Will- iamson County (Slide 7). 28. Axial section (X 50) of a microspheric shell from the Absher (?) lime- stone at station 498 (Slide A 7). [177 PLATE 5 Fusulina leei Skinner p # 109 (See also plate 6) Fig. 1. Six paratypes (X 1) from a marl just above the Bluejacket sandstone in the Cherokee shale in sec. 7, T. 21 N., R. 18 E., east of Claremore, Oklahoma. Gift to the senior author from John W. Skinner. 2. Free specimen (X 5) from the Curlew limestone at station 235 in Saline County, Illinois (Slide 58). 3,7,4. Holotype, axial section (X 10 and X 25), and first paratype, sagittal sec- tion (X 10), from the same locality as figure 1. These are the speci- mens figured by Skinner. U. S. Nat. Mus. No. 84621. 5. Axial section (X 10) from station 235 (Slide Y 1). 6. Axial section (X 10) from the Curlew limestone at station 234 in Saline County, Illinois (Slide 1). 8. Sagittal section (X 10) from station 235 (Slide 1). Fusulina pumila Thompson p. 107 9-11. Two specimens (X 1 and X 5) from the Seahorne (?) limestone at station B3 in Randolph County, Illinois. 12. Axial section (X 10) of the specimen shown as figure 11 (Slide Y 1). 13. Axial section (X 10) of another specimen from the same locality (Slide Y 1). 14,15. Axial section of another specimen (X 10 and X 20) from same locality (Slide A). 16, 17. Sagittal sections (X 10) from Seahorne limestone at station 452 in Fulton County (Slides 6 and 31). 18. Sagittal section (X 10) from station B3 (Slide B). 19. Sagittal section (X 21) from station B3 (Slide C). 20. Enlarged detail of figure 15 (X 50). 21. Enlarged detail of figure 18 (X 50). 178] Illinois State Geological Survey Bulletin 67, Plate 5 Illinois State Geological Survey Bulletin 67, Plate 6 PLATE 6 Fusulina leei Skinner p. 109 (See also plate 5) Fig. 1. Axial section (X 10) from Curlew limestone at station 235 (Slide Y 2). 2,3. Axial sections (X 10) of young specimens from the same locality (Slides 20 and 22). 4,5. Axial sections (X 10) from the Curlew limestone at station 464. 6. Axial section (X 10) from the Curlew limestone at station 234 (Slide 24). 7. Sagittal section (X 25) from the same station (Slide 13). 8. Sagittal section (X 25) of the paratype shown as figure 4 on plate 5. 9. Axial section (X 25) from the Curlew limestone at station 235 (Slide 17). 10. Center of an axial section (X 50) from the Curlew limestone at station 235 (Slide 27). In this shell the chomata are poorly developed and the first half volution was coiled at an angle oblique to the rest. Fusulina sp. A p. Ill 11. Axial section (X 10) of a specimen from the Stonefort limestone at sta- tion 237 in Saline County, Illinois (Slide 1). This specimen was figured by Henbest in 1928 (p. 79, pi. 10, figs. 2 and 4). Fusulina cf . F. leei Skinner p. Ill 12,13. Axial sections (X 10) from the Seahorne (?) limestone at station B3 in Randolph County, Illinois (Slides 8 and 15). Fusulina knighti Dunbar and Henbest, n. sp p. 112 14. Paratypes (X 1) from the Lower Fort Scott limestone at Knight's local- ity 45, y 2 mi. N. of Olive St. Road at juncture with Spoede Road in the city of St. Louis, Mo. Y. P M. 14427. 15. An immature axial section (X 10) from the Bankston Fork limestone near Bunkum, Illinois, at station Kd8 (Slide Y 1). 16. 17. Paratype axial sections (X 10) from the same locality as figure 12. Y. P. M. 14427. 18. Holotype axial section ( X 10) from the same locality. Y. P. M. 14427. 19-21. Paratype sagittal sections (X 10) from the same locality. Y. P. M. 14427. [181 PLATE 7 Fusulina spissiplicata Dunbar and Henbest, n. sp p. 105 Figs. 1,2. Group of types (X 1 and X 5) showing various stages of growth, from a marine zone over the Colchester No. 2 coal at station E9 in Madison County, Illinois (Slide B 1). 3,4. Holotype, a thick axial section (X 10 and X 27). This is the largest specimen of figure 2 (Slide Y 1). 5. Axial section (X 25) from the same locality (Slide C 2). 6. Sagittal section (X 25) from the same locality (Slide B 3). 7,8. Axial section of a paratype (X 10 and X 25) from the same locality (Slide Y 2). 9, 10. Axial section (X 10 and X 25) from the same locality (Slide F 2). 