HARVARD UNIVERSITY MES i LIBRARY OF THE Museum of Comparative Zoology rice bhine 254 ine OAR ey 4 ii Eales yy eon. — oa "> > ae | J al ’ ) i 4 a as .- - : ‘ i F . és ¢ nite OSS i BWREBGINS OF AMERICAN Par EONTOlOGy * VOL XLT MUS. COMP. ZOOL LIBRARY DEC 21 1961 HARVARD UNIVERSITY CONTENTS OF VOLUME XLIII Bulletin No. Plates 194. Ordovician Stromatoporoidea of North America By J. J. Galloway and J. St. Jean, Jr. .. 1-13 195. Names and Variation in Certain Indo-Pacific Camerinids—No. 2. A Rey By. WwW. Storrs Cole A...6- 14-16 196. Mississippian Smaller Foraminifera of Kentucky, Southern Indiana, Northern Tennessee, and Southcentral Ohio Bye JamMess Fi COMRGN i. eo. net cee erg reese 17-27 197. An Analyses of Certain Taxonomic Problems in the Larger Foraminifera By -W. storrs Cole) 3....:3: (eee 28-39 198. Rudist Assemblages in Cuba By Li. Chubb: ....... Pages 1-106 107-128 129-368 369-408 409-422 — See 5 5) ~~ MUS. COMP. Z00L LIBRAKY JUN-1 1961 HARVARD WAIVERSITY BULLETINS OF AMERICAN PALEONTOLOGY VOL, SAT © NUMBER 194 1961 Paleontological Research Institution Ithaca, New York U.S.A. PALEONTOLOGICAL RESEARCH INSTITUTION 1960-61 FIREOIDENT oe lh abe OUND NPN ae ae RD NorRMAN E. WEISBORD VIGE“PRESIDENTY 2-0! Oe it Ea TS a OO ORIN YA ES SECRETARY-EREASURER. 2 “Go ok eS. AN Pea REBECCA S. HARRIS DOURBRETOR f(r) 4 ST ee eM 3 ait? eR a KATHERINE V. W. PALMER COMNSE LY: Pa. 12 Weol n ee LL! sessstsseeeeeee ARMAND L, ADAMS REPRESENTATIVE AAAS CouNnclu. _..........KENNETH E. CASTER Trustees KENNETH E. CASTER (1960-1966) KATHERINE V. W. PALMER (Life) WINIFRED GOoLpRING (1955-1961) RALPH A. LippDLE (1956-1962) Repsecca S. Harris (Life) AXEL A. Otsson (Life) SOLOMON C. HOoLuisTeR (1959-1965) NoRMAN E. WErsBorD (1957-1963) Joun W. WELLS (1958-64) BULLETINS OF AMERICAN PALEONTOLOGY and PALAEONTOGRAPHICA AMERICANA KATHERINE V. W. PAtmer, Editor Mrs. Fay Brices, Secretary Advisory Board KENNETH E. CASTER " Hans KUGLER A. Myra KEen Jay GLENN Marks Complete titles and price list of separate available numbers may be had on application. All volumes available except vols. I-VI, VIII, X, XII, XIV, and XV of Bulletins and vol. I of Paleontographica Americana. Subscription may be entered at any time by volume or year, with average price of $16.00 per volume for Bulletins. Numbers of Paleontographica invoiced per issue. Purchases in U.S.A. for professional purposes are deductible from income tax. For sale by Paleontological Research Institution 109 Dearborn Place Ithaca, New York U.S.A. BULLETINS OF AMERICAN PALEONTOLOGY VOL. 43 NO. 194 ORDOVICIAN STROMATOPOROIDEA OF NORTH AMERICA by J. J. GaALLoway Indiana University and JOST: JEANS IR: University of North Carolina May 8, 1961 Paleontological Research Institution Ithaca, New York, U.S.A. Library of Congress Catalog Card Number: 61-301 JUN= 1 1961 HARVARD | | UNIVERSITY. Printed in the United States of America CONTENTS Page ENN OSE TN GO cee ec cee ee PF Se ee Sn EE En eR ro ee 5 HTirartetg lit Cty Oi pres e ce oe rect a Net aN ra NRO aes acids each erates sonatas seu 5 PANGKGTE OVW CLECTIN CEU ate ote es eae eee ae eae tee LD a TN A ee oo ants eae 9 SHWETA MENUS OUR EOE ce esas ta ee Ree Neer PE nee Se ane 9 ORES EHOMMA TOP OT O1CC ae eee ee eens or mee epee Sage Nee eee ene ee 9 De nlovarel siririaleictt aR le oi Ae RET I saree Re ee ee ee ee eS 10 Cystostroma vermontense Galloway and St. Jeam .................-..------------ 2 Gystostnoniaesinp lec, Gallonyay vaiderS ts) sam ese ee erece eee eee 13 (GSE OS TOIL MTILLTOUTILILT TOMA (les DT, KG) ems eee ee eee 14 Cystostroma fritzae Galloway and St. Jean, Nn. Sp. ....-..-.-------c-2c-eeceeee-oe 16 Onaypltophnagrnmsnantrgni cts) IR abyirny on eee ees ee eee 19 An aGencmp untiie ria G allovwiayaralG iS tone an) eee eee ree eee 27 ARID CCCI CEMTLTECL IL CEL Clam (GEM 1S) ) meee eae ee eee ea 30 nlacenanadavatanG.al ovvaiyaran dS tye || alsUsSDeeeesseeeen ee 32 Alnlawara. mogloosa: (QRS) cassecce see aeceocectecesceeaneanereect veccce aa orac gor saaee REE 34 PAH CCT LMILO CALLE LETC GEIO CLS Ce) pees eee eee ee 36 DN AGC AMI NLC AI Gam COCTSUC)) sa eee ee eee ee ee te ee ee eee 37 PAGE CAGE COI Cay LDTECLG UCC (OL OCS UC) ae ee rae ae eee ce soe 38 Pscudostylodictyor yea lamvotrense= (Seely) eee eee 40 SEUAOSEVIOMUCE) O71 me cue LOTLU (S.C Eliya) erase ee ne ee 41 Pseudostylodictyon ? kayt Galloway and St. Jean .............-.--------------- 42 IPseudostylodicty om 2 GHAZLATIUTID mn (Seely) iste se 43 Pseudostylodictyon ? montoyaense Galloway, 0. SD. .....-----------------0--------- 44 Rosencla cummings: Galloway and: St) Jiean; ms Sp) 2-2 45 ECDC GUT amy PAU SL LUL O'S; Clam (Ses OTL) eee ee 47 CEG EU CMMI LE Tg O TLC TES Sia) (OES UN LUNGS) fpr ee re 50 WEUECHTGNTIACEOSHY av AG Ks Ey Roce Pate Bat ek Ue Sate ee 53 SE GONTLALOCCITIOTE AT1UG.O SRL TTN Nel alll tgs ee one ee ee ee 56 IS LIgO TID CLLOIGE/ LIU ITU TAL TTLUCL IOTTDMMNW (lll S O10 pe nent meaner aE eel ee eee 58 Stromatocerium amsterdamense Galloway and St. Jean ~............-........ 59 Stromatocerium canadense Nicholson and Murie ..............-- 60, 89 Stromatocerium leipersense Galloway and Ehlers, n. sp. -.......-...-...----- 62 SEONIVAL OCC TAL ILTIINNTINEGILUG ATLGTUS Cas iT KS pee eee 63 DSL TOTL CLOGS ULL G THM CLAUS 19, CU Cap ExT: KS jee ee eens ee see ne 64 SLGOTLALOCEIIALTIE NOT ATUULLOS E710) 4 A\VATINES)) essere sneer neers eee 66 Stromatocerium platypilae Galloway, n. sp. .......-.-----------------------eee 67 DEG IRALOSTONUCMS COU TIETIDM (G)fATILCS) peeree eee eee is ae 69 Demmatostroma 2 cornnugatun (Hoerste)) ee Wl Derg valOo St GOmeCa in Gy PLL TIL am (CELO.G TS Ce) faee eerste eae ee 72 Dermatostroma ? escanabaense Galloway and Ehlers, n. sp. —-............ 73 Dermatostroma costatum Galloway and St. Jean, n. sp. -.....-.-.-------------- 74 Dermatostroma nodoundulatum Galloway and St. Jean, n. sp. —.......... 75 Dermatostroma concentricum Galloway and Ehlers, n. sp. 76 Checklist of Ordovician genera and species of Stromatoporoidea —...... 78 Oxdovictane bibliio pirap hiya sates -o Oe ne ee eee ee Ben teen eee 82 ANGUGIGTAGUUE TAN, [OBR EE Fee a, CS ad a seek aed Se el eee Ee 87 ORDOVICIAN STROMATOPOROIDEA OF NORTH AMERICA J. J. GALLoway Indiana University, Bloomington, Indiana and (St EANMTR. University of North Carolina, Chapel Hill, North Carolina Pu RI ANC Ih Ten genera and 37 species of North American Ordovician stromatoporoids, all in the family Labechiidae, are described and figured, including 10 new species. INTRODUCTION The late Dr. W. A. Parks made an attempt in 1910 to clarify the knowledge of Ordovician stromatoporoids, in which he described or redescribed 19 species and varieties, but still it was difficult to identify any species. In the past half century, several new forms have been added and some clarifications of the structure have been made, ‘here are only about 77 species of Ordovician stromatoporoids known; 50 occur in North America, of which we have restudied, described, and figured 37 of the most important species, mostly from authentic specimens. This paper is a further attempt to clarify the structure, classification, nomenclature, and stratigraphic ranges of Ordovician forms; we have restudied specimens of every species we could obtain. As noted by Parks (1910, p. [295]), many Ordovician forms are in a “very bad state of preservation”; ad- ditional specimens, some well preserved, have served to make Ordovician stromatoporoids better but not completely known. Ordovician stromatoporoids have been known since 1843, when Dr. John T. Plummer of Richmond, Indiana, discovered and named Aulacera from the latest Ordovician, a few miles south of Richmond. The next discovery was that by James Hall, 1847, who named Stromatocerium rugosum from the Black River of western New York and from Isle La Motte, Vermont. The Ordovician forms were first included in the hydrozoan order Stromatoporoidea by Nicholson, 1886. Some 11 valid genera of Ordovician stromato- poroids have been erected and about 77 valid species have been named, and 5 generic synonyms made. Ordovician stromatoporoids are now known from North America, including Baffin Island, Quebec, 6 BULLETIN 194 Anticosti, Ontario, Manitoba, Vermont, New York, Pennsylvania, Virginia, Alabama, Indiana, Ohio, Kentucky, Missouri, Tennessee, New Mexico, Colorado, Wyoming, Nevada, and Alaska. They have been described from the Ordovician of China, Manchuria, Korea (not from Japan), Siberia, the Urals, and the Baltic area. In the regions mentioned the Ordovician stromatoporoids are isolated or occur in great layers or biostromes. In a few places, as in Vermont and New York, they made reefs or bioherms. Ordovician stromatoporoids occur in three kinds of coenostea: (1) thin flattish layers or parasitic, Dermatostroma,; (2) in hemi- spherical masses, Cystostroma, Rosenella, Pseudostylodictyon, Labechia, Pseudolabechia, Stromatoceriwm, and Labechiella; or as (3) vertically erected cylindrical or branching forms, Crypto- phragmus, Aulacera, and Sinodictyon. Most forms in life were attached to some substratum, frequently to other stromatoporoids. Vhey are found attached to broken and overturned pieces of the same species, as Labechia huronensis from Indiana, indicating that they lived in shallow water where they were beaten by the waves. They, like other stromatoporoids, are made up of layers a few milli- meters in thickness, as were the algae, corals, and bryozoans with which they occur, suggesting that the latilaminae are annual or seasonal growth layers, hence there were changes of seasons in the Ordovician. Ordovician stromatoporoids are as well preserved as are any other fossils. They have been infiltrated with calcium carbonate and generally the original structures are as well preserved as are those of corals and Bryozoa with which they occur. Weathered specimens, such as Labechia pustulosa (Safford), are leached and partly dolomitized and the minute structure has been largely destroyed, preserving only the latilaminae and the mamelons. In other cases specimens weathered out have been silicified and the structure almost entirely destroyed, as is true of Auwlacera from the late Ordovician of Manitoba. Some specimens of Aulacera from the Bernheim Forest of Kentucky, have been replaced by calcite or iron oxide inside, and the outside covered by Dermatostroma, simu- lating or preserving the surface characters of the Awlacera. ‘The oldest stromatoporoids known are those from the Middle Ordovician of Vermont and New York. We think the objects ORDOVICIAN STROMATOPOROIDEA N. AMER.: GALLOWAY & ST. JEAN 7 described by Yavorsky (Centralbl. Min., Geol. Paleo., 1932, Abt. B, p. 613) are not Cambrian in age; the first belongs to the Mesozoic genus Actinostromaria, and the second one has all the characteristics of the Devonian stromatoporoid Anostylostroma. The most primi- tive stromatoporoid known to us from the middle Chazyan from Isle La Motte, Vermont, has a skeleton composed of cysts only, which we named Cystostroma. We consider it to be the ancestor of all Silurian and Devonian stromatoporoids. Pseudostylodictyon, occurring in the same beds has regular laminae, no cysts or pillars, and might be considered to be even more primitive than Cystostroma. Ordovician stromatoporoids have skeletons composed funda- mentally of imbricating, arcuate plates or cysts, which overlap some of the underlying plates, with or without radial pillars. They all belong to the family Labechiidae. The surface is either smooth or with mamelons, and in some species there are small but typical astrorhizae. The cyst plates are composed of a thin dark, dense median layer generally with an upper thin layer of less dense or flocculent tissue and generally with a thicker lower layer of floc- culent tissue. In addition to the cysts in most of the genera, there are long round or flat pillars. The pillars are composed of loosely aggregated granular material somewhat more closely arranged on the outside of the pillars. The pillars seem to have been continuous, not super- posed; they arose from the tops of the cysts and continued through the cyst plates. The pillars seem to have been composed of less easily preserved tissue than that of the cysts and often are only partially preserved, as in the type specimen of Aulacera plummeri; at other times there are only radial vacuities to show where the pillar had been, as seen in several species from the Liberty formation of Kentucky, and in Cryptophragmus antiquatus and Labechia pustulosa. The tissue of both cysts and pillars is either compact of floc- culent; in rare cases there are pores through the cyst plates. In no case is the tissue composed of, or provided with, the round dots or maculae as seen in the family Stromatoporidae. Seven genera of stromatoporoids are confined to the Ordovician. Four, Rosenella, Labechiella, Labechia, and Pseudolabechia extend 8 BULLETIN 194 into the Devonian. Cyst plates or dissepiments are characteristic of the Ordovician forms but cyst plates occur in the skeletons of all the families of the Stromatoporoidea and in most of the genera. ‘The presence of cysts, pillars, and astrorhizae in the Labechiidae is considered as sufficient proof that the family Labechiidae belongs to the order Stromatoporoidea and do not constitute a distinct order. The Labechiidae were ancestral to the other families of Stromatoporoidea, embracing a small group of genera, and it is more convenient to refer to the Ordovician forms as a family of the Stromatoporoidea. Stromatoporoids might well be found in the Lower Ordovician; they should consist of arcuate cysts or some other modification of a sphere. Repair tissue throughout the order Stromatoporoidea is usually cystose, suggesting that cysts are primitive structures. Ordovician stromatoporoids are difficult to identify because, (1) most of the early named species were described from surface features, and most subsequent references are based on outside char- acters; (2) Ordovician species commonly are poorly preserved be- cause the structures were poorly calcified, as may be true of speci- mens of Stromatocerium, Labechia, Aulacera, and others; (3) many specimens have been dolomitized, as Labechia pustulosa from the type locality; others have been silicified during the weathering of the enclosing rock, leaving a form showing latilaminae but no other determinable structures (Parks, 1910, pl. 21, fig. 7); (4) as many as five synonyms have been made for one species (Labechia huronensts); (5) few persons who have identified species had ade- quate knowledge of stromatoporoids or their structures; (6) several of the types cannot be located. Although we have studied all the types and topotypes possible to obtain and have devoted a great deal of time to Ordovician stromatoporoids, there are still some unsolved questions such as: is Dermatostroma a stromatoporoid? What is Stromatocerium canadense? We hope we have made it possible to identify most known species of the Ordovician of North America. We have not recognized subspecies because we cannot distinguish those taxa from species. ORDOVICIAN STROMATOPOROIDEA N. AMER.: GALLOWAY & ST. JEAN 9 ACKNOWLEDGMENTS We have received for study by gift or loan many Ordovician specimens, types or topotypes. We especially acknowledge assistance from the following persons: Mrs. Ruth G. Browne, Louisville, Kentucky; Dr. Guy Campbell, Corydon, Indiana; Dr. G. Arthur Cooper, U.S. Nat. Mus.; Dr. Rousseau H. Flower, New Mexico In- stitute of Mining and Technology; Dr. Otto Haas, American Museum of Natural History; Dr. Marshall Kay, Columbia Uni- versity; Dr. T. G. Perry, Indiana University; Dr. Bruno M. Schmidt, Middlebury College; the late Dr. William H. Shideler, Miami University; Dr. W. J. Wayne, Indiana Geological Survey; Dr. Harry B. Whittington, Harvard University; Dr. D. J. McLaren and Dr. Alice E. Wilson, Geological Survey of Canada; and Dr. Charles W. Wilson, Jr., Vanderbilt University. Professor G. M. Ehlers of the University of Michigan, has sent us for study many specimens which had been collected by Dr. Carl Rominger, Pro- fessor R. C. Hussey, and him. We also owe thanks to the late Dr. Charles F. Deiss, Chair- man of the Geology Department of Indiana University, for ob- taining quarters, apparatus and secretarial assistance; to the Gradu- ate School of Indiana University, for providing a grant for the cost of the plates. Mr. George Ringer, Indiana Geological Survey, made the photographs. The retouching was done by J. J. Galloway, where necessary. SYSTEMATIC PART Phylum COELENTERATA Class HY DROZOA Owen, 1843 Order SEROMATOPOROIDEA Nicholson and Murie, 1878 Layered, calcareous, attached animal skeletons, composed of curved plates and pillars in Ordovician forms and of laminae and pillars in later forms. They occur in marine, shallow, warm water rocks of Ordovician, Silurian, and Devonian age. They have no 10 BULLETIN 194 spicules nor a cup-shaped body as do sponges, and they have no corallites as do corals. They are considered to be Hydrozoa by all living authorities. Family LABECHIIDAE Nicholson, 1879 Family Labechiidae Nicholson, 1879, “Tabulate Corals of the Palaeozoic Period,” pp. 28, 330. Coenosteum laminar, massive, conical, columnar or fasciculate, without or with axial, cystose column. Skeleton composed of small or large curved, imbricating plates, forming latilaminae but rarely continuous microlaminae. Pillars thin to thick, long, round, flat or irregular, primitive or absent. Tissue of primary plates compact, usually with inner and outer flocculent layers. Primitive astrorhizae may occur. Middle and Upper Ordovician abundant, Silurian uncommon, Devonian rare. KEY TO GENERA OF LABECHIIDAE la. Pillars absent in all parts of the coenosteum 2a. Coenosteum massive, without axial column On POUL ATS ted ae sca ence ee etc ee Cystostroma 2b. Coenosteum columnar, with axial column Of cysts, Cimmmatune)) cc..0: Cryptophragmus and Aulacera lb. Pillars represented by denticles or wrinkles on laminae 2c. Coenosteum laminar or massive 3a; Cysts and identicles: domimant:-.o-cescacch Rosenella 3b. Laminae and wrinkles dominant ......Pseudostylodictyon 2d. Coenosteum columnar; lateral sheaths like TROPIC Gere Bu Nik on het te eae eee ae MR Sinodictyon le. Pillars continuous through several layers of cysts 2e. Pillars round in tangential section 3c. Coenosteum columnar; pillars in mature stage 4a. Lateral cysts strongly curved; pillars ‘small (3 Sone eee eee Aulacera 4b. Lateral cysts slightly curved; pillars large} sic. Ment Paice eee Cryptophragmus ORDOVICIAN STROMATOPOROIDEA N. AMER.: GALLOWAY & ST. JEAN 11 3d. Coenosteum massive 4c. Pillars not in groups Hann ystspancheds imbriCating|ij..2cchwtee Labechia 5b. Cysts edge to edge, simulating eames erates teers cece esr Labechiella 4d. Pillars in diverging groups ........000 Pseudolabechia 3e. Coenosteum a thin encrustation ........... Dermatostroma 2f. Pillars broad, many flanged in tangential section; cysts wide, low, simulating laminae ........... Stromatocerium Genus CYSTOSTROMA Galloway and St. Jean, 1957 Type species (originally designated), Cystostroma vermontense Galloway and St. Jean, in Galloway, 1957, Bull. Amer. Paleont., vol. 37, No. 164, p. 421. (Middle Ordovician, middle Chazy, one mile southeast of Isle La Motte village, Vermont.) Coenosteum massive, without cystose column, composed of imbricating, curved plates, forming latilaminae a few millimeters thick. Tissue of compact primary plates usually with inner and outer flocculent layers. The lower plate may be composed of clusters of flocculent tissue, and between the clusters there may be pores which pass through all three plates. Pillars absent. Surface smooth or with small or large mamelons, and primitive astrorhizae. Middle and Upper Ordovician: C. vermontense, middle Chazyan, Isle La Motte, Vt.; C. stmplex, Carters |s., Tenn.; C. minimum, Bigby |s.. Ky. and Black River or Trenton, Escanaba River, Mich.; C. fritzae, Richmondian, Haileybury, Ont. This genus embraces the simplest, oldest, and most primitive stromatoporoids known, with skeleton composed only of arcuate cysts. It lacks the axial column of Awlacera, and lacks the pillars of Labechia and of the mature stage of Awlacera. It lacks the denticles of Rosenella and has smaller, more regularly imbricating cysts. [he mamelons of C. minimum (Parks), and the large knobs of C. fritzae, n. sp., are not generic but only specific characters. KEY TO SPECIES OF CYSTOSTROMA la. Surface smooth, without mamelons 12 BULLETIN 194 2a. Cyst plates large, variable; without villi Petes C. vermontense Galloway and St. Jean 2b. Cyst plates small, uniform; villi abundant ees C. simplex Galloway and St. Jean lb. Surface with mamelons 2c. Mamelons small, 5-6 mm. diameter .....C. minimum ( Parks) 2d. Mamelons large, 30-40 mm. in diameter .....C. fritzae, n. sp. Cystostroma yermontense Galloway and St. Jean Pl eS ties slaps Cystostroma vermontense Galloway and St. Jean, 1957, in Galloway, Bull. Amer. Paleont., vol. 37, No. 164, p. 421, pl. 31, fig. 1; pl. 32, fig. 1; pl. 36, fig. 3 (M. Ord., Vt.) Coenosteum.—Coenosteum massive; a fragmental specimen is 55 mm. high, 90 mm. wide, and 175 mm. long. Latilaminae conspicuous, smoothly curved, 2 to 6 mm. thick. Surface without mamelons, astrorhizae or papillae. Irregularly shaped cyst plates are 0.7 to 3 mm. in the longest dimension, and average 1 to 2 mm. in diameter. Vertical section—The latilaminae are prominently marked by thin layers of black, calcareous mud, obviously not a specific char- acter but due to seasonal deposition. The low-arched cyst plates are variable in size, 0.3 to 3 mm. broad, and 0.2 to 0.7 mm. high, 1% to 6 cyst plates in 4 mm. horizontally, and an average of 5 cyst plates in 2 mm. vertically. No pillars occur in seven sections. ‘The cyst plates are composed of three layers, a median, thin, dense layer, an outer, indefinite, flocculent layer, and a lower, thick, floc- culent layer which occupies much of the chamber space and joins with the outer layer of the plates below. In places the flocculent plates have clear vertical areas resembling pores. (Nicholson, 1886, Diey tig. 5-) Tangential section.— The cysts join to form round or polygonal patterns. [he wall tissue is cut obliquely and appears thicker than in vertical section. [here are no pillars nor astrorhizae. Comparisons.—Cystostroma vermontense is characterized by the large size and variability in the size and shape of the cyst plates, ORDOVICIAN STROMATOPOROIDEA N. AMER.: GALLOWAY & ST. JEAN 13 by the thick lower plate, and by the lack of mamelons. It has larger and more variable cysts than C. simplex and lacks the small villi on the outer layer of the cyst plates. In some specimens at the base of a Jatilamina there is a spher- ical chamber, about 4 mm. in diameter, attached to the substratum directly or by a spool-shaped neck. From the chamber, curving downward are two or three pairs of arcuate cysts, in structure like ordinary cysts, which may extend laterally into normal cysts of Cystostroma, and an alga covers the structure. The spherical cham- ber with its pairs of cysts may be the beginning of the coenosteum, which we named the protocoenosteum (1957, p. 45, pl. 36, fig. 3). Such spherical chambers are not found in the bodies of any coenostea. No other organism except the alga occurs with the described struc- ture. In one slide (300-72) there are three similar structures (PI. 1, ne 2.) Occurrence —Middle Ordovician, middle Chazyan, one mile southeast of Isle La Motte village, Vermont, collected by Dr. Mar- shall Kay, of Columbia University—the oldest known stromato- poroid occurrence in North America. Holotype——Indiana University, Paleo. Coll. No. KA2; slides Nos. 300-15, 16, 17, 18, 25, 26, 27. Cystostroma simplex Galloway and St. Jean Pl. 1, figs. 3a, b Cystostroma simplex Galloway and St. Jean, 1957, in Galloway, Bull. Amer. Paleont., vol. 37, No. 164, p. 421, pl. 32, fig. 2. (M. Ord., Tenn.) Coenostewm.—Coenosteum massive, oval, 160 x 100 mm. in diameter and 80 mm. thick, composed of lJatilaminae 5 to 10 mm. thick, Surface smooth, without mamelons or astrorhizae. Vertical section—The skeleton is composed of arcuate cysts which are from 1 to 2 mm. broad and half as high, and regular within those limits; they tend to be flat on top with nearly vertical ends. Ihe cystose plates are smaller at the junction of latilaminae. Each cyst overlaps about % of each subjacent cyst. Pillars absent. Cyst plates are tripartite, consist of a thin, dense, dark, median layer, 0.05 mm. thick, and thicker inner and outer layers; inner layer 0.15 mm. thick, composed of a thin light-colored upper com- pact layer and a thicker, gray, flocculent lower layer; outer layer 14 BULLETIN 194 0.10 mm. thick, flocculent, from which extend upward, gray floc- culent villi, about one-half as high as the cysts. The triple walls and the villi appear to be organic structures, for they differ from the chamber filling of clear, crystalline calcite. It is remarkable that a similar kind of wall structure occurs in the coral Paleoalveolites paquettensis Okulitch, including even the villi, indicating that early corals and the Labechiidae are related and in the same phylum. Tangential section—The cysts are cut into round or oblong figures. The walls are cut obliquely, are thicker than in longitudinal section, but the composition is the same. The villi appear as roundish, flocculent dots, abundant in some places, but not qualifying as pillars, because they are not developed from, nor do they cut the primary plates, as real pillars do in the Labechiidae. his species is characterized by its simple structure, without pillars, mamelons or astrorhizae, the limited variability of the cysts, the tendency for the ends of the cysts to be vertical and the tops flat, the amount of overlap of the cyst plates, and the abundant villi. Occurrence —Common in the Middle Ordovician, basal Trenton, Carters limestone, at Mill Creek, seven miles south of Nashville, Tenn., collected by Prof. C. W. Wilson, Jr., of Vanderbilt University. Holotype—Part in the Vanderbilt University collection, and part in the Indiana University Paleo. Coll., slides 299-60, 61, 62. Cystostroma minimum (Parks) Pied tis an Stromatocerium canadense var. minimum Parks, 1910, Univ. Toronto Studies, Geol. Ser. No. 7, p. 20, pl. 22, fig. 3. (M. Ord., Trenton, Bigby ls., Frank- fort, Ky.) Coenostewm.—Coenosteum massive to discoidal, at least 20 cm. in diameter and 5 cm. thick, The specimens from Escanaba River, Michigan, are massive cones, up to 27 cm. high and up to 18 cm. in diameter near the base. Surface has hemispherical mame- lons, 2 mm. high, 3 mm. in diameter and 6 to 10 mm. apart, regular in size, shape, and distribution. Small astrorhizae, 2 to 3 mm. in diameter, occupy the summits of most of the mamelons; the astrorhizae have three to five radiating canals, and some of the canals branch sparingly. ORDOVICIAN STROMATOPOROIDEA N, AMER.: GALLOWAY & ST. JEAN 15 Vertical section—The coenosteum is composed of latilaminae, 10 to 15 mm. thick, in both Kentucky and Michigan specimens, and the mamelons are not ordinarily superposed from one latilamina to the next above; each latilamina is taken to be a year’s growth, with cessation of growth in the cold seasons. The skeleton is com- posed entirely of low, arcuate cysts, which are from 0.5 to 3 mm. broad, averaging less than 1 mm., and averaging about 7% mm. high; the cysts overlap from % to % of the two subjacent cysts, and the layers of cysts rise sharply over each mamelon. Narrow astro- thizal tubes occur in some mamelons, rarely between mamelons; some are perpendicular but most astrorhizal tubes make small angles with the vertical; they have no proper walls. The walls of the cysts consist of a dark, dense upper layer, 0.03 mm. thick, usually with- out an overlying flocculent layer, but with a lighter colored lower layer, 0.12 mm. thick, filling over half of the cyst vesicle. The lower plate is composed, in some specimens, of oval, gray clusters, with darker, flocculent centers, giving a vague moniliform appearance. The oval clusters are separated by thin, dark partitions extending into the thin, upper layer; in places there are pores between the clusters which pass through the upper plate. The chambers are filled with clear calcite. Pillars absent; foramina between cysts might be interpreted as remnants of pillars, but there is no pillar substance. Tangential section—The cysts curve in layers around the mamelons, in which there is usually a small astrorhiza with short canals. There are no indications of pillars. Compartsons.—Cystostroma minimum is characterized by the massive form, with regular mamelons which do not make long mamelon columns, the small astrorhizae, and the usually bipartite walls of the cysts, with the lower, moniliform layer, and lack of pillars. It is indistinguishable from Labechia pustulosa (Safford), with which it occurs, excepting for the absence of pillars, but pillars are missing in parts of L. pustulosa. Labechia huronensis, from the Cincinnatian series, has smaller cysts, and round pillars. Occurrence ——Common in the Bigby limestone of Trenton age, Frankfort, Kentucky; the type specimen, figured by Parks, is num- bered 36930 in the U.S. Nat. Museum. A specimen from the U.S. 16 BULLETIN 194 Nat. Museum is labeled “Holotype, Stromatoceriwm canadense minimum Parks. Trenton (Flanagan), Frankfort, Kentucky.” It has abundant round pillars and is indistinguishable from Labechia pustulosa (Safford). It has no museum number. The pillars are so large and conspicuous that Parks could scarcely have missed seeing them, whereas his figure (1910, pl. 22, fig. 3) shows thin plates in the cysts and no pillars. We, therefore, hesitate to accept the un- numbered U.S. Nat. Mus, specimen as the type of subspecies, even if it is from the type locality. Bassler (1915, p. 1213) recognized the Museum’s specimen as Stromatocerium pustulosum (Safford) and referred to No. 36930 as a plesiotype of S. pustuloswm. In many large areas in the section, pillars are missing and cyst plates are thin, as shown in Parks’ figure. We have part of a good topotype from the top of the Bigby limestone, at the Old Crow Distillery, Frank- fort, Kentucky, collected by Dr. W. H. Bucher; Cat. No. 4087, Geo- logical Museum of the University of Cincinnati. It also occurs in large masses in the Trenton on Escanaba River, three miles south of Bony Falls, Michigan; collected by R. C. Hussey; Univ. of Michigan, Cat. No. 39455, 39489, 39490, 39491. Hypotype—lIndiana University Paleo. Coll., slides 299-68, 69; 302-32; 308-88. Cystostroma fritzae Galloway and St. Jean, n. sp. Coenosteum.