11,12. Axial section (X 10) and enlarged detail (X 50) of a microspheric indi- vidual from the same locality, tentatively identified with this species (Slide B 6). Wedekindellina excentrica (Roth and Skinner) ( ?) p. 102 13. Excentric sagittal section (X 10) from the Stonefort limestone at station 250 in Saline County, Illinois (Slide 4). 14. Axial section (X 10) from a marine zone over Colchester No. 2 coal at station 581 in Greene County, Illinois (Slide 7). 1182. Illinois State Geological Survey Bulletin 67, Plate 7 >;■ r«ti Illinois State Geological Survey Bulletin 67, Plate 8 J»M, ^mx 22 .• PLATE 8 Wedekindellina euthysepta (Henbest) p 98 (See also plate 9) Fig. 1. A group of specimens (X 1) showing different stages of growth, from a nodular limestone just over No. 2 coal at station E9 in Madison County, Illinois. 2-5. Four paratypes, enlarged (X 5), from the Stonefort limestone at station 370 in Williamson County, Illinois. Number 2 possibly belongs to W. minuta. 6-10. Five of the specimens from figure 1, enlarged (X 5). 11. Axial section of a paratype (X 10) from the Stonefort limestone at sta- tion 370 in Williamson County, Illinois (Slide B). 12. Axial section (X 10) from the Stonefort (?) limestone at station Bl in Jackson County, Illinois (Slide 5). 13,14. Axial sections (X 25) of young and adult specimens from the caprock of Colchester No. 2 coal at station E9 in Madison County, Illinois (Slide Y 1). 15-17. Axial section of the holotype ( X 10, X 25, and X 40) from the Stonefort limestone at station 370 in Williamson County, Illinois. 18,19. Sagittal section of a paratype (X 10 and X 25) from the Stonefort lime- stone at station 250 in Saline County, Illinois. 20. Whole specimen enlarged (X 10), showing the characteristic appearance of the plane septa of Wedekindellina as seen through the translucent wall. Same as figure 5. 21. Part of figure 6, ( X 40) to show row of septal pores along the base of the antetheca. 22. Part of figure 11, enlarged (X 250) to show pores (p) passing through all layers of the wall. 23. Portion of the holotype (figures 15-17), enlarged (X 250) to show porosity (p). 185" PLATE 9 Wedekindellina euthysepta (Henbest) p 98 Figs. 1,2. Axial section of a typical specimen (X 10 and X 24+) from a nodular limestone just over Colchester No. 2 coal at station E9 in Madison County, Illinois. Septal pores are well shown in the last volution (Slide Y 1). 3,4. Sagittal sections (X 24+) from the same locality (Slide Y 2). Wedekindellina henbesti (Skinner) 5,8. Axial section of the holotype (X 10 and X 25) for comparison with W. euthysepta. This specimen, figured by Skinner, is in the collections of the U. S. National Museum. Cat. No. 84622. 6,7. Sagittal section of the figured paratype (X 10 and X 25) from the same locality. From a marly zone overlying the Bluejacket sandstone in Sec. 7, T. 21 N., R. 18 E., near Pryor, Oklahoma. Wedekindellina ellipsoides Dunbar and Henbest, n. sp p. 101 9,10. External views of the holotype and the first paratypes (X 6), before sectioning. 11,14. Axial section of the holotype (X 10 and X 40). 12,13. Sagittal section of the first paratype (X 10 and X 40). All from a ; marine zone above Colchester No. 2 coal at station 581 in Greene County, Illinois. 1861 Illinois State Geological Survey Bulletin 67, Plate Illinois State Geological Survey Bulletin 67, Plate 10 <& 17 PLATE 10 Wedekindellina minuta (Henbest) p. 100 Figs. 1, 4. Holotype ( X 10 and X 50) from the Stonefort limestone at station 370 in Saline County, Illinois. 2.5. Sagittal section (X 10 and X 100) of first paratype, from same locality (Slide 0). 3.6. Sagittal section (X 10 and X 100) from the same locality (Slide A). This is probably an immature specimen of W. euthysepta. Fusulina novamexicana Needham p. 113 7. Axial section (X 10) from the Stonefort (?) limestone at station Bl (Slide 1). 8. Axial section of lectoholotype (X 10) from the Lower Magdalena lime- stone 3 miles west of Socorro, New Mexico. This is the specimen figured by Needham as figure 13 of plate 2. 