—Coenosteum large, irregularly hemispherical, 60 cm. in diameter and 25 cm. high, composed of latilaminae 2 to 5 mm. thick. The surface is in general smooth but has groups of large, subconical knobs, 3 or 4 cm. in diameter and height. Astror- hizae apparently absent. In many places the latilaminae are separ- ated by 1 to 3 mm. of lime mud, apparently laid down in the winter season; in other places there is no median arcuate layer in the winter parts of the latilaminae, Vertical section—The skeleton is composed of low, arcuate cysts, from 0.3 to 0.8 mm. broad, averaging about % mm., over- lapping about 4% to % of each subjacent cyst at each end. The chambers are 0.2 to 0.3 mm. high. The cyst plates are tripartite, with a thin, compact, median layer, 0.026 mm. thick, a thin, floc- culent upper plate, and a thick, flocculent, lower plate, which us- ORDOVICIAN STROMATOPOROIDEA N. AMER.: GALLOWAY & ST. JEAN 7) ually fills the chamber cavity, but is not moniliform. Where the coenosteum is well preserved, the thick, lower layers of the cyst plates show clear, radial spaces, possibly pores (Nicholson, Mono., p. 89, pl. 8, fig. 5) which are common in the Labechiidae and which in places appear to pierce the dark, median layer of the cyst plates and extend through the upper plate. Pillars and astrorhizae are absent. Tangential section—TVhe cut cysts appear as small circles and irregular curves. The median layer of the cyst walls appears as small circles and irregular curves with dark spots of variable size, but thicker than in vertical section. In places there seems to be pores in the median layer. This species is characterized by large, conical knobs, and by low-arched, closely spaced cyst plates, and lack of pillars. Occurrence —Upper Ordovician, Richmondian, Liskeard forma- tion, Farr Quarry, Haileybury, Lake Timiskaming, Ontario. The specimen was collected by Prof. Madeleine A. Fritz, of the Uni- versity of Toronto, for whom we are pleased to name it. T'ype.—Holotype in the Royal Ontario Museum of Zoology and Paleontology, and five slides, a fragment in the Indiana Uni- versity Paleo. Coll. and slides 301-88, 89, 90, 91, 92; 302-76, 77. Genus CRYPTOPHRAGMUS Raymond, 1914 Type species (originally designated), C. antiquatus Raymond, 1914, Canada Dept. Mines, Geol. Surv. Mus., Bull. No. 5, p. 8, pls. 1-4, holotype, pl. 1, fig. 1. (M. Ord., Pamelia ls., Aylmer, Quebec); Bassler 1932, Tennessee Div. Geol., Bull. 38, p. 102, 214; pl. 16, fig. 9; 1935, Jour. Washington Acad. Sci., vol. 25, No. 9, p. 404; Shrock and Raasch, 1937, Amer. Midland Natur., vol. 18, p. 536, pl. 2, figs. 1-3; Shimer and Shrock, 1944, Index Fossils of North America, p. 63, pl. 19, figs. 6-8; Wilson, 1948, Canada Geol. Surv., Bull. 11, p. 46, pl. 22, figs. 3-5; Yavorsky, 1955, Trudy Vsesoyuznogo Nauchno-issledovatelskogo Geol. Inst., Minister. Geol. i Okhrany Nedr, nov. ser., vol. 8, p. 68, pls. 31, 32, 34 (doubtful) ; Galloway, 1957, Bull. Amer. Paleont., vol. 37, No. 164, p. 426, pl. 32, fig. 8. Thamnobeatricea Raymond, 1931, Bull. Mus. Comp. Zool. Harvard, Geol. Ser., vol. 9, No. 6, p. 180, pl. 2, figs. 4-6 (M. Ord., Bellefonte, Pa.) Cladophragmus Raymond, 1931, ibid., p. 182, pl. 3, figs. 1-4. (M. Ord. Ottawa, Ont.) Rosenellina Radugin, 1936, Records of the Geology of the West Siberian Regions, No.9355p..92, figs. 8,9) 11: 18 BULLETIN 194 Coenosteum upright, cylindrical or rarely branching, 2 to 20 mm. in diameter and up to 46 cm. long, consisting of a tube, with thin, cystose wall about 1 mm. thick; the tube is crossed by large, superposed, highly arched tabulae or cysts. The cysts are composed of a primary, median, compact layer, and thin inner and outer flocculent layers. Both inner and outer flocculent layers have irreg- ular villi. The outer sheaths of cysts and large pillars when present are the adult stage of the Cryptophragmus. Middle Ordovician, six species, Upper Ordovician doubtful. The sheaths are rarely continuous with the axial tube or at- tached directly to it but are attached to mud or calcite between it and the axis. They seem to have been little calcified and ordinarily incapable of preservation, similar to the pillars of Labechia pustulosa and of L. huronensis. The sheath organism has the structure of Labechia, composed of curved plates and large, long pillars. It must have grown downward from the top of the column, after a cold sea- son in which mud was deposited, making latilaminae. This genus differs from Aulacera in the larger pillars, and in not ordinarily developing the lateral layers, whereas Awlacera nearly always has the lateral layers of cysts and pillars. The pillars of Cryptophragmus are much larger and less well preserved than in Auwlacera, and the lateral cyst plates are less curved and less well preserved than in Aulacera. Raymond mistook the pillars for tubes although he noted the papillae (1914, pl. 4, fig. 2) or “elevations are at the apertures of the tubes.” KEY TO SPECIES OF CRYPTOPHRAGMUS la. Not branching 2a. Axial cysts irregular ... C. antiquatus Raymond Db: Axial eystsereerl ato. andecctaenececa nabs C. gracilis (Ulrich) 2c. Axialcysts 1mknowiiees.cet eee C. ? rochensis Wilson Ib. Branching 2d. With cysts outside the tube ........... C. parallelus (Raymond) 2e. Without cysts outside the tube 3a. Stems 10 mm. in diameter .......... C. arbusculus Bassler 3b. Stems 5-7 mm. in diameter C. bifurcatus (Raymond) ORDOVICIAN STROMATOPOROIDEA N. AMER.: GALLOWAY & ST. JEAN 19 Crytophragmus antiquatus Raymond Pl. 2, figs. 2a, b, c, 3a, b, ¢ Cryptophragmus antiquatus Raymond, 1914, Canada Dept. Mines, Geol. Surv. Mus., Bull. No. 5, p. 1-10, pls. 1-4. (M. Ord., Pamelia ls., Aylmer, Que. and Carden twp., Ont.) ; Butts, 1926, Geol. Surv. Alabama, Spec. Rep. 14, p. 128, pl. 32, figs. 4-7; Raymond, 1931, Bull. Mus. Comp. Zool., Harvard, Geol. Surv., vol. 9, No. 6, p. 182, pl. 3, fig. 8; Shrock and Raasch, 1937, Amer. Mid. Natur., vol. 18, p. 536; Wilson, 1948, Canada Dept. Mines, Geol. Surv., Bull. 11, p. 46, pl. 22, figs. 3-5; Shimer and Shrock, Index Fossils of North America, 1944, p. 63, pl. 19, figs. 6-8. Exterior—Coenosteum upright, cylindrical, unbranched, up to 20 cm. long and 25 mm. in diameter, consisting, in immature stages, of an axial column 5 to 12 mm. in diameter, of large superposed, hemispherical cysts, which arch upward (Butts, 1926, pl. 32, figs. 4-7, shows the axial cysts arched downward) and a thin layer of small cysts composing the lateral walls of the tubular axis. The adult has sheaths or latilaminae, 2 to 5 mm. thick. There are no mamelons nor astrorhizae. Vertical section —The axial cyst plates consist of a thick, com- pact median plate, with thick flocculent upper and lower layers. In places the median plate of the large axial cysts is sharply bent upward into small hollow cones. The lateral cysts of the tube, when present, are 0.2 to over 1 mm. broad and arcuate rather than hemi- spherical. Outside of the zone of small cysts there may be a zone of disturbed cysts and pillars of the sheaths, more often a zone of clear calcite up to 2 mm. thick. In some cases there is a zone of mud 1 or 2 mm. thick. In one case the axial column is followed by a zone of calcite of varying thickness, and this by a well-preserved bryozoan, Monticulipora. At the type locality near Ottawa, Canada, and in Loysburg and in Lee County, Virginia, the axial column or tube is covered by two to four layers of sheaths or latilaminae of different structure than the axial column, and only rarely connected to or erading from it. ‘The sheaths generally he on calcite or a layer of mud deposited in the non-growing season, The sheaths are composed of broad, arched cyst plates, perpendicular to the axial column, and large, long radial pillars; the pillars are oval to prismatic and tend to be round. The cyst plates have been largely destroyed or have not been preserved because of insufficient calcification in life. The pillars have been 20 BULLETIN 194 entirely destroyed or recrystallized, causing Raymond (pp. 4, 9) to mistake the pillars for “radial canals.” The outer sheaths are like Labechia in the curved plates and large pillars. In several sections, and in Raymond’s plate 4, figure 2, the pillars extend into the surrounding mudrock as papillae, showing that the radial structures are pillars rather than tubes, as Raymond thought. Tangential section—The pillars are large, closely spaced, four to six-sided or oval, tending to be round, 0.2 to 0.3 mm. in diameter, and the same distance apart. Cyst plates are rarely observable; they are indicated by a dark, granular network enclosing the spaces where the pillars had been. Numerous reported specimens of C. antiquatus do not have the outer sheaths, so that the sheaths are not necessary for the indentification of the species. The sheath zones may have been composed of soft material, with little calcareous structures, so that they were preserved only under favorable condi- tions. Cross section ——The axial tube is 5 to 12 mm. in diameter, with sections of the axial tabulae. The wall of the axial tube consists of small, outwardly convex plates, The tube is followed by either clear . calcite or mudrock, and these by a zone of curved, imbricating plates and large pillars. The layer of calcite or mud and radial zone may be repeated two or three times, making latilaminae. It is likely that the sheaths grew down from the growing upper end of the column. In the clear calcite zone there may be remnants of the curved plates and pillars. Occurrence.—C. antiquatus has been reported from the Pamelia and Lowville limestones of the Black River group of Quebec, Ontario, New York, Pennsylvania, Virginia, Alabama, Kentucky, Tennessee, Missouri, and Indiana. We are indebted to Dr. Alice E. Wilson, of the Geological Survey of Canada, for loaning us a piece of one of Raymond’s paratypes from Carden twp., Ontario, from which we have made sections for study (PI. 2, fig. 3c), and to Dr. H. B. Whit- tington, of Harvard University, for loaning us five of Raymond’s slides, two fragments of Raymond’s material from Carden twp., Ontario, from which we made three slides, and a complete specimen of Raymond’s Carden twp. material from which we made seven slides. Some of the Carden twp. specimens have no sheaths. We ORDOVICIAN STROMATOPOROIDEA N. AMER.: GALLOWAY & ST. JEAN 21 have specimens from the Lebanon limestone of Tennessee, and from the Middle Ordovician of Kentland, Indiana, which have no sheath zones, which is true of most reported occurrences excepting those from near Ottawa, Canada, and Lee Co. and Loysburg, Virginia. Genus AULACERA Plummer, 1843 Type species (only species described), Aulacera plummerit Galloway and St. Jean. No species of Aulacera was named by Plummer, but the species was described and figured and is recognizable, hence is the type species under the Rules of Zoolog. Nomen., Opinion 46: “if only one species is involved, the generic description is equivalent to the publication of ‘X-us albus, n. g., n. sp.”” (U. Ord., late Richmondian, near Richmond, Ind.) Aulacera Plummer, 1843, Amer. Jour. Sci., vol. 44, p. 293, fig. 8. The name is valid, under Rules of Nomenclature, Art. 2, and Opinion 46; a species is available as type species when it can be recognized from the original generic publication; Schuchert, 1919, Amer. Jour. Sci., 4th ser., vol. 47, p. 293, fig. 1; Kuhn, 1928, Foss. Cat.. Hydrozoa, p. 38; Ozaki, 1938, Jour. Shanghai Sci. Inst., sec. 2, vol. 2, p. 217; Kuhn, 1939, in Schindewolf, Hand- buch Palaozoologie, Bd. 2A, p. A53; Galloway, 1957, Bull. Amer. Paleont., VOM NOs L64 p42" pleases hic 2 eple SQ ehlea se plushies. diac Beatricea Billings, 1857, Geol. Surv. Canada, Rep. Prog. for 1853-6, p. 343. (Type species, B. nodulosa Billings, selected by Miller, 1889, N. A. Geol. Paleo., p. 155.) (U. Ord., Anticosti Island); 1865, Canadian Nat., 2d. ser., vol. 2, p. 405, figs. 1, 2; Nicholson, 1886, Palaeont. Soc., vol. 39, p. 86, pl. 8, figs. 1-8; Foerste, 1909, Bull. Sci. Lab. Denison Univ., vol. 14, p. 298; Parks, 1910, Univ. Toronto Studies, Geol. Ser., No. 7, p. 37, pl. 25; Yavorsky, 1955, Trudy Vsesoyuznogo Nauchno-issledovatelskogo Geol. Inst., Minister. Geol. i Okhrany Nedr, nov. ser., vol. 8, p. 69-80, pls. 32-42. Coenosteum subcylindrical, with axial column usually made of large, hemispherical, upwardly curved cysts, simulating a tabulate tube; in some specimens the large cysts grade into the small, lateral cysts, showing that all are parts of the same organism. Lateral skeleton latilaminate, composed of small, imbricating, cyst plates. The cyst plates consist of a thin, dense, median layer, about 0.03 mm. thick, a thin flocculent outer layer, and a thick flocculent inner layer, Pillars present or absent in the inner part of the lateral zones, and with long, narrow, round pillars sporadically developed in the outer zone; pillars loose in texture, with outer more compact zone, but not hollow, Surface even or with mamelons or longitudinal ridges. Astrorhizae absent. BULLETIN 194 rh is) Upper Ordovician, abundant in and apparently confined to the Richmondian group. North America, Russia, and China. Seven- teen species. The axial zone of cysts grading into the lateral zone cannot be a generic character, for several of the species have both tubular and gradational axes; both phases occur in the same specimen. Awlacera differs from Cystostroma in the columnar form and in having pillars in the outer zone of adult specimens. It differs from Cryptophragmus in having the outer zone of imbricating cysts and small pillars. Sinodictyon is columnar with a cystose axis, sporadic lateral pillars, and there are strong denticles on axial and lateral cysts. The genus Aulacera was named and described by Dr. John T. Plummer in 1843. It was the second stromatoporoid named, the first one named from North America, and moreover, was the first fossil named from Indiana. The etymology of the word Aulacera was not given by Plummer, and we can only surmise what he had in mind. The gender of the word is important in that the endings of the names of species of the genus are affected. Probably the first two syllables were derived from the Greek aulos, a pipe. Because Plummer included the genus _ under the univalves, there is a possibility that he had an orthoceroid cephalopod in mind; if so, the second part of the word should have been ceras. If he meant the Latin term aula, which in poetic usage means the cell of a queen bee, the Latin term cera, meaning wax, would be logical, referring to the crude honeycomb appearance of the specimen on a broken edge, produced by imbricating cyst plates. Plummer may have used the term cera in reference to the tapering candle-like shape of the fossil. Words ending in ceras are neuter; adjectival, specific names are, therefore, neuter. The word ending cera would indicate feminine gender and the word Auwlacera has been considered to be feminine by Kiihn (1928, p. 38), Shimer and Shrock (1944, p. 63) and most recent authors. In conformity with our principle not to make changes unless we are sure that corrections need to be made, we are also considering the name Aulacera to be feminine, and the specific names are feminine, excepting plwm- meri, a patronym. The same genus was named Beatricea by Billings in 1857 (p. 343), which name was used for the genus until the name Aulacera ORDOVICIAN STROMATOPOROIDEA N. AMER.: GALLOWAY & ST. JEAN 23 was resurrected by Schuchert in 1919 (p. 293), since then the genus has gone under both names. The recent text, Invertebrate Fossils by Moore, Lalicker and Fisher, preferred Beatricea, and Shimer and Shrock’s Index Fossils of North America, 1944, used both Beatricea and Aulacera, as do Shrock and Twenhofel in Principles of Inver- tebrate Paleontology, 1953. The generic name, Aulacera, is the valid name of the organism, for Plummer used Linnaean nomenclature. Although no species was named, the description and figure given by Plummer are entirely sufficient for recognition of the species. We have several topotypes from Plummer’s original locality near Richmond, Indiana, one was described and figured by Galloway and St. Jean (Galloway, 1957, p. 423, pls. 31, 32, 37) who named it Auwlacera plummert, in honor of the discoverer of the genus. The generic name is valid according to the International Rules of Zoological Nomenclature, Opinion 46; a species is available as type species if it can be recognized from the original generic publication. Because only one species is involved, “the generic description is equivalent to the publication of ‘X-us albus, n. g.,n. sp.’”’ We, therefore, consider that Aulacera plummeni, is the type of the genus Awlacera, for that species is different from Beatricea undulata Billings which becomes Aulacera undulata ( Billings ). The type species of Beatricea is B. nodulosa, which was the first species described by Billings, and B. nodulosa was selected as the type species by Miller (1889, p. 155). B. nodulosa cannot be the type species of Auwlacera because it is different from Plummer’s species, and it has never been reported from the Midwest. Beatricea undulata cannot be the type species of Auwlacera as indicated by Shimer and Shrock (1944, p. 63), for we find upon studying a type specimen of B. undulata that not only are the ridges more sharp in B. undulata, but internally, the cysts of B. wndulata are twice as large as the cysts of A. plummeri, and the cysts are more highly convex and are arranged radially to the axis; whereas in A. plum- meri, the cysts are low-arched and are arranged concentrically about the axis. The genus Auwlacera has a subcylindrical coenosteum, which 1s considered to have stood upright when it was alive, although nearly all specimens are found broken from their bases and lying in frag- 24 BULLETIN 194 ments. It is regrettable that the base has never been scientifically described; and although we have studied over a hundred specimens, not one shows the base. The base of Au/acera should have precisely the structure of Cystostroma. The center of the column is occupied generally by an axis of large, hemispherical cysts, which were con- vex upward, and in their superposition, formed a structure similar to a tabulate tube. In some specimens, the axial zone consists of large cysts which grade out into the lateral cysts. The lateral zone consists of small outwardly convex cysts, and in large specimens, there are scattered round, long, thin pillars in the outer zone. The cystose structure, with pillars, is similar to that of all Ordovician genera of stromatoporoids which belong in the family Labechuidae. Most specimens are found with their long axis parallel to the bedding; none has been reported attached to a base, but the speci- mens must have stood upright in life, for all sides are alike. All authorities consider that they lived upright. Yavorsky (1957, p. 71) discussed the position in life, citing the observations of Hyatt (1865), Raymond (1914) and Schuchert (1919), some of whom saw speci- mens in an upright position but without bases. Yavorsky (1957, pl. 36) figured a specimen of A. conica with a flaring foot which he surmised was the broken attachment. The latilaminae are from 2 to 4 mm. thick, suggesting an age of three to five years for the small specimens | to 3 cm. in diameter, to 10 years or more for larger specimens 5 to 10 cm. in diameter. The specimens must have been broken from their bases by storms and killed and moved to their present locations, for none shows evidence of growth at the places where they are found. Bases should have the characters of Cystostroma, but that genus shows no evidence of having been a base of an erect form, nor do Cystostroma and Aulacera occur in the same part of the Ordovician. The genus Aulacera is similar in the structure, particularly in the lateral zone, to a simple and primitive genus occurring in the Middle Ordovician, whose skeleton is composed entirely of arcuate cysts, Cystostroma Galloway and St. Jean, described above. Aulacera also seems to be identical in the tubular axis with the older genus, Cryptophragmus, of the Black River group, which may consist of only a tubular form with large upwardly convex cysts and a few smaller lateral cysts. In other examples there are sheaths ORDOVICIAN STROMATOPOROIDEA N, AMER.: GALLOWAY & ST. JEAN 25 around the cystose axis which resemble the genus Labechia. In the case of Aulacera, we consider it established that the lateral zones are part of the organism. We consider that Aulacera was derived from the older and simpler genus, Cryptophragmus, by the addition of a thick zone of cysts to the axial column and greater calcification of the outer zone, Cystostroma is considered to be the ancestor of Cryptophrag- mus. All of the genera of the family Labechiidae, excepting Dermato- stroma, have skeletons composed of arcuate cysts of various sizes and shapes. A closely related genus is Labechia, which has strong, round pillars and the coenosteum is hemispherical to subconical. The form of the coenosteum is a family character in the Idio- stromatidae and a generic character in the genera Clavidictyon, Cryptophragmus, Sinodictyon, and Aulacera. Surface characters, such as ridges and mamelons, are found by experience to be rather constant characters and are considered by authors to be of specific value. here are gradations between the smooth A. cylindrica and A. plummeri with low ridges. There are, also, gradations in size of mamelons on the same specimen and between different specimens. Specimens occurring in any one locality have characters which are rather constant. For instance, no specimen of A. nodulosa, with large nodes, has been reported from the Midwest, although there are rare examples of A. nodulifera and A. intermedia. The genus Aulacera is confined to the Richmond group; the oldest and simplest specimens occur in the lower Liberty formation of Kentucky, most of the specimens are small examples of A. plum- ment and A. cylindrica, with rare examples of A. nodulifera and A. intermedia. The most favorable collecting locality is on Wilson Creek, two miles southwest of Deatsville, Kentucky. In east-central Indiana, south of Richmond, Aulacera occurs commonly in the Saluda and Elkhorn formations but not in the Liberty. The speci- mens in the region of Richmond, Indiana, mostly are of moderate size, with prominent, low, longitudinal ridges. Some specimens, such as the one figured by Plummer are four or five inches in diameter, and up to three feet long. Foerste (1919, p. 298) also reported A. cylindrica south of Richmond, and an intermediate form, partly ridged and partly smooth, in the Liberty formation, north of Canaan, 26 BULLETIN 194 Indiana. Specimens of Aulacera occur abundantly and are of largest size in the uppermost Richmond of Anticosti Island, where they may attain a diameter of 14 inches and a length of 15 feet. The genus has also been reported from Ohio, Lake St. John, Quebec, Rabbit and Club Islands, Lake Huron, Ontario, Manitoba, Akpatok Island in Ungava Bay, and Novaya Zemlya. Ozaki also found an Aulacera, apparently a typical specimen but smooth, in the Upper Ordovician of Shangtung. Yavorsky found ten species from the Ordovician of Russia, including three species first found in North America. The Russian specimens all seem to have small, arcuate cyst plates, as those in A. plummeri and pillars are rare and obscure, as is true of Indiana and Kentucky specimens. A. wndulata has large, hemispherical cysts, and A. radiata has smaller and lower cysts than those of the A. plummeri group of species. KEY TO SPECIES OF AULACERA la. Surface with vertical or spiral ridges 2a. Ridges not making radii internally; cysts small, 0.5-1 mm. broad, not superposed A. plummeri Galloway and St. Jean 2b. Ridges making radii of superposed cysts 3a. Cysts large, 1-2 mm. broad, highly arched to SEMPCIRCU aT .saat eee te eee A. undulata (Billings) 3b. Cysts small, 0.5-1 mm. broad, low arc 4a. Radi narrow, prominent ...e A. radiata, n. sp. 4b. Radi wide, vague A undulatadirecta ( Yavorsky ) lb. Surface nodulose 2c. Nodules round or oval, in vertical or spiral lines 3c. Nodules large, at least 5 mm. diameter, ASS TVINMs WTO. ees, ees mee A. nodulosa (Billings ) 3d. Nodules small, 2-3 mm. diameter, 2-3 mm. Wiggs de et Pornstar seems A. nodulifera ( Foerste) 2d. Nodules elongate in vertical lines A. intermedia ( Foerste ) ORDOVICIAN STROMATOPOROIDEA N. AMER.: GALLOWAY & ST. JEAN 27 lc. Surface smooth, cysts small 2e. Not overgrown by Labechiella-like organism 3e. Pillars rare; cysts 2-3 times as broad as high 4c. Coenosteum cylindrical .....A. cylindrica (Foerste ) A. sibirica ( Yavorsky ) 4d. Coenosteum conical .......... A. conica (Yavorsky) A. vulgaris (Yavorsky ) 3f. Pillars common; cysts 3-8 times as broad as ni guage se ter conte etc Beceem A. peichuangensis Ozaki 2f. Overgrown by Labechiella-like organism; inside like VAC SEQIUNG T1 Gl eserves A. tenuipunctata (Yavorsky) A. bacula (Yavorsky ) hdSe SERUGEUTES mini chetiNIe <2Ae ca. te tt caccac: A. telposensis (Riabinin) Aulacera plummeri Galloway and St. Jean Pies hiss. laybiesZas bs IP, WA, ese al, Ay 33 Aulacera Plummer, 1843, Amer. Jour. Sci., vol. 44, p. 293, fig. 8. (U. Ord., u. Richmond, Richmond, Ind.) ; Schuchert, 1919, Amer. Jour. Sci., 4th ser., vol. 47, p. 293, fig. 1; Galloway, 1957, Bull. Amer. Paleont., vol. 37, No. 164, p. 422. Aulacera plummeri Galloway and St. Jean, in Galloway, ibid., p. 423, pl. 31, fies 2 ple S25 fies. 3); pl.-37, figs, lla-c. (U. Ord. Saluda fms, S5 of Rich= mond, Ind.) Beatricea undulata Billings, 1865, (not Billings, 1857), Canadian Nat. and Geol., Ser. 2, vol. 2, p. 406, figs. 1, 2. (U. Ord., Rabbit Island, Lake Huron) ; Nicholson and Lydekker, 1889, Manual of Palaeontology, vol. 1, fig. 118A; Cumings, 1908, 32nd Ann. Rept. Geol. and Nat. Res., Indiana, p. 701. (U. Ord., Saluda ls., Ind.), pl. 1, fig. 1, (after Nicholson and Lydekker, 1889) ; Foerste, 1909, Bull. Sci. Lab. Denison Univ., vol. 14, p. 298, pl. 8, fig. 3. (U. Ord., Liberty fm., Ind. and Ky.) ; Yavorsky, 1955, Trudy Vsesoyuznogo Nauchno-issledovatelskogo Geol. Inst., Minister Geol. i Okhrany Nedr, nov. sain; WOle 8, De Wy iol S45 tree. 25 So poll, Bo ies lS joy SiH, save, GB aU, Wink, Russia) Coenostewum.—Coenosteum subcylindrical to club-shaped, us- ually enlarging upward, 12 to 50 cm. long, diameter 2 to 11 cm., normally 3 to 6 cm. Specimens 1-2 cm. in diameter are neanic. Plummer (1843, p. 294) reported his specimen to be about 3 feet long and 2 to 2% inches in diameter at the base. All specimens are fragments, generally 2 to 6 inches long, always broken at the lower end, usually also broken at the upper end, and the ends are sealed with mud, showing that the specimens were broken before burial. Surface with spiral or straight, longitudinal ridges, 5 to 10 mm. broad, 6 to 25 mm. from crest to crest, 1 to 5 mm. high. The ridges 28 BULLETIN 194 are not superposed from one latilamina to the next, as they are in A. undulata and A. radiata. Surface smooth between ridges, with small, round, blister-like plates averaging about 0.5 mm. in di- ameter; not papillate. The base is not preserved in any North American specimen. The apex may be conical or hemispherical. Astrorhizae absent. Cross section—The axial zone is 5 to 10 mm., ordinarily 6 to 8 mm., in diameter, simulating a tube, the cysts rarely grading into those of the lateral zone in size. The lateral zone consists of latilam- inae or annual growth rings, 1 to 10 mm. thick, ordinarly 2 to 4 mm. thick. The skeleton is composed of small, outwardly convex cyst plates, of similar diameter vertically and _ circumferentially, regularly overlapping about %4 of the subjacent plates. Each cyst plate embraces about % of a circle; 6 to 10 cysts in 2 mm. radially, 2 to 5 in 2 mm. concentrically. Cyst plates tripartite, with a thin, dark, compact median layer, 0.03 mm. thick, a thin, gray, flocculent outer layer, a thick flocculent inner layer. Chambers filled with flocculent material from the cyst plates or with clear, crystalline. calcite. Radial pores pierce the median and upper plates in places. Small, round, straight pillars 0.07 to 0.13 mm. in diameter, with light centers and thin, dark borders are intermittently present in the outer, mature part of the coenosteum, usually scarce, in some cases abundant (slides 299-39, 40), arising from the apex of the cysts, and continuing through several overlying cysts. Longitudinal section—The axial column is composed of large, thick, upwardly arched, hemispherical plates which are largely superposed. The median layers of the cysts are thin, dark and com- pact, extend around the column, and simulate the wall of a tube; the outer layers are flocculent and thin; the inner layers are thick, gray, flocculent, transversely fibrous, and tufted or moniliform, much like the cysts of the outer zone. Pillars in the outer layers are inclined upward about 70° to the axis, and slightly curved up- ward, Comparisons—Aulacera plummeri is characterized by large, low, widely spaced longitudinal ribs, by small, evenly convex and regularly imbricating cysts, and by the scarcity of pillars in the young stages. It differs from A. undulata in having larger ridges, ORDOVICIAN STROMATOPOROIDEA N. AMER.: GALLOWAY & ST. JEAN 29 small low, arched, regularly imbricating cysts, and the lack of superposition of the cysts in the ridges from one latilamina to the next, and in having long, round pillars. After comparing the type of Awlacera undulata (Billings) from Anticosti Island, with topotypes of Aulacera from the Richmond, Indiana, area, it is apparent that the midwestern species is distinct from the Anticosti species. Because Plummer did not give a specific name to the species he discovered, we named it Aulacera plummert in honor of Dr, John T. Plummer, who first named, figured, and described the genus, in 1843. Our specimens are topotypes from the upper Richmond, Whitewater, and Saluda formations, four miles south of Richmond, Indiana. Some of the Indiana specimens have an abundance of pillars, especially in the outer part, but most of them have few pillars, even in the outer layers. Kentucky specimens from the basal Liberty formation, have few pillars, even in the outer layers, but are not con- sistently different from Indiana specimens, although they are slightly older and should be less specialized in size, number of pillars, and the like. Preservation.—Most specimens are solidly infiltrated with calcium carbonate, and are as well preserved as other kinds of fossils, such as bryozoans and corals. Some specimens are crushed to half their original diameters, and other specimens are crushed at the upper end. Crushing indicates that these specimens were not fully calcified but were frail structures where they were broken from their moorings and covered with mud where we now find them. Several specimens from Nelson County, Kentucky, were covered either directly, or after a layer of mud had accumulated, by Derma- tostroma, in which cases the outer layer of Aulacera has been largely destroyed, but showing rootlike prolongations into the tissue of the Aulacera (specimen RB 5). In no case does the Dermatostroma have any organic structure, only coarsely crystalline calcite, although at the surface there are ridges, knobs and papillae as usually seen in Dermatostroma (RB 56). In several specimens the spiral ridges and cylindrical form are that of A. plummeri (RB 55, 56), but below the surface there is no organic structure, only coarsely crystalline, twinned calcite, and the central half of the specimens is calcite and iron oxide, or is empty. The ridges resembling those of Aulacera 30 BULLETIN 194 are mostly smooth, but in part have papillae as in Dermatostroma papulatum. In four specimens of A cylindrica the surfaces show ridges and nodules, resembling A. nodulifera, but outer layers are Dermatostroma, with ridges, nodes and papillae, with substrata of coarsely crystalline calcite or of mud, with no direct connection with the Aulacera which is cylindrical and not crushed. No specimens covered with Dermatostroma have been found in Indiana, only in Kentucky. Type and occurrence ——From the Saluda formation, Elkhorn Creek, four miles south of Richmond, Indiana, collected by Wm. H. Shideler; Indiana University Paleo. Coll., slides 285-46; 299-35, 36; 300-9. Also found abundantly in the Liberty formation on Wilson Creek, two miles southwest of Deatsville, Kentucky, collected by Dr. Guy Campbell, of Corydon, Indiana, and Mrs. Ruth G. Browne, of Louisville, Kentucky. Reported by Foerste from Bullitt, Nelson, Marion, Casey, and Madison Counties, Kentucky. Also reported from Ohio, Ontario, and Russia. Not definitely known from Anticosti Island. It occurs also in the Richmond of Rabbit Island, three miles: east of Manitoulin Island, Lake Huron, reported by Billings (1865, p. 406), and Univ. Mich. No. 6465. Rarely found in the Liberty of Indiana. Aulacera undulata (Billings) Pile 3 higss gay by Cena 124, Wy, tee Beatricea undulata Billings, 1857 (for 1853-1856), Geol. Surv. Canada, Rept. Prog., p. 344; 1866, Geol. Surv. Canada, Cat. Sil. Foss. of Anticosti, p. 8, (U. Ord., Anticosti Island) ; Nicholson, 1886, Palaeont. Soc., vol. 39, p. 89; Whiteaves, 1897, Canadian Rec. Sci., vol. 7, p. 133; Parks, 1910, Univ. Toronto Studies, Geol. Ser. No. 7, p. 43, (part), pl. 25, fig. 1 (?); Twenhofel, 1927, Canada Dept. Mines, Geol. Surv., Mem. 154, p. 104; Foerste, in Foerste and Cox, 1936, Geol. Mag., vol. 73, p. 304. (U. Ord., Akpatok Island.) Not Beatricea undulata Billings, 1865, Canadian Nat., ser. 2, vol. 2, p. 405, figs. 1, 2, (Aulacera plummeri Galloway and St. Jean, U. Ord., Rabbit Island, Lake Huron). Beatricea sulcata Hyatt, 1865, Proc. Boston Soc. Nat. Hist., vol. 10, p. 19. Aulacera undulata Galloway, 1957, Bull. Amer. Paleont., vol. 37, No. 164, p. 423, pl. 37, fig. 2. (U. Ord., Anticosti.) Coenostewm.—Coenosteum subcylindrical, up to 10 feet, 5 in. in length and 14 inches in diameter (Billings, 1857, p. 344), usually in broken pieces, 4 to 6 cm. in diameter and 6 to 8 em. long. Billings’ type specimen is 4 to 5 cm. in diameter, in two pieces aggregating 18 ORDOVICIAN STROMATOPOROIDEA N. AMER.: GALLOWAY & ST. JEAN 31 cm. long before sectioning at one end. Surface with sharp, longi- tudinal or slightly spiral discontinuous ridges, 2 to 6 mm. high, and 5 to 10 mm. apart; small ridges are intercalated between larger ridges. Surface minutely papillate between the ridges, due to the highly arched cysts, not due to pillars nor overgrown object. Cross section—Axial column 6 to 7 mm. in diameter, with hemispherical cysts. Lateral zones consist of indistinct latilaminae 5 to 10 mm. thick. The skeleton is composed of large strong, outwardly convex cyst plates arranged perpendicular to the axial column. The cysts in the ridges are hemispherical, embracing ¥ to % of a circle, and tend to be superposed, overlapping three-fourths or more of the preceding cyst; 0.9 to 1.8 mm. in length and two-thirds as high. Between the ridges the cysts are smaller and irregular in shape. The cyst plates have a thin, dark, compact, outer plate and a thick, flocculent, moniliform, inner layer. The chamber cavities were mostly open, now filled with coarsely crystalline calcite. There are no indications of pillars. Longitudinal section—The axis is composed of large, upwardly arched plates. There is no tube wall separating the axial zone from the lateral zone, but there is a sudden decrease in size of cysts. The lateral cyst plates seem to be irregularly arranged at first, then form ridges of larger more hemispherical cysts. The ridges are about 2 mm. wide and 5 or 6 mm. apart. Comparisons—This specimen differs from A. plummert, with which it has been confused, in the larger cysts which make radial zones, not seen in A. plummeri, and there are no pillars. Preservation—The specimen is well preserved by infiltration of calcite, but the chambers are not completely filled. Occurrence.—This species occurs in the Vauréal and Ellis Bay formations of late Richmond and Gamachian age, on Anticosti Island. Dr. Alice E, Wilson, of the Canadian Geological Survey, was kind enough to loan us a specimen marked “TYPE,” and considered by the Survey to be one of J. Richardson’s specimens used by Bill- ings for his original description. It also has been doubtfully reported from the Richmondian of Manitoba. We do not find it in the region of the Cincinnati Arch. T'ype—Canadian Geological Survey, specimens Nos. 1969g, 32 BULLETIN 194 2583 (two pieces of the same), collected by J. Richardson in 1856; not the one figured by Billings, 1865, which is A. plummeri from Rabbit Island, Lake Huron. Fragment, Indiana University Paleo. Coll., slides 299-88, 89, 90, 91; 300-54. Aulacera radiata Galloway and St. Jean, n. sp. Pl. 4, figs. 1a, b; PIRI eae: Aulacera undulata Shimer and Shrock, (not Billings), 1944, Index Foss. of N.A. p. 63, pl. 19, figs. 19, 20. (Richmond, Anticosti Island.) Coenosteum.—The type specimen, (No. 702A) figured by Shimer and Shrock, is a fragment 8 cm, in diameter and length. ‘Lhe surface has sharp intercalated, nearly straight, longitudinal ridges of different lengths, 8 to 15 mm. apart, separated by concave furrows. Surface with small contiguous papillae, which are the cysts, rather than the ends of pillars. The specimen is well preserved by infiltration of calcium carbonate, except the axial column which is largely missing and areas between latilaminae. Another specimen (No. 702B) is poorly preserved, with much recrystallized calctum carbonate, and vacuities lined with calcite; the outer 5 to 10 mm. is largely coarse crystals of calcite, but the specimen is embedded in calcareous clay, showing well the sharp ridges, 2 to 5 mm. high and 5 to 8 mm. apart. Cross section—The axial column is 4 to 5 mm. in diameter, and has a thick wall. The lateral zones consist of thin latilaminae, 1 to 2 mm. thick which are well preserved by infiltration of calcite (the inner and outer zones shown in Shimer and Shrock’s figure are due to different preservation, not to different structure). Be- tween latilaminae there are thin layers of calcite, imperfect cysts and thin, radial pseudopillars, all denoting imperfect calcification of the skeleton during life or possibly due to the presence of a non- calcareous parasite, similar to the parasitic Dermatostroma cos- tatum and Dermatostroma nodoundulatum on Kentucky specimens of Aulacera, rather than poor preservation during fossilization. The skeleton is composed of small, arcuate cyst plates, convex outward, each cyst embracing 1/6 to 1/4 of a circle; four to five cysts in 2 mm. the broad way, and 8 to 10 in 2 mm. radially. Each cyst overlaps 1/2 or less of each subjacent cyst. The latilaminae rise sharply into ORDOVICIAN STROMATOPOROIDEA N. AMER.: GALLOWAY & ST. JEAN 33 narrow, radial ridges, or radu, 1 to 1.5 mm. thick, in which the cysts are smaller than those between the ridges, and there are some pillars. The rays are not solid, as seen by the eye or by the lens, but are better preserved and more highly infiltrated than the areas between the rays. The radii are from 20° to 30° apart; at the surface there are small, intercalated ridges, so they may be only 10° to 15° apart. The cyst plates are tripartite, with a dense, median layer, a thin, flocculent outer layer and a thick lower layer which completely fills the chambers. Small, round pillars, with broad bases, occur intermittently in the radial ridges. The pillars appear short and conical because they extend upward 20° to 30° from the cross sec- tion and consequently are cut obliquely. Longitudinal, radial section—The axial column is 4 to 6 mm. in diameter (not 13 mm., as interpreted by Shimer and Shrock, pl. 19, fig. 20); the large cysts, as wide as the column, are hemispherical in shape, not exactly superposed. The axial cyst plates are tripartite, with a thin, dense median layer, and thin upper and lower floc- culent layers. The large axial cysts do not grade into the lateral cysts, but are covered by cyst plates averaging less than 1/2 mm. broad. The thin latilaminae are separated by thin layers of calcite, in which are small, flocculent pseudopillars. Round, radial pillars are developed only sporadically, and are mostly in the rays in the mature zone. They extend through a single latilamina and are inclined up- ward about 20° from the horizontal. Tangential sections show little of significance. Comparisons.—Aulacera radiata is characterized by the sharp, straight ridges, the small, low cysts, which overlap about half of each subjacent cyst, and the narrow sharp, continuous radi. It differs from A. undulata in having much smaller cysts, only 1/3 the length and height of those of that species, and in the sharp, radial ridges. ‘The cysts are only one-half the length of those of Aulacera plum- mert in which there are no radi. A. wndulatadirecta Yavorsky, is similar; but the radii are vague, the cysts are higher and do not overlap as much; there are no indications of pillars. Yavorsky’s species appear to be a variation of A. plummeri rather than a dis- tinetly different form, as is A. radiata. Occurrence —Richmondian and Gamachian, Anticosti Island. 34 BULLETIN 194 Holotype—Mus. Comp. Zool., Harvard College, No. 702A, and two figured slides; paratype No. 702B, and two slides. Fragment of holotype in Indiana University Paleo, Coll.; slides from 702A, 308-7, 8, 9; from 702B, paratype, 302-71, 72, 308-54. Aulacera nodulosa (Billings) Ple4 hese Zab VPI IPA, sae, Beatricea nodulosa Billings, 1857, (for 1853-1856), Geol. Surv. Canada, Rept. Prog., p. 344. (U. Ord., Anticosti Island) ; Billings, 1858, Canadian Nat., vol. 3, p. 332; 1866, Geol. Surv. Canada, Cat. Sil. Foss. Anticosti, p. 8; Nicholson, 1886, Palaeont. Soc., London, vol. 39, p. 86-90, pl. 8, figs. 4, 5; Whiteaves, 1895, Geol. Surv. Canada, Palaeozoic Fossils, vol. 3, pl. 2, p. 114; Parks, 1910, Univ. Toronto Studies, Geol. Ser. No. 7, p. 45, pl. 25, figs. 4, 5 (from Nicholson, 1886, pl. 8, figs. 4, 5); Foerste, 1924, Geol. Surv. Canada Mem. 138, p. 76. (U. Ord., Ontario and Quebec) ; Twenhofel, 1926, Nat. Hist., vol. 26, p. 518. (U. Ord., Anticosti Island.) Coenosteum.—Coenosteum large, subcylindrical, usually 5 to 12 cm. in diameter (up to a foot in diameter and up to 15 feet in length, according to Billings, 1866, p. 406; p. 408, 30 feet!). The surface has large, regular, round or oval mamelons, arranged in vertical rows; 5 mm. or more in diameter, 4 to 5 mm. high (6 to 7 lines in length and half as wide, 1 to 3 lines high, Billings, 1857, p. 344), and 10 mm. from center to center. The mamelons are not developed in the syntype until the axial diameter is nearly 40 cm., so that neanic specimens may not be distinguishable from the young of A. nodulifera. The cyst plates at the surface appear as little knobs, 1/2 to 1 mm. in diameter. Astrorhizae absent. Cross section—The axial zone is 6 to 15 mm. in diameter, not simulating a tube in the syntype, as is mostly true for the genus, but the large, axial cysts grade into the small, lateral cysts. The lateral zones consist of latilaminae, 2 to 3 mm. thick, demarked by small cyst plates. The skeleton is composed of small, outwardly arcuate cyst plates, embracing 1/4 to 1/3 of a circle; 1/2 to 1 mm. broad and 1/2 as high. Each plate overlaps about 1/4 of the sub- jacent plates. The cyst plates are smallest and closest together at the junction of the latilaminae. The cyst plates are tripartite, with a thin, dense, median layer, a thick lower, flocculent layer, and a thin upper flocculent layer. The mamelons are not superposed ORDOVICIAN STROMATOPOROIDEA N. AMER.: GALLOWAY & ST. JEAN 35 from one latilamina to the next, and do not form mamelon columns nor radii. Longitudinal section—The axial column consists of large, hemi- spherical cysts. In the lateral zone, long, thin pillars are directed outward and upward at 20° to 30° from the horizontal, on one side of the syntype, in which they occur in the outer 10 mm. Some pillars appear to intersect as they turn outward in the mamelons. The pillars might be mistaken for tubes, for they were originally composed of loosely compacted material, as in many genera of the Labechiidae, and upon infiltration and crystallization, the pillars lost their original structure, and now appear as clear, granular calcite, much like the chamber fillings. Nicholson (1886, pl. 8, fig. 4) showed pillars in the first published figures of this species. The light, radial streaks of the inner layer of the cysts, shown by Nicholson (fig. 5), are a common feature of the genus; the light streaks were pores, and they extend through the median and upper cyst plates of this and other species of the genus. Comparitsons.—Aulacera nodulosa is characterized by the large mamelons. The nodules of the midwestern form, A. nodulifera, are smaller than they are in A. nodulosa. The small cysts and sporadic development of pillars are usual for the genus. Occurrence.—A. nodulosa occurs in the Vauréal and Ellis Bay formations, latest Richmond and Gamachian of Anticosti Island, and the Stony Mountain formation of Manitoba. It has not been reported from the Upper Ordovician of Indiana, Ohio, or Kentucky. Dr. Alice E. Wilson, of the Canadian Geological Survey, kindly loaned us a median slice of one of Billings’ syntypes (No. 1971), from which we made four thin sections, on which much of the above description is based. She also loaned us a large specimen from Manitoba, with large nodes, but the interior was entirely destroyed. Syntype—Canadian Geol. Surv., No. 1971, and a thin section; Indiana University Paleo. Coll., slides Nos. 299-85, 86, 87. Topotype.—Yale Peabody Mus. No. 19556, and 9200A, and thin sections; Indiana University Paleo. Coll., fragment and slides Nos. 302-38, 75. 36 : BULLETIN 194 Aulacera nodulifera (Foerste) Pl, 4, figs) 3a, ps Pl 2s ticeet Beatricea nodulifera Foerste, 1909, Bull. Sci. Lab. Denison Univ., vol. 14, p. 299, pl. 7, fig. 13, pl. 8, fig. 5. (U. Ord., basal Liberty fm., 3 mi. southeast of Lebanon, Ky.) ; Parks, 1910, Univ. Toronto Studies, Geol. Ser., No. 7, oe HE ob ASS sever, Ib Beatricea nodulosa Nicholson (not B. nodulosa Billings), 1886, Palaeont. Soc. London, vol. 39, p. 87, pl. 8, figs. 1-3. (U. Ord., Marion Co., Ky.) ; Shimer and Shrock, 1944, Index Fossils of N. A., p. 63, pl. 19, fig. 17. (Locality not given.) Beatricea conosimilis Yavorsky, 1955, Trudy Vsesoyuznogo Nauchno- issledovatelskogo Geol. Inst., Minister Geol. i Okhrany Nedr, nov. ser., VOleS; Por/Sy PletOstiee ten (Ue Ord Umass) Coenosteum.—Coenosteum of moderate size, 4 to 5 cm. in diameter and in fragments 10 to 15 cm. long. Surface with small mamelons; 3 mm. in diameter, and 5 to 7 mm. apart laterally, round or oval lengthwise of the stem, and arranged in vertical or slightly spiral rows. Between the mamelons there are small papillae. Latilaminae 2 to 5 mm. thick. Astrorhizae absent. Cross and vertical sections—The axial column is 10 mm. in diameter and in fragments 10 to 15 cm. long. Surface with small superposed cysts. Lateral zones composed of latilaminae 2 to 4 mm. thick. Small, regularly arcuate cysts embrace 1/6 to 1/4 of a circle, 4 in 2 mm. broad and half as high. The cyst plates are tripartite, with a thin, dark, dense, median layer, a thin, upper flocculent layer, and a thick lower flocculent layer nearly filling the chamber. Each cyst overlaps about 1/3 of each subjacent cyst. Small, long, narrow pillars, which are intermittent in the outer part of the lateral zone, are common but are difficult to detect. They are inclined up- ward 20° to 30° from the horizontal. Comparisons.—This species is characterized by the small nodes. The cysts, pillars, and axis appear to be identical with those of A. plummen, A. intermedia, and A. cylindrica. The nodes are much smaller than those of A. nodulosa (Billings), who said (Billings, 1857, p. 344), “The surface of this species is covered with oblong, oval, or sub-triangular projections from one to three lines in height.” Occurrence and hypotypes—This species occurs sparingly in the Liberty formation near Lebanon and Bardstown, Kentucky. We have two specimens, apparently typical of A. nodulifera, one from the upper Richmondian, Vauréal formation of Anticosti Island, ORDOVICIAN STROMATOPOROIDEA N. AMER.: GALLOWAY & ST. JEAN 37 Yale Peabody Mus., No. 9200B, and thin sections, Indiana Uni- versity Paleo. Coll., fragment and slides 302-35, 73, and one from the Richmondian, Anticosti Island, Museum of Comparative Zoology, Harvard University (no number), and one slide; fragment in In- diana University Paleo. Coll., and slide 302-67. Aulacera intermedia (Foerste) jell, 2h snes, Abe JN, alley, 3 Beatricea nodulifera intermedia Foerste, 1909, Bull. Denison Uniy. Sci. Lab., vol. 14, p. 300, pl. 8, figs. 4a, b. (U. Ord., Liberty fm., Marion Co., Ky.) ; Parks, 1910, Univ. Toronto Studies, Geol. Ser. No. 7, p. 47, pl. 25, fig. 9. (From Foerste.) Coenosteum.—Coenosteum cylindrical, slightly tapering. Three incomplete specimens are 24 to 40 mm. in diameter. Surface with vertically elongate nodules, arranged in slightly twisted, longitu- dinal rows. Nodules 3 to 5 mm, from crest to crest, 0.5 mm. high, 1.0 to 1.5 mm. wide, and 3 to 12 mm. long. Astrorhizae absent. Cross and vertical sections —Latilaminae 2 to 4 mm. thick. The axial zone is about 5 to 10 mm. in diameter and consists of large cysts, variable in size, 2 to 7 mm. broad, | to 6 mm. high, which grade into the lateral cysts in one specimen and make a tube in another. The lateral cysts are highly arched and variable in size from axis to periphery, 0.2 to 2 mm. broad, averaging 0.5 mm. and half as high. The cystose plates consist of a thin, dense, median primary plate, a thin, flocculent upper layer, and a thick floc- culent lower layer. Pillars are rare in the outer latilaminae and rare or absent in the inner latilaminae. Comparisons —Aulacera intermedia (Foerste) is characterized by small, elongate nodes. The large, cystose axial zone, which does not make a tube, applies to some specimens of other species also and the cysts are the same size as for A. plummeri, A. nodulifera, and A. cylindrica. A. intermedia differs from A. nodulifera in sur- face characters. Occurrence.—A. intermedia occurs sparingly in the Upper Ordo- vician, basal Liberty formation of Kentucky, but has not been reported from Indiana, Ohio, nor from Russia. It has been reported from Manitoba by Okulitch (1943, Trans. Roy. Soc. Canada, ser. 3, 38 BULLETIN 194 vol. 37, sec. 4, p. 62-68). We are grateful to the University of Cincinnati Museum for the loan of a typical specimen; the exact locality in Kentucky is unknown. It also occurs rarely in the lower Liberty two miles southeast of Deatsville, Kentucky. Hypotype—University of Cincinnati Museum, No. 17542, one slide; Indiana University Paleo. Coll., slides, Nos. 299-48, 92. Liberty formation, Wilson Creek, two mi, southwest of Deatsville, Kentucky, collected by Mrs. Ruth G. Browne, Louisville, Kentucky, specimen RB 18, slides 308-11, 57, 58. Aulacera cylindrica (Foerste) Pl. 5) figsedar bs Pde ss Oslo Beatricea undulata cylindrica Foerste, 1909, Bull. Sci. Lab. Denison Univ., vol. 14, p. 298, pl. 9, fig. 7. (U. Ord., Liberty fm., Ophelia, Ky.) ; Parks, 1910, Uniy. Toronto Studies, Geol. Ser., No. 7, p. 44. Beatricea sibirica Yavorsky, 1955, Trudy Vsesoyuznogo Nauchno-isseldovatel- skogo Geol. Inst., Minister. Geol. i Okhrany Nedr, noy. ser., vol. 8, p. 76, pl. 38, figs. 1-6; pl. 39, fig. 1. (U. Ord., Siberia.) Beatricea conica Navorski: 1955, 2bids, pe 74.) pla sé. tgs. 3,84 pleasi7y ema. ib ee wate PAZ, (UE Ord., Siberia.) Beatricea vulgaris Naverky, 1957, zbid:, vol. 918, p. 45, pl.) 225 ehigsoed, 2. (U. Ord., Novaya Zemlya.) Coenosteum.—Coenosteum small, subcylindrical or elongate conical, up to 25 mm. in diameter, in fragments up to 100 mm. long. Surface smooth, with minute, round, convex, cyst plates. The axial column is 6 to 8 mm. in diameter, and generally occupied by a single row of large, nearly superposed, upwardly arched cyst plates. Latilaminae 2 to 5 mm. thick. Astrorhizae absent. Cross section—The large axial cysts are covered by smaller, outwardly convex cyst plates. In one specimen, of the 16 or more in our collections, the axis is a zone in which the largest cysts grade into the lateral cysts (PI. 5, fig. 1b). Cysts variable in size, 4 to 6 cysts in 4 mm. horizontally, 12 to 16 cysts in 4 mm. vertically, averaging 0.8 mm. broad, and one-third as high; regularly arcuate, making 1/6 to 1/4 of a circle. Cyst plates tripartite, consisting of an upper flocculent layer 0.15 mm. thick, a dense median layer 0.03 mm. thick, and a lower flocculent or tufted layer 0.3 mm. thick which fills most of the cystose vesicles. Small, long pillars are inclined slightly upward from the horizontal and occur rarely in the outer part of the lateral zone. ORDOVICIAN STROMATOPOROIDEA N. AMER.: GALLOWAY & ST. JEAN a9 Comparisons.—Aulacera cylindrica (Foerste) closely resembles A. plummeri G. and St. J., with which it occurs, but the surface is smooth rather than undulate. It may be the young stage of A. plummeri, but many specimen of A. plummeri, with ridges, are much smaller than those of A. cylindrica. The name is useful in referring to one of the two smooth forms of Aulacera. A. peichuangensis 1s smooth but has flatter cysts and more pillars. We see no difference between Foerste’s species and those of Yavorsky. The conical form of A. conica is not of itself sufficient to distinguish A. comca from A. plummeri or from A. cylindrica. Occurrence-——This species occurs abundantly in the Liberty formation, two miles southwest of Deatsville, Kentucky. The ma- terial was collected by Mrs. Ruth G. Browne, Louisville, Kentucky, and Dr. Guy Campbell, Corydon, Indiana. The same or similar forms occur in Russia. Hypotypes—lIndiana University .Paleo. Coll., Nos. GC4, 20; RB 30, 34, 59, 60, 61, 62, G/, 68, 69; slides 302-20, 21, 22, 23, 24, 74; BUS=oe 52) 33534, 355.360, 375 38,39; 4054 Le 42: Genus PSEUDOSTVLODICTYON Ozaki, 1938 Type species (monotypic), P. poshanense Ozaki, 1938, Jour. Shanghai Sci. Inst., sec. 2, vol. 2, p. 208, pl. 24, fig. 2; pl. 25, figs. la-e. (M. Ord., Shan- tung); Galloway, 1957, Bull. Amer. Paleont., vol. 37, No. 164, p. 424, pl. BY sits, De Rosenella (part) Ozaki, 1938, Jour. Shanghai Sci., sec. 2, vol. 2, p. 216, pl. 32, fig. 1 (M. Ord., Shantung). Coenosteum massive or attached to other stromatoporoids, strongly latilaminate, composed of long, regular laminae which may be wrinkled or straight, with or without denticles, and without cysts, pillars or astrorhizae. Middle and Upper Ordovician, China, Vermont, and Texas. Six species. Pseudostylodictyon differs from Rosenella in not being com- posed of cysts and generally lacking denticles. The presence of mamelons and mamelon columns is a specific character; a genus may have species with columns and other species without columns. 40 BULLETIN 194 ‘The genus has simple structure compared with most stromatopor- oids, but it is most similar to the family Labechiidae. KEY TO SPECIES OF PSEUDOSTYLODICTYON la. Mamelon columns strong Za, atilaminae mots waver eces es P. poshanense Ozaki 2p. datilamainae waynes ete eee P. 2? lamottense (Seely) lb. Mamelon columns vague or absent 2c. Laminae not wrinkled Sa, Waminae 8_to- Oem 2 mm ee P. ? eatont (Seely) 3b. Laminae 20 or more in 2 mm...P. ? chazianum (Seely) 2d. Laminae wrinkled in places 3c. Without denticles .....P. ? kayt Galloway and St. Jean 3d. With denticles and corrugations .....P. 2 montoyaense Galloway, n. sp. Pseudostylodictyon 2% lamottense (Seely) Pl. 5, figs. 2a, D Stromatocerium lamottense Seely, 1904, Rept. State Geol. Vermont, vol. 4, p. 147, pls. 69, 72, pl. 74, fig. 1 (M. Ord., B Chazy, Fisk’s Quarry, Isle La Motte, Vt.) Exterior—Coenosteum massive in isolated masses “two to six or more feet in section,” (Seely, 1904, p. 147) apparently not forming bioherms, surrounded by black limestone, The limestone is attached to the worn edge of the specimen. Surface with unequal mamelons, 3 to 6 mm. in diameter and 10 to 15 mm. apart. Astrorhizae absent, Vertical section—The specimens are composed of white lati- laminae, 2 to 5 mm. thick and wrinkled in more or less parallel layers, and forming irregular mamelon columns 2 to 6 cm. long. The lati- laminae are separated by black limestone, similar in thickness and contortion to the latilaminae, so that when the specimens are cut vertically and polished a striking, banded marble results. The banding obviously results from a winter’s layer of lime mud on the living organism, which rejuvenated the next spring and formed annual layers. The banding is not the specific character, but rather the size of the wrinkles and the finer structure of the latilaminae are the specific characters. The latilaminae, the white bands, are composed of fairly regular laminae, 0.17 to 0.26 mm. thick, closely ORDOVICIAN STROMATOPOROIDEA N. AMER.: GALLOWAY & ST. JEAN 41 appressed, and numbering 15 to 18 in 2 mm, The laminae have a thin, dark upper layer, and a thick, flocculent lower layer, which is darker in places but is not moniliform. The lower layer is trans- versely fibrous in places. The laminae are not wrinkled, other than conforming to the wrinkles of the latilaminae, and do not make arcuate plates except at the top of the latilaminae where the mud stopped the growth of the organism. There are no denticles on the laminae, and there are no vertical or horizontal tubes or canals, nor astrorhizae, nor pillars. The tangential section shows nothing diagnostic. Comparitsons.—This species differs from P. ? eatoni in the more wrinkled latilaminae. The size of the coenosteum and the alternating latilaminae and mud layers can scarcely be taxonomic characters. It occurs stratigraphically below P. ? eatont, in the B Chazy hori- zon. The black limestone is composed of small euhedral crystals of calcite and smaller, rounded grains of calcite, with a thin matrix of black, carbonaceous material. P. ? chazyanum, from the basal or A Chazy, lacks the wrinkles of the latilaminae, and the laminae are finer. Types—B Chazy, Fisk’s Quarry, Isle La Motte, Vermont, specimen figured by Seely, 1904, pl. 72. Our figures are from syn- types from Goodell’s Quarry, collected by Seely, 1885, now in the Paleontological Collection of Middlebury College, and fragments in Indiana University, slides 301-59, 60, 61. Pseudostylodictyon ? eatoni (Seely) Pl. 5, figs. 2a, b Stromatocerium eatoni Seely, 1904, Rept. State Geol. Vermont, vol. 4, p. 146, pl. 71; pl. 74, fig. 2. (M. Ord., upper or C Chazy, Goodell’s Ridge, south of Village, Isle La Motte, Vt.) Description.—The following description is based on Seely’s holo- type in the Middlebury College Paleontological Collection. Exterior—Coenosteum massive, up to 20 cm. in diameter, composed of latilaminae 5 to 10 mm. thick. Surface with convex knobs 6 to 20 mm. in diameter. Astrorhizae absent. Vertical section —tThe latilaminae are broadly undulating, form- ing large, sharp knobs which do not make continuous mamelon columns. The latilaminae are in turn composed of fairly regular laminae, 0.12 to 0.2 mm. thick; 8 to 10 in 2 mm.; there is a thin upper 42 BULLETIN 194 layer, and a thick lower layer, which is moniliform in the type speci- men (1904, pl. 71) but not conspicuously moniliform in other specimens (1904, pl. 74, fig. 2). The laminae le mainly one on an- other, but there are numerous places in which the laminae are separated by clear spaces of differing width. In some places the lower layer has a transversely fibrous or porous appearance. The laminae are not wrinkled, and there are no denticles nor pillars. ‘The laminae rise smoothly over the mamelon columns, in some cases leaving vacuities in the mamelons, but there are no astrorhizal nor axial tubes, nor are there astrorhizal canals. Tangential section—TVhe tangential section shows irregular patterns made by the cut laminae. Comparisons.—This species is simple for a stromatoporoid, lacking cysts, pillars, denticles, and astrorhizae. It is much like the type species of Pseudostylodictyon excepting for the monticular columns. It is much like P. ? lamottense from the B or middle Chazy. It might, with the other species of the genus, be considered as a calcareous alga, but there are no cells such as is usual in an alga. Holotype—The specimen figured by Seely, 1904, on pl. 71, in Middlebury College, Middlebury, Vt., from C Chazy horizon, Goo- dell’s Ridge, Isle La Motte, Vt. A section from that specimen, slide 301-58, Indiana University Paleo. Coll., is figured on our Plate 5, figure 3b. Pseudostylodicton ? kayi Galloway and St. Jean Pl: 5, figs. 4a, by Pll 6, fics. Lave Pseudostylodictyon kayi Galloway and St. Jean, 1957, in Galloway, Bull. Amer. Paleont., vol. 37, No. 164, p. 425, pl. 32, fig. 6. (M. Ord., middle Chazy, “Fleury” Quarry, one mile southeast of Isle La Motte village, Vt.) Exterior.—Coenosteum massive, up to 20 cm. in diameter with latilaminae 5 to 10 mm. thick, and with large, irregularly developed, pointed mamelons 10 mm. in diameter and about 30 mm. apart. Astrorhizae absent. Vertical section—The laminae are fairly regular. They are 0.15 to 0.18 mm. thick, 10 or 12 in 2 mm., mostly closely appressed, but in zones of 4 to 6 laminae separated by narrow zones of calcite. ‘The laminae have a thin dark upper layer and a thick lower ORDOVICIAN STROMATOPOROIDEA N. AMER.: GALLOWAY & ST. JEAN 43 flocculent or fibrous layer. In places the laminae are strongly wrinkled wtih some of the wrinkles open at the top. In addition to strong mamelons in places five to six laminae rise abruptly leaving a vacuity, as if the laminae had erupted. Tangential section—In places in the section there are con- spicuous rings 0.14 to 0.18 mm. in diameter, made by the cutting of the wrinkles. Comparison.—P. ? kayi differs from P. ? eatont mainly in hav- ing wrinkled laminae; it also occurs at a lower horizon, middle instead of upper Chazy. Occurrence and types —The holotype, KAI, is from the middle Chazy, “Fleury” Quarry, one mile southeast of Isle La Motte vil- lage, Vermont. Collected by Marshall Kay. Indiana University Paleo. Coll., slides 300-21, 22, 23, 24. A paratype, KA5, from the same quarry, has abundant wrinkles of the laminae. Slides 300-19, 20. Vseudostylodictyon ? chazianum (Seely) Pl. 6, figs. 2a, b Stromatocerium lamottense var. chazianum Seely, 1904, Rept. State Geol. Vermont, vol. 4, p. 148, pl. 73, upper figure. (M. Ord., middle or B Chazy, South Hero, Vt.) Exterior—Coenosteum conical, several inches tall, composed of latilaminae 1 to 2 mm. thick; surface without regular mamelons or knobs, and without astrorhizae. Vertical section.