9. Axial polished surface (X 10) of a somewhat deformed shell from the Stonefort limestone at station 370 in Williamson County, Illinois (Slide C). 10,12. Axial sections (X 10) from the Stonefort limestone at station 371 in Williamson County, Illinois (Slides 1 and Y 1). 11. Deeply corroded specimen (X 10) from station 371, showing the strong septal folding. 13,14. Sagittal sections (X 10), both somewhat oblique, the first a thin section and the second a polished surface, from station 371 (Slides P and E). 15,17. Axial section (X 10) and enlarged detail (X 40) from station 371 (Slide A). 16. Polished axial slice (X 10) of another specimen from station 371 (Slide D). [189] PLATE 11 Fusulina girtyi (Dunbar and Condra) p. 115 (See also plate 12) Fig. 1. Five typical specimens (X 1) from the Brereton limestone, Peoria Coun- ty, Illinois. From the Braun-Schuchert collection at Yale. Y. P. M. 15248. 2-6. Same (X 5). 7-8. Typical specimens (X 5) from the Brereton limestone at station B9 in Monroe County, Illinois (Slide D 1). 9. Holotype (X 5) from same horizon near Canton, Fulton County, Illinois. Y. P. M. 11002. This specimen was figured by Dunbar and Condra (1927, pi. II, fig. 3). 10-14. Axial sections (X 10) from the Brereton-Herrin limestone. No. 10 is from station G9 (Slide D 2); No. 11 from station 464A in Saline County (Slide Y 1); No. 12 is from station G9 in Fulton County (Slide Y 4); Nos. 13 and 14 are from station 528 in Greene County (Slide Y 2 and Y 3). 15-17. Sagittal sections (X 10) from the Brereton-Herrin limestone. No. 15 is a cotype from near Canton, Illinois and was figured by Dunbar and Condra (1927, pi. II, fig. 4); (Y. P. M. 11002); No. 16 is from station 583 (Slide 4); and No. 17 is from station 377 in Saline County, Illinois (Slide 17). The last was also figured by Henbest in 1928 (PI. 9, fig. 3). Fusulina illinoisensis Dunbar and Henbest, n. sp p. 118 (See also plates 12, 13) 18-23. Five cotypes (X 1 and X 5). Nos. 19-22 are from the Brereton limestone at station B9 in Monroe County, Illinois; No. 23 is from the Bankston Fork limestone at station 232, Saline County, Illinois. 24-26. Sagittal sections of 3 cotypes (X 10) from station B9 in Monroe County, Illinois (Slides 4, C 1, and B 6, respectively). 27-30. Axial sections of 4 cotypes (X 10) from station B9 (Slides C 5, C 4, B 1, and A 3, respectively). [190] Illinois State Geological Survey Bulletin 67, Plate 11 Illinois State Geological Survey Bulletin 67, Plate 12 t^mk ], Q >I3& ■*V '*- V- PLATE 12 Ftjsulina hawokthi (Beede) emend. Dunbar and Henbest p. 119 (See also plate 14) Central part of specimen shown on plate 14, figure 3 (X 50). Ftjsulina girtyi (Dunbar and Condra) p. 115 (See also plate 11) 2. Enlarged detail (X 100) of a sagittal section from the Herrin limestone at station 377 in Saline County, Illinois (Slide 3). Pores in the wall appear dark. 3. Part of a sagittal section (X 43 ) from the Bankston Fork limestone at station 232 in Saline County, Illinois (Slide 4). 4. Axial section of the figured paratype (X 10) from the Brereton limestone near Canton, Fulton County, Illinois. Y. P. M. 11002. See Dunbar and Condra, 1927, plate II, figure 2. 5,8. External view (X 5) and axial section (X 10) of specimens from the Bankston Fork limestone at station 232 in Saline County, Illinois. 6,7. Sagittal and axial sections (X 10) from the Brereton limestone at station 528 in Greene County, Illinois (Slides A 3 and A 1). 10. Enlarged detail (X 100) from figure 7 showing the fine tubular pores crossing the wall. The pores appear as dark lines. 11. Proloculum of figure 7 greatly enlarged (X 236). Note that its wall is much thicker than that of the first volution. Ftjsulina illinoisensis Dunbar and Henbest, n. sp p. 118 (See also plates 11, 13) 9. Enlarged detail (X 72) of an axial section from the Herrin limestone at station 464A in Saline County, Illinois (Slide 3). Septal pores are conspicuous. [193] PLATE 13 Fusulina illinoisensis Dunbar and Henbest, n. sp p. 118 (See also plates 11, 12) Fig. 1. Axial section (X 10) from the Brereton limestone at station 528 in Greene County, Illinois (Slide Y 1). 2. Axial section (X 10) from the Bankston Fork limestone at station 407 in Saline County (Slide Y 1). 3. Sagittal section (X 10) from the Bankston Fork limestone at station 232 in Saline County (Slide 3). 4,5. Axial sections (X 10) of specimens tentatively identified with this species. From the Herrin limestone at station 464A in Saline County, Illinois (Slides G 4 and 3). 6. Axial section (X 10) from the Brereton limestone at station B9 in Mon- roe County, Illinois (Slide B 2). 7. Axial section (X 10) from the Brereton limestone at station 583 in Ful- ton County, Illinois (Slide 3). 8. Axial section (X 10) of a specimen tentatively referred to this species, having a double proloculum, from the Brereton limestone at station B9 in Fulton County, Illinois (Slide 3). 9. Enlarged detail (X 50) of center of figure 8. 10,11. Sagittal sections (X 10) from the Brereton limestone at station B9 in Monroe County, Illinois (Slides C 2 and D 4). 12. Enlarged detail (X 100) of a part of a sagittal section from station B9, showing the structure of the wall. (Slide B 4). 194] Illinois State Geological Survey Bulletin 67, Plate 13 Wkw Illinois State Geological Survey Bulletin 67, Plate 14 PLATE 14 Fusulina haworthi (Beede) p. 119 (See also plate 12) Fig. 1. External view (X 5) of a specimen from the Brereton limestone at sta- tion B9 in Monroe County, Illinois. 2-4. Axial sections (X 10) of three specimens from the same lot. The ends of No. 3 are broken away so as to make the shell appear shorter than it should (Slides A 4, C 6, and A 6, respectively). 5. Sagittal section (X 10) of a specimen from the same lot (Slide A 1). 6-9. Axial sections (X 10) of 4 topotypes from the Lower Fort Scott Lime- stone at station H8, Fort Scott, Kansas (Slides 8, 10, 3 and N 1, re- spectively). 10. Tangential section (X 10) in the penultimate whorl showing intensity of septal folding. Same locality (Slide 3). 11-14. Sagittal sections (X 10) of plesiotypes from the same locality (Slides 12, 3, 2 and 11, respectively). 15. Thick axial section (X 20) showing the character of the septal folding. Same locality (Slide 6). 16. Bit of the spiral wall (X 250) of the outer volution of a specimen from the same locality, stained with malachite green, showing the mural pores. (Slide 25). 17. Bit of spiral wall in the outer volution of another specimen (X 100), stained with malachite green in xylene. Same locality (Slide SAA). 18. Central portion of figure 9 enlarged (X 50). Fusulina cf. F. haworthi (Beede) p. 121 19. Axial section (X 10) from the Brereton limestone at station 464A in Saline County, Illinois (Slide G 10). This shell is more slender than the normal for this species. 20. Axial section (X 10) from the Brereton limestone at station 528 in Greene County, Illinois (Slide C 4). This also is more slender than normal for the species. [197] Fig. 1. 3-5. 2,6. 7. 8. 9,10. 11. 12. PLATE 15 Fusulina acme Dunbar and Henbest, n. sp p. 122 (See also plate 16) Lonsdale limestone, station 545, Fulton County, Illinois. Three paratypes (X 1). The same enlarged (X 5). Young and mature specimens (X 5). Axial section (X 10) of paratype (Slide 30). Axial section (X 10) of another paratype which appears abnormally thick and short because the last half volution is incomplete at the poles (Slide F). Holotype and paratype, axial sections (X 10) (Slide Y 2). Paratype, axial section (X 10) (Slide 39). Axial section (X 10) of slightly deformed specimen (Slide 31). 13,14. Sagittal section (X 10) (Slides 21 and 25). 15. Detail (X 25) of figure 11 showing pyramiding of septal folds in last volution. The tunnel (left of center in penultimate whorl) has not yet opened in the last whorl (Slide 39). 16. Enlargement (X 44) of part of figure 14, plate 16, showing septal loops and pores. 17. Enlargement (X 25) of detail of figure 8, showing the septal loops and pores. 18. Enlarged detail (X 25) of left end of figure 6, showing septal pores and folds in the antetheca (Slide 40). [198] Illinois State Geological Survey Bulletin 67, Plate 15 Illinois State Geological Survey Bulletin 67, Plate 16 PLATE 16 Fusulina lonsdalensis Dunbar and Henbest, n. sp p. 125 Lonsdale limestone, station 545, Fulton County, Illinois. Fig. 1. Mature and two young specimens (X 1). 