—Seely does not give a vertical thin section. Our description is drawn from a specimen labeled by Seely, from “A Chazy,” South Hero, Vermont, although the text says “B Chazy.” The specimen is somewhat silicified. The latilaminae are thin, averag- ing less than 2 mm., are undulating but not forming knobs, as in P. ? eatoni, nor wrinkles, as in P. ? lamottense. The laminae are thin, 0.02 to 0.03 mm. thick, numbering 20 or more in 2 mm. The laminae con- sist of a thin, dark upper layer and a thicker, gray, flocculent lower layer. There are no corrugations nor denticles, pillars, nor cysts. ‘The simplicity of this form suggests an alga, and the thin la- minae of the hypotype (PI. 6, fig. 2b) might be interpreted as cells of a calcareous alga. Comparisons —This species differs from P. ? eatont in the thin laminae and few knobs; from P. 2 lamottense in the thinner laminae and it lacks the wrinkled latilaminae of that form. 44 BULLETIN 194 T'ypes——Syntypes were from the B Chazy horizon from Basin Harbor, Vermont, Appletree Point, South Hero, Vermont, and from Chazy, N. Y. Seely’s specimens are in Middlebury College, Vermont., and part of one specimen from South Hero, Vermont, in Indiana University, slides 301-62, 63, and from the Maclurites beds, South Hero, % mile west of Rt. 2, Grand Isle Co., Vermont, collected by Marshall Kay, 1954, specimen KB1, slides 300-30, 31, 32, 33, 34; specimen KB2, 300-35, 60, 73. Pseudostylodictyon 2? montoyaense Galloway, n. sp. Pi. 6) Lessa Exterior—Coenosteum massive, more than 10 cm. in diameter. Surface smooth or papillate, without mamelons, but gently undu- lated, making nodes of various sizes and spacing. Latilaminae con- spicuous, 2 to 8 mm. in thickness, averaging about 5 mm. Astror- hizae absent. Vertical section—The coenosteum is composed of laminae, which are thin, 10 to 12 in 2 mm., mostly parallel, rarely making arcuate plates. Most of the laminae consist of a lower, finely granular, nearly straight plate, and an upper plate to which are attached short, conical denticles or the upper plate is finely cor- rugated, making cones, 10 to 12 denticles or corrugations in 2 mm. In places the denticles and corrugations are regular and touch the overlying lamina, making oval galleries wider than high. Nodes are irregularly developed, but without axial structures common in mame- lons, such as larger pillars, an axial tube or tubes and astrorhizal canals. Some places in some specimens show no denticles or wrinkles, but the laminae are flat, either directly superposed, or separated by carbonate crystals. Tangential section—The sections show small round spots in places which are the conical wrinkles. In other places there are annuli of laminae, indicating nodes, but not showing mamelons. Many tangential sections show no structure but granular areas. Remarks——Vhe Montoya specimens have been considerably altered by calcification and dolomitization, but the structures are apparent in sections thicker than in unaltered specimens. The lack of large arcuate cyst plates is different than for Rosenella which is ORDOVICIAN STROMATOPOROIDEA N. AMER.: GALLOWAY & ST. JEAN 45 much coarser in structure. The specimens are intergrown with an alga, a sponge, and a coral in places. Occurrence —Abundant in the Upham formation of the Mon- toya group, of Upper Ordovician age, crest of Scenic Drive, E] Paso, Texas, collected by R. H. Flower, 1958. Holotype.—No. S6, and slides numbered S6, collections of the New Mexico Institute of Mining and Technology; part of holotype and slides 308-22, 23, 24, 25, in Indiana University Paleo. Coll. Paratypes Nos. $2, S3,-S4, S5, S7, and S8, parts of S4 and S7 im Indiana University Paleo. Coll., and slides. Genus ROSENELLA Nicholson, 1886 Type species (originally designated), R. macrostyla Nicholson, 1886, Palaeont. Soc., vol. 39, p. 84, pl. 7, figs. 12, 13 (Middle Silurian, Gotland) ; Nicholson, 1886, Ann. Mag. Nat. Hist., ser. 5, vol. 18, p. 19; Kiihn, 1928, Foss. Cat., Hydrozoa, p. 46; Parks, 1907, Univ. Toronto Studies, Geol. Ser., No. 4, p. 23; No. 5, 1908, p. 42; Gorsky, 1935, Trans. Arctic Inst., vol. 28, p. 94; Ozaki, 1938, Jour. Shanghai Sci. Inst., sec. 2, vol. 2, p. 215; Yavorsky, 1955, Trudy Vsesoyuznogo Nauchno-issledovatelskogo Geol. Inst., Minister. Geol. i Okhrany Nedr, nov. ser., vol. 8, p. 67, pl. 30; Galloway, 1957, Bull. Amer. Paleont., vol. 37, No. 164, p. 424. Coenosteum laminar or massive, composed of convex plates on which are conical denticles, or which have conical wrinkles. Plates compact, porous, or flocculent. Astrorhizae obscure. Rosenella differs from Cystostroma in the irregularity in size of the cysts and in having denticles. Middle Ordovician, China, North America. Middle Silurian, Europe, North America. Devonian, Russia, Novaya Zemlya. About 12 species. Rosenella cumingsi Galloway and St. Jean, n. sp. JPL (IMSS, 41215 1p Exterior—Coenosteum massive, at least 12 cm. in diameter. Surface not preserved, but a vertical weathered section shows lati- laminae 2 to 5 mm. thick, and mamelon columns, with evenly convex mamelons 10 mm. in diameter and 5 mm. high. Astrorhizae and pillars absent, Vertical section——The skeleton is composed entirely of coarse arcuate cysts. Pillars are absent excepting for conical spines or denti- cles on the upper cyst plate. The denticles are uneven in size, 46 BULLETIN 194 thickness, and in distribution, and extend only a short way through the chambers. The cysts are irregular in shape and size; some are arcuate 1 mm. broad and % mm. high, but the cysts are mostly broad, irregularly undulating and low, about 8 in 2 mm. vertically, and 2 in 2 mm. horizontally. The cyst plates are tripartite, with a thin, dense median plate, 0.02 mm. thick, and a thick upper plate, 0.05 mm. thick, and a thin lower plate. The specimens have been infiltrated, recrystallized and partly silicified, so that as is usual with weathered-out specimens, the structures have been more or less destroyed, and description unsatisfactory. Comparisons—The tangential section shows nothing of con- sequence. This species is characterized by the thin, variable cyst plates, especially the thin, lower plate, and the mamelons, from which it differs from R. woywensis Ozaki (1938, p. 215, pl. 31, figs. la-d), as well as in the stronger denticles. Such simple, as well as variable forms, cannot be distinguished with certainty. The ir- regularities of growth seem to be due to the rugged conditions of life. Holotype.—Middle Ordovician, lower Trenton limestone, new lock above Amsterdam, New York, collected by Dr. E. R. Cumings, 1914; Indiana University Paleo. Coll., slides 299-66, 67; 300-84; paratype, Middle Ordovician, Black River limestone, Watertown, New York, also collected by Dr. Cumings, 1914; slide 235-21. It also occurs in the upper Black River limestone of Quebec, slides 302-43, 44, 45; from the Chaumont limestone east of McBride Bay, South Hero twp., Grand Isle Co., Vermont, 301-11-20, from the Chaumont limestone, Otter Creek, southwest of Fort Cassin, Vermont, 302-5, 6, 7, 8, and from the lower Trenton, Rockland fm., “% mi. west of Bridge, Crown Point, New York, 302-4, 9. The Vermont and New York material was collected and presented to us by Prof. Marshall Kay of Columbia University, Genus LABECHIA Edwards and Haime, 1851 Type species (monotypic), Monticularia conferta Lonsdale, 1839, in Murchi- son, Silurian System, p. 688, pl. 16, fig. 5 (Lower Silurian, Wenlock, England). Labechia Milne-Edwards and Haime, 1851, Mon. Polyp. Foss. Terra. Paleo., p. 155, 279; Nicholson, 1879, “Tab. Corals Palaeo. Per.,” p. 330, fig. 44; ORDOVICIAN STROMATOPOROIDEA N. AMER.: GALLOWAY & ST. JEAN 47 1886, Palaeont. Soc., vol. 39, p. 81-84, fig. 13A, B; pl. 3, figs. 7-15; 1891, vol. 44, pl. 20, figs. 1-3; 1886, Ann. Mag. Nat. Hist., ser. 5, vol. 18, p. 11; Yavorsky, 1931, Bull. United Geol. and Prosp. Ser. U.S.S.R., vol. 50, fase. 94, p. 1408 (Devonian age doubtful) ; Smith, 1932, Summ. Prog. Geol. Serv. Great Britain, for 1931, pt. 2, p. 23 (Visean, doubtfully a stromatoporoid) ; Ozaki, 1938, Jour. Shanghai Sci. Inst., sec. 2, vol. 2, p. 210-213, pls. 26-28; Kiihn, 1939, in Schindewolf, Handbuch Palaozoologie, Band 2A, p. A50, A51; Yavorsky, 1955, Trudy Vsesoyuznogo Nauchno-issledovatelskogo Geol. Inst., Minister Geol. i Okhrany Nedr, nov. ser., vol. 8, p. 58-65, pls. 24-28, 41; ibid., 1957, vol. 18, p. 29-36, pls. 13-17; Galloway, 1957, Bull. Amer. Paleont., vol. 37, No. 164, p. 427, pls. 31, 32. Coenosteum laminar, encrusting or massive, possibly subcylin- drical, consists of outwardly convex cyst plates, and large, round, long pillars. Pillars with light centers not hollow. Tissue of primary plates compact, with inner and outer flocculent layers. Surface papillate. Astrorhizae not typically developed. Upper Ordovician and Silurian, Europe, Russia, China, North America. Upper Devonian, Russia. About 20 species. The genus was named for Sir Henry de Labech; it is pronounced l4-bésh’-1-a. KEY TO AMERICAN ORDOVICIAN SPECIES OF LABECHIA la. Mamelons 5 mm. in diameter or less 2a. Cysts broad, low, thick; pillars large, L. pustulosa (Safford) 2b. Cysts short, high, thin, regularly overlapping; polaris gelatinase ee csten. Saece3. dneelecl Ceara L. huronensis (Billings) 1b. Mamelons large, 10 mm. in diameter; pillars thick SAA eae 22 L. macrostyla (Parks) Labechia pustulosa (Safford) IPL, Yo TSS, WA, Io, Bet, 10 Stromatopora pustulosa Safford, 1869, Geol. Tenn., p. 276, 285. (M. Ord., College Hill Is. Catheys fm., Nashville gr., Nashville, Tenn.) Stromatocerium pustulosum Hayes and Ulrich, 1903, U.S. Geol. Sury. Folio 95, figs. 23, 24, (M. Ord., Catheys fm., Columbia Quadrangle, Tenn.) ; Bassler, 1932, Geol. Surv. Tenn., Bull. 38, p. 226, pl. 22, figs. 10, 11. (Hayes and Ulrich’s figures repeated.) Wilson, C. W., Jr., 1948, Geol. Surv., Tenn. Bull. 53, p. 38, 41, 43, pl. 12, figs. 6, 7; 1949, Bull. 56, p. 119, 129, 143, ols UA, sie (As Ze ?Stromatocerium canadense Nicholson and Murie, 1878, Jour. Linn. Soc. Zool., vol. 14, p. 223, pl. 3, figs. 9, 10. (M. Ord., Trenton, Peterborough, Ontario.) 2Stomatocerium canadense var. minimum Parks, 1910, p. 20, pl. 22, fig. 3. (M. Ord., Trenton, Frankfort, Ky.) Surface —Coenosteum massive, hemispherical to tuberose, up to 20 cm. in diameter and 10 cm. thick, composed of latilaminae 2 48 BULLETIN 194 to 10 mm. thick. Surface with minute papillae, small cysts, and low conical mamelons, 5 mm. in diameter, 2 to 3 mm. high, and 10 to 12 mm. apart from center to center. Small astrorhizae with few canals may occupy the summits of the mamelons. Vertical section —The skeleton consists of small, slightly arched cysts 4 to 2 mm. broad and 1%, to % mm. high, the broader ones flattened and no higher than the shorter ones; each cyst overlaps 2 to % of the subjacent cysts, with a tendency to form layers of cysts only one cyst in thickness. The layers of cysts rise smoothly over the mamelons. The walls of the cysts consist of a thin, outer, dark, dense plate, 0.03 mm. thick, and a lower, thick, gray, floccu- lent, moniliform layer 0.16 mm. thick, leaving a narrow chamber cavity up to 0.13 mm. high, filled with clear calcite. An outer floc- culent layer is thin or missing. Pillars are common, long, straight or curved, 0.10 to 0.25 mm. thick, and 4 occur in 2 mm. The pillars usually have been completely recrystallized or replaced by white calcite, rarely leaving a narrow, dark shell on the outside, and in many places cannot be detected. Astrorhizae are scarcely distin- guishable in vertical sections in the mamelons and do not make vertical tubes. Tangential section—The cysts are cut at many angles, and many odd patterns of curves and gray masses result; around the mamelons the cyst plates curve in bands, with the cysts convex outward, presenting the same structure as seen in vertical section. The darker, abundant material in the section is the flocculent material of the lower, thick layer of the cysts. Astrorhizae are not distinguishable. Pillars are rarely distinguishable, but the few that can be recognized are round. In the Cannon limestone specimens from Flat Rock, Tennessee, which have smaller cyst plates than the typical form, the pillars are round, averaging 0.24 mm. in diameter and 0.5 mm. apart, some ringlike; the pillars surely never were hol- low, but the centers have been recrystallized more than the borders (PL 7, fie. 2b): Remarks.—The original locality and horizon of Safford’s speci- mens are the College Hill limestone, in Nashville, Tennessee. “The section commences in the river beneath the wire bridge, and ascends to the top of Capitol Hill,” (Safford, 1869, p. 276). The horizon of Safford’s “Stromatopora pustuloswm” has been determined to be ORDOVICIAN STROMATOPOROIDEA N. AMER.: GALLOWAY & ST. JEAN 49 lower and upper members of the Catheys formation, at Nashville. (Bassler, 1932, p. 109; Wilson, 1948, p. 35-44). The species was not described other than as “having conical pimple-like elevations on its surface,” (Safford, 1869, p. 285). Both Labechia and Cysto- stroma, from the Trenton group, have mamelons, as does Stromato- cerium, from the Black River group. These genera are distinguished by flat pillars in Stromatocerium, round pillars in Labechia and absence of pillars in Cystostroma. A stromatoporoid identified as Stromatocerium pustulosum by Hayes and Ulrich occurs abundantly in the Catheys limestone of the Columbia Quadrangle area, Tennes- see; the specimen figured has slightly larger mamelons than the ones we have, but they may be the same species. Bassler (1932, p. 88) indicated that the middle part of the Cannon limestone is “filled with Stromatocerium pustulosum” and also (p. 112) named the middle Catheys the “Stromatocerium pustulosum bed” because of “many large colonies” of the species. It is much like L. macrostyla Parks in the strong, abundant, round pillars, but the cysts are larger, have thick lower, and less curved plates. On weathered specimens, the pillars and mamelons are first to dissolve, leaving holes. The presence of round pillars places this form in the genus Labechia. Stromatocerium has flat, vermicular, or irregular pillars. Stromato- certum minimum Parks (1910, p. 20, pl. 22, fig. 3), also from the ‘Trenton group, has mamelons and arched cysts but no pillars, and is, therefore, Cystostroma, but the ostensible type specimen has large, round pillars, as in Labechia pustulosa (Safford). Types and occurrence.—We have three specimens which appear to be topotypes, from which the above description is drawn, collected especially for us from Safford’s type section, “beneath the wire bridge to the top of Capitol Hill” (Safford, 1869, p. 276; Wilson, 1948, p. 38, Loc. 18), from the lower four feet of the Catheys forma- tion or Constellaria beds ( Wilson, 1949, p. 140, 143) by Prof. C. W. Wilson, of Vanderbilt University. Indiana University Paleo. Coll., slides 302-81, 85, 92. Dr. Wilson also collected two poorly preserved. specimens from the upper Catheys formation, City Quarry, Nash- ville, Tennessee; slides 302-86, 87. The species occurs rarely in the Bigby-Cannon limestone (Wilson, 1949, p. 119, 129) but is abund- ant in various layers and localities in the Catheys formation. We have parts of two specimens from the Cannon limestone of Flat 50 BULLETIN 194 Rock, Nolensville Pike, southeast of Nashville, Tennessee, which has abundant round pillars and smaller cyst plates but it is identified with the Catheys form; slides 299-82, Pl. 7, figs. 2a, b. L. pustulosa also occurs at the top of the Benson formation, Valley View, Ken- tucky, and in the Flanagan formation, at Frankfort, Kentucky, Labechia huronensis (Billings) 1G feu: Bs 1S Lh. 1p Stenopora huronensis Billings, 1865, Canadian Geol. Surv., Pal. Foss., vol. 1, p. 185. (U. Ord., Richmond, Cape Smyth, Lake Huron, Ont.) Not Alveolites granulosus, James, 1871, Cat. Foss., Cincinnati Group, p. 2. (U. Ord., Waynesville fm., Clarksville, Ohio) ; James, 1892, Jour. Cincin- nati Soc. Nat. Hist., vol. 15, p. 148, fig. 9. Type, Univ. Chicago, No. 2250, vertical section by Parks, 1910, pl. 22, figs. 6, 10 (12) =Stromatocerium granulosum (James). Tetradium huronense Foord, 1883, (part) Contr. Canadian Cambro-Sil. Micro- pal., vol. 1, p. 25, pl. 7, figs. 1, la. (U. Ord., Cape Smyth, Lake Huron, Ont.) Stromatopora subcylindrica James, 1884, Jour. Cincinnati Soc. Nat. Hist., vol. 7, p. 20, fig. 1. (U. Ord., Waynesville, near Morrow, Ohio.) Labechia ohioensis Nicholson, 1886, Palaeont. Soc., London, vol. 39, p. 31, 32, pl. 2, figs. 1, 2. (U. Ord., Waynesville, Ohio) ; 1886, Ann. and Mag. Nat. Hist., ser. 5; vol. 18, p. 13; pli 2) figs. 1,2: (U. Ord: (Cape ‘Smyth, Wake Huron, Ont.) Labechia montifera Ulrich, 1886, Contrib. N. Amer. Paleont., vol. 1, p. 33, pl. 2, figs. 9, 9a. (U. Ord., Madison, Ind.) (Description and figures of internal characters are based on a specimen from the U. Ord., Waynesville, Ohio) ; Cumings, 1908, 32nd. Ann. Rept. Geol. and Nat. Res. Indiana, p. 704, pl. 1, figs. 2, 2a, 2b. (U. Ord., Saluda fm., Osgood, Ind., and Waynes- ville, Ohio.) Labechia huronensis Whiteaves, 1897, Canadian Ree. Sci., vol. 7, p. 131. (U. Ord., Lake Huron and Lake Ontario, Ont.) ; Lambe, 1899, Ottawa Nat., vol. 13, p. 170. Stromatopora indianiensis James, 1892, Jour. Cincinnati Soc. Nat. Hist., vol. 15, p. 92, (U. Ord., Elkhorn fm., 5%4 mi. west of Connersville, Ind.) Labechia subcylindrica Parks, 1910, Univ. Toronto Studies Geol. Ser. No. 7, p. 27, pl. 23, figs. 3, 4, 6, 7. James’ type, from the Waynesville fm., Mor- row, Warren Co., Ohio, in Walker Mus., University of Chicago, No. 1199. Stromatocerium indianaense Foerste, 1916, Bull. Sci. Lab. Denison Univ., vol. 18, p. 302. Stromatocerium huronense Foerste, 1924, Geol. Surv. Canada, Mem. 138, p. 74, pl. 2; pl. 3, fig. 2 is a Stromatocerium. (U. Richmond, Cape Smyth, Manitoulin Island, Canada). Exterior —Coenosteum massive, hemispherical or conical, up to 27 cm. in diameter and 12 cm. high. The mamelons are small round, dome-shaped, 2 to 3 mm. high, 2 to 5 mm. in diameter and 5 to 8 mm. apart; the surface may appear smooth because the ORDOVICIAN STROMATOPOROIDEA N. AMER.: GALLOWAY & ST. JEAN 51 mamelons are covered with rock, or have been broken off. Papillae are variable, from 4 to 24 may occur in 10 mm., averaging 16 in 10 mm. Latilaminae are prominent, from 2 to 10 mm. thick, often separated by layers of mud. Specimens with mamelons 5 to 8 mm. in diameter and nearly as high, with large, round pillars which diverge in each mamelon, are L. macrostyla Parks. Vertical section— The coenosteum displays arched cyst plates and long pillars. There are seven to nine cyst plates in 2 mm. vertically, and two to four plates in 2 mm. horizontally. The cyst plates are composed of a thin outer, compact layer 0.02 to 0.05 mm. thick, a thick, secondary, flocculent lower layer, which is 0.10 mm. thick, or which may fill the entire cystose vesicle; the outer, flocculent layer is thin. The pillars vary from 0.2 to 0.3 mm. thick. Three to five pillars occur in 2 mm., they extend through several rows of cysts, and may be slightly curved. The pillars are composed of loosely aggregated, granular material which tends to be arranged in vertical rows. There is no outside wall on the pillars, and the pillars are not hollow as considered by Nicholson (1886b, p. 13). There may be mamelon columns through one or several latilaminae, but some specimens do not show mamelons in section. In some speci- mens there are groups of dividing and flaring pillars (Galloway, 1957, p. 393, pl. 36, fig. 9, slide 285-80), which we interpret as patho- logic not a taxonomic character. Tangential section—rThe pillars are round, of variable size, 0.15 to 0.4 mm. in diameter, and joined by the cyst plates in an irregular manner. The pillars have no walls and are not hollow. Some pillars join into stellate aggregates. Astrorhizae small, not us- ually developed. In poorly preserved specimens, the pillars and even the cysts may not be seen in the tangential section. Remarks —Labechia huronensis has been given many names, mainly because different authors could not recognize the species of Billings, and species were differentiated only by external shape. Much confusion also has resulted from descriptions based on speci- mens from widely spaced localities. For example, Ulrich (1886, p. 33) used a specimen from Madison, Indiana, to describe the external characteristics; and a specimen from Waynesville, Ohio, to describe and figure the internal characteristics of his L. montifera. Nicholson BULLETIN 194 WN bo (1886, p. 21) also named L. ohioensis for a specimen from Waynes- ville, Ohio. Later the same year, in another article, Nicholson (1886b, p. 13) based the description and figures of L. ohioensis on a specimen from Cape Smyth, Lake Huron, Ontario, which is a topotype of L. huronensis (Billings). This is the nearest to an authentic figure of L. huronensis (Billings) we know of. To add further confusion to the matter, Billings’ type is a composite, con- sisting of L. huronensis growing on a Tetradiwm, a condition not recognized by either Billings nor Foord (1883, p. 25) and first pointed out by Foord in Nicholson (1886b, p. 14). Billings’ type has apparently been lost; it is not in the Canadian Geological Survey Museum. Comparisons —L. huronensis has many small pillars, and smaller and more curved cysts than L. pustulosa (Safford) from the ‘Trenton. The pillars are frequently poorly preserved and it takes several slides to determine the shape of the pillars. L. macrostyla Parks has many large pillars, as well as large mamelons. L. huron- ensts differs from the Silurian species of Labechia in having smaller pillars. It is a typical Labechia and not Stromatoceriwm which has flat pillars. At the type locality it occurs with a Stromatocerium. The identity of L. huronensis is based on Nicholson’s figure of a topo- type furnished by Foord (1886b, p. 14, pl. 2, figs. 1, 2), and on a topotype collected and figured by Foerste (1924, pl. 2, fig. 2.) The pillars in Foerste’s specimen are abnormally large, up to 0.4 mm. in diameter, about as large as they are in L. macrostyla Parks, but the mamelons are smaller, and the pillars do not diverge in the mamelon columns. Occurrence.—Labechia huronensis occurs at the localities given in the synonomy. It also occurs commonly in the Waynesville at Waynesville, Morrow, Clarksville, and Wilmington, Ohio. We have specimens from the Upper Ordovician, Saluda, and Whitewater formations in Indiana, and it seems to be an index fossil of those horizons. It occurs in abundance at the damsite in Muscatatuck State Farm; in the Versailles State Park, Ripley County; in the Tri- County Quarry, northwestern Switzerland County, and three miles west of Madison, Jefferson County, all in Indiana. It is the most common of the stromatoporoids in the Richmond group. Specimens ORDOVICIAN STROMATOPOROIDEA N. AMER.: GALLOWAY & ST. JEAN 53 indistinguishable from L. huronensis occur in the upper Maysville at the old Agawam Station on the L. & N. R. R., Clark Co., Ken- tucky, slides 301-30, 31; 308-64, 65, 66, 67, 77, 78, 79. Topotype—Foerste’s specimen from Cape Smyth, Manitoulin Island, Geol. Surv., Canada, No. 5596, 3 slides; Indiana University Paleo. Coll., slides 308-96, 97. Hypotype, slide 299-33. Typical specimen, slide Nos. 278-20; 282-33, 99, 100; 285-47, 48, 49, 50, 73, 79, 80; 299-32-34, 38, 41, 96-100; 300-1, 2, 21, 22, 23, 24, 33, 34, 35. 36,57, 38, 39, 40, 41, 77, 78, °72, 80;-302-39, 40; 41;°308-1-6, S990; 91 92,93 94,95. Labechia macrostyla Parks Pl. 8, figs. la, b Labechia macrostyla Parks, 1910, Univ. Toronto Studies, Geol. Ser. No. 7, p. 25, pl. 22, fig. 12 (incorrectly numbered fig. 10); pl. 23, figs. 1, 2, 11. (“Lower Trenton Drift,’ Ann Arbor, Mich.) Exterior —Coenosteum massive, up to at least 10 cm. in length, composed of lJatilaminae, 5 to 10 mm. thick. Surface with large, dome-shaped mamelons, 6 to 10 mm. in diameter, 4 to 6 mm. high, and averaging 10 to 12 mm. apart from center to center. At the apex of each mamelon is a small astrorhiza, with three to six radiating grooves. The surface is covered with strong papillae, the ends of the pillars, which are larger on the mamelons, where they tend to coalesce; they are round and about 14 mm. in diameter in the depressions, and up to 4 mm. in diameter on the mamelons. Vertical section—Latilaminae, annual growth layers, are de- marked by a concentration of flocculent material and reduced, closely spaced cyst plates, and by layers of mud. Astrorhizae do not form vertical tubes in the mamelon axes. The mamelons are confined to a single latilamina at least where there are interruptions in growth, The skeleton is composed of small, arcuate, imbricating cyst plates and abundant, large, long, round pillars. The cyst plates number about 4 in 2 mm. horizontally and 8 to 10 in 2 mm. vertically. In the holotype the cyst plates seem to consist of only one plate, but in the paratype and in other specimens, the cyst plates have thin, compact, upper plates, and thicker, lower flocculent layers, with obscure lower boundaries. The pillars are large, 0.3 to 0.4 mm. in diameter, extending through many cyst plates, diverging in the mamelons and converging between mamelons, five or six in 2 54 BULLETIN 194 mm. The pillars have no definite outer boundaries, and are composed of gray, granular tissue, which tends to be arranged in vertical lines, much as if they were vertical rods and pores, probably layers of which the pillars are composed, but there is no axial canal (cf. Parks, 1910. p26): Tangential section—Obscure astrorhizal canals occur in the large mamelons. The cut cyst plates form an irregular reticulation, and the pillars are large, 0.2 to 0.4 mm. in diameter, abundant, mostly separated by one to two pillar diameters. The pillars are composed of granular bodies and have no definite boundaries, being fuzzy at the edges, show no indication of being hollow, but show indications of having had small, vertical pores and rods, A section across a mamelon, such as Parks’ figure (1910, pl. 22, fig. 10 [12 in error] ), will be oblique and will not show the shape of the pillars in transverse section. Comparisons.—L. macrostyla differs from L. huronensis, in the larger mamelons, larger pillars, and the divergence of the pillars in the mamelons. This species occurs with L. huronensis in the Rich- mond and differs mainly in having larger mamelons, more abundant, and larger pillars. The pillars are round, but where the large pillars converge and coalesce the resulting compound pillar may be mis- taken for the broad pillars of Stromatocerium. Occurrence.—We have several well-preserved specimens of this species from the late Richmond, Elkhorn formation, from Elkhorn Falls, four miles south of Richmond, Indiana, and from Huffman’s Dam, near Dayton, Ohio, and from the Whitewater formation, three miles west of Madison, Indiana. Typical examples occur in the Saluda formation one mile south of Milan, Indiana, and in the Waynesville formation in Ohio, but have not been reported from the Waynesville or Liberty formations of Indiana and Kentucky. It also occurs in the Leipers formation seven miles upstream from Ro- wena, Kentucky. It occurs in the Catheys formation of Nashville, ‘Tennessee. It is not represented in material from the Richmond of Escanaba River, Michigan. A typical specimen, silicified but showing all structures, was collected by Dr. R. H. Flower, from the Upper Ordovician of Lone Mountain, south of Silver City, New Mexico. It occurs abundantly in the Cynthiana formation, “Strom. Zone,” ORDOVICIAN STROMATOPOROIDEA N. AMER.: GALLOWAY & ST. JEAN 55 five miles southeast of Winchester, Kentucky. This species is un- usual because of its long stratigraphic range from Trenton to late Richmond, but there seems to be no difference between the forms in the different horizons. Lectotype-—“Lower Trenton Drift,” Ann Arbor Mich.; U.S. Nat. Mus., No. 36929A, slides NM1-9, 10, collected by Dr. Carl Rominger, designated as “type specimen” by Parks (1910, p. 26), and “beautifully preserved.” Lectoparatype, Parks pl. 23, figs. 2, 11, which is poorly preserved. Typical specimens—Indiana University Paleo. Coll., slides 282-59, 60; 301-25, 26, 27, 28, 29, 41, 42, 43, 44, 45, 46, 47; 302-3, 39° AW, 41." 308-14, 15; 16, 17. Genus STROMATOCERIUM Hall, 1847 Type species (monotypic), Stromatocerium rugosum Hall, 1847, Pal. New York, vol. 1, p. 48, pl. 12, fig. 2 (M. Ord., Black River gr., Watertown, N.Y.) ; Seely, 1904, Rept. State Geol. Vt., vol. 4, p. 144, pl. 70; pl. 74, fig. 5; Parks, 1910, Univ. Toronto Studies, Geol. Ser., No. 7, p. 8, pl. 21, figs. 3-7; Kuhn, 1928, Fossilium Catalogus, Hydrozoa, p. 47; 1939, in Schinde- wolf, Handbuch Palaozoologie, p. A 52, fig. 80; Galloway and St. Jean, 1955, Amer. Mus. Novitates, No. 1728, pp. 1-11, figs. 1-7 (holotype) ; Gallo- way, 1957, Bull. Amer. Paleont., vol. 37, No. 164, p. 431, pl. 33, fig. 3 (holotype). Coenosteum hemispherical, latilaminate, composed mostly of broad cysts, some short and arcuate; pillars long, platelike or with flanges, not round. Primitive astrorhizae may occur. Middle Ordovician, Black River, Trenton, and Cincinnatian, North America and Russia. Eight species. KEY TO SPECIES OF STROMATOCERIUM la. Pillars broad, thick, diameter 0.3 mm. Za. Surface without mamelonss rccecsenscssnsccseeeecen S. rugosum Hall 2b. Surface with large mamelons essen S. tumidum Wilson 1b. Pillars broad, thin, diameter 0.03 to 0.07 mm. 2c. Pillars with narrow flanges 3a. Pillars platelike, sporadic iti sans ty ak OP S. canadense Nicholson and Murie 56 BULLETIN 194 3b. Pillars irregular in shape, abundant 4a. Pillars small, without vacuoles cnr ct Me S. amsterdamense Galloway and St. Jean 4b. Pillars large, with vacuoles poh ee neta S. lerpersense Galloway, n. sp. 2d. Pillars with broad flanges 3c. Cyst plates mostly straight, not overlapping Leone eae S. michiganense Parks 3d. Cyst plates arched, overlapping S. granulosum (James) 2e. Pillars with few or no flanges Ze.) Pillars7m: tadial Oroupse. ween ects S. australe Parks 3f. Pillars not in radial groups Nes fees S. platypilae Galloway, n. sp. Stromatocerium rugosum Hall Pl. 8, figs. 2a bac Stromatocerium rugosum Hall, 1847, Pal. New York, vol. 1, p. 48, pl. 12, figs. 2, 2a, 2b. (M. Ord., Black River Is.. Watertown, N.Y.) ; Hitchcock, 1861, Proc. Boston Soc. Nat. Hist., vol. 7, p. 290, fig. 190; Chapman, 1861, Can- adian Jour., new ser., vol. 6, p. 508, fig. 72; 1864, Expos. Min. Geol Canada p. 102, fig. 72; Nicholson and Murie, 1878, Jour. Linn. Soc. Zool., vol. 14, p. 222, 223; Winchell 1886, Geological Studies, p. 321, fig. 223 (from Hall’s fig. 2b); Miller, 1889, North American Geol. Pal., p. 165, fig. 123; Lesley, 1890, Pennsylvania Geol. Sury., Rep. P4, vol. 3, p. 1102, text fig.; Whiteaves, 1896, Canadian Rec. Sci., vol. 7, p. 149; Seely, 1904, Rept. State Geol. Vermont, vol. 4, p. 144, pl. 70; pl. 74, fig. 5. (Ord., Isle La Motte, Vt.) ; Grabau and Shimer, 1909, N. A. Index Fossils, p. 46; Parks, 1910, Univ. Toronto Studies, Geol. Ser. No. 7, p. 11-15, pl. 21, figs. 3-7; Butts, 1926, Geol. Surv. Alabama, Spec. Rep. 14, p. 128, pl. 32, fig. 8; Wilson, 1948, Canada Geol. Surv. Bull. 11, p. 47, pl. 23, figs. 1-3; Shimer and Shrock, 1949, Index Fossils of N. A., p. 63, pl. 19, figs. 12, 13 (from Parks) ; Galloway and St. Jean, 1955, Amer. Mus. Nat. Hist., Novitates, No. 1728, 11 pp., 7 figs. (type specimen). Stromatopora rugosa d’Orbigny, 1849-1850, Prod. Paléont. Strat. Univer., p. 26; Chapman, 1863, Canadian Jour., new ser., vol. 8, p. 197, fig. 169; Billings, 1863, Geol. Surv. Canada, Rept. Prog., p. 140, fig. 72; Billings, 1865, Geol. Surv. Canada, Pal. Foss., vol. 1, p. 213; Nicholson and Murie, 1878, Jour, Linn. Soc. Zool., vol. 14, p. 195, fig. 1, (from Billings) ; Lesley, 1890, Geol. Surv. Pennsylvania, Rep. P4, vol. 3, p. 1108, text fig. (after Billings, 1863). Surface —Coenosteum hemispherical; the type is 120 mm. in diameter, 78 mm. high and is a fragment 30 mm. thick. Parks re- ported coenostea up to eight inches in diameter. Surface irregular but without mamelons or distinct papillae. Astrorhizae are not observable at the surface, although they are obvious on a smoothed ORDOVICIAN STROMATOPOROIDEA N. AMER.: GALLOWAY & ST. JEAN 57 surface. Undulatory latilaminae are distinct on a weathered surface, 2 to 4 mm. thick, and must have been the “rugae” Hall had in mind. The type specimen has been infiltrated with calcium carbonate, recrystallized, somewhat leached and in small part silicified, yet the structure can be satisfactorily made out. The chamber cavities are in part filled with clear, crystalline calcite, and in part filled with black, fine-grained, calcareous and carbonaceous material. ‘The structures are white in a dark background, the reverse as seen in most stromatoporoids. The specimens from Isle La Motte mentioned by Hall (1847, p. 48) as abundant and “completely silicified,” show no internal structure, as mentioned by Hall. Specimens from the solid limestone of Isle La Motte and elsewhere, are infiltrated with cal- cium carbonate and in part recrystallized, and structures can be seen satisfactorily. Vertical section— The skeleton consists mainly of broad cysts, which might be mistaken for laminae, some short, arcuate cysts, and long vertical pillars. The broad cyst plates are from 2 to 5 mm. broad, nearly flat, but are shown to be cyst plates rather than laminae, for they come down to the underlying cyst plates at the ends, and the cysts on two sides of the pillars frequently do not match. There are also narrow, arcuate cysts, 14 to % mm. broad. The cyst plates are close together vertically, 7 to 10 in 2 mm. The cyst plates are tripartite, the median plate 0.05 mm. thick and com- posed of clear, granular calcite; the upper and lower plates are each about half as thick as the median plate, and composed of dark, finely granular, and flocculent tissue. The pillars are long, extend through one or two latilaminae; the pillars are in general straight, but they branch, bend, and some join other pillars; they are irregular in distribution, varying from 2 to 6 in 2 mm. They are narrow or broad, depending on the direction in which they are cut; where cut through the thin part of the pillar, they have a thickness of 0.12 to 0.3 mm., and when cut the broad way, the breadth runs up to 1/2 mm. or more. The pillars consist of a median zone of light- colored, finely granular calcite, the recrystallized original material, and an outer zone of dark, granular and flocculent tissue, precisely like the upper and lower layers of the cyst plates. The median cyst 58 BULLETIN 194 plate in some places joins the median zone of the pillars. We consider it unlikely that pillars or median cyst plates were hollow. Neither astrorhizal canals, tubes, nor columns are apparent in vertical sections. Tangential section—The pillars radiate from the mamelon centers, with short astrorhizal canals between. The astrorhizal centers are from 7 to 10 mm. apart. The astrorhizal centers do not have vertical tubes. The pillars are vermicular, variable in thick- ness, curve, branch, and have short, spinelike flanges, and some few pillars tend to be round. The pillars have a normal thickness of about 0.27 mm., and a normal breadth of 1 mm., but range in breadth up to 4 mm. Some of the pillars are outlined by black rims; most of the pillars are white calcite, and the interspaces or chambers are filled with dark, fine-grained material. In the early part of the latilamina the pillars are thinner than normal. Comparisons —S. rugoswm is characterized by the broad cyst plates, and large pillars which radiate from the astrorhizal axes. S. rugosum has larger and broader pillars than any other species of the genus except S. tumidum. S. canadense may be the same species; it has thin, broad pillars. Occurrence.—S. rugosum occurs in the Middle Ordovician, Black River of Watertown, New York, Escanaba River, Michigan, and has been reported from northeastern New York, northwestern Vermont, Paquette Rapids, Ontario; specimens from other localities and hori- zons should have identifications checked, especially those from the ‘Trenton. It is remarkable that Seely (1904, pl. 74, fig. 5), and Parks (1910, pl. 21) correctly identified the species, considering that their specimens were not from the type locality, and neither had studied the type specimen. The above description is based on the holotype. Holotype-—Middle Ordovician, Black River limestone, Water- town, New York. American Museum of Natural History, specimen No. 590/5, and eight thin sections, 590/5, A to H. Stromatocerium tumidum Wilson Teale th, ac Stromatocerium rugosum tumidum Wilson, 1948, Can. Geol. Surv. Bull. 11, p. 47, pl. 23, fig. 3, (S. tumidum encrusting another stromatoporoid) ; ? figs. 6, 7, (M. Ord., Leray-Rockland beds, Paquette Rapids, Ottawa River, Ont.) Exterior —Coenosteum massive or tuberose. Surface with large, ORDOVICIAN STROMATOPOROIDEA N. AMER.: GALLOWAY & ST. JEAN 59 conical mamelons, 6 to 10 mm. in diameter, 5 to 10 mm. high, and 10 to 15 mm. apart from center to center. The surface of the type, and of a topotype we have sectioned, are silicified and so distorted by chalcedony in the form of beekite rings that smaller features have been destroyed; internally, the topotype has been in part silicified but the structures can be determined. Vertical section—The coenosteum is composed of latilaminae from 4 to 10 mm. thick. The skeleton is composed of thin, broad cyst plates, about 10 in 2 mm., and long, thick vertical pillars, about 5 in 2 mm. The cyst plates consist of a thin, dark, compact outer layer and a thick, flocculent, and moniliform lower plate. The earliest stage consists of arcuate cyst plates. The pillars are variable in thickness, 0.06 to 0.09 where cut the narrow way and up to 0.3 mm. where cut the broad way. Pillars have been infiltrated with calcium carbonate and recrystallized and now appear as clear calcite with no definite boundaries. Tangential section—Structures are obscure. The mamelons may have had astrorhizae. The pillars are thick and broad, as in S. rugoswm. Comparisons—The large mamelons are the diagnostic feature. Occurrence —S. tumidum occurs at the top of the Black River and base of the Trenton, Leray-Rockland beds, Paquette Rapids, Ottawa River, Ontario, the same horizon as other typical species of Stromatocerium. Topotype.—Part in the University of Cincinnati Museum, No. 22822, and part in the Indiana University Paleo. Coll., slides 299- 76; 302-31. Stromatocerium amsterdamense Galloway and St. Jean Pl. 8, figs. 4a, b Stromatocerium amsterdamense Galloway and St. Jean, in Galloway, 1957, Bull. Amer. Paleont., vol. 37, No. 164, p. 432, pl. 33, fig. 4. (M. Ord. Black River, Amsterdam, N.Y.) Exterior—Coenosteum massive; the incomplete holotype is 100 mm. wide, 70 mm. high and 30 mm. thick. Polished surfaces show low mamelons, 2 to 3 mm. in diameter and 8 to 10 mm. apart from center to center. Latilaminae are not well marked, 2 to 4 mm. thick. 60 BULLETIN 194+ Vertical section—The skeleton consists of thin, flat cyst plates, so flat and broad that they might easily be mistaken for laminae. The cyst plates are from % to 5 mm. broad, thin, 0.02 to 0.03 mm., and appear to have been composed of only one layer; there are about 12 cyst plates in 2 mm. Pillars are long, mostly narrow, but variable from 0.02 to 0.2 mm in width; they widen, narrow and branch up- ward, and number about 6 in 2 mm. The cyst plates and pillars have been infiltrated and recrystallized, so that no original tissue remains, ‘The cysts or interspaces are filled with dark, calcareous and appar- ently carbonaceous material, so that the appearance is the reverse of that of most stromatoporoids. Small low mamelons occur in the vertical section, but there are no mamelon tubes. Tangential section—The mamelons are conspicuous, marked by large vacuities, not astrorhizal tubes, but vacuities between lati- laminae, and by pillars radiating from the mamelon centers, which are from 4 to 8 mm. apart. Vague astrorhizal canals, shown in black, radiate between the pillars, but do not clearly branch. The pillars are in general flat and thin 0.03 to 0.05 mm. thick, oval, vermicular and irregular in shape, with numerous small flanges. Some of the pillars are outlined by black borders, perhaps the original outer boundary tissue; most of the pillars are indicated by white finely granular calcite, the reverse of the original condition, There is no evidence that the pillars or the cyst plates were hollow. Comparisons.—S. amsterdamense is characterized by the thin, broad cyst plates, and by the abundant small, thin, crooked and spiney pillars, as seen in tangential section. The cyst plates are also closer together, and the pillars are only one-fifth the breadth of those in S. rugoswm. Superficially, the two species are similar, even to color and preservation. Holotype——Upper Black River limestone, at the new lock just above Amsterdam, New York, Indiana University Paleo. Coll., No. 4629; slides 235-11, 12; 299-44-47. The type specimen was collected by Dr. E. R. Cumings in 1914. It also occurs in the basal Trenton at Crown Point, New York (slides 302-11-14). Stromatocerium canadense, Nicholson and Murie Pl. 9, figs. lla, b Stromatocerium canadense Nicholson and Murie, 1878, Jour. Linn. Soc. Zool., vol. 14, p. 223, pl. 3, figs. 9, 10. (M. Ord., Trenton ls., Peterborough, ORDOVICIAN STROMATOPOROIDEA N. AMER.: GALLOWAY & ST. JEAN 61 Ont) ; Parks, 1910, Univ. Toronto Studies, Geol. Ser., No. 7, p. 15, pl. 21, mikey (3 9 tol AA sate, lh Labechia canadensis Nicholson, 1886, Mon. Brit. Strom., ‘pl. 2, figs. 3-5; 1891, p. 163, pl. 20, fig. 9; 1886, Ann. Mag. Nat. Hist., ser. 5, vol. 18, p. 14, pl. 2, fig. 5 (Russian specimen.) Surface-—Coenosteum massive to laminar, some attached to other fossils. Surface with mamelons, 3 to 4 mm. in diameter, 4 to 6 mm, apart and 2 mm. high. On most mamelons there are three to five obscure, radiating grooves, qualifying as primitive astrorhizae. On and between the mamelons are prominent round papillae. Vertical section—There are prominent mamelons about 5 mm. apart. lhe skeleton consists mostly of broad, flat cysts, and of large, convex cysts in places. The cyst plates are tripartite, consisting of a median, thin, dark, compact layer, and outer, thin, light-colored, granular layer, and an inner, thick light-colored, flocculent layer. The cyst plates average about 8 in 2 mm. vertically. On the upper layer, in places, there are short, conical spines or denticles, In a few places the cyst plates are flat, close together, and without pillars of any kind. Pillars are unequally developed; mostly they are long and straight, some curved, mostly narrow, others broad, varying from none to 5 in 2 mm. The pillars are white and granular, obviously re- crystallized, with dark borders, hke the lower and upper plates of the cysts. Tangential section—Mamelons are indicated by concentric bands of cyst plates, and by radiating pillars; astrorhizae are ob- scure. [he pillars are flat, averaging about 0.07 mm. thick, and 1 to 3 mm. broad. The pillars are vermicular and irregular, they curve, branch and have short, spinelike flanges. Some of the pillars have dark rims. Comparisons—The specimens have been infiltrated with cal- cium carbonate, and most of the skeletal material has been re- crystallized. The chambers or galleries are filled with clear calcite. This form, as understood by Parks and by us, is a Stromatocerium, as first recognized by Nicholson and Murie, for the cyst plates are flat and the pillars are broad. The denticles on the outer plate are un- usual for Stromatocerium, but the structures emphasize the close relationship to the labechioid genera Cystostroma, Rosenella, Pseu- dostylodictyon, and Labechia. Vhe specimen from Girvan figured by 62 BULLETIN 194 Nicholson (Mono., pl. 20, fig. 9) is likely not this genus, but a Cystostroma. Nicholson gave no tangential section of this species, and we have been unable to study the type specimen. Nor did Parks (1910, p. 15), in numerous specimens, determine or figure the shape of the pillars, whether round or flat, with flanges or with- out. Our specimens have scattered pillars, and resemble Parks’ figures (1910, pl. 21, figs. 8, 9; pl. 22, fig. 1), and they also show flat pillars, much like the immature pillars of S. rugoswm (Galloway and St. Jean, 1955, pl. 10, fig. 6). Considering the poor preservation and the great variation in the species noted by Parks (1910, p. 16), it may be that this species is really S. rugoswm from the same hori- zon, showing irregular or injured growth and poor preservation. The sporadic pillars may not be a reliable character, because any species of Stromatocerium and Labechia may have places which show few or no pillars. Occurrence.—S. canadense occurs at the top of the Black River and Lower Trenton, originally from Peterborough, Coutchiching, and Paquette Rapids, Ontario; it has also been reported from New York, Michigan, Kentucky, and Tennessee. We have specimens from the Black River from Fort Cassin, Vermont, and from Chazy and Pattersonville, New York, and from the lower ‘Trenton from Escanaba River, Michigan and from the Cynthiana limestone, Cyn- thiana, Kentucky. Indiana University Paleo. Coll., slides 235-23; 299265" 30169 / Oe e721 See TA eG LO: Stromatocerium leipersense Galloway and Ehlers, n. sp. Pl. 9) figs. 2a, dD Exterior —Coenosteum a large head, 14 cm. in diameter and 6 em. thick. Surface nearly smooth, without mamelons or astrorhizae, but with abundant papillae, which are elongate and flanged, but not arranged in linear nor radial order. Astrorhizae absent. Vertical section—The skeleton is composed of straight or out- wardly convex and overlapping cyst plates and long pillars. There are about four cyst plates in 2 mm. horizontally, and about 10 in 2 mm. vertically. The cyst plates appear to be composed of only one thin layer; the chambers are filled with clear calcite or with dusty appearing calcite. The pillars are continuous and variable ORDOVICIAN STROMATOPOROIDEA N. AMER.: GALLOWAY & ST. JEAN 63 in size, from 0.1 to 0.2 mm. thick, and some appear to split into two branches, or may cut from one flange to another in the same pillar. The pillars have round or vertically elongate vacuoles, 0.04 to 0.1 mm. in diameter. The appearance of tubules in some pillars is prob- ably due to cutting a depression between two flanges. Tangential section—The pillars are irregular in size, 0.06 to 0.26 mm. thick and up to 0.6 mm. broad, irregular in shape with many short flanges. Each pillar has from one to six round vacuoles or tubules, averaging 0.05 mm. in diameter. There are also small round vacuoles outside the pillars, seen especially when the section is near the surface, and outlined by mud, in which case the vacuoles in the pillars are scarcely apparent. The pillars are arranged in hap- hazard manner and show no indication of astrorhizae nor mame- lon columns. Comparison —The pillars of this species resemble those of S. amsterdamense, but they are larger, not arranged in radial lines, and have vacuoles. Holotype.—A single specimen in the University of Michigan Paleontological Collections, No. 39500, Leipers formation, from the bank of the Cumberland River, opposite the downstream end of Belk Island, about seven miles upstream from Rowena, Kentucky, collected by Dr. G. M. Ehlers. Slides 01-15, 16, 17. Indiana Uni- versity Paleo. Coll., slides 308-80, 81, 82. Strematocerium michiganense Parks Veils G), also Bel, 10) Stromatocerium michiganense Parks, 1910, Uniy. Toronto Studies, Geol. Ser., No. 7, p. 9, pl. 21, figs. 1, 2. (M. Ord., “Lower Trenton Drift” of Ann Arbor, Michigan.) Exterior—The type specimen, U. S. Nat. Mus., 56843, is now only a slab, 55x 38x 6 mm., polished on both sides. It has grown on and was overgrown by Labechia macrostyla. It 1s inconspicuously latilaminate, but there are no indications of monticules nor astror- hizae. The specimen is strongly infiltrated by calctum carbonate, the cysts and pillars recrystallized, but their shapes are well pre- served, Vertical section—-We have made three good sections of the holotype, one vertical and two tangential sections. The cyst plates are thin, 0.03 to 0.06 mm. thick, and composed of only one layer. 64 BULLETIN 194 They are convex and overlapping or flat betweeen the pillars. There are six to eight plates vertically and up to four cyst plates hori- zontally in 2 mm. The pillars are long, thin where cut the narrow way, 0.07 to 0.10 mm. thick, and two to six times that thickness where cut the broad way. There are about four to six pillars in 2 mm. The pillars are composed of finely granular calcite, with thin, dark borders. Both cyst plates and pillars have been recrys- tallized. The cysts are smaller and closer together at the base of each latilamina, There are no indications of mamelon axes nor of astrorhizae. Tangential section—tThe pillars are thin, 0.07 to 0.09 mm., and broad, about 0.3 mm., branched so that the arms come together, making polygonal figures 0.3 to 0.4 mm. across, with frequent branches extending into the polygons, remindful of the figures made by the corallites and septa in Tetradiwm, but the polygons of the present species are not corallites. The flanges of the pillars branch at about 120°, and in places the flanges do not meet, as shown by Parkse(1910. ple 21 ttre. 2). Comparisons—This species differs from others of the genus in the broad flanges of the pillars. It cannot be substituted as the type of Stromatocerium (Parks, 1910, p. 10), since S. rugoswm Hall, 1847, is the monotypic type, and it is now well understood. The age of the only specimen known is in doubt, particularly as the type is intergrown with Labechia macrostyla, which occurs also in many places in the late Richmond. Stromatocerium is largely confined to the Black River and lower Trenton. 1'ype.—The holotype and only known specimen was collected by Dr. Carl Rominger from the lower Trenton Drift of Ann Arbor, Michigan. It should be looked for around Peterborough, Ontario, in the Trenton, where Nicholson and Murie found Stromatocerium canadense. U. S. Nat. Mus. No. 56843. Slides NM1-6, 7, 8. Stromatecerium australe Parks Pl. 9, figs. 5a, b Stromatocerium huronense var. australe Parks, 1910, Univ. Toronto Studies, Geol. Ser., No. 7, p. 24, pl. 22, fig. 11. (U. Ord., Leipers fm., Nashville, Tenn. Type U. S. Nat. Mus., No. 49507.) Stromatocerium huronense australe Foerste, 1916, Bull. Sci. Lab. Denison Univ., vol. 18, p. 302. ORDOVICIAN STROMATOPOROIDEA: N. AMER.: GALLOWAY & St. JEAN 65 Exterior—Coenosteum massive, nodular, 7 cm. in longer di- ameter, Surface rough with adherent rock debris, showing mamelons in places, 5 mm. in diameter, 10 to 12 mm. apart; in places showing elongate pillars. The latilaminae are scarcely discernible; astrorhizae were not observed. Vertical section—The skeleton is well preserved for Ordo- vician forms, by infiltration of calcium carbonate. The skeleton consists of irregular arcuate cyst plates, many of which are fairly straight between pillars. The cyst plates consist of thin, dark, median plates with lower and upper thin granular plates. The pillars are mostly close together, about 4 in 2 mm. in the columns; be- tween the columns the pillars are scarce. The pillars are mostly thin, 0.05 mm.; others, which are cut obliquely near the broad way, are much thicker and look hollow, as noted by Parks (1910, p. 24) due to lack of original calcification, as is true of the pillars of many Ordovician forms. Langential section—There are mamelon columns, 4 to 8 mm. in diameter, composed of 12 to 24 radiating flat pillars, between which there are close cysts, part of which are curved inward toward the center of the column, part of which join each other, and part of which are fairly straight. The pillars have few flanges, and are from 0.1 mm. to 0.15 mm. in thickness, with irregular edges. Some of the pillars branch a few times. There appears to be no substance in the pillars other than crystallized calcite. The radiating columns show no indications of astrorhizae nor of an axial tube. Comparisons —This species is a real Stromatocerium as shown by the broad pillars. It is one of the better characterized species, but whether it is a variation of Labechia huronensis remains to be demonstrated. It is not unique in the variation in the number of pillars in different parts of the coenosteum; many Ordovician forms of Stromatocertwm and Labechia have a variable number of pillars which Parks took to be a principle characteristic of his variety, stating that the pillars, “appear to be hollow and which fail entirely in many parts of a section, leaving vesicular tissue only,” (1910, p. 24). Although we have many specimens of Stromatocerium from the Ordovician, including other specimens from the Leipers formation, this is the only specimen of S. australe we have seen, The flat pillars radiating from centers is an important characteristic, but does not 66 BULLETIN 194 occur in Labechia huronensis, which has round pillars, not flat, as considered by Parks, (1910, p. 23). The other specimens enumerated by Parks at the end of his original description of S. australe, most of which we have studied, belong to other genera and species, having no more in common than the variation in the number of pillars. L’ype and occurrence.—Although Parks did not designate a type specimen, the only specimen figured is a vertical section of U.S. Nat. Mus., No. 49507, middle Cincinnatian, Nashville, Tennessee. That specimen was designated as the “Holotype” by Bassler (1915, p. 1213), and its age determined as Maysville (Leipers). The above description is drawn entirely from that specimen, of which we have five thin sections, three in the U.S. Nat. Mus., and Nos. 309-37, 38, in Indiana University Paleo. Coll. Stromatocerium granulosum (James) Pl 9, figs: 44, ) Alveolites granulosus James, 1871, Cat. Foss. Cincinnati Group, p. 2. (U. Ord., Waynesville fm., Clarksville, Ohio); 1892, Jour. Cincinnati Soc. Nat, Hist.,. voli 15. pi 148s figs 9). Stromatocerium huronensis Parks (part), 1910, Univ. Toronto Studies, Geol. Ser., No. 7, p. 20, pl. 22, figs. 6, 9, 12 (error for 10). James’ type of Alveolites granulosus. Exterior—Coenosteum massive; surface with low mamelons, 4-5 mm. in diameter and 10-12 mm. apart from center to center. Latilaminae are 4 to 8 mm. thick, Astrorhizae are present but ob- scure. [he description is drawn from a topotype similar to James’ type. Vertical section—The skeleton is composed of thin, convex, overlapping plates and thin pillars, much as in Labechia huronensis, for the thin, flat pillars are rarely cut to show their breadth. There is no outer plate, and the inner plate is obscure. Langential section—Some of the pillars are flat, with minute flanges, and radiate from the center of mamelons, as shown by Parks, (1910, pl. 22, fig. 12); many pillars have three radiating branches, others have broad flanges and join, making odd-shaped polygons or figures. Comparisons—This species has been confused with, and its characteristics have been attributed to, Labechia huronensis which has round pillars and which occurs higher in the Richmond. It differs from S. michiganense in having smaller pillars, with both ORDOVICIAN STROMATOPOROIDEA N. AMER.: GALLOWAY & ST. JEAN 67 broad and narrow flanges, and, in vertical section, the plates are arched and overlap. Occurrence and types——So far known only from the Waynes- ville formation near Clarksville, Ohio. The type is in the Walker Mus. Univ. of Chicago, No, 2250. A topotype, from the Fort Ancient member of the Waynesville formation, from Penquite Run, two mi. southwest of Clarksville, Ohio, from which the above description is largely drawn, is in the Mus. Paleont., University of Michigan, No. 7774, slides 01-18, 19, and a piece of the topotype in the Indiana University Paleo. Coll., slides 308-18, 19, 84, 85, 86. Stromatocerium platypilae Galloway, n. sp. Pe On ie setaseb Exterior —Coenosteum a large head, at least 16 cm. in diameter, composed of thick latilaminae up to 15 mm. in thickness, well pre- served by infiltration of calctum carbonate. The base is not pre- served. Surface fairly smooth without mamelons, papillae or as- trorhizae. Vertical section—The skeleton is composed of slightly up- arched cysts, which are thin, with thin median, lower, and upper plates. The cysts are larger and farther apart than in almost any other species of the genus, four or five in 2 mm., tending to be arranged edge to edge but many overlap subjacent cysts, Cutting through the cysts are fairly straight, flat, and thin vertical pillars. The pillars show a clear white line in the middle or on one side. The pillars number four or five in 2 mm., varying in distribution. The resulting frail skeleton had partly collapsed before fossilization, as shown at the upper left of Plate 10, figure la. Tangential section—The cysts make a pattern of oval figures, or make curved lines which show the dark median layer and the upper and lower layers. Cutting through the section in no readily apparent order, are the thin vertical pillars. They mostly show a median white layer, which is not a geometric line but is variable in width. The pillars cut through the cyst plates and join each other at various angles. There is no radial pattern nor suggestion of astrorhizae. The pillars are thin, about 0.03 mm., although they are not parallel-sided. 68 BULLETIN 194 Comparison.—This species is a typical Stromatoceritum, and the thin flat pillars distinguish it at once from other species of the genus. It lacks the flanges on the pillars of S. michiganense. Holotype—This type specimen was collected by Frank H. Walker, of the Kentucky State Geological Survey, Liberty formation, near Highway 30, 2% miles northwest of Owingsville, Bath County, Kentucky. Indiana University, slides 308-20, 21, 68, 70, 71, 72, 73, 74. 78. Genus DERMATOSTROMA Farks, 1910 Type species (originally designated), Stromatopora papillata James, 1878, The Paleontologist, No. 1, p. 1 (U. Ord., Maysville gr., Cincinnati, Ohio). Dermatostroma Parks, 1910, Univ. Toronto Studies, Geol. Ser., No. 7, p. 29, pl. 23, figs. 8-10; Foerste, 1916, Bull. Sci. Lab., Denison Univy., vol. 18, P2297, Dine hives: Coenosteum laminar, encrusting foreign objects, 1-10 mm. thick and up to 10 cm. in diameter, consisting of several, irregular, undu- lating laminae, with oval chambers, the D. papillatum group, or of prisms, D. ? corrugatum group, or of clear calcite crystals with no recognizable organic structure, D. costatwm group. Pillars large, conical, with lumina but not hollow, extending from peritheca to surface, and some short, small, solid pillars, or pillars absent. ‘Tangential sections show round pillars becoming polygonal at their bases; tissue compact. Surface papillate, without or with small monticules, or weathered smooth. Astrorhizae unknown. Ordovician, Black River to Richmond. North America. Thirteen species. ‘The surface of typical species resembles that of Labechia, as do the strong pillars, but the skeleton is not definitely cystose. The second group, D. ? corrugatum, D. ? glyptwm, and D. ? escana- baense, has radially crystalline prisms and has no internal charac- acteristics of typical Dermatostroma. The third group, that of D. costatum, shows no internal structure, but a thin, structureless layer of crystals of calcite, The forms assigned to Dermatostroma agree in being a thin encrustation, generally attached to other organisms, and in having papillae. They are not typical stromatoporoids. ORDOVICIAN STROMATOPOROIDEA N. AMER.: GALLOWAY & ST. JEAN 69 KEY TO SPECIES OF DERMATOSTROMA la. Coenosteum composed of laminae and pillars; surface papillate 2a. Surface papillate but not monticulate. 3a. Pillars long (Cincinnatian ) 4a. Papillae wnitorin, es ccceccsc D. papillatum (James) 4, Papillae: variable: chncccaesenn-cn D. diversum Parks 3be Pillars short-( Isrenmtom))) cescscec: D. cavernosum Parks 2b. Surface monticulate and papillate 3c. Monticules 2 mm. in diameter .....D. scabrum (James) 3d. Monticules 4 mm. in diameter...D. canaliculatum Parks 1b. Coenosteum composed of prisms; surface papillate 2c. Prisms 0.4 to 0.8 mm. in diameter 3e. Surface without sharp, vermiform ridges, aera D. ? corrugatum (Foerste ) 3f. Surface with sharp, vermiform ridges abe Me ace D. ? glyptum (Foerste) 2d. Prisms 0.2 to 0.4 mm. in diameter ea ape eee D. ? escanabaense Galloway & Ehlers, n. sp. lc. Coenosteum one or more wrinkled laminae lying on polygonal crystals of calcite; surface papillate 2e. Surface costate Ser RCOstae jWiChOut sNOGUlES: , Radial, longitudinal section, X 10, cutting a radial zone of cysts, showing their large size and hemispherical form. Same speci- men as for fig. 3a. Slide 299-90. Unretouched. . Oblique tangential section, X 10, showing round cysts, dark, compact outer plate and inner, thick moniliform plate, open chambers, and absence of pillars. Same specimen as for fig. 3a. Upper Ordovician, Vauréal fm., Battery Cliff, Anticosti Is., Can. Canadian Geol. Surv., No. 2583, marked “TYPE”. Indiana University Paieo. Coll., slide 299-90. Retouched. 30 9 v LATE P 43 VOL AMER. PALEONT., BULL BULL. AMER. PALEONT., VOL. 48 PLATE 4 tne St ee Figure il ORDOVICIAN STROMATOPOROIDEA N. AMER.: GALLOWAY & ST. JEAN Explanation of Plate 4 Aulacera radiata Galloway and St. Jean, n. sp. ........2-2-------2000------ : a. Cross section of holotype, X 10, showing a ray of cysts little different from cysts between rays, a few pillars in the ray, small cysts with low plates of flocculent tissue nearly filling the chambers, and latilaminae separated by calcite with pseudo- pillars, denoting imperfect calcification in life. Specimen 702A, Mus. Comp. Zoo]., Harvard University, slide 302-70. Retouched. b. Vertical, radial section of holotype, X 10, cut between rays, showing latilaminae of small cysts, without pillars, the lati- laminae separated by layers of calcite with pseudopillars. Specimen 702A. Richmondian, Anticosti Is., Can. Harvard Uni- versity Paleo. Coll., slide 308-55. Unretouched. AMAcCemA NOdn OR! CBillines)) 22 xe a Ne ee Se Pee a. Cross section of topotype, not well preserved, X 10, showing a mamelon, latilaminae, small, low cysts and scattered, poorly preserved pillars. Indiana University Paleo. Coll., slide 299-85. Retouched. b. Cross section, nearer the center than fig. a, X 10, showing curved cysts but no pillars. Same specimen as for fig. a. Upper Ordovician, Vauréal fm., Battery Cliff, Amnticosi Is., Can. Loaned by Canadian Geol. Surv., No. 1917. Indiana University Paleo. Coll., slide 299-86. Retouched. Anlacéranodulitera’ (hoerste) 2050.28... 32s See a. Cross section of hypotype, X 10, showing large cysts rising into the nodes, but no pillars. Richmondian, Anticosti Is.. Mus. Comp. Zool. Harvard University. Fragment in Indiana University Paleo. Coll., and slide 302-67. Retouched. b. Cross section of hypotype, X 10, poorly preserved, showing cysts and a few strong pillars. Vauréal fm., Battery Point, Anti- costi Is., Can. Peabody Museum, Yale University, No. 9200B. Collected by W. H. Twenhofel. Indiana University Paleo. Coll., fragment and slide 302-73. Retouched. AUlacera intermedia: (CHoenste) 2... =o ee Ea Cross section of hypotype, X 10, showing inner curved cysts without pillars. The outer cysts were incompletely calcified in life. Lower Liberty fm., 2 miles southwest of Deatsville, Ky., collected by Ruth G. Browne, Louisville, Ky. Indiana University Paleo. Coll., RB18, slide 308-11. Unretouched. 