2-4. Same enlarged (X 5). 5,6. Axial sections of young and immature specimens (X 10) (Slides X 6 and 13). 7. Axial section, slightly tangential, of a typical adult shell (X 10) (Slide 10). 8. Axial section (X 10) (Slide 7). 9. Axial section (X 10) of specimen shown as figure 4 (Slide Y 1). 10. Axial section (X 10) of a specimen thicker than normal (Slide K 8). 11. Tangential slice (X 10) (Slide K 10). Enlarged details are shown in figures 18, 20, and 21. 12,13. Sagittal sections (X 10) (Slides 6 and 25). 15. Enlarged detail (X 250) of figure 10, showing septal pores where slice in- tersects the nose of a fold (Slide K 8). 16. Enlarged detail (X 50) of figure 6, showing the double prolocula, each surrounded by nearly % of a volution of independent and dissimilarly oriented chambers, followed by complete fusion and unit growth (Slide 13). 17. Enlarged detail (X 250) of figure 6, at the position of the tunnel in the last volution (lower side), showing corrosion of the septum where the tunnel is to form (Slide 13). 18. Enlargement (X 100) of small crushed area of figure 11, in which both transverse and tangential sections of the wall appear (Slide K 10). 20,21. Other details (X 250 and X 100) of figure 11, showing the porous nature of the wall as revealed by staining (Slide K 10). 19. Enlarged detail (X 250) of figure 10, showing the porous character of the wall as revealed by staining (Slide K 8). Fusulina acme Dunbar and Henbest, n. sp p. 122 14. Axial section (X 10) of specimen of which enlarged details are shown in plate 15, figure 16. [201] PLATE 17 Fusulina eximia Thompson p. 123 (See also plate 23) Fig. 1. Three specimens (X 1) from the Piasa limestone at station F5, Jersey County, Illinois. 2-4. The same enlarged (X 5 ) . 5. Sagittal section (X 10) from the same locality (Slide CI). 6. Axial section of cotype (X 10) from the Cooper Creek limestone, about 80 feet above the Mystic coal in Appanoose County, Iowa. Y. P. M. 14687. 7,8. Axial sections (X 10) from station F5, Jersey County, Illinois (Slides C 9 and K). 9,10. Two weathered specimens (X 5) from the same locality with the spiro- theca removed and the septa freed of matrix. 11. Greater enlargement (X 25) of a bit of the last specimen showing the intense septal folding. Fustjlina megista Thompson p. 126 12-14. Three juvenile specimens (X 5) from the Lonsdale limestone at station 545, Peoria County, Illinois. 15,16. Axial section (X 10 ) from the same locality (Slides 41 and HI). 17. Cotype (X 5) from the "fifty-foot" limestone, 50 feet above the Mystic coal iy 2 mi. west of Sunshine, Appanoose County, Iowa. Y. P. M. 14685. 18-20. Axial and sagittal sections of cotypes (X 10) from the same locality. Y. P. M. 1468S and 1470Q. 202 Illinois State Geological Syztzy Buiaehh Y Plate '_' A \ 15 4 v^. &§^G*mP* 17 .■££•< Illinois State Geological Survey Bulletin 67, Plate 18 PLATE IS Fusulina mysticensis Thompson p. 127 Fig. 1. Axial section (X 10) of a specimen tentatively identified with this species, from the Lonsdale limestone at station 545 in Peoria County, Illinois (Slide E). 2. Axial section of cotype (X 10) from the "fifty-foot" limestone, about 50 feet above the Mystic coal in Appanoose County, Iowa. Y. P. M. 14682. 3. Axial section (X 10) from the Piasa limestone at station F5 in Jersey County, Illinois (Slide L). Fusulina piasaensis Dunbar and Henbest, n. sp p. 129 4,7. Holotype (X 1 and X 10) from the Piasa limestone at its type locality, station F5 in Jersey County, Illinois (Slide 12). 5,6. Axial sections (X 10) of two paratypes from the same locality. (Slides A and C). 8, 9. Sagittal sections (X 10) of paratype from the same locality. (Slides M 3 and 174). [205; PLATE 19 Triticites ohioensts Thompson p. 130 (See also plate 20) Livingston limestone station 286 in Edgar County, Illinois. Pig. 1. Four specimens (X 1) (Slide A 1). 2-8. The same and 3 other specimens (X 5). 9-13. Axial sections (X 10) (Slides B 1, A 11, A 4, A 9, and A 15, respectively). 14-16. Sagittal sections (X 10) (Slides A 3, A 14, and M 3, respectively). 17. Middle part of an axial section (X 10) showing abundant septal pores in the middle of the last volution (Slide 3). 18,19. Sagittal section (X 10 and X 40) (Slide B 4). 20. Sagittal section (X 10) (Slide A 7). 21. Enlarged detail of figure 11 (X 100) showing the alveolar wall structure. (Slide A 4). 22. Enlarged detail of another specimen (X 250) showing the alveolar wall structure (Slide J). 206] Illinois State Geological Survey Bulletin 67, Plate 19 Illinois State Geological Survey Bulletin 67, Plate 20 PLATE 20 Triticites secalicus var. oryziformis Newell Pig. 1. Two paratypes (X 1) from the Douglas Group in Anderson County, Kansas. 2-3. Same enlarged (X 5). 4. Axial section (X 10) of a paratype from the same lot, introduced for com- parison with the next species. Triticites venustus Dunbar and Henbest, n. sp p. 132 5-8. Three axial and one sagittal sections (X 10) from the Omega limestone at station 504 in Effingham County, Illinois (Slides Y^ Y 2 , Y 3 and Y 4 ). 9. Axial section (X 10) from the Omega limestone at station W 11 in Effingham County, Illinois (Slide Y 5 ). 10. Axial section (X 10) from the Livingston limestone at station 490 in Christian County, Illinois (Slide B 13 ). 11. Sagittal section (X 10) from the Omega limestone at station W 10 in Effingham County, Illinois (Slide Y 6 ). 12,13. Axial section (X 10 and X 25) from the Livingston (?) limestone at station 490 in Christian County, Illinois (Slide A 8 ). This specimen is less slender than the normal form. These photographs were made with dark-field illumination. 14* Axial section (X 10) from the Calhoun limestone at station 329, in Law- rence County, Illinois (Slide A 4 ). 15,16. Axial section (X 10 and X 25) of another specimen from station 329 (Slide A 5 ). 17. Sagittal section (X 10) from station 329 (Slide B 2 ). 18, 19. Sagittal sections (X 25) from the Livingston (?) limestone at station 490 (Slides A 2 and A 3 ). Triticites ohioensis Thompson p. 130 (See also plate 19) 20,21. Axial sections (X 10) from the Omega limestone at station W 10 in Effingham County, Illinois (Slides Y 3 and YJ. 22. Axial section (X 10) from the Omega limestone at station W 11 in Effing- ham County, Illinois (Slide Y t ). 23, 24. Axial sections (X 10) from the Livingston (?) limestone at station 490 in Christian County (Slides B 14 and B 4 ). [209] PLATE 21 Triticites mediocris Dunbar and Henbest, n. sp p. 134 Figs. 2-5. Axial sections (X 10) of 4 syntypes from the Greenup limestone at sta- tion H9 (Slides Y 9 , Y 7 , Y 8 , Y 6 ). 7,8. Sagittal sections (X 10) from the same locality (Slides M 2 , M 3 ). 16. Enlarged detail from figure 8 (X 100) showing structure in the wall and septa (Slide M 3 ). Triticites mediocris var. angustus Dunbar and Henbest, n. var p. 135 1. External view (X 5) of a specimen slightly more pointed than is typical. Greenup limestone at station H9. 6. Axial section (X 10) tentatively referred to this variety. It is not quite so slender as the types. Same locality (Slide M 4 ). 9-12. Axial sections (X 10) of 4 syntypes from the same locality (Slides S 4 , Y 2 4, M 5 , I 22 ) • 13,14. Sagittal sections (X 10) from the same locality (Slides S 3 , S 5 ). Triticites callosus Dunbar and Henbest, n. sp p. 136 (See also plate 22) 15. Axial section (X 10) of a syntype from the same locality (Slide 7). [210] Illinois State Geological Survey Bulletin 67, Plate 21 Illinois State Geological Survey Bulletin 67, Plate 22 PLATE 22 Triticites callosus Dunbar and Henbest, n. sp ■ . . .p. 136 (See also plate 21) Figs. 1-5. Axial sections (X 10) from the Greenup limestone at station H9 in Cumberland County, Illinois (Slides L 5, 8, 5, 1, and 2 respectively). No. 1 is immature; No. 2 is tangential to the proloculum; No. 3 had the tip of the fourth volution broken away on the right end and the injury was repaired but caused some deformation of the next 3 volu- tions; No. 5 has a portion of the eighth volution preserved at each end, making the poles appear more extended than is really true. The last specimen is selected as holotype. 