93 34 36 9+ Figure il eo BULLETIN 194 Explanation of Plate 5 Aulacera® cylindrica-:(Poerste) — 2-3... eee a. Vertical section of hypotype, X 3, showing axial column which is not a tube, large axial cysts, small lateral cysts which are incompletely calcified, and lack of pillars. Basal Liberty, 2 miles southwest of Deatsville, Ky., collected by Ruth G. Browne, RB69. Indiana University Paleo. Coll., slide 308-32. Retouched. b. Cross section of small specimen, X 3, showing gradation of larger cysts into small ones, and lack of pillars. RB68. Same locality and collector as for 3a. Indiana University Paleo. Coll., slide 302-74. Retouched. Pseudostylodictyon ? lamottense (Seely) .....000...00000eccceeeeee eee a. Vertical section of one of Seely’s syntypes, X 10, showing wavy latilaminae separated by mud, the irregular laminae, without denticles, corrugations or pillars. Indiana University Paleo. Coll., slide 301-61. Retouched. b. Vertical section of the same specimen, X 3, to show irregular latilaminae separated by calcareous and carbonaceous mud and thin laminae. Middie of B Chazy, Goodell’s Quarry, Isle La Motte, Vt., collected by H. M. Seely, 1885. Indiana University Paleo. Coll., slide 301-60. Retouched. Pseudostylodictyon *‘eatoni “(Scely)* = = a. Weathered surface of holotype, X 2/3, showing mamelons of various sizes. Same specimen as figured by Seely (1904, pl. 71). Upper or C Chazy, Goodell’s Ridge, south of Isle La Motte, Vt. Unretouched. . Vertical section of holotype, X 10, showing a mamelon, regular laminae with thin upper layer and thick, flocculent and monili- form lower layer, and lack of wrinkled laminae. Indiana Uni- versity Paleo. Coll., slide 301-58. Retouched. — eS Pseudostylodictyon ? Kayi Galloway and St. Jean 200... a. Vertical section of holotype, X 10, showing a mamelon and eruption of several laminae, regular laminae with upper, thin, dark layer and lower, thick flocculent layer, and some wrinkled laminae. The laminae are separated into groups with clear calcite between, apparently due to noncalcification of laminae in life. Middle Chazy, 1 mile southeast of Isle La Motte village, Vt. Collected by Marshall Kay. Indiana University Paleo. Coll., KA1, slide 300-21. Retouched. Tangential section of holotype, showing rings where the section cuts the wrinkles of the laminae, and flocculent laminae. Same locality, collector and depository. Slide 300-24. Retouched. b. 40 41 42 5 ATE PL 43 ., VOL. PALEONT ER BULL. AM BULL. AMER. PALEONT., VOL. 43 PLATE 6 a ee y (3 a <= Ct) 7 tx ee 542 Re Figure 1. Pseudostylodictyon ? kayi Galloway and St, Jean ORDOVICIAN STROMATOPOROIDEA N. AMER.: GALLOWAY & ST. JEAN Explanation of Plate 6 a. Vertical section, paratype, X 10, showing regular, wrinkled laminae. Middle Chazy, “Fleury” Quarry, 1 mile southeast of Isle La Motte village, Vt. Collected by Marshall Kay, Indiana University Paleo. Coll., KA5, slide 300-20. Unretouched. b. Vertical section from the some specimen as for la, X 10, showing groups of laminae separated by calcite and few wrinkles; slide 300-19. Retouched. Pseudostylodictyon ? chazianum (Seely) —..................-2-...-------------- a. Vertical section of one of Seely’s syntypes, X 10, labeled “A Chazy, South Hero, Vt.,” although Seely’s description (1904, p. 148) stated “B Chazy.”’ Largely silicified, shows thin laminae. Indiana University Paleo. Coll., slide 301-63. Retouched. b. Vertical section of hypotype from near the type locality, X 10, showing the thin laminae, lack of corrugations, denticles, cysts, or pillars. Middle Chazy, Maclurities beds, South Hero, %4 mile west of Route 2, Grand Isle Co., Vt. Collected by Marshall Kay, Indiana University Paleo. Coll., KB1 and slide 300-30. Unre- touched. Pseudostylodictyon ? montoyaense Galloway, n. sp. -...........-------- a. Vertical section of holotype, X 10, showing regular laminae, wrinkled laminae, and denticles. Slide 308-22. Unretouched. b. Tangential section of holotype, X 10, showing cut laminae and denticles; wrinkles are more common than usual. Upper Ordovician, Montoya gr., Upham fm., crest of Scenic Drive, El Paso, Texas. Collected by R. H. Flower, 1958. Part in New Mexico Inst. Min. Tech., No. S6, and slides, part in Indiana University Paleo. Coll., and slide 302-23. Unretouched. Rosenella cumingsi Galloway and St. Jean, n. sp. -....W..----- a. Vertical section of holotype, X 10, showing irregular develop- ment of cysts and wrinkles and denticles on the thin cyst plates. Middle Ordovician, upper Black River, new lock above Amsterdam, N.Y. Indiana University Paleo. Coll., slide 300-84. Unretouched. b. Vertical section of paratype, X 10, showing the same features. Lower Trenton, Rockland fm., % mile west of bridge, Crown Point, N.Y. KG1, Indiana University Paleo. Coll., slide 302-4. Unretouched. 95 43 44 96 Figure il; bo Co BULLETIN 194 Explanation of Plate 7 Labechia) pustulosa, (Safford): 225 ee ee a. Vertical section of topotype, X 10, showing thick, low cysts and vertical, calcite streaks where the pillarg had been, Lower Catheys formation, Tennessee Central Railroad Station, Nash- ville, Tenn. Collected by C. W. Wilson, Jr., 1954. Indiana Uni- versity Paleo. Coll., slide 302-83. Unretouched. b. Tangential section, X 10, of the same specimen, showing cysts and obscure, large round pillars. Slide 302-82. Retouched. Labechia pustulosa (Safford)) 23) eee a. Vertical section of hypotype, X 10, showing the low cysts with thin upper plate and thick flocculent and moniliform lower plate, (the plates are smaller than those of the topotype), and abundant, large pillars replaced by calcite but leaving the out- side rim in places. Cannon ls., Flat Rock on Nolensville Pike, southwest of Nashville, Tenn. Part in Vanderbilt University Paleo. Coll., part in Indiana University Paleo. Coll., slide 299-83. Unretouched. b. Tangential section, X 10, of same specimen, showing a mamelon, thick cysts, and many round pillars, some with darker rim. Slide 299-82. Unretouched. Labechia huronensis (Billitgs) — a. Vertical section of hypotype, X 10, showing typicai, thin, curved cyst plates with lower, poorly defined, flocculent plate, and typical small, long, straight pillars which have vague, vertical rods and no definite outer boundary. Whitewater fm., Muscata- tuck State Farm, Ind., Indiana University Paleo. Coll., slide 299-33. Unretouched. . Tangential] section, X 10, of same specimen, showing numerous small pillars which tend to be round but without definite boundaries. Slide 299-63. Unretouched. ~ ~ Labéechia huronensis, (Billings)) 2 ee a. Vertical section of topotype, X 10, showing small, thin, arched, overlapping cyst plates, and large, straight and loose-textured pillars which are not hollow. Upper Richmond, Meaford fm., Cape Smyth, Manitoulin Is., Can. Specimen figured by Foerste, 1924, pl. 24, fig. 2. Canadian Geol. Surv., No. 5596. Indiana University, slide 308-96. Unretouched. b. Tangential section, same specimen, X 10, showing large round and coalescent pillars, which are loose-textured but not hollow, and joined by the cyst plates, simulating radial arms of pillars of Actinostroma,. Slide 308-97. Unretouched. 47 50 50 BULL. AMER. PALEONT., VOL. 43 PLATE 7 PLATE 8 BuLL. AMER. PALEONT., VOL. 43 we DES 1 ORE ORDOVICIAN STROMATOPOROIDEA N. AMER.: GALLOWAY & ST. JEAN 97 Explanation of Plate § Figure Page ieabechianmacrostyla “Parks 2s.) iene Sie 53 a. Vertical section of lectotype, one of Parks two syntypes, x 10 showing two latilaminae, cne mamelon, thin, curved, over- lapping plates, and large pillars, some confluent with variable texture. “Lower Trenton Drift,’ Ann Arbor, Mich. U. S. Nat. Mus., No. 36929A, slide NM1-9. Unretouched. b. Tangential section of the same specimen, X 10, showing large pillars of granular texture, some confluent, many joined by curved cyst plates, slide NM1-10. Unretouched. oy SStromatoceriom= CUSOSum Hall 0.0 8. A= Ae ee ene 56 a. Vertical section of holotype, X 6.7, showing broad, slightly curved cyst plates, and long thin pillars where cut the narrow way and broader pillars where cut the broad way. Middle Ordovician, Black River, Watertown, N. Y. Amer. Mus. Nat. Hist., slide No. 590/5B. Unretouched. b. Tangential section of same specimen, X 6.7, showing mature, thick, broad pillars in white, in radial arrangement, but no definite astrorhizae; slide 590/5C. Retouched. c. Tangential section, same specimen, X 6.7, showing immature, thin, broad pillars in white, radially arranged, but no astro- rhizae; slide 590/5C. Retouched. Je stromatocerium: tuniidum: ‘Wilson <..-!2 2.05 eee ce 58 Vertical section of partly silicified topotype, X 10, showing remnants of cyst plates and pillars, and mud between lati- laminae. Middle Ordovician, Black River, Paquette Rapids, Ottawa R., Can. Univ. Cincinnati Museum, No. 22822; Indiana University, slide 299-76. Retouched. 4. Stromatocerium amsterdamense Galloway and St. Jean ........... 59 a. Vertical section of holotype, X 10, showing thin, broad cyst plates which approach laminae and long thin pillars with spurs. Upper Black River limestone, Amsterdam, N. Y. Indiana University Paleo. Coll., No. 4629, slide 235-11. Retouched. b. Tangential section, same specimen, X 10, showing a mamelon with radiating pillars; the pillars are small, irregular in shape, with many small flanges. Slide 299-47. Retouched. 5 98 Figure il De BULLETIN 194 Explanation of Plate 9 -Stromatocerium canadense Nicholson and Murie _.......................... a. Vertical section of hypotype, X 10, showing broad, thin cyst plates and thin pillars which are sporadic in occurrence. Middle Ordovician, top of Black River, Pattersonville, N. Y. Indiana University Paleo. Coll., slide 235-23. Unretouched. b. Oblique tangential section of same specimen, X 10, showing a mamelon with radial, thin, broad pillars with small flanges. The cyst plates are broad, thin and many have denticles on the upper side. ‘Slide 299-65. Unretouched. Stromatocerium Jeipersense Galloway and Phlers, n. sp. ........--. a. Vertical section of holotype, X 10, showing small, arcuate cyst plates, long pillars of variable size, and small, round vacuities in the pillars. Upper Ordovician, Leipers fm., opposite Belk Is., 7 miles upstream from Rowena, Ky. Mus. Paleont. Uni- versity of Michigan, No. 39500. Indiana University, slide 308-80. Retouched. . Tangential sections of Same specimen, X 10, showing irregular flanged pillars outlined by mud at left, and irregular pillars with many round vacuoles at right. Slide 308-81. Retouched. — So Stromatocerium michiganense Parks —..............22000--02..-....e.. a. Vertical section of holotype, X 10, showing curved and flat cyst plates, and long, straight mostly thin pillars, both outlined by dark material. Middle Ordovician, lower Trenton, from glacial drift, Ann Arbor, Mich. U. S. Nat. Mus., No. 56843; slide MNI-6. Unretouched. b. Tangential section of same specimen, X 10, showing broadly flanged, narrow pillars, which meet, forming polygons, and absence of mamelons and astrorhizae. Slide NMI-7. Retouched. Stromatocerium australe Parks 2.2.22.) ee a. Vertical section of type specimen, X 10, showing thin pillars and close cyst plates in a mamelon. Upper Ordovician, Leipers fm., Nashville, Tenn. U. S. Nat. Mus., No. 49507; Indiana Uni- versity Paleo. Coll., slide 309-37. Unretouched. b. Tangential section of same specimen, X 10, showing thin radi- ating pillars with few flanges, and thin, irregular, branching pillars between columns, where pillars are usually lacking. Indiana University Paleo. Coll., slide 309-38. Unretouched. Stromatocerium granulosum (James. .......--.-.0.0.0-2222c2-:ccceccceeeeeeeeeeeee ees a. Vertical section of topotype, X 10, showing arched cyst plates and thin plates and thin pillars. Upper Ordovician, Fort Ancient mem., Waynesville fm., Clarksville, Ohio. Mus. Paleont. Uni- versity of Michigan, No. 7774, slides Ol-18, 19; part in Indiana University Paleo. Coll., slide 308-18. Retouched. . Tangential section of same specimen, X 10, showing platelike pillars with large and small flanges. Slide 308-19. Retouched. — =) 62 63 64 66 PLATE 9 BULL. AMER. PALEONT., VOL. 48 Cae iy ett iy. aS SEL rae RR AS nae BULL. AMER. PALEONT., VOL. 48 PLATE 10 ORDOVICIAN STROMATOPOROIDEA N. AMER.: GALLOWAY & ST. JEAN 99 Explanation of Plate 10 Figure Page 1. Stromatocerium platypilae Galloway, n. sp. —....0-202 67 a. Vertical section of holotype, X 10, showing the large cysts with three thin plates, the thin, long, straight, rarely branching, vertical pillars, without flanges, mostly with a thin, median white line. Upper Ordovician Liberty fm., 2% miles northwest of Owingsville, Ky. Indiana University Paleo. Coll., slide 308-70. Retouched. b. Tangential section of same specimen, showing the cyst plates with thin, dark line, and the flat or curved pillars with median white line; the pillars do not have flanges, but the white, median line is minutely variable in width. Indiana University Paleo. Coll., slide 308-68. Retouched. 2. Dermatostroma secabrum (James) ............22..222.222.022.20e-22ee eee eeee eee 69 a. Vertical section of typical specimen, X 10, attached to Escharopora pavonia. Upper Ordovician, Leipers fm., Mt. Parnassus, Columbia, Tenn. Miami University, No. 821. Indiana University, Paieo. Coll., fragment and slide 302-10. Retouched. b. Tangentia] section of same specimen, X 10, showing mamelons by lighter color and cut laminae, and round pillarg with dark ring and light center. Same slide. Unretouched. 3. Dermatostroma ? corrugatum (Foerste) 2.000000... (ial a. Vertical section of topotype, X 10, showing the contiguous prisms of fibrous, feathery calcite, with the fibers diverging upward, darker in places, and lack of laminae, pillars, cysts, galleries or tissue of typical Stromatoporoidea. Upper Ordovi- cian, Whitewater fm., Wilmington, Ohio. Coll. by W. H. Shideler, Miami University. Indiana University Paleo. Coll., fragment and slide 308-98. Unretouched. b. Tangential section of same specimen, X 10, showing mamelons? prisms, with radiating fibers, darker in places. Slide 308-98. Unretouched. 4. Dermatostroma ? glyptum (Foerste) —_. 2... eee eee 7 a. Vertical section of topotype, X 10, showing three layers with lacunae between, large, contiguous, fibrous prisms, and large papillae. Upper Ordovician, Whitewater fm., Wilmington, Ohio., collected by W. H. Shideler, No. 815. Indiana University Paleo. Coll., slide 302-15. Unretouched. b. Tangential section of same specimen, X 10, showing irregular surface and large prisms with radial, fibrous structure, and smaller, round, radially fibrous structures, the papillae. Slide 302-15. Retouched. bo 100 Figure BULLETIN 194 Explanation of Plate 11 Page 1. Dermatostroma ? escanabaense Galloway and Ehlers, n. sp. ........ 73 a. Vertical section of holotype, X 10, showing the small, vertical prisms and the diverging fibers and indications of growth layers. Middle Ordovician, Black River of Trenton fm., Escanaba R., Delta Co., Mich., University of Michigan, No. 39449. Indiana University Paleo. Coll., slide 308-98. Left half retouched. b. Tangential section of same specimen, X 10, showing the small prisms, as compared with those of D. glyptum, each with a dark ring with light center inside, each terminating in a papilla. The radial fibers are obscure. Slide 308-99. Unretouched. Dermatostroma costatum Galloway and St. Jean, n. sp. —............. a. Cross section of holotype, X 10, showing outer layer with costae and papillae, consisting of debris of Aulacera cyst plates, and inner layer of less disturbed cyst plates. Upper Ordovician, Lower Liberty fm., Wilson Cr., 2 miles southwest of Deatsville, Ky. Collected by Ruth G. Browne. Indiana Uni- versity Paleo. Coll., RB11, and slide 308-99. Slightly retouched. .Cross section of paratype, X 10, showing outer thin layers With organic debris, lying on coarsely crystalline calcite with organic debris inclusions, which pass downward into Aulacera cysts and pillars partly destroyed. Same collection. RB5, slide 308-10. Slightly retouched. — Dermatostroma nodoundulatum Galloway and St. Jean, n. sp. -... a. Part of cross section of holotype, X 10, showing surface with papillae, outer zone of Aulacera debris and calcite, and inner zone of less disturbed Aulacera cysts. Upper Ord., basal Liberty fm., Wilson Cr., 2 miles southwest of Deatsville, Ky. Collected by Ruth G. Browne. Indiana University Paleo. Coll., RB73. Slide 308-23. Retouched. . Paratype, X 10, showing papillae on outer layer of Aulacera debris, passing downward into calcite and less disturbed Aulacera cysts. Same locality, collection and depository. RB1, slide 302-27. Retouched. — C Dermatostroma concentricum Galloway and Ehlers, n. sp. —.....-.... a. Cross section of holotype, X 10, cutting a mamelon, showing the disturbed cysts of the Aulacera, the calcite layer, and the wrinkled laminae of the Dermatostroma. Upper Ordovician, Blackbridge, 10 miles upstream from Louisville, Ky. Collected by Dr. Carl Rominger, 1903. Mus. Paleont., University of Michigan, specimen and slide 01-25. Indiana University Paleo. Coll., slide 308-62. Unretouched. Vertical section of holotype, X 10, showing only one layer in the laminae, which are flocculent and wrinkled, slide 308-63. Unretouched. », Tangential section of holotype, X 10, showing round denticles and wrinkles, slide 308-63. Unretouched. b. ~~ Q 7 r 4 5 6 BULL. AMER. PALEONT., VOL. 43 PLATE 11 PLATE 12 LL. AMER. PALEONT., VOL. 438 Bt ORDOVICIAN STROMATOPOROIDEA N. AMER.: GALLOWAY & ST. JEAN 101 Explanation of Plate 12 All figures natural size except No. 1 Figure Page 1. Aulacera plummeri Galloway and St. Jean _.W0000.2.020 22. eee 27 Hypotype, X 2/3, with spiral, longitudinal ridges characteristic of large specimens. Basal Liberty fm., Wilson Cr., 2 miles south- west of Deatsville, Ky. Collected by Ruth G, Browne. Indiana University Paleo. Coll., No. RB4. 2. Aulacera plummeri Galloway and St. Jean ........................... rai Paratype, immature. Same locality, horizon and collector. RB2. 3. Aulacera plummeri Galloway and St. Jean Topotype, with nearly straight ridges. Whitewater fm., Elkhorn Cr., 4 miles south of Richmond, Ind. Collected by C. H. Hill. 4. Aulacera radiata Galloway and St. Jean, n. sp. .............-0----.02.-. 32 Holotype, showing thin rays of cysts. Richmondian, Anticosti Island. Mus. Comp. Zool., Harvard University, No, 702A. Pea LcCeras mndniata: (Bilkings)) -e a. oe ee Net ed S h ke 30 Part of lectotype, with surface somewhat weathered, showing short, slightly spiral ridges. Late Richmond, Anticosti Island. Canadian Geol. Surv., No. 2583, Marked “TY PR.” Collected by J. Richardson. (eanlacera nodulosa. CBillines)* 228 28 be 34 Topotype, showing large nodes in vertical lines. Upper Ordovician, Anticosti Is. Peabody Mus., Yale University, No. 19556. Hee A aeera NOCULI eras CHOCTSLG): 22 et Se ea ee es, 36 Small hypotype, too poorly preserved to furnish a thin section. Basal Liberty fm., 2 miles southwest of Deatsville, Ky. Collected by Ruth G. Browne. Indiana University Paleo. Coll., No. RB74. RewAMNACCTA- MLELMOGIAy GHOOrSte) 4. oo! Ae ee 37 Hypotype, poorly preserved, showing discontinuous ridges and elongate nodes. Basal Liberty fm., 2 miles southwest of Deats- ville, Ky. Collected by Ruth G. Browne. No. RB20. Sid sanlvcers cylindrica: (hoerste): 2... 2 ee 38 Hypotypes, curved specimens, showing lack of nodeg and ridges. Basa] Liberty fm., 2 miles southwest of Deatsville, Ky. No. RB60, 61. 102 Figure il: i) ol 10. BULLETIN 194 Explanation of Plate 13 All figures natural size Dermatostroma. scabrum) (Games)) =e Hypotype, showing monticules and papillae. Upper Ordovician, Richmond gr., Kentucky end of bridge, Madison, Ind. Indiana University Paleo, Coll., No. 5076, slide 299-50. Dermatostroma ? glyptum (Foerste) _...22222......2.22222cce-cceeeeeeeceeeeeeeeeee= Topotype, showing surface ridges and papillae. Whitewater fm., Dutch Cr., Clinton Co., Ohio. Coll. by G. M. Austin. Mus. Paleont., University of Michigan, No. 7665, slide 01-21. Dermatostroma ? escanabaense Galloway and Ehlers, n. sp. ........ Holotype, attached to Cystostroma minimum, showing irregular surface with small papillae. Black River or Trenton, Escanaba River, Delta Co., Mich. Collected by Dr. Car] Rominger. Mus. Paleont., University of Michigan, No. 39449; part in Indiana University Paleo. Coll., slides 308-98, 99. Dermatostroma costatum Galloway and St. Jean, n. sp. ...............- Holotype, attached to a largely destroyed Aulacera, showing nearly straight longitudinal ridges and papillae. Lower Liberty fm., Wilson Cr., 2 miles southwest of Deatsville, Ky. Collected by Ruth G. Browne. Indiana University Paleo. Coll., RB11, slides 308-99, 100. Dermatostroma costatum Galloway and St. Jean, n. sp. -......--...... Paratype, ova] in section 24% X 1% inches, attached to a layer of calcite 1-5 mm. thick, in turn attached to a cylindrical Aulacera cylindrica, 20 mm. in diameter, with the outside largely de- stroyed by the parasitic Dendrostroma. Liberty fm., 2 miles southwest of Deatsville, Ky. Collected by Ruth G. Browne. Indiana University Paleo. Coll., RB5, slides 308-10, 11. Dermatostroma costatum Galloway and St. Jean, n. Sp. ....-....--.---- Paratype, young specimen, on immature and largely destroyed Aulacera plummeri. Same collection. No. RB52, slides 302-19, 20. Dermatostroma nodoundulatum Galloway and St. Jean, n. sp. .... Holotype, showing nodes on nearly vertical costae. The small, abundant papillae do not show in the figure, Lower Liberty fm., 2 miles southwest of Deatsville, Ky. Collected by Ruth G. Browne, Indiana University Paleo. Coll., No. RB73, slide 302-22. Dermatestroma nodoundulatum Galloway and St. Jean, n. sp. .... Paratype, attached to Aulacera plummeri, but spreading onto mud on both sides. Same collection. No. RB75, slides 308-56, 57. Dermatostrema nodoundulatum Galloway and St. Jean 00... Paratype, attached to one side of A. plummeri, spreading out on both edges, with larger ridges and nodes than usual, with papillae. Same coilection, No. RB1, slides 302-24, 27. Dermatostroma concentricum Galloway and Ehlers, n. sp. -....... Holotype, showing surface with mamelons. Upper Richmond, Blackbridge, 10 miles upstream from Louisville, Ky. Collected by Dr. Car] Rominger. Mus. Paleont., University of Michigan, No. A, slide 01-25. Indiana University Paleo. Coll., sections 302-62, 63. 72 73 74 74 75 75 76 E13 PLAT VOL. 43 . PALEONT., ER M BULL. A ‘ ; : iW + ; BAe ee ps a + Sere s \) | oa ers eee — =} o n x ‘ eae . vy a! rae ee} yy \ yoke Sh J < ay, " ti ve ve i 2 i an ; 7 se 5 ‘ | } 7 a) SS a 7 - + a ut A a ) a4 5 . at i : 4 ed : - -— a i) 5% a = a - 7 ay . : a = j 9 * slp. Gon > 5 — 4: =i cee. fi 7 =) Aur 4 ; t -_ i a INDEX VOLUME XLIII NO. 194 Note: The left hand bold face figures refer to plates, the right hand light face figures refer to pages. A A Chazy se hes Actinostroma _.. Actinostromaria Agawam Station, Kentucky . ais Akpatok Island ........ ANI OB WINE! esse teecencoae: PlaSkapc me ten eee. of Natural History amsterdamense, Stromatocerium 8 Amsterdam, New NOK sea. Ann Arbor, Michigan .... Anostylostroma ...... Anticosti Island antiquatus, 56, 59, 60 , 63 46, 59, 60 53, 55, 63, 64 7 _. 6, 21, 29, 30, 34 Cryptophragmus 2 7, 17, 18, 19-21 Appletree Point, Wermont. 44 arbusculus, Cryptophragmus 18 Aulacera ........ 5} (5, chy AIO)s 1b 18, 21-39, 74, 75, 76, 77 Austine Ge Mie) 2 73 australe, Stromatocerium 9 56, 64-66 australe, Stromato- cerium huronense §4 Aylmer, Quebec .... 17 bacula, Aulacera Baffin Island, Quebec ... Baltic area Bardstown, Kentucky . Bassler, R. S. Bath County, Kentucky . BuChazy. 2: Beatricea . Belk Island, Kentucky Bellefonte, Pennsylvania Benson, formation, Kentucky: -. 27 9) 6 36 16, 49, 66 68 41, 42, 43, 44 21, 22, 23 63 17 50 Bentonsport, Iowa Bernheim Forest, Kentucky ........ bifurcatus, Cryptophragmus Bigby limestone Kentucky Tennessee Billings, E. Blackbridge, Kentucky . Black River limestone ...... , Black River stage Alabama Indiana... Kentucky ... Michigan IMISSOUTIa ee ee New York _.. Ontario Pennsylvania Quebec Tennessee __. Vermont Virginia . Bony Falls, Michigan British Museum of Natural History Browne, Ruth G. Bucher We He... Bullitt County, Kentucky ........ Butts Charles ..... Cambrian Siberiae.. Campbell, Guy . Canaan, Indiana __. Canada, Geological Survey of ..... canadense, Stroma- tocerium Stromatocerium canadensis, Labechia tO, 1 6 18 14 156 49 22, 30, 31, 32, 34, 35, 36, 52 78 46 D, 24, 49, 55, 20, 46, 55, 56, 58, 59, 60, 62 20, 62 89 9, 30, 38, 39, 75, 76 16 30 19 9, 30, 39, 75 25 20, 31, 35, 53 8, 47, 55, 58, 60-62, 64, 87, 89 canadense minimum, 14, 16, 47 61 INDEX Canadian Geological Survey Museum .. 52 canaliculatum, Dermatostroma .. 69 Cannon limestone, Tennessee 48, 49 Cape Smyth Manitoulin Island 53 Ontario 50, 52, 53 Capitol Hill, Nash- ville, Tennessee 48, 49 Carden township, Ontario 19, 20 Carters limestone, Tennessee lets 11, 14 Casey County, Kentucky ........... 30 Catheys formation .. 50 Tennessee ............ 47, 49, 54 cavernosum, Derma- LOSTROM Ges eee 69 CiChazye = 41, 42 Chaumont limestone, Vermont 46 chazianum, Pseudo- stylodictyon 6 40, 41 chazianum, Stroma- tocerium lamottense 43 Chazy limestone, New York 44, 62 Vermont ie lelenlos 4ilr 42, 43, 44 Chazyan .. .. 7,11, 13, 41-44 China Le tee _ 6, 22, 39, 45, 47 Cincinnatian series 15, 55 Ken tue Kyi tl. OQHiOw Se ee 68, 70 Tennessee ......... 66 Cincinnati Museum, University of 16, 38, 59 Cladophragmus .... ly Clark County, Kentucky 53 Clarksville, Ohio . 50, 52, 66, 67 Clavidictyon .... 25 Club Island, Lake Huron .... 26 College Hill limestone, Tennessee 47, 48 Colorado 6 Columbia Quadrangle, Tennessee 47, 49 Columbia, Tennessee 70 concentricum, Der- matostroma 11, 13 69, 76-78 conferta, Monti- cularia 46 conica, Aulacera 24, 27, 39 conica, Beatricea 38 Connersville, Indiana 50 conosimilis, Beatricea 36 Constellaria beds, Tennessee .......... 49 Cooper, G. Arthur .. 9 corrugata glypta, Habechian cc ie corrugata, Labechia al: corrugatum, Derma- LOSEROM Au eee 10 ~=—-68, 69, 71, 72 costatum, Derma- tostroma ...11,13 32, 68, 69, 71, 74, 75, 76, 78 Ceutchiching, Ontariome ca eee 62 Crown Point, INEWRYOrks (20 46, 60 Cryptophragmus 6, 10, 17-21, 22, 24, 25 Cumberland River, Kentucky. = ...= 63 Cumings, E. R. ........ 46, 60 cumingsi, Rosenella .......6 45, 46 cylindrica, Aulacera, 225, 12) 25520 noo: 37, 38, 39, 74, 75, 76 cylindrica, Beatricea UNnGulatayeess: 38 Cynthiana limestone, Kentucky 2.5 ee 54, 62 Cystostroma ,............ 6, 7, 10, 11-17 22, 24, 25, 45, 49, 61, 62, 89 LRItZaC meee Zhe ge A. Ge aly TTT eee eee 11, 12, 14-16, 73, 74 Simp lS Xa eee 1 Iba ales we! vermontense ...1 Hail, alps als: D DaytonynOhiow se: 54 Deatsville, Kentucky ............ 25, 30, 38, 39, 75, 76 Deiss, Charles F. .... 9 de Labech, Sir Henry 47 Delta County, Michican essere 74 Dermatostroma (teh, LIL, Pt) 29, 30, 68-78 canaliculatum 69 cavernosum ........ 69 concentricum 11, 13 69, 76-78 corrugatum 10 ~=«68, 69, 71, 72 costatum ..11,13 32,68, 69, 71, 74, 75, 76, 78 diversum .........: 69 escanabaense 11,13 68, 69, '73 ,74 INDEX glyptum ...... 10, 13 68, 69, 71, 1P45 108 nodoundulatum 11, 13 32, 69, 71, 75, 76 ottawaense ........... 30, 68, 69, papillatum ........ 30, 68, 69, 10s zal seabrum ......10, 13 69-71 tyronense ............ 69 Devonian .............. 7, 8, 10, 45, 47 diversum, Derma- tostroma ......... 2 69 Dutch Creek, Ohio Ta 163 E eatoni, Pseudostylo- dietyon, =.....2....5. 4074142. 43 Stromatocerium 41 Khlers=s GoM. =...-- 9, 63 Elkhorn Creek, nGiatiat eee 30 Elkorn Falls, ny Gicinaee eee ee 54 Elkhorn formation, Indiana ........ ae 25, 50, 54 Ellis Bay formation, Anticosti Island . BL Be El Paso, Texas ........ 45 England Lower Silurian .. 46 Wenlock............... 46 escanabaense, Der- matostroma 11,13 68, 69, 73, 74 Escanaba River, Michigan .............. 11, 14, 16, 54, 58, 62, 74 Escharopora pavonia 70 Estonia Pireu. stage o).......: 88 Upper Ordovician 88 FE ferax, Plumatalinia | 88 HishervA-iG..........-. 23 Fisk’s Quarry, Vermonti ess 40, 41 Flanagan formation, Kentucky va.) 2.<» 16, 50 Flat Rock, Tennessee ........... 48 Fleury Quarry, Vermont ........ 42,43 Flower, Rousseau H. 9, 45, 54 Bligel, Erik ~...7 88 Foerste, A. F. ........ 25, 30, 52 BOOT Ate Ee ees 52 Fort Ancient member, Ohio .... 67 Fort Cassin, Vermont 46, 62 Frankfort, Kentucky 15, 16, 47, 50 fritzae, Cysto- SULOMan eee Det. A251 Gray Fritz, Madeleine A. 1L7/ G Galloway, J. J......... OMISa Zon Gamachian age .... Sil, 33}, 33> Gamachian group, Anticosti Island .. Sil eBs, SO. Girvan, Scotland .... 61, 89 glypta, Labechia Cornu gatas 72 glyptum, Dermato- SUnOMapeeee 10, 13 68, 69, 71, 14 TB: Goodell’s Quarry, VEEMOnNtie 41 Goodell’s Ridge, VET MON tee ae 41, 42 Gotland, Middle Silurian 3s 45 gracilis, Crypto- phrasmuss. eee 18 Grand Isle County, Wiermonite yee 44, 46 granulosum, Stroma- LOCERIUM: = 9 50, 56, 66, 67 granulosus, Alveolites ............ 50, 66 H Haass Otto ee 9 Haileybury, Ontario aL Thy Fall eantes) eee 5, BY7/ Harvard University 20 ayviest Crane 49 Hebertella sinuata 70 Huffman’s Dam, Ohio 54 huronense, ensis australe, Stroma- LOCETIUNIae ee 64 iabechiae=. 7 6, 8, 15, 18, 47, 50-53, 54, 65, 66 Stenopora ............ 50 Stromatocerium .. 50, 66 Tetradium. ............ 50 EWUISSCy an an © eee 9,16 Hyattc Ae 3. ae Bar: 24 I Hately mee Pre od eater 65225255265 30, 35, 37 INDEX Milan 54 Muscatatuck State Farm 52 Osgood ss aes 50 Richmond PANG PAT) CAT 29, 30, 54 Ripley County .... 52 Saluda formation DAN. Par(. PAS) S10) 50, 52, 54 Switzerland County 52 Tri-County Quarry 52 Upper Ordovician PAL PAs eID» 50, 52 Versailles State Park 52 Waynesville formation ; 54 Whitewater formation 29, 52, 54 indianaense, -is Stromatocerium 50 Stromatopora .... 50 intermedia, Aulacera 4,12 25 20,005 37, 38 Beatricea noduli- fera 37 Institute of Mining» and Technology, New Mexico ........ 45 Isle La Motte, Vermont 5, 7, 11, 40: 41, 42, 56, 57 J Japan ! 6 Jefferson County, Indiana 52 K Kalfina, V. K. 88 kayi, Pseudostylo- dictyon 5,6 40, 42, 43 Kay, Marshall 9, 13, 43, 44, 46 Kentland Indiana 21 Kentucky 6, 26, 30, 32, 35, 38, 62, 76 Korea 6 Korovinella 88 Kihn, O. 22 bs Labech, Sir Henry de 47 Labechia Ree GAO lle gs 20, 25. 46- 55. 61, 62, 65, 68, 78, 89 Eabechiellas 6, 7, 11 Labechiidae ............ 7, 8, 10-78, 88 Lake Huron Club Island ........ 26 Manitoulin Island. 30 Ontarione 50, 52 Rabbit Island 26, 27, 30, 32 Richmond stage 30 Upper Ordovician 27, 30 Lake Ontario, Ontario =. 50 Lake St. John, Quebec ...... 26 Lake Timiskaming, Ontariow 17 alickersCaGa eee 23 lamottense chazianum, Stro- matorcerium 43 Pseudostylodic- ty One 40, 41, 42, 43 Stromatocerium 40 Lebanon, Kentucky 36, 71 Lebanon limestone, Tennessee ............ 21 Lee County, Virginia ..... 19, 21 leipersense, Stro- matocerium .... 56, 62, 63 Leipers formation 65 Kentucky 54, 63 Tennessee 64, 66, 70 Leningrad 88 Leray beds, Ontario 58 Liberty formation, Indiana 25, 27, 30, 54 Kentucky Tey 240 240) 30, 36, 37, 38, 39, 54, 68, 75, 76 Liskeard formation, Ona OMe 17 Lone Mountain, New Mexico 54 Lower Ordovician 8 Lower Silurian, England 46 Lower Trenton Drift, Michigan Louisville, Kentucky Lowville limestone 53, 55, 63, 64 78 INGWe OnK 20 Ontanlomeen. een 20 Pennsylvania ........ 20 Quebec ...... laa 20 Virginia 20 Loysburg, Virginia | Maclurites beds, WETMIONG fo. soerccce-ee: macrostyla, Labechia ............8 Rosenella Madison County, Kentucky .............. Madison, Indiana .... Manchuria ................ IManitobay ec ee-c Richmond stage Stony Mountain formation |... ; Manitoulin Island Cape Smyth ........ Lake Huron ........ Marion County, Kentucky Maysville group Kentucky tae ONTO pe see Tennessee McBride Bay, Vermont ............... McLaren, D. J. ........ Miami University Michigan michiganense, Stro- matocerium ..... 9 Middlebury College Middle Ordovician Indiana ...... Kentucky .... Michigan ....... New York ............ Ontario Pennsylvania ...... Quebec ....... Shantung Tennessee Vermont INDEX 44 47, 49, 51, 52, 53-55, 63, 64 45 30 50, 51, 52, 54, 70, 76, ue 6, 26, 35, 37 31 35 53 30 30, 36, 37 53 68, 70 66 46 9 70 62 56, 63, 64, 66, 68 41, 42, 44 10, 11, 18, 24, 39, 45, 55 39, 40, 41, 42, 43 Middle Silurian _. Gotland Milan, Indiana Mill Creek Tennessee .......... Mme She Avnet es minimum, Cystostroma .....1 Stromatocerium 45 45 4 14 23 11, 12, 14-16, 73, 74 49 Stromatocerium canadense Missouri ..... Black River stage Monticularia con- ferta Monticulipora montifera, Labechia montoyaense, Pseud- stylidictyon wal Montoya limestone, Texas specimens Re Moore, R. C. ... Morrow, Ohio _. Mount Parnassus, Tennessee Murie, J. .. Muscatatuck State Farm, Indiana N Nashville group, Tennessee .. Nashville, Tennes- SC Cir rdaaiem Al Mkin nat Capitol Hills. 2 Nelson County, New Mexico _......... Institute of Min- ing and Tech- nology ... ox Lone Mountain oe SilvyersCity Upper Ordovician New York Nicholson, H. he nodoundulatum, Der- matostroma 11, 13 nodulifera Aulacera Beatricea intermedia, Beatricea nodulosa Aulacera ... 4,12 Beatricea _. Nolensville Pike, Tennessee Novaya Zemlya Upper Ordovician 4,12 14, 16, 47 47 14, 47, 48, 49, 50, 54, 64, 66 48, 49 29, 30 88 5, 6, 58, 62 5, 35, 51, 52, 62, 64, 89 32, 69, 71, 75, 76 25, 26, 30, 34. 36, 37, 76 36 37 25, 26, 34, 39, 36 21,23, 34, 36 50 26, 38, 45 38 (@) Obrutschew, W. A. Ohio ohioensis, Labechia QNUaARIO. Aes nee Ophelia, Kentucky Ordovician (see lower, middle and upper) Osgood, Indiana Ottawa, Ontario River, Ontario . ottawaense, Derma- tostroma ........ ; Otter Creek, Vermont Owingsville, Kentucky Ozaki, K. Paleoalveolites paquettensis Pamelia limestone New York Ontaciowe a Quebec papillata, -um, Dermatostroma Stromatopora paquettensis, Paleoalveolites .... Paquette Rapids, Ontario parallelus Crypto- phragmus Parks, W. A. INDEX 88 6, 26, 30, 35, 37 50, 52 6, 26, 30, 34 38 26, 78 30, 68, 69, NOS 68 14 58, 62 18 5,0; 15, 16; 55, 58, 62, 64, 65, 66, 71, 72, 89 Pattersonville, New York . pavonia, Escharopora Peabody Museum, Yale University peichuangensis, Aulacera Pennsylvania Penquite Run, Ohio Perry, LG: Petersborough, Ontario Pirgu stage, Estonia platypilae, Stroma- tocerium 0 Plumatalinia 47, 60, 62, 64, 89 88 58, 67, 68 88 plummeri, Aulacera 3,12 Tis Palle PAB}, O45}, 3 26, 27-30, 32, 33, 36, 37, 39, 74, 75 Plummer, John T. . SV PAL OR) ORY 25, 27, 29 poshanense, Pseudo- stylodictyon ........ 39, 40 Praeactinostroma ... 88 Pseudolabechia ........ 6, 7, 11, 88 Pseudostylodictyon .. 6,7, 10. 39- 45, 61 pustulosa, -um bed, Stromato- COLIN eee eee 49 Labechia .......... 7 OMA Gwlo: 16, 18, 47-50, 52 Stromatocerium .. 16, 47, 49 Stromatopora . 47, 48 Q Quebec) 22 ee 34 R Rabbit Island, Lake Huron ........ 26, 27, 30, 32 radiata, Aulacera ...... 4,12 26, 28, 32-34 Inenoaoyael, 126 1B, ance 18, 20, 24 Rychardson Jes eer olvac Richmond, Indiana Sy All, Aa}, CAT : 29, 30, 54 Richmond stage (CLOUD) eee PAL Pag), pA, Is15), 64, 66, 68 Anticosti Island PAG}, Bl SP, 336+. SD OONot inaciainiceeeee 2a PAU 248) 54, 70 TOWal 255. ae ee 70 Kentucky ............ 70, 78 Lake Huron ......... 30 Manitoba ...... 31 Manitoulin Island 50 Mirchivani see 54 Ohio. 54, 70 Ontario Sik ialsily/, Ste) Ringer, George ........ 9 Ripley County, Indiana .... 52 rochensis, Crypto- phragmus ete 18 Rockland formation New York ............. 46 Ontarionesee ore 58 Rominger, Carl ........ 9, 55, 64, 74, 78 Rosenelilaw eases CeO late 39, 44, 45, 46, 61, 78 Rosenellina .............. Rowena, Kentucky © Royal Ontario MGSeUIM), 2. rugosa, -um, Stromatocerium 8 Stromatopora tumidum, Stroma- tocerium Russia INDEX 17 54, 63 Li 8, 55, 56-58, 60, 62, 64 56 58 22, 26, 27, 30, ~ 37, 39, 45, 47, 55, 61 Safford, J. M. St. Jean, Je St. John, Lake, Quebec 0a ge ee te Saluda formation Indiana OIG ee scabra, -um Dermatostroma 10, 13 Labechia Stromatopora ...... Schmidt, Bruno M.. Schuchert, C. Scleractinia Scotland, Girvan _. Seelyes Hee Mn ke Shantung pale, William Shimer, H. W. Shrock, R. R. Siberia eee siberica Aulacera Beatricea. ....... Silver City, New Mexico ......... Siunane Lower, England .. Middle dee Middle, Gotland > simplex, Cystos- LrOMaw se ee oe L 1 Sinodictyon .. a sinuata, Hebertella South Hero township, Vermont Vermont =2222..-4 Stenopora huronensis Stony Mountain for- mation, Manitoba 28 25, 27, 29, 30, 50, 52, 54 50 9, 30, 73 22, 23, 32, 33 22, 23, 32, 33 6, 38 27 38 54 7, 10, 47, 52 11, 12, 13, 14 6, 10, 22, 25 70 46 43, 44 50 35 Stromatocerium Stromatopora subceylindrica Labechia Stromatopora suleata, Beatricea Switzerland County, Indiana T telposensis, Aula- cera See Tennessee tenuipunctata, Aulacera Tetradmimi- Texas Thamnobeatricea .... Thomas, Dighton .... Timiskaming Lake, Ontario ees... Trenton, Drift, Michigan Trenton limestone INeW VODkes= to Ontario ates Trenton stage ...... Kentucky Michigan New York Ontario moe Tennessee ........... Tri-County Quarry, Indiana tumidum Stromatocerium 8 Stromatocerium TUcosuM = Twenhofel, W. H. tyronense, Derma- tostroma Wirich eh OF = undulata Aulacera Beatricea cylindrica, Beatricea . undulatadirecta, Aulacera Ungava Bay, Ak- patok Island .... 7 14, 15, 16, 47 11, 16, 62, 74 46,60 47, 62 14 52 55, 58, 59 58 23 69 49,51 23, 26, 28, 29, 23, 27 38 26, 33 26, 30 United States Na- tional Museum Upham formation, Texas Upper Devonian Upper Ordovician Akpatok Island Anticosti Island . . Estonia Indiana Iowa : Kentucky . Lake Huron New Mexico Novaya Zemlya Ohio ; Ontario Quebec .... Russia - Shantung Siberia Tennessee .... Texas Urals Urals Valley View, Kentucky Vanderbilt Uni- versity Vauréal formation, Anticosti Island Vermont vermontense, Cystostroma Versailles State Park, Indiana Virginia Visean vologdeni Actinos- troma 1 INDEX 15, 16, 55, 63, 64, 66 45 47 10, 11, 18, 22, 39, 47 50 14 31, 35, 36 6, 39, 58 11, 12, 13 52 6 47 88 vugaris Aulacera, 4 27 Beatricear 38 WwW Walker, Frank H. .... 68 Walker Museum, University of Chicaso@ = 50, 67 Warren County, Ohio 50, 70 Watertown, New VOD hod aes: 46, 55, 56, 58 Wayne, W. J. 9 Waynesville formation Indiana es 54 Kentucky ............ 54 Onioyes 50, 52, 54, 66, 67, 70 Waynesvile, Ohio .... 50, 51, 52 Wells, J. W. a 71 Wenlock, England 46 Whitewater formation Indiana ees 29, 52, 54 O1O ee ee elemionates Whittington, H. B. 9, 20 Wilmington, Ohio 52, 70, 71, We Ve Wilson, Alice E. 9, 20, 31, 35 Wilson, Charles W., ries nes 9, 14, 49 Wilson Creek, ; Kentucky 25, 30, 38, Thay, Ths) Winchester, Kentucky ... 55 woyuensis, Rosenella ........ ¥ 46 We OMovVOVS sa conasaccee 6 Y Yale University Peabody Museum SDHoil Yavorsky, V. I. 7, 24, 26, 75, 88 fre me of il J} — } | h {= Oi 4e a ji » 7 | i] 6 e aie. we a -~_ XXIX. XxX, XXXI. XXXVI. XXXVII. XXXVITI. XXXEX, Xi. XII. XLU. XLit. Volume I. TI. TH. Iy. (Nas. DBO IMG). Tas uppe be PISh bse lic ee es. 18.00 Bowden forams and Ordovician cephalopods. (Nee RZ). bos SDD.) One DIS. Mis cle es: 15.00 Jackson Eocene mollusks. (Nos, Uis-128).) "408 op.; 27 pls; yt eee ck 12.00 Venezuelan and California mollusks, Chemung and Pennsylvanian crinoids, Cypraeidae, Cretaceous, Miocene and Recent corals, Cuban and Floridian forams, and Cuban fossil localities. (N@s: 129-153). "294 np. Bon pls ial co OS. 10.00 Silurian cephalopods, crinoid studies, Tertiary forams, and Mytilarca. (NOs) 184-189), \ 448):pps)! BD: psy. -.c seiko) es ase eee ld Devonian annelids, Tertiary mollusks, Ecuadoran stratigraphy and paleontology. (Nos, -140-145).°400. pp.,) 19. pis/3 dui a eR. 12.00 Trinidad Globigerinidae, Ordovician Enopleura, Tas- manian Ordovican cephalopods and Tennessee Or- dovician ostraecods, and conularid bibliography. (Nos, 146-164) i)'386 spp, 31 pls, Se ek 12.00 G. D. Harris memorial, camerinid and Georgia Paleo- cene Foraminifera, South America Paleozoics, Aus- tralian Ordovician cephalopods, California Pleisto- cene Eulimidae, Volutidae, Cardiidae, and Devonian ostracods from Iowa. (Nes; 169-160). 412 pp.; S82 pls. Cote 13.50 Globotruncana in Colombia, Eocene fish, Canadian- Chazyan fossils, foraminiferal studies. (Nos) 161-164). 486pp.; 37: WB eo ea 15.00 Antillean Cretaceous Rudists, Canal Zone Foramini- fera, Stromatoporoidea Nos. 165.176).\447..pp.. 53. DIS. hin ak a 16.00 Venezuela geology. Oligocene Lepidocyclina, Miocene ostracods, and Mississippian of Kentucky, turritellid from Venezuela, larger forams, new mollusks. geology of Carriacou, Pennsylvanian plants. CNOss 277=183)s 448 spp. 2360plsl Mee ek 16.00 Panama Caribbean mollusks, Venezuelan Tertiary for- mations and forams, Trinidad Cretaceous forams, American-European species, Puerto Rico forams,. CNOS 184)0996 “pp deplete ea We 20.00 Type and Figured Specimens P.R.I. (Ne@s.. 185-192). 381) pp, \35e pls. of. oon Md 16.00 Australian Carpoid Echinoderms, Yap forams, Shell Bluff, Ga. forams. Newcomb mollusks, Wisconsin mollusk faunas, Camerina, Va. forams, Corry Sandstone. p (No. 193). In press. (NOs. 194: 995) \198 Sp py 16. iplsy ts. TA ea to: Ordovician stromatoporoids, Indo-Pacific camerinids. 3.50 PALAEONTOGRAPHICA AMERICANA (Nos. 1-5). 519 pp., 75 pls. Monographs of Arcas, Lutetia, rudistids and venerids. (Noa, 6-12). “531° pps,’ 37: pis. 3.000 al et 21 Heliophyllum halli, Tertiary turrids, Neocene Spon- dyli, Paleozoic cephalopods, Tertiary Fasciolarias and Paleozoic and Recent Hexactinellida. (NOs,/'18-2aye;\ 519 pp: Gt pls oe ee 25.00 Paleozoic cephalopod structure and phylogeny, Paleo- zoic siphonophores, Busycon, Devonian fish studies, gastropod studies, Carboniferous crinoids, Creta- ceous jellyfish, Platystrophia, and Venericardia. (Nos. 36-28) (128) pp.) 18 psi ee Rudist studies, Busycon .00 6.50 CONDENSED TABLE OF CONTENTS OF BULLETINS OF AMERICAN PALEONTOLOGY AND PALAEONTOGRAPHICA AMERICANA Vols. I-VI. VII. Vill. XVI. XVII. XVIII. XIX. XXVII. XXVIII. BULLETINS OF AMERICAN Out-of-print. (NO."S2) 6) 730 Dp. OB pe ae i kN ee 15. 00° Claibornian Eocene scaphopods, gastropods, and cephalopods. (Nos. 33-36). 357 pp., 15 pls. Mainly Tertiary Mollusca. (Nos.'37«39).., 462: pp. 35 wisy ons ee Bee 14.00 Tertiary Mollusca mainly from Costa Rica. (Nos. 40-42). 382 pp., 54 pls. Tertiary forams and mollusks mainly from Trinidad and Paleozoic fossils. (Nos. 49-46). -272-pp., 41, play ic. e Tertiary, Mesozoic and Paleozoic fossils mainly from Venezuela. (Nos. 47-48). 494 pp., 8 pls. Venezuela and Trinidad forams on Mesozoic inverte- brate bibliography. (Nos. 49-50). 264 pp., 47 pls. Venezuelan Tertiary Mollusca and Tertiary Mammalia. (Nos. 51-54). 306 pp., 44 pls. Mexican Tertiary forams and Tertiary mollusks of Peru and Colombia. PALEONTOLOGY 11.00 (Nos. 55-58). 314 pp., 80 pls. Mainly Ecuadoran, Peruvian and Mexican Tertiary forams and mollusks and Paleozoic fossils. ; (Nos: 69-62). .140: pp.) 48) pie. ete ceeeetenenoegiens 6.00 Venezuela and Trinidad Tertiary Mollusca. (Nos, 63-63) +283 pp, '38pls: 222 es 11.00 Peruvian Tertiary Mollusca. (NOs. 64-67). 286. DD. 29) DIB. pa pnned eentanccthbaensanbancndebesdedbnaltes 11.00 Mainly ‘ertiary Mollusca and Cretaceous corals. (NOS 68)e" 272 "pik, OS piss cell oe es eae 10.00 Tertiary Paleontology, Peru. (NOs. 695700) 5.266 Dp, 26 PS. Ve ULL. AMER B INDO-PACIFIC CAMERINIDS: COLE 27 EXPLANATION OF PLATE 15 Figure Page Transverse sections, x 46, except figure He 38 AVG 1. Camerina complanata (Defrance)........00000.00.00000 eee 120 Upper part of the specimen illustrated as figure 2, Plate 16, to show the structure of the spiral sheet and the marginal cord. 2-11. Camerina ammronoides (Gronovius)....................................115, 118 2. Specimen similar to the one (Cole, 1959, fig. 9, pl. 29) selected by Smout and Eames (1960, p. 110) to represent Operculina hanzawai. 3-5. Specimens to illustrate the progressive shortening of the alar pro- longations as the test becomes more evolute and compressed; 3, see: fig. 2, Pl. 14; 4, see: fig. 8, Pl. 14; 5, see: figs. 10, 11, Pl. 14. 6. Small specimen. 7,9. The same specimen; fig. 9 enlargement of fig. 7; see: fig. 9, pl. 28, Cole, 1959. 8. The same specimen illustrated as fig. 8, pl. 29, Cole, 1959. 10. A slightly evolute specimen; see: fig. 17, Pl. 14. 11. Evolute specimen; compare with fig. 7, pl. 28, Cole 1959 to dem- onstrate differences in the embracement of the final volution. 1. Loc. 1—see text for description of localities. 2=§, 10. Locy 7 (S535 iil, llayes 5) Ta LOCNG BULLETIN 195 EXPLANATION OF PLATE 16 Page Figure 1-6, 9, x 20; 7, x 40; 8, x 12:5 1-9. Camerina complanata (Defrance) 1, 8,9. Median sections. 2-8. Transverse sections; see: fig. 1, Pl. 15 for an enlargement of fig. 2; 7, enlargement of the upper part of fig. 3. Loc. 8—see text for description of localities. (Sv), eyes. Il ye 7q a Ieeyey 7 R. PALEONT., VOL. 43 =, “a. Buu. AME S — a Vv | > : aS} _. { ‘ 16 ne it ee iw “7 XXVII. XXVIII. XXIX. XXX. XXXI. XXXII. XXXITI. XXXIV. XXXV. XXXVI. XXXVI. XXXVI. XXXIX. Volume I. II. C Noss 101-108)!’ 376. pps 36 ‘pls. Nie i ahs sce tle Tertiary Mollusca, Paleozoic cephalopods, Devonian fish and Paleozoic geology and fossils of Venezuela. (Nes."108-114)\! /412pp5'$4 pls ih a i fo Paleozoic cephalopods, Devonian of Idaho, Cretaceous and Eocene mollusks, Cuban and Venezuelan forams. (Nosy 115-116)...’ 738 pp. S2iplse 8 i le POS ay Bowden forams and Ordovician cephalopods, (Nov Lh) i) S68" pp.) GS pls. fh UR AA? eal Jackson Eocene mollusks. . CNos,-118-128);.., 458: pps!'27 ‘pls/e ee yh eee Na Venezuelan and California mollusks, Chemung and Pennsyl- vanian crinoids, Cypraeidae Cretaceous, Miocene and Recent corals, Cuban and Floridian forams, and Cuban fossil local- ities. (Nos. 129-133). 294 pp., 39 pls. Silurian cephalopods, crinoid studies, Tertiary forams, and Mytilarca. CNos: | 134-139) 448). py 58 pls. oo Nae Gul Ey Devonian annelids, Tertiary mollusks, Ecuadoran stratigraphy and paleontology. (Nos. 140-145). 400 pp., 19 pls. Trinidad Globigerinidae, Ordovician Enopleura, Tasmanian Ordovician cephalopods and Tennessee Ordovician ostra- cods, and conularid bibliography. (Nos. 146-154). 386 pp., 31 pls. 20.03. csc en. G. D. Harris memorial, camerinid and Georgia Paleocene Foraminifera, South America Paleozoics, Australian Ordo- vician cephalopods, California Pleistocene Eulimidae, Vol- utidae, Cardiidae, and Devonian ostracods from Iowa. (Nos. 155-160); . 412\pp.) 53) pis. 2 he Globotruncana in Colombia, Eocene fish, Canadian-Chazyan fossils, foraminiferal studies. (Nos. )'161-164)) '486:np.,'37 pls). hh a Antillean Cretaceous Rudists, Canal Zone Foraminifera, Stromatoporoidea. (Nos. {165-176).: '447, pp..'53 iplss. tank Me Ih A Venezuela geology, Oligocene Lepidocyclina, Miocene ostra- cods, and Mississippian of Kentucky, turritellid from Vene- zuela, larger forams, new mollusks, geology of Carriacou, Pennsylvanian plants. tNoas177-183). \'448 ‘pp. 36 pls. Bin BN Panama Caribbean mollusks, Venezuelan Tertiary formations and forams, Trinidad Cretaceous forams, American-Euro- pean species, Puerto Rican forams. (No. 184). PALEONTOGRAPHICA AMERICANA (Nos. 1-5). 519 pp., 75 pls. Monographs of Arcas, Lutetia, rudistids and venerids. (Nos. 6-12). 128 pp., 18 pls. Rudist studies, Busycon. oO Reade aca dlescccsocccccesuwtccsesesccagsecesscen 10.00 10.00 13.00 14.00 12.00 10.00 12.00 12.00 12.00 13.50 15.00 16.00 16.00 20.00 16.50 21.00 25.00 CONDENSED TABLE OF CONTENTS OF BULLETINS OF AMERICAN PALEONTOLOGY AND PALEONTOGRAPHICA AMERICANA BULLETINS OF AMERICAN PALEONTOLOGY Vols. I-VI. Out-of-print. VEl.. GNO%32) 2) +730; pp 90) pls. ol 7) Ne an 14.00 Claibornian Eocene scaphopods, gastropods, and cephalopods. VIII. (Nos. 33-36). 357 pp., 15 pls. Mainly Tertiary Mollusca. EX. \QNost: 37-39)’ 462: pps, 35 pla of. 8. ue AA ee 13.00 Tertiary Mollusca mainly from Costa Rica. X. (Nos. 40-42). 382 pp., 54 pls. Tertiary forams and mollusks mainly from Trinidad and Paleozoic fossils. KC: (Nosy. 43-46) «7.272 ppGAr: pls) Kral p ig he upon sees Mesozoic and Paleozoic fossils mainly from Vene- uela, XII. (Nos, "47-48). 494 pp., 8 pls. Venezuela and Trinidad forams and Mesozoic invertebrate bibliography. XE’ (Nos..49-50);” 264’ pp. 47 pists). LON eae 10.00 Venezuelan Tertiary Mollusca and Tertiary Mammalia. XIV. (Nos. 51-54). 306 pp., 44 pls. Mexican Tertiary forams and Tertiary mollusks of Peru and Colombia. XV. (Nos. 55-58). 314 pp., 80 pls. 2 Mainly Ecuadoran, Peruvian and Mexican Tertiary forams and mollusks and Paleozoic fossils. XVI. (Nos; 59-61)...\140 \pp.; 48) pls) ok 6.00 Venezuela and Trinidad Tertiary Mollusca. XVII. .\(Nos,, 62-63)... 283’ pp, 33. plsi(3.056. Zs. Leesa etaal 10.00 Peruvian Tertiary Mollusca. XVII.» ‘ (Noa: 64-67); 286 pp., 29 pls. sci pode iyakentuegbeet gelbue ben 9.00 Mainly Tertiary Mollusca and Cretaceous corals. XD: (Nel.68)5 4272 pow 24 iplss ke RS eT eerie ete 9.00 Tertiary Paleontology, Peru. KX: -(Nos:, 69-200)... 266- pp), 26 pls: .2... de el eae 9.00 Cretaceous and Tertiary Paleontology of Peru and Cuba. MXAI;. (Nos. 71-22), 321 pps 12.pls. eo ss ee 9.00 Paleozoic Paleontology and Stratigraphy. SEE. CN086 73-76) 5" 356 pp. 31, pls.) iia. piss onncsseorsh sndvarnayarighdecrans 9.50 Paleozoic Paleontology ‘and Tertiary Foraminifera. MXIT. (Nos... 97-79)... 251 ppg 35 pls’... ecl saspetl Ne cscshelen sol aeedtane 9.00 Corals, Cretaceous microfauna and biography of Contad. XXIV. Nos, $0-87). 334 pp. 27 piso cc ee eae 9.50 Mainly Paleozoic faunas and Tertiary Mollusca XXV.- (Nos. 88-94B). 306 pp., 30 pls. 23....04.0..8 St 9.00 Paleozoic fossils of Ontario, Oklahoma and Colombia, Meso- zoic echinoids, California Pleistocene and Maryland Mio- cene mollusks. XXVI-.. CNos. 95-100) .) "420. pp:,,. 58 piscina eo ae 11.00 Florida Recent marine shells, Texas Cretaceous fossils, Cuban and Peruvian Cretaceous, Peruvian Eogene corals, and geology and paleontology of Ecuador. MUS. COMP. ZOOL LIBMARY DEC 12 1968 BULLETINS |) kisim c OF _ AMERICAN PALEONTOLOGY VOL. XLII NUMBER 196 1961 Paleontological Research Institution Ithaca, New York U.S.A. 7. =. ide ua ad a fg? ee ee a Ae! tet PRES Sane bas Seba LW A y PALEONTOLOGICAL RESEARCH INSTITUTION 1961-62 PRESIDENT 7 SiGe heh Ae pat athe esta A 2 i Nat Joun W. WELLS VICE-PRESIDENT: SF 6 oo Aha NU te Ne coh ae) A oe pe a AXEL A. OLSSON SECRETARY~GREASURER © 22-0. 35010 aoe Shap ee rote REBECCA S. HARRIS | DIRECTOR i... Me SAL IS 2 es ot E ISATHERINE V7 Ws SEAL ME COUNSED fs. sr DOE A ANS eS oe ea ls VAR EANDY cD AMS REPRESENTATIVE /AAAS COUNCIL 02.20.66... 2)isheceeee ies iencee Kennetu E. Casrer Trustees | KENNETH E. CASTER (1960-1966) KATHERINE V. W. PALMER (Life) DONALD W. FisHER (1961-1967) RALPH A. LippLe (1956-1962) Resecca S. Harris (Life) Axe. A. Oxsson (Life) _Sotomon C. Ho.uisTerR (1959-1965) | NoRMAN E. WetsBorD (1957-1963) Joun W. WELLS (1958-64) BULLETINS OF AMERICAN PALEONTOLOGY and PALAEONTOGRAPHICA AMERICANA KATHERINE V. W. Patmer, Editor Mrs. Fay Briaccs, Secretary Advisory Board KENNETH E. CASTER Hans KuGLER A. Myra KEEN Jay GLENN Marks Complete titles and price list of separate available numbers may be had on application. All volumes will be available except vol. I of Paleontographica Americana. : Subscription may be entered at any time by volume or year, with average price of $16.00 per volume for Bulletins. Numbers of Paleontographica Amer- icana invoiced per issue. Purchases in U.S.A. for professional purposes are deductible from income tax. For sale by Paleontological Research Institution 109 Dearborn Place Ithaca, New York U.S.A. y oo. a on 7 BULLETINS OF AMERICAN PALEONTOLOGY VOL. 43 No. 196 MISSISSIPPIAN SMALLER FORAMINIFERA OF KENTUCKY, SOUTHERN INDIANA, NORTHERN TENNESSEE, AND SOUTHCENTRAL OHIO By James E. ConkKIN University of Louisville December 1, 1961 Paleontological Research Institution Ithaca, New York, U.S.A. Library of Congress Catalog Card Number GS 61-303 MBS. COMP. 700F LIBRARY DEC 12 196] | HARVARD UNIVERSITY Printed in the United States of America TABLE OF CONTENTS PM OYS ERE NG/ Ee La 2s abr Saat Ae Sal age, eee eA EY EN eh Oe SOE, ee SR eae 135 intro dich omippee sere eee = oe oe ce Peet) Ne Ly tee ae Ne at Ae 136 EAU DOSE ate tee Se OM eI es 6 Re Ye at nc eS eg tae NO shag 136 PTEEW ALO US Re VV.O Miia ee poets AP Bonar PR MR se aes eB ee Se oe eee 136 IB ES EM HEV VOL Kae ee eee en en hs cS tae ore ie ey ie Bales HE ree 138 Acknowledgments tte ee ee ee ak eae Be Stas her dae tere eA Re 138 DE POSTELONNTO Limi Cy. CS see ec ee en Nat ag aa ee eh ee ee ee. ae eee aes 139 S Clea 2 Trap bye ne eee ene ee eg Teen ee Ae lta NLR. RAI Ce A 140 TGS tate fae Lo Gall i ties yee eee ee tee cee ann ee 2 Set eda ess 140 NESS TG Cay sa a eee Se se eos oenr se BON Ses ee eee ee 140 Vato UF yw Vee Pal P SU RE lt ANE TO Ser AO ek Le eo Ete OE eee 146 HIG@TIINE SS CGH pacts tee eet i RR ast Die se SON en PRE PEELS AN Lehre ene he Serco 146 © ii ope eee es RT IR ane ro pe MA aN Aa Poa, 2 Shee ah By Gee 147 Gorrella toms chiants ics ncc on: 8 soe oe ieee, eee se eee sn Me te ae se ee 148 Me asumed tase Cli Om'S) ya: et eect aes ae ees ne ee 148 Stratiigoalpincapialleomt ol og ya. cert Se see ee eles eee 198 Compositronmotethessh ama shee: see se ee ee eee ee ee 198 Genera and species important in stratigraphic division ~..............-.---.--.-- 200 TLR DCH UTIETIULTE eke oe Re ree SEN ee cE BIA rier PARI ne Teeth Ae 200 LADO SGT Bok Sse eg SO 2 HA VAD rp NEEM OT RA SE Mp ee TS a cle nee 201 gE COTELTU CL eres OT to Meee Ee oe IR ER OI ae cE 5 A eR rohan, ee ws 201 TUG CUTTUTI DULL LLC SiMe) D2 CLE TG OTLCLClLT Sane meena ne me eee eee eure eo 201 DRE POLLO PS UG prc te eee aaa NE Dien ha 8 ARH ON ON Se SOE OOS 202 WATTETIUO OCT CULE ae eee ON Al te ea Sea Reece erg a Pee hah DN See ea 202 CA TTIUOUGGILUILC Scapa tare oe aR Tes re SO dere a fi NE Tce nea ee eer 202 CNG HEIL CLITETTELIL CE A ese aD en Rg Ae oe eee nc Re 203 CTIEUG OT ATU Secor ei ae leans ed ie re Nae VA ey ee eh oe cd ae e we 203 TBAT AUG TG IG genet RL AEA aa RED Ne 8 A ORE ae ae aid UREN 2... 22.-0---2-- 267 >) bo BULLETIN 196 Barlandia.-Plummers* 1930 es-25 ee he ee Bie ES consternation NoiSpy eee NO ee Se Sr 273 Reophax=Montiortes3 0 Sis eee ee oi ee ee 274 RecheeR. arenatuss (Cushman! and aVWiaters)),) 1927) 278 ReiaspersCushmanvandawWiatersy 1928) ee 279 Re Runklerenstsen: iSpy feet ee aN hee 280 R. cf. R. lachrymosus Gutschick and Treckman, 1959. 282 RE ai cdomial dt Mes pe aoe eISSN eee ee 284 IR oniniwttssaris mee lume) 9194: Si eee eee ee ee 285 Envolutina Ter queny 36205 cc tree a i ke 286 I vexsertay (CGushmian)):" 190) eee oe a 287 i-longexserta Gutsehickevand Wreckmian, 11959 ss e ee 289 Tetsernicomstriciae (NVAtETS) | ml 27) ee ee eee eee eae 291 Glomos pira-Rzehiales 883) Wie Mew Ss Be Ee 2 Ee ee 295 Gs-articilosa Plummer 945) cc ee 296 Eituotuba Riummbler 89 Sie erases aaa ek 297 Ex semiplanas nis sp: lies a ee ae Ne 297 Rolypamminat Rhumbller, USO 5 ee eect ae ene ere 299 i bpotonuncus) Gutschick and) direcknmany 1959s ee ee 301 Dercyclops Gutschicky ands direckmary 91959) geen eee 302 Eacouschapelensas, (Ms. SP soc steer 304 TP LAOCOG I, WS "Sec cance sees ea oe ee 307 T. tortwosa > Winn; 1942) oe ee ioasececcscncecenccestececessaccuere tects eee eee 308 Armmovertella Cushman p19 280 oreo ee 309 A Cla Ainclusas Cushman sang iaterss 9 2m eee 309 A-labyrintha Trelandy W9S60.4-233 ae ee ee 312 Anict Ae prinaparva Mrelamnds) ol95 Gn eee ee ce ee 313 Drepedlopsis Cushman and Waters; 1928 sees cetera ee eee 314 T. glomospiroides Gutschick and Dreckman, 1959) 2..-2.c-cccccceee es 315 T. recurvidens Gutschick and Dreckman, 1959 22 2ecceecceceeeeeeee 316 D. spiralis Gutschick sand) Dreckmram, 1959) Ssteeeesrsteceeenee crea ae 318 Ammovaculites (Cushman. 1910) 222 ece ses ee 319 Ais GUUbhS CHUCK TAINS |S Piers aoe csee hess tee see toea eases ees nos a erases asec ee 322 Glimacammina SB Ady, US73) vos ses re cease eee 325 Gi, MASSISSTP PLGMA, De SPs eda ceeescecees ects csen ncn tece sa raetee es eee oes ae 326 AG AER ATIGTUIA UNE WTA CLS Sia ees ea ea ance eae 329 Als MmtSSiS SUP PLA, Wi. SPs cclescscsceessbec secdeesesne-heecedees a cecs sccaeesett evaee ae cena 331 Eiemigor diuse Schuibent:) 19 08) secesee cesses cosa 334 ED anorillemsis. 1s iSps,. oh aecccce ces ca reece ece cate eae oe eee 334 Tirochamminas Parkers ANG OMNES sy 1859) pce eter nese cee cee erage ene serene eee 335 f RRC 11 FTL IGRIES 0 SQ) © ee nee eee er ee ret cee decocscocces 336 ISLA CH CEG BAC Si/ 6 testers reese eee ee ae ea ee 338 Sen cicatri nls Sp ees Noes A Te NOE ee eee 339 SPUACOPU POSES. Te Shs, Ae) So» ’ ‘ - Le Be é v 4 a rh i "a 4 » i>." fc * ~ MISSISSIPPIAN SMALLER FORAMINIFERA: CONKIN 141 Section measured in road cut where State Highway 61 and County Road 1020 join at Gap-in-Knob. Brooks Quadrangle, Lat. 38° 1’ N, Long. 85° 42’ 15” W. Samples from within the Brodhead formation 6” to 10” (Bed 1) and 16’ to 33’ (Bed 2) above road level in road cut north of Knob Creek Church on State Highway 44 about 9 miles west of Shepherdsville. Kosmosdale Quadrangle, Lat. 38° 55’ N, Long. 85° 53’ 15” W. . Section measured on west slope of knob on northwest edge of Lebanon Junction. Lebanon Junction Quadrangle, Lat. 37° 54’ 24” N, Long. 85° 44’ 15” W. Nelson County K-11. Section measured in road cut along U.S. Highway 62, .5 miles south- west of Boston. Lebanon Junction Quadrangle, Lat. 37° 47’ 8” N, Long. 85° 40’ 30” W. . Section measured in road cut along U.S. Highway 31E, .5 miles south- west of Balltown. New Haven Quadrangle, Lat. 37° 44’ 7” N, Long 85° 30’ 20” W. . Section measured at Blue Gap, 2.65 miles north of RR tracks at New Haven on U. S. Highway 31E. New Haven Quadrangle, Lat. 37° 41’ 20” N, Long. 85° 33’ 55” W. Larue County K-14. K-15. K-16. Marion K-17. K-18. K-19. K-20. Section measured along secondary road leading west up hill, .25 miles north of Athertonville. New Haven Quadrangle, Lat. 37° 38’ 22” N, Long. 85° 36’ 38” W. Section measured along U. S. Highway 31E at Muldraugh Escarpment just northeast of White City; base of section about 3 miles southwest of Athertonville. (Modified after Stockdale, 1939, p. 208). Hodgenville Quadrangle, Lat. 37° 35’ 32” N, Long. 85° 39’ 35” W. Sample from the upper part of the Somerset shale member (Bed 1) of the Salem limestone along road leading up hill northwest of old Ginseng Post Office, across West Fork of Otter Creek, 10 miles southeast of Hodgenville. Howardstown Quadrangle, Lat. 37° 30’ 27” N, Long. 85° 35’ 15” W. County Section measured across from church on County Road 457 at Holy Cross. Loretto Quadrangle, Lat. 37° 40’ 22” N, Long. 85° 26’ 52” W. Section measured in road cut 2.5 miles east of Marion-Nelson County line, west of Raywick on State Highway 84. Raywick Quadrangle, Lat. 37° 33’ 45” N, Long. 85° 29’ W. Samples taken from Falling Run member (Bed 1) of Sanderson for- mation and lower 6” to 1’ (Bed 2) and 2’ to 3’ (Bed 3) of New Providence formation in road cut just across from St. Joseph Church, at St. Joseph. Raywick Quadrangle, Lat. 37° 31’ 20” N, Long. 85° DIAL Oa Samples taken from the 6 foot fossiliferous shale in the Caney Creek member of the Brodhead formation (Bed 1), from near the top of the Brodhead formation (Bed 2), and from the Floyds Knob formation (Bed 3) along State Highway 55, 8.5 miles south-southwest of Lebanon, just north of Taylor County line near Findley Post Office. (Stockdale, 1939, p. 159). Spurlington Quadrangle, Lat. 37° 27’ 45” N, Long. 85° 20 alOLAVec 142 BuLLeETIN 196 Taylor County ; K-21. Sample taken from Somerset shale member (Bed 1) of the Salem lime- stone at Willowtown, 3.5 miles northwest of Soloma and up hill from Good Hope Baptist Church. (Stockdale, 1939, p. 210). Soloma Quad- rangle, Lat. 37726 307 °N, Long. 85 = 240 45% We Caldwell County K-22. Sample taken from the Renault limestone (shale) (Bed 1), in road cut at Flynn Creek at east edge of Princeton on U. S. Highway 62. Olney Quadrangle, Lat. 37° 7’ 34” N, Long. 87° 50’ 22” W. K-23. Samples taken from the Paint Creek (Bed 1), Cypress (Bed 2), Menard (Bed 3), and Kinkaid (Bed 4) formations at Walches Cut on Illinois Central RR track about 1.9 miles east-northeast of Scotts- burg. Princeton East Quadrangle, Lat. 37° 6’ N, Long. 87° 47’ W. K-24. Sample from shale in Paint Creek limestone (Bed 1) west of farm north of Sand Lick Road about 2.5 miles east of Bald Knob. Princeton East Quadrangle, Lat. 37° 4’ 20” N, Long. 87° 45’ 25” W. Breckenridge County K-25. Sample from the Glen Dean limestone (Bed 1) in old abandoned quarry west of creek at Glen Dean. Glen Dean Quadrangle, Lat. 37° 39’ 10” N, Long. 86° 32’ 30” W. Grayson County K-26. Sample from Glen Dean limestone (Bed 1) one mile south of Grayson Springs on State Highway 88. Clarkson Quadrangle, Lat. 37° 26’ 50” N, Long. 86° 13’ 25” W. Metcalfe County K-27. Sample taken from transition between New Providence and Brodhead formations (Bed 1) in road cut on north side of Edmonton just south of South Fork of Little Barren River, on State Highway 80. Edmonton Quadrangle, Lat. 36° 58’ 50” N, Long. 85° 36’ 47” W. Cumberland County K-28. Section measured on big hill on State Highway 90 northwest of Burkesville. Waterview Quadrangle, Lat. 36° 47’ 37” N, Long. 85° 22' 32” W. Pulaski County K-29. Sample from the Glen Dean limestone (Bed 1) on RR cut just east of Sloans Valley at Sloans Valley Tunnel. Burnside Quadrangle, Lat. 36° 56’ 40” N, Long. 84° 33’ 30” W. K-30. Sample from upper 16.5 feet of Pennington shale (Bed 1) above 6 foot siltstone bed, 1.5 miles northwest of turnoff to Sloans Valley on U. S. 27. Burnside Quadrangle, Lat. 36° 57’ N, Long. 84° 34’ W. K-31. Samples from the top of the Golconda limestone (Bed 1) at top of quarry and from the Hardinsburg shale (Bed 2) at Tatesville Quarry, .5 miles south of Tatesville on U. S. Highway 27. Burnside Quadrangle, Lat. 36° 56’ 45” N, Long. 84° 34’ 40” W. K-32. Section at Fishing Creek, Lake Cumberland, west of Somerset. Delmer Quadrangle, Lat. 37° 3’ 55” N, Long. 84° 41720” W. Casey County K-33. Samples from the silts in the Floyds Knob formation (Bed 3), the upper 10 feet of the Brodhead formation (Bed 2), and from the McKin- K-34. MIsSISSIPPIAN SMALLER FORAMINIFERA: CONKIN 143 ney Knob siltstone member (Bed 1) of the Brodhead formation about 7 miles northwest of Liberty along State Highway 49 at steep hill from plateau to valley of Martins Creek. (Stockdale, 1939, pp. 210, 211). Bradfordsville NE Quadrangle, Lat. 37° 25’ 15” N, Long. 85° 0’ 2.5” W. Sample from within lower 80 feet of the New Providence formation (Bed 1) in road cut on State Highway 78 west of junction of 78 and County Road 906 at Turkeyfoot Gap, one mile west of county line. Ellisburg Quadrangle, Lat. 37° 27’ 55” N, Long. 84° 52’ 45” W. Boyle County K-35. Lincoln K-36. Section measured at exposures on slopes behind farm on north side of County Road 300, west of Junction City, and 1.4 miles west of State Highway 35. Junction City Quadrangle, Lat. 37° 35’ 22.5” N, Long. 84° 48’ 15” W. County Samples from the lower 2-3” of the New Providence formation (Bed 1); from the upper 40 feet of the New Providence formation (Bed 4) ; from the lower (Bed 2) and upper (Bed 3) part of the lower 70 feet of the New Providence formation; from shaly siltstone with calcareous concretions, about 70’ below the Floyds Knob, in the Brodhead forma- tion (Bed 5); and from the Floyds Knob formation (Bed 6); along U. S. Highway 27, at Halls Gap, 4.5 miles south-southeast of Stanford. (Stockdale, 1939, pp. 162, 163). Halls Gap Quadrangle, Lat. 37° 27’ 40” N, Long. 84° 38’ W. . Sample from the lower 2 feet of the New Providence formation, 3.3 miles west of Crab Orchard on the Halls Gap Road. Crab Orchard Quadrangle, Lat. 37° 25’ 45” N, Long. 84° 32’ 30” W. . Section measured in road cut on east side of U. S. Highway 150, at county line of Rockcastle and Lincoln counties, 2.6 miles south of inter- section of 150 and State Highway 39. Brodhead Quadrangle, Lat. 37° 26’ N, Long. 84° 27’ 58” W. . Samples taken from the Brodhead (Bed 1) and the Floyds Knob (Bed 2) formations; section measured from the New Albany through the New Providence formations; at Cruzes Gap, 3.2 miles south of Crab Orchard on State Highway 39. Crab Orchard Quadrangle, Lat. 37° 25’ N, Long. 84° 30’ 30” W. Rockcastle County K-40. K-41. K-42. K-43, Sample from the lower part (Bed 1) of the New Providence forma- tion, about 1.5 miles southeast of Brodhead on U. S. Highway 