6-8. Sagittal sections (X 10) from the same locality (Slides L 2, 4, and 6 respectively). 9. Enlarged detail (X 30) of the center of figure 8. The thickening of the wall is a part of the chomata. 10. Enlarged detail (X 20) of the center of figure 4. 11. Great enlargement (X 100) of a bit of the upper right margin of figure 7, showing the wall structure. The thick external layer is a part of one of the chomata. 12131 PLATE 23 Tkiticites pauper Dunbar and Henbest, n. sp p. 139 Figs. 1-4. Axial and sagittal sections (X 10 ) of syntypes from the Shumway lime- stone at station W12 in Effingham County. 5. Axial section (X 10) of another syntype from the Shumway limestone at station W14 in Effingham County. Triticttes turgidus Dunbar and Henbest, n. sp p. 138 6-8. Axial sections of immature syntypes (X 10 ) from the Shumway limestone at station W12 in Effingham County. 9-11. Axial sections of syntypes (X 10) from the Shumway limestone at station W14 in Effingham County. 12. Sagittal section from the last locality. Triticites cullomensis Dunbar and Condra p. 136 13-16. Sagittal and three axial sections (X 10) of cotypes from the Beal lime- stone iy 2 mi. north of Big Springs, Kansas. No. 16 is one of the types originally figured by Dunbar and Condra. 17,18. Axial sections (X 10) from the Ames limestone at Brilliant Cut, Pitts- burgh, Pennsylvania. Collected by Dr. William Darrah. Y. P. M. 16501. Fusulina eximia Thompson p. 123 (See also plate 11) 19,20. Axial section of a microspheric shell (X 10 and X 50) from the Piasa limestone at station F5 (Slide Y 7 ). 214] Illinois State Geological Survey Bulletin 67, Plate 23 INDEX Bold face type indicates the main reference Absher limestone 17, 18, 23, 29, 32 Antetheca 35 36 Anvil Rock sandstone . 17' 25 Babylon cyclothem -m Bald Knob coal J? Bankston Fork limestone ....'.'.'.'.' *;"'.' • • • "••••; 17, 18, 24, 25, 29, 32 Battery Rock cyclothem. . .16, 20 (footnote) Bogota cyclothem 16 19 Boskydell sandstone 15," 18,* 20,' 29', 32 Boultonia 4Q Kn 70 Brereton limestone . . . /. ' ' 9 ^a^v:.v::^:. 14 ' 16 ' 17 ' 18;24; ' 29 i^ Brouillett cyclothem . .,. ' " \ q 17 Calhoun limestone " 27 ' 29 Cancellina g~ Carbondale group 10 14* 17 18 Caseyville formation * ' ' 10 ' 14 Chomata 35, 36, 40, 46-47, 53, '54,' 55 Codonofusiella 75 80 Cohn cyclothem 1 a ^ Colania ." ±b ' " Colchester coal '.'.'. ' 14 Collinsville cyclothem 16 19 Covel conglomerate '22 Craborchard cyclothem .. Yfi' 17 funiculi ;;;; ^ i' Curlew coal ' j!j Curlew limestone .'.'.' .* .'15/ 20* 29, 32 Curlew sandstone 15 18 Cutler limestone 17," 18,' 25,' 29, 32 Cyclothems in iqiq Davis coal DeKoven coal ' ' DeLong coal Delwood coal '" ' 15 " 16 Delwood sandstone ' 15 Depratella 90 Diaphanotheca 38 39 40 41 Dimorphism .....' ' '48 Endothyroid juvenarium 49 50 Eos chub ertella 49 50' 77 Eoverbeekina 54 ' 86 EjPitheca '.'.".36,' 39, '47,' 53' 54 b aunal zones 28-30 Plannigan cyclothem 16 19 l^ejia 39 40 ; 49 ; 50 ; 78 Fusuhna 39, 42, 43, 44, 46,' 47, '49, '56,' 52,' '53', 54, 80 90 acme 14, 17, 25, 26, 29, 30, 53, 122 cf. F. haworthi 112 cf. F. leei ill cylindrica p " 55 ' '90-92 eooimia 14, 17, 25, 26, 29/49, 53 123 eximia subzone 30 girtyi...U, 17, 23, 25, 29, "53," 54,"55,'l15 girtyi subzone 30 haworthi 14, 17, 23, 25, 26, 29 119 15, 16 15, 16 Fusulina, Cont'd p fnltT 818 ^ 17, 23, 25, 29, A 1lI fZf H 17, 25, 29, 112 III 1 ."-' 15, 20, 21, 24, 29 109 leei subzone . . l 7 e ™cula '.'.'.' .'l7,' 23,' 24, 29/104 lonsdalensis 14,26,29 30 125 lucasensis 17, 23, 24, 25, 29 103 megista 14, 17, 25, 26, 29, 53,' 126 mysticensis 14, 25, 26, 29 127 novamexicana 15,22 24 29' 113 piasaensis 14, 17, 25, 26,' 29,' 30 ' 129 P^mila i 4) 21, 22, 24, 29' 107 serotina 9ft s p-. a ::::::::::::::::::::m spissiplicata 14, 22, 29 49 105 Fusulina zone 30 Fusuline-bearing beds .'. . " ' 1 c oq Fusulinella 39, 40, 42, 43, 44, 46,' 49,'56,"52','53,"54' 77 oocki ' ro cad y i 17, 20, 23,' 24,' 29, 96 gephyrea i4> 2 0, 29, 96 lowensis 14, 20, 21, 28, 29, 49, 53 93 lowensis var. stouti 14, 20,' 29' 95 iowensis subzone '. . ' '28 Fusulinella zone ' , ' " 28 Fusulines, evolutionary trends ..... 53.55 external form " 55.55 morphology '.'.'.'.'.'. 35-55 preparation and study 57.74 shell measurement 60-65 Fusulinidae, defined " 75 Fusulininae ! 53 75 G-allowaiinella ' " ' §5 Gila cyclothem //./..... 16 19 Gimlet cyclothem .14] 16/ 17^ 18 Girtyina ' ' g 9 ' gi Greenbush cyclothem ///././///...' 14 Greenup limestone 18, 19, 27, 29, 32 Grindstaff sandstone .'.15,' 16,' 18 Hanover limestone 14, is', 22' 32 Harrisburg coal '....'...' 17 Hemifusulina g'i g2 Herrin coal 7. .' 17 Herrin limestone 17, 18, 24, 29, 32 Isabel sandstone ...'....' 14 Jamestown limestone . . .16, 17, 18, 24, 25, 32 Keriotheca 39 t 41' 54 Leella '.'.'.. .'.55.' 77 Lepidolina gg Liverpool cyclothem 17, ig Livingston limestone 11, 14, 16, 17, IS, 19, 27^ 29. 32 Lonsdale limestone 14, 18. 26, 29, 30, 32 Lowell cyclothem ' 10 Lusk cyclothem 16 Macedonia cyclothem 15, 16, is McLeansboro group 10, 14. 18, 19, 26 Macoupin cyclothem ig, iy 217 218 INDEX Pages Marine horizons 10-11 Misellina 86 Murphysboro coal 31 Murray Bluff sandstone 15 Nankinella 55, 77 Neofusulinella 89 Neoschwagerina 49, 87 Neoschwagerininae 54, 55, 87 Newton cyclothem 16, 19 Nipponitella 75, 85 No. 1 coal 14 No. 2 coal 14 No. 5 coal 14 No. 5A coal 17 No. 6 coal 17 No. 8 coal 14 Nummulostegina 75 Oak Grove limestone 14, 18, 22, 29, 32 Omega limestone 16, 18, 19, 27, 29, 32 Ontogeny 50-55 Ozawainella 40, 53, 55, 76 Paleofusulina 84 Palzo sandstone 15, 17 Parachomata 54 Parafusulina 43, 44, 46, 47, 48, 49, 50, 54, 56, 83 Paras chwagerina 50, 55, 84 kansasensis 55 Piasa limestone 14, 18, 25, 29, 30, 32 Pisolina 76 Pleasantview sandstone 23 Pokeberry formation 32 Polydiexodina 44, 46, 47, 49, 50, 56, 83 Pope Creek cyclothem 14 Porosity of shell 41-42, 47-48 Pounds sandstone 15, 16 Profusulinella 78, 79 Proloculum 35, 36-38 measurement of 63 Protheca 36, 39, 47, 53 Pseudodoliolina 87 Pseudofusulina 82 Pseudoschwagerina 50, 55, 83 Pyknotheca 39, 45 Radius vector 62-63 Recapitulation 50-55 Reynoldsburg coal 15 Rock Island coal 14 Rugofusulina b2 Quasifusulina 80 Schellwienia 80, 91 Schubertella 39, 49, 50, 78 Schwagerina 42, 44, 46, 47, 50, 82 compacta 55 eras sit ectoria 55 linearis 55 Schwagerininae 53, 54, 81 Seahorne limestone 14, 18, 21, 29, 32 Sectioning 65-66 Sections, axial 57-59 sagittal 59-60 tangential 59 Sellers limestone 20 (footnote) Pages Septa 35, 36, 42-45, 53, 54, 55 counting of 63 Septal furrows 35, 3(5 loops '43 plications 53, 54 55 pores 36, 39, 45, 47 Septula 55 Seville limestone 14, 18, 20, 29, 32 Shoal Creek cyclothem 11, 13, 16, 18, 19 Shumway limestone 16, 18, 19, 28, 29, 32 Sparland cyclothem 14, 16, 17, 18 Spirotheca 35, 36 Springfield No. 5 coal 14 St. David limestone 13, 14, 16, 17, 18, 23, 29, 32 Staff ella 39, 40, 42, 44, 53, 54, 55, 76 mollerana 76 (footnote) Staining 72-74 Stonefort limestone 15, 16, 18, 21, 29, 32 Sumatrina 89 Summum cyclothem 14, 16, 17, 18 Tartar cyclothem 14 Tectoria 38, 39, 40, 53 Tectum 38, 39, 40, 41 Tradewater formation 10, 14, 15, 18 Triticites 41, 42, 44, 46, 47, 49, 50, 53, 81 callosus 19, 28, 29, 31, 136 cullomensis 135, 136 irregularis 55 mediocris 19, 28, 29, 134 mediocris var. angustus . . .19, 28, 29, 135 moorei 55 nebraskensis 55 ohioensis 19, 27, 29, 130 ohioensis subzone 31 pauper 19, 28, 29, 139 plummeri 55 secalicus 45, 54 turgidus 19, 28, 29, 138 ventricosus 54 venustus 19, 27, 29, 31, 132 Triticites zone 30-31 Trivoli cyclothem 14, 16, 17, 19, 26 Tunnel 35, 36, 45-46, 50, 55, 56 angle, measurement of 63-64 Verbeekina 86 Verbeekininae 54, 55, 85 Wall structure 38-42 fusulinellid type 38-41 schwagerinid type 41-42 Wall thickness, measurement of 63 Wedekindellina, 39, 42, 44, 46, 47, 53, 54, 79 ellipsoides 14, 22, 29, 101 euthy septa... 14, 15, 21, 22, 24, 29, 45, 98 euthysepta subzone 30 excentrica 14, 15, 22, 29, 102 minuta 15, 22, 29, 100 Wedekindellina zone 30 Wiley cyclothem 14 Willis coal 15 Woodbury cyclothem 16, 19 Yabeina 88 Yangchienia 39, 49, 50, 79 Zellia 84 Illinois State Geological Survey Bulletin 67 1942