150. Brodhead Quadrangle, Lat. 37° 23’ N, Long. 84° 24’ 55” W. Samples taken from the uppermost part (Bed 1) of the Brodhead for- mation and the Wildie siltstone member (Bed 2) of the Muldraugh formation, just south of Renfro Valley on U. S. Highway 25. Wildie Quadrangle, Vat. 37> 23’ N, Wong: 845 19% 50% We Sample from the Paint Creek limestone (shale) (Bed 1) at top of road cut at top of hill about 4 miles north of Renfro Valley on U. S. Highway 25. Wildie Quadrangle, Lat. 37° 25’ N, Long. 84° 19’ W. Sample from the Pennington marine limestone (Bed 1), on U. S. Highway 25, 1.1 miles north of the Rockcastle River, 2.6 miles south of Livingston. Bernstadt Quadrangle, Lat. 37° 14’ 40” N, Long. 84° 1S See Madison County K-44. Section measured at Boone Gap, along U. S. Highway 25, 3.5 miles south-southwest of Berea. Berea Quadrangle, Lat. 37° 31’ 40” N, Long. 84° 19’ 10” W. 144 K-45. BuLLETIN 196 Section measured along U. S. Highway 421 at Big Hill, about 5 miles southeast of Berea. Big Hill Quadrangle, Lat. 37° 32’ 10” N, Long. 84° 12’ 45” W. Jackson County K-46. Samples taken from the horizon of the Big Clifty sandstone (Bed 1) and from shale in the Hardinsburg sandstone (Bed 2), at Clarks Station Quarry, 2.4 miles south of Morill on U. S. Highway 421. Johnetta Quadrangle, Lat. 37° 29’ 55” N, Long. 84° 8’ 52.5” W. Estill County K-47. K-48. K-49. K-50. Samples taken from the Trousdale formation (Bed 2) and upper 1.75 feet of the Portwood formation (Bed 1) on State Highway 52 at entrance to the McLaughlin farm, one mile east of Waco. (Campbell, 1946, p. 366). Moberley Quadrangle, Lat. 37° 34’ 15” N, Long. 84° 7’ 40” W. Sample taken from lower 4 feet of the New Providence formation (Bed 1) at cliff along north side of L&N RR track, just east of Cow Creek where it joins the Kentucky River, 2.5 miles southeast of Irvine. (Stockdale, 1939, p. 121). Irvine Quadrangle, Lat. 37° 40’ 55” N, Long. 83° 56’ 30” W. Sample taken from the Conway siltstone (Bed 2) and the lower part of the New Providence formation (Bed 1) along State Highway 52 below Estill County Quarry, at steep hill about 4 miles east of Irvine. (Stockdale, 1939, p. 168). Irvine Quadrangle, Lat. 37° 42’ 30” N, Long. Hee BN HOS Wife Section measured in L&N RR cut, .5 miles north of Hargett, 6 miles northwest of Irvine. (Measured by Campbell, 1946, p. 866). Palmer Quadrangle, Lat. 37° 47’ 7” N, Long. 84° 0’ 53” W. Powell County K-51. K-52. Section measured on Pompeii Hill up from quarry, .4 miles northeast of Clay City. Clay City Quadrangle, Lat. 37° 51’ 45” N, Long. 83° 54’ 40” W. Section measured in road cut on County Road 213, 7.4 miles south of Jeffersonville. Means Quadrangle, Lat. 37° 53’ 8” N, Long. 83° 51’ 49” W. Clark County K-53. K-54. Section measured at Lulbegrud Creek along secondary road which leads east and then south from State Highway 52 at the north edge of Indian Fields, about .5 miles east of Indian Fields and .75 miles northwest of Powell County line. Levee Quadrangle, Lat. 37° 56’ 10” N, Long. 83° 59’ 10” W. Section measured on west side of Lulbegrud Creek at barn on poor road, 1.1 miles in straight line east-southeast of Indian Fields. Levee Quadrangle, Lat. 37° 56’ N, Long. 83° 58’ 45” W. Montgomery County K-55. Section measured along secondary road leading north from U. S. Highway 460, .6 miles north of junction, .25 miles east of bridge over Slate Creek, 2.25 miles east of Jeffersonville. (Measured by Stockdale, 1939, pp. 93, 94). Means Quadrangle, Lat. 37° 58’ 30” N, Long. 83° 48’ 55” W. MISsSISSIPPIAN SMALLER FORAMINIFERA: CONKIN 145 Menifee County K-56. Samples from the Frenchburg freestone (Bed 1) and the Haldeman siltstone (Bed 2) at Frenchburg Quarry, .5 miles west of Frenchburg on U. S. Highway 460, and 300 yards north of the highway. French- burea@Ouadrangle wats 5742-0 Nw ones Som 684 224) We Bath County K-57. Section measured along “Old Virginia State Road,’ .25 miles west of Olympia Springs. Olympia Quadrangle, Lat. 38° 3’ 37” N, Long. 83° 40’ 45” W. Rowan County K-58. Section measured in roadcut on U. S. Highway 60, .4 miles east of Bluestone, 5.5 miles west of Morehead, just northeast of RR track. (After fig. 7, Geol. Soc. Kentucky Field Trip Guidebook, 1955). Farmers Quadrangle, Lat. 38° 8’ 55” N, Long. 83° 30’ 15” W. K-59. Samples from the Farmers siltstone member of the New Providence formation (Bed 2) and the New Providence formation (Bed 1), in road cut on U.S. Highway 60, .5 miles southwest of intersection of 60 and County Road 519, southwest of Morehead. Morehead Quadrangle, Lat. 38° 9’ 50” N, Long. 83° 26’ 50” W. K-60. Sample from the Rothwell shale (Bed 1), on Morehead Lookout Tower road about 1.5 miles in straight line east of Morehead. Morehead Quadrangle, Lat. 38° 10’ 25” N, Long. 83° 24’ 25” W. K-61. Section measured in road cut on State Highway 32, 1.85 miles south of Hilda Post Office. Haldeman Quadrangle, Lat. 38° 11’ N, Long. 83° 30’ W. Fleming County K-62. Section measured along State Highway 32, extending .7 miles west- northwest of Rowan County line, 9 miles southeast of Goddard. (Measured by Stockdale, 1939, p. 96). Plummers Landing Quadrangle, Eat 38 15) 45 Ne ong: 83253 457 We K-63. Section measured along county road leading from Wallingford to Poston School, at hill one mile northeast of Wallingford. (Modified after Stockdale, 1939, pp. 96, 97). Burtonsville Quadrangle, Lat. 38° 24302 N one: 83.635) 457° WV. Carter County K-64. Sample from the upper 6 feet of the Rothwell shale (Bed 1), in road cut on U. S. Highway 60, 2.75 miles southwest of Olive Hill. (Stock- dale, 1939, p. 218). Olive Hill Quadrangle, Lat. 38° 17’ 30” N, Long. SS iene sual Se We : Lewis County K-65. Sample from green-gray shale (Bed 1) in New Albany at road level and above 40 feet of New Albany in road cut 2 miles west of Vance- burg and .3 miles southwest of bridge over Salt Lick Creek, on State Highway 10. Vanceburg Quadrangle, Lat. 38° 35’ 20” N, Long. 83° PR TS NY K-66. Section measured along road from Vanceburg to Tannery, at north side of Ganders Branch; bottom of section 1.25 miles south of C&O RR station at Vanceburg; section continues east-southeast up hill for .75 miles. (Measured by Stockdale, 1939, pp. 98, 99). Vanceburg Quad- rangle, Lat, 38- 35/°5” N.onp, $3 19% We 146 BuLLETIN 196 K-67. Section measured along poor secondary road at head of Montgomery Creek, leading up steep hill to Greenup County line; top of section 5 miles southeast of Garrison; bottom of section 2 miles along road south of Rexton Post Office. (Measured by Stockdale, 1939, pp. 187, 188). Brushhart Quadrangle, Lat. 38° 35’ 15” N, Long. 83° 6’ 30” W. Greenup County K-68. Section measured near south end of Ohio River bridge, along secondary road ascending bluff, in steep ravine and on hillside. (Measured by Stockdale, 1939, p. 181). Portsmouth Quadrangle, Lat. 38° 43’ 15” N, Long. 82° 59” 40’ W. INDIANA Perry County I-1. Section measured in Kunkler Quarry, on U. S. Highway 460, 1.3 miles west of Uniontown Post Office. (After fig. 7, Geol. Soc. Kentucky Field Trip Guidebook, 1952). Lat. 38° 14’ N, Long. 86° 42’ W. Clark County I-2. Samples from the Button Mold Knob member (Bed 1) of the New Providence formation along secondary road 1.25 miles north of Car- wood. Speed Quadrangle, Lat. 38° 27’ 30” N, Long. 84° 52’ 30” W. I-3. Samples from the Coral Ridge (Bed 1) and Button Mold Knob (Bed 2) members of the New Providence formation at the Louisville Cement Company Quarry, on State Highway 60, 2.6 miles northwest of the intersection of Highway 60 and U. S. 31W, about 8 miles north of New Albany. Speed Quadrangle, Lat. 38° 24’ N, Long. 85° 38’ W. Floyd County I-4+. Samples from the Jacobs Chapel shale (Bed 1), Rockford limestone (Bed 2), and the lower 3 feet of the New Providence formation (Bed 3), one mile northwest of Jacobs Chapel Church and U. S. Highway 31W, where creek crosses Chapel Lane Road. New Albany Quad- rangle, Lat. 38° 21’ 55” N, Long. 85° 47’ 35” W. I-5. Sample from the Floyds Knob formation, at Spickert Knob, along road up the escarpment, 3.5 miles northwest of New Albany. New Albany Quadrangle, Lat. 38° 19’ 53” N, Long. 85° 51’ W. I-6. Section measured at Goetz Quarry, .5 miles west of New Albany city limits on U. S. Highway 460. New Albany Quadrangle, Lat. 38° 16’ 30” N, Long. 85° 50’ 35” W. TENNESSEE Davidson County T-1. Sample from the Maury shale (Bed 1) at Bakers, a station on the L&N RR. (Campbell, sec. 43, 1946, p. 887). Ridgetop Quadrangle, Lat. 36° 22’ N, Long. 86° 17’ W. Sumner County T-2. Section measured 200 yards north of Garretts Creek Church, north of Westmoreland. (After Campbell, sec. 37, 1946, p. 885). Lat. 36° 33’ 30” N, Long. 86° 14’ 30” W. Macon County T-3. Section measured in road cut on State Highway 52, 8 miles west of Red Boiling Springs. (After Campbell, sec. 42, 1946, p. 887). Red Boiling Springs Quadrangle, Lat. 36° 30’ 8” N, Long. 85° 57’ 20” W. MIsSsISSIPPIAN SMALLER FORAMINIFERA: CONKIN 147 Clay County T-4. Section measured along State Highway 52, 4 miles southeast of Celina. (After Campbell, sec. 41, 1946, p. 887). Lillydale, Kentucky, Quad- rangle, Lat. 36° 30’ 20” N, Long. 85° 27’ 30” W. OHIO Scioto County O-1. Section measured at cliffs north of Buena Vista, on U. S. Highway 52. (Modified after Hyde, 1953, pp. 196, 197). Buena Vista Quad- angle: seat. 382 37. 145% N leone. 683001544524) Wee O-2. Section measured behind Greystone Motel on U. S. Highway 52, just west of Portsmouth. Pond Run Quadrangle, Lat. 38° 43’ 47” N, Long. 83 (2/302 We O-3. Section measured in road cut at hill 3 miles north of Portsmouth on U. S. Highway 23. Sciotoville Quadrangle, Lat. 38° 45’ N, Long. 82° 57’ W. O-4. Section measured on secondary road leading north from State High- way 73 at Henley, up hill northeast of Henley. Otway Quadrangle, ates Siero Ne ong 8S 9 015.2 Wis Pike County O-5. Section measured at bridge over Beaver Creek, .75 miles southeast of Piketon. Waverly Quadrangle, Lat. 39° 3’ 30” N, Long. 82° 59’ 50” W. O-6. Section measured along County Road 772, south of Nipgen and just south of Ross-Pike County line. Nipgen Quadrangle, Lat. 39° 11’ 14” N, Long. 83° 9’ W. Ross County O-7. Section measured along Jester Hill Road, 1.5 miles south of U. S. Highway 50 at Bainbridge. Sunbury shale at sharp bend in road where poor road intersects Jester Hill Road. Sample of Bedford shale taken one mile south of Highway 50 on Jester Hill Road. Bainbridge Quadrangle, Lat. 39° 12’ 25” N, Long. 83° 16’ 12” W. O-8. Section measured on N&W RR track, one mile north of Higby. Waverly Quadrangle, Lat. 39° 11’ 30” N, Long. 82° 52’ W. Fairfield County O-9. Sample from shale in the Maxville limestone (Bed 1), Rush Creek Limestone Company Quarry, Rushville. Thornville Quadrangle, Lat. 39° 45’ 30” N, Long. 82° 27’ 45” W. ; Franklin County O-10. Sample from transition bed between Bedford shale and Ohio shale (Bed 1), at southeast side of dam at Central College. Westerville Quadrangle, Lat. 40° 46’ 15” N, Long. 82° 52’ 50” W. Wayne County O-11. Sample from shale bed no. 4 in the lower 5 feet of the Black Hand sandstone member (Bed 1) of the Cuyahoga formation at Armstrong. West Salem Quadrangle, Lat. 40° 54’ 40” N, Long. 82° 0’ 30” W. 148 BULLETIN 196 CORRELATION CHARTS Chart 1 shows the correlation of Upper Devonian and Lower and Middle Mississippian formations in southern Indiana, Kentucky, northern Tennessee, and southcentral Ohio. In general, only those names of formations and members are used in which Foraminifera were found. Each column is generalized from the measured sections at the localities indicated at the top of the column. Chart 2 correlates the Upper Mississippian (Chesterian) forma- tions of southern Indiana, and western and southeastern Kentucky. MEASURED SECTIONS Beds in which Foraminifera were found are indicated by an asterisk before the bed number, Not all other beds were sampled, but most were, and thus beds without an asterisk may generally be taken to be unfossiliferous as regards Foraminifera. Most of the sections were measured by me; many of them in Kentucky and southern Indiana were based on Stockdale’s (1939) locations and determinations as to stratigraphic level, and a few of the sections are given as measured by Stockdale. The sections in ‘Tennessee are based on Campbell’s (1946) work as to location and stratigraphic placement. The sections in Ohio are largely based on Hyde’s (1953) locations and stratigraphic determinations, but most were measured by me. Samples were taken throughout 5.5 foot intervals, or from lithologically and stratigraphically distinct units thinner than 5.5 feet. MISSISSIPPIAN DEVONIAN KINDER- HOOKIAN Hannibal- Chouteau MERAMECIAN OSAGIAN Salem-St. Louis- Ste. Genevieve Fern Glen- Burlington Dre War Upper saw | Harrodsburg Southern Indiana 1-2-6 Northwestern Kentucky K-1-19 Edwardsville \ Brodhead Brodhead New Providence |Jacobs Chapel | Ridge ami | IV New Albany New Albany N Providence Chart]. Southern Kentucky K-20, 32-41 ZL, ety 28; Bedford [FallingRun} "| jee ree = 1 aaa Correlation of Upper Devonian and Lower and Middle Mississippian Formations in southern Indiana, Kentucky, northern Tennessee, and south-central Ohio (after Stockdale, 1939, Plate 6, and Campbell, 1946, Plate 2). ° 2 Thickness of beds is generalized. Thickness 5 A ee Ta) of thinnest units is 3 exaggerated. o hastern a o Kentucky iF i<-51-04 ry 2 Bin a Southeastern a I) : fy | Kentucky Rothwell S Ba K-44, 45, 47-50 Floyds Knob ro) 2 are [ st. Louis | i S St. Louis Muldraugh =) (igi ds Knob Northern Indian Christ Tennessee Fort uf eT Creek Combs Mountain Brodhead Conway Cut New ovidenc New Providence Pp Sunbur Sanderson 1 o Bk) + a cs O = New Albany New Albany [____] Sunbury | Bedford Blackistor Northeastern Kentucky and southern Ohio K-65-68, O-l, 2 South-central Ohio O-6-l1 Haldeman Southern Ohio / 0-3-5 Brodhead Christy Creek Cuyahoga Cuyahoga Bedford Bedford Sanderson os i i a . pS et aS af ON Pine es ee Se ‘or | ot ee jas .; a ) , 2 “7 7 4. | 4 t ; \ 7 ' 7 é — - oo han : , a = } >a : f yi : ‘ . ° t io i Ax, anil - ee i j ; m i‘ ‘ I ’ A 7 ' ; 4 e ; ei mei = ; i ~ ¥ * MIssIssipPIAN SMALLER FORAMINIFERA: CONKIN 149 Chart 2. Correlation of Chesterian formations of southern Indiana, and western and southeastern Kentucky. Southern Indiana and western Kentucky I-l, K-22-26 Clore Palestine Southeastern Kentucky Menard K-29e 30m ity 425045. 46 Waltersburg Vienna Pennington | Tar Springs [cienDean [| [ten Dean _| Hardinsburg ea Hardinsburg ier [oleae G lCypress |__| Big City Paint Creek Paint Creek MiIssIlsslP PLAN Cr S le Ree Sample Renault 150 BULLETIN 196 LOCALITY K-1 ye w . Shale, olive gray; covered above. . Siltstone. . Shale, olive gra I il | Shale with two thin siltstone layers. 116" . Shale, olive gray. KENWOOD SS. MBR Siltstone. Shale, olive gray; no large ironstone concretions. Shale, olive gray, silty at various horizons; large ironstone 158' exposed sll HI Whit concretions, rarer in upper Iv“ feet. \ 2 O a O m4 A, Shale, olive gray; worm markings; Conularia in float. NEW BULDTON MOLD KNOB MEMBER MAUL . Shale, blue gray. 4 < 4 4 4 . Double ironstone cone-in-cone. Shale, olive gray; worm markings. 2. Ironstone lenses. *], Shale, blue gray; transitional to olive gray in upper part; covered below. (OTHER Coral Ridge mbr. MISSISSIPPIAN SMALLER FORAMINIFERA: CONKIN 151 TOGA, K-2 . Sandstone, buff; middle bed with ironstones; olive gray shales —< between sandstone beds. KENWOOD SANDSTONE MEMBER (ero nalerwolineso nays 6. Shale, dive gray, with ironstone concretions; no megafossils. =e . Shale, olive gray, with ironstone = oe. concretions; Button Mold Knob fama. 15'4!" aD *4. Shale, olive gray, with fossiliferous — limestone lenses. SINT OME Seis Visi mba Ee IER CO) W/ IID) 1) ISG Vd} TP OR MULAN WEIL OY IN Lower N EW 183 UW) IE AW LOVIN| MLO) ILD) — *3, Shale, olive gray, with rare lime- — stone lenses; cone-in-cone layer ; SLD eee aD - Coral Ridge fauna. *2. Shale, olive gray, mostly covered. member 22'1'! Coral Ridge sees 1, Shale, olive gray, with phosphatic ~— nodules; not measured. Run 152 BuLLETIN 196 LOCALITY K-3 : ce * 6, Siltstone, sandstone, and shale; buff to olive gray. KENWOOD SANDSTONE *5, Shale, olive gray; no megafossils. 7'9" *4, Shale, bluish gray, ironstone concretions; no megafossils. 189' exposed 1 i itt * MIDDLE *3, Shale, bluish gray; very rare Button Mold Knob fauna. BUTTON MOLD KNOB MEMBER LOWER HUT CTE Ga il 4 4 4 4 4 *2, Shale, bluish gray; cone-in-cone layers, kidney ironstone concretions; Coral Ridge fauna. iti NEW PROVIDENCE FORMATION UPPER nT * 1. Shale, olive gray; no megafossils; covered below. CORAL RIDGE MEMBER a \ MISssISSIPPIAN SMALLER FORAMINIFERA: CONKIN 153 LOCALITY K-4 *8. Shale, olive gray, soft; fossiliferous lenses, crinoidal concretions; large ironstone concretions, . Covered. MIDDLE . Shale, olive gray, soft, fossiliferous. . Covered. . Shale, blue gray, soft; many fossils. BUTTON MOLD KNOB MEMBER . Shale, blue gray; rare fucoids; no other megafossils noted. ~ Z O HH < a ~ O fa fx] O Z fx] Q > O ox A, = By Z . Shale, blue gray; small kidney iron- stones; cone-in-cone layers at top and base of unit; Coral Ridge fauna. . Shale, gray blue; no megafossils noted. CORAL RIDGE MBR. LOWER UPPER 154 BULLETIN 196 LOCALITY K-6 * 8. Sandstone and siltstone. KEN WOOD SS. 0 ~y- ag | | (BiH [| | Lit if: * 7, Shale, olive gray; rare Button Mold Knob fauna, ZS) ele THANTHIE *6,. Shale, olive gray; crinoidal limestone patches; Button Mold Knob fauna *5,. Shale, olive gray; crinoidal lime- stone patches; large ironstone concretions; Button Mo nob E BUTTON MOLD KNOB MEMBER §\¢ iK *4, Shale, olive gray, with limestone lenses and ironstones. oy GU Z. O H < 2 ee O fx, a] O Zz ey al > O px, A, = fe Z. * 3, Shale, olive gray; kidney ironstones mostly covered. member *2. Shale, olive gray; no megafossils. Coral Ridge MIssIssipPIAN SMALLER FORAMINIFERA: CONKIN 15 On LOCALITY K-8 *9, Shale, blue-gray, green-gray, partly covered; covered above; kidney-ironstones throughout. {iit (Nii (EMME) <8. Cone-in-cone layer and coprolites. * 7. Shale, blue-gray. 20'5'' exposed Will 6. Ironstone nodules, 1'! thick ledge. *5, Shale, blue-gray; scattered coprolites. ITNT *4, Shale, blue-gray, with three layers of Coral Ridge nodules, GOR AE RY DiG HR THRHLE Z. O H g 2 a7 e) fy G] U Z fa] a > O ec A, = 7) zi ith bo . Shale, blue-gray. Hil a iy FALLING *2, Shale, orange-olive-gray, with RUN phosphatic nodules at base. rate I Shale» black) fissile. meas ALBANY | meas 156 BuLLETIN 196 LOCALITY K-10 Siltstone, massive, weathers shaly; blue gray to buff; worm markings; covered above. LEBANON JUNCTION SILTSTONE MBR. Shale, silty, olive gray; buff in uppermost part; partly fossiliferous. BRODHEAD FORMATION ad fz] Q = (2) = [x] ra < + WY WY O Z ~ a, n (od fx] > «J 5 O PTET FLEET PEREE TET EEPLSEHP EEE MISSISSIPPIAN SMALLER FORAMINIFERA: CONKIN LS7 LOCALITY K-11 *5. Siltstone and shale; not measured. siltstone Keith Knob RHUL *4, Shale, blue brown gray to blue gray; browner at base, 1OWo * 3. Shale, green gray; one Bellerophon noted. *2, Shale, green gray; glauconitic in upper part. Z O fH < 2 mx O fy fy] O Zi ea) A > Oo fo A, = ea Z, 1. Shale, green gray, with phosphatic nodules. Falling Run le { Hil H TAHA i | Ir | { I Hit nt HII Hi | { 158 BULLETIN 196 HOGADTIT Yi ake 12 *5, Shale, green gray; partly to mostly covered, *4, Shale, green gray; some kidney ironstone nodules; less fossiliferous than below; partly covered. @ HHH Hitt cs O H < 2 fx O fy fx] O A ea A > O me a, = fz) Z *3, Shale, green gray, fossiliferous; infrequent kidney ironstones; crinoid stems replaced by limonite. int | ihe ill| I *2, Shale, soft, green gray. * 1, Shale, hard, green gray, with phosphatic nodules. MISSISSIPPIAN SMALLER FORAMINIFERA: CONKIN 159 HOGA Yok=13 *12. Shale, olive gray; frequent ironstone chips, but no large ironstones noted; covered above. ll. Ironstone bed. *10. Shale, olive gray. Ironstones, large, in discontinuous band. *8. Shale, blue gray; Conularia in an ironstone chip. Ironstones, large. *6. Shale, blue gray. *5. Shale, blue gray; frequent kidney iron- stones; common coprolites; Conularia, one Bembexia ellenae noted. * 4. Shale, blue gray to olive gray. me) o n fe) Q » ) + ive) Zz O i < = fag O fy ea) O Z fx a) > O fae A, = fy Zz *3. Shale, olive gray, with two thin calcar- eous bands with incipient cone-in-cone structure. *2,. Shale, olive gray. *1, Shale, olive gray, with phosphatic nodules. 160 BuLLeTIN 196 LOCALITY K-14 — *10. Siltstone, shaly; not measured. 9. Covered; not measured. * 8. Shale, sandy, olive gray, slumped, weathered to red clay; gravel on surface. * 7. Shale, olive gray, clayey. Za O Se O om . Covered N E W . Shale, olive gray to blue gray. . Shale, not sampled. . Shale, olive gray to blue gray. . Shale, hard, olive gray, with large phosphatic nodules. . Shale, black, fissile; not measured, MIssIssIPpPIAN SMALLER FORAMINIFERA: CONKIN 161 LOCALITY K-15 6. Limestone, fine grained to dense, blue gray. SALEM LIMESTONE * 4, Shale, with limestone lenses; bryozoans. il iA Ni ft \ ed Q 2 fy 4 a6 ae ep) H ey WY mG G 2 O WwW 3. Limestone, massive, crinoidal; bryozoans. (resi | ae ( | *2, Shale, crinoidal streaks; bryozoans. i —= — Ce 1. Limestone, massive, gray; bryozoans, HARRODSBURG LIMESTONE 162 BULLETIN 196 bt OG AILEY (Koh? *5, Shale, green gray, partly covered. * 4. Shale, green-gray. Z. O H < 2 ed O ty ] O Z e) a) > O a A, NEW *3, Shale, gray green; at top, common coprolites and one shark's tooth, *2, Shale, green gray, with phosphatic nodules. 1. Shale, black, fissile; not measured, MIssIssIpPIAN SMALLER FORAMINIFERA: CONKIN 163 LOCALITY K-18 8. Shale, olive gray, siltier than below, no ironstones, very rare coprolites; covered above. *7, Shale, clayey, olive gray. A yu le i {\@, (i tI HH *6. Siltstone, shaly, ferruginous. Ol. bt *5, Shale, clayey, olive gray; coprolites and ironstones, Ot | 4 | *4, Shale, clayey, olive gray; coprolites. ue) oO n ° jee * 1?) Sa Ww Z O H xt a a fe) bey es O Z &] A. > O ee a, = es Z, *3. Shale, olive gray. CHANIA HH ECT AHALHL 8 (| *2, Shale, olive gray, with phosphatic nodules. 1. Shale, black, fissile; not measured. 164 LOCALITY K-28 192' exposed PROVIDENCE FORMATION NEW BULLETIN 196 . Siltstone, hard, blue gray, with rare shaly spots; covered above. . Shale, silty. . Siltstone, massive, medium to fine grained; rare geodes noted. . Siltstone, hard, gray blue, calcareous; frequent quartz geodes. . Siltstone, hard, gray, calcareous, massive, weathers like shale; rare, impure limestone seams. Shale, hard, blue gray; rare, impure limestones about 1 foot thick. . Shale, hard, blue gray, with ironstone- cherty-crinoidal-limestone seams. . Shale. Limestone, crinoidal, . Shale, mostly covered. Limestone and shale; 3 inch limestone bed at base. . Shale, green yellow gray, with phosphatic bed near middle; rare nodules. . Shale, brown, with phosphatic nodules, Shale, black, fissile; not measured. MIssISSIPPIAN SMALLER FORAMINIFERA: CONKIN 165 LOCALITY K-32 Ssre== 14 Siltstone, bluish, weathering brown; fossiliferous. a 3. Limestone, cherty and silty. Ges-lce}: *12, Limestone, crinoidal, oblitic?. * 11, Limestone, cherty and silty; crinoidal omy EI in upper part; rare clay seams. KEOKUK LIMESTONE . Shale, silty, soft, bluish; fossiliferous. * 9. Siltstone and shaly siltstone; no fossils — noted in upper part; lower part with argillaceous limestone ledges; rare 190! crinoidal limestone lenses near base; lower one-fourth fossiliferous. 8. Covered. cies *7. Shale, fossiliferous; thin limestone lenses 6. Covered. 16'6" GS * 5. Shale, fossiliferous; common crinoidal limestone lenses up to 1. 5' thick. =—— * 4, Shale with siltstone layers. “crop -~ *« 3. Shale, fossiliferous, with thin crinoidal ap limestone lenses, 1-2'' thick, in INGE Wee ea @)hVe ley NiCr be ENOuRNieAuw inl @)IN| upper part. * 2, Shale, green gray, with ironstone nodules; snails? *1, Shale, green gray, with phosphatic nodules; New Albany shale below. 166 BULLETIN 196 LOCALITY K-35 * 7. Shale, olive gray; covered above, 6. Covered. 17'6'' exposed Z O H < a oa O fx, [3] O Z. (2) al = O fad A, NEW Shale, olive gray. Shale, olive gray to yellow, mixed. Shale, olive gray, with phosphatic nodules containing fossils. Shale, gray, with plant fossils. Shale, black, fissile, with many nodules; not measured. MIssissIpPIAN SMALLER FORAMINIFERA: CONKIN 167 LOCALITY K-38 Shale, blue gray, partly covered at top; rare coprolite? structures throughout. at =) Shale, blue gray, with regular-sized OHURATIOCHT Ha A kidney ironstones in middle portion; O coprolite? structures of limonite. H - < == a = lad os — O = fy [3] == = = *6. Shale, blue gray, softer than below; (3) Sapaaere no kidney ironstones noted. a) > — oO = mx = Ay = = = ea) — Z p_a>_ . ; : ; — *5. Shale, with rare kidney ironstones which = are larger than usual. S>-~ wl * 4. Shale, blue gray; partly covered. 22 3. Shale, olive gray, with phosphatic nodules. * 2, Shale, hard, gray, with some black shale in middle. Shale, black, fissile; not measured. 168 BuLLETIN 196 LOCALITY K-39 8. Siltstone, buff to olive gray, iron stained yellow-orange. a. «7. Shale, butt to olive gray, silty. 6. Large ironstone concretions in single bed. *5, Shale, olive gray, with some kidney ironstones. | it It i t HELEFEEUE it ae) vo n ° ey * o + +t Z O H < a x, O fay i] U Z 2) fal = O cx, A, NEW Nill mt 4. Covered. 3. Shale, gray to buff to olive gray, with phosphatic nodules; Tasmanites. *2. Shale, olive gray to brown. 1. Shale, black, fissile. MISSISSIPPIAN SMALLER FORAMINIFERA: CONKIN 169 LOCALITY K-44 ll. Siltstone, light gray to buff; worm markings and Taonurus. 10. Siltstone, olive gray. 9. Shale, gray to dark gray, very silty. BRODHEAD FORMATION CONWAY SILTSTONE 8 . Limestone, dense, gray. 7, shale, silty, blue gray, 6. Limestone lenses. *5, Shale, silty, dark gray to blue gray; ironstone concretions, ie *4, Shale, clayey, blue gray to olive gray. uw) N Z O H < 2 ae O fy Ea] O Zs ea] QA > O mG A, = [2] ZG dH TMi hell ite | 3. Siltstone lens, clayey. *2,. Shale, olive gray, clayey. 1. Shale, black, fissile; not measured. 170 BULLETIN 196 LOCALITY K-45 . Shale, buff to olive gray, silty; with large ironstone concretions; covered above. Brodhead Conway siltstone 10. Covered. 143! *9. Shale, olive gray. Shale, olive gray, partly blue gray, silty; rare small medium sized ironstones at top. . Covered. . Shale, blue gray to olive gra . Covered. Zi O H < 2 fd O ts, (2) UO Z re) a) = O fx, A, = fe Z. . Shale, blue gray to olive gray, silty, clayey. . Shale, olive gray, partly covered. Covered. . Shale, black, fissile; not measured. MIssISSIPPIAN SMALLER FORAMINIFERA: CONKIN 71 LOCALITY K-50 * 13. Shale, black and gray layers inter- bedded. BLACKISTON . Shale, black, fissile; with Schizobolus concentricus , Orbiculoides lodiensis. NEW ALBANY SHALE . Shale, gray, calcareous, with hard shale layers. . Shale, subfissile, black, calcareous; Lingulopora williamsana. Limestone. 8. Shale, fissile, black; no fossils. Limestone and calcareous shale. Shale, calcareous, black. Shale, earthy, greenish to black. Limestone, brown. Limestone, shaly, gray to black. = — = x) a uv 3 Me 13) oo h 3 a Zi e = gt a eg O fay a) O O = al od oO A, a ie) 5O) n =) fe) uy HH ad Gy Ay =) ta 4 a) Sr a od fj = fo) = Limestone, brown. Hamilton A Limestone. limestone iW BULLETIN 196 LOCALITY K-51 * 9. Shale, green gray, with some small ironstone nodules; covered above. 8. Ironstone bed, * 7, Shale, green gray in part, red to purple in part; partly hard silty beds; kidney ironstone nodules; fucoids. * 6. Shale, green gray, with some darker shale; partly covered. Z O al < 2 ea O 4 ea) O Z ca a) > O ag A, = &] Zi * 5. Siltstone. 4. Shale. 3. Shale, black, fissile, with some SuON softer brown and dark gray clay shale. . Shale, gray to olive gray. . Shale, black, fissile, with some soft yellow brown shale; not measured. MIssISSIPPIAN SMALLER FORAMINIFERA: CONKIN 173 LOCALITY K-52 “cee, 9. Siltstone ledge; covered above. | *8. Shale, green gray. — /*7.Shale, green gray, with phosphatic nodules. ~--; *6. Shale, black fissile; thin white sandstone cata ans layers with carbonaceous streaks in upper Z feet. ia] 4 < oc WY a) ag 2) Q Z =) 19] 5. Shale, brownish gray, softer than above and below. 4. Shale, black, fissile; no fossils. *3, Shale, upper 3'' thin bedded; lower 2"' hard chunky bed. *2. Shale, hard and soft. 1. Shale, black, fissile; not measured. NEW | BEDFORD 174 BULLETIN 196 LOCALITY K-53 *10. Shale, green gray to buff, covered above. . Siltstone, single bed, gray to drab, stained brown to black; no fossils. Shale, green gray to buff, clayey, iron stained. NEW PROVIDENCE FORMATION Falling . Shale, hard, greenish, with phosphatic Run nodules . Shale, hard to soft, brown. . Shale, black, fissile; phosphatic nodules with Lingula and Orbiculoidea, 510" by] -] t 00 WY i Mm >) Q a ~~ WY . Shale, grayish yellow to gray, weathered; no fossils, . Shale, black, fissile. . Shale, siliceous, brittle, olive gray to plue gray; 6 feet long, wedge in Sun- Shale, black, fissile; upper 2 feet sampled. MIssIssIpPIAN SMALLER FORAMINIFERA: CONKIN L/5 LOCALITY K-54 *8. Shale, green gray. Waddh i it ; } {1 | f . Shale, green gray; no nodules; some brown shale. lil * oO Shale, green gray; no nodules noted. a O al < 2 ag e) fy fx] O Zz ea) Q > O le Ay = fx] a * oa) Shale, green gray, some brown; no nodules noted. . Shale, hard, green gray; phos. noduleg Shale, hard, brown, some gray brown; some soft shale. Falling Ru SUNBURY? Atta abe! a eh Ladi BEDFORD; 2. Shale, soft, brown gray, clayey. . Shale, black, fissile. NEW ALBANY SH. ae 176 LOCALITY K-55 SUNBURY SHALE BEDFORD] 3:2" ea) 4 < a0) wn ALBANY NEW BULLETIN 196 % Ne) . Shale, clayey, green gray; not measured. . Siltstone, calcareous, hard, buff. . Shale, clayey, buff gray, weathered yellow. . Shale,. black, fissile; upper foot weathered soft, coffee-colored. * 5, Contact seam; weathered shale *4, Shale, sandy, semi-fissile in part; clayey, olive gray to buff at base. 3. Shale, black, fissile; upper 5 feet and lower 1 foot sampled. *2, Shale, clayey, olive green. l. Shale, black, fissile; not measured, MIssISSIPPIAN SMALLER FORAMINIFERA: CONKIN | WAT EOGALITY K-57 FS Le tisitomie) wsihailiy. Shale, olive gray, with ironstone concretions. NEW PROVIDENCE | a(/{ils init 7. Shale, black, fissile; some softer gray and brown shale in lower 3 feet. SUNBURY SHALE *6.Shale, gray to buff brown, sandy, calcareous. Sa o 5. Shale, black, fissile. fx] 4 < a0 n I Z xt ea) 4 oF ec A, = es Zz *3, Shale, clayey, blue gray, with thin silty layers. 2, Shale, black, fissile, SUNBURY SHALE 1. Shale, soft, sticky, yellow to buff to gray, some black; spores; not measured, MIssIssIpPIAN SMALLER FORAMINIFERA: CONKIN 179 LOCALITY: K-61 Siltstone, in smooth, even beds, with intercalated shales, gray, green, and purple. FARMER'S SILTSTONE Shale, olive gray to blue gray, clayey; silty in upper part, and gray to buff; middle part weathered; samples < O O 0 < mH 2 O A e) = < = a 2) fy fx] O Zz ea) A > e) m4 A, = ea) Zi taken from upper 2.5' and lower 2'. HENLEY SHALE MAHA * 1, Shale, black, fissile. SUNBURY 180 BULLETIN 196 HOCALITS- K=62 8. Shale, very silty. 7. Siltstone in single bed, gray to buff. 6. Shale and siltstone; no samples taken. 5. Siltstone, in smooth even beds separated by shale partings; gray to buff; ironstone concretions; PROVIDENCE FORMATION Taonurus. n a S o& 20 E+ o H » or Coal ky wn N EW 4, Shale, clayey, olive gray; sample taken from upper 2.5 feet. 3. Shale, black, fissile. 2. Shale, partly arenaceous, blue gray, with pyrite. BEDFORD l. Shale, black, fissile; not measured. MIssISSIPPIAN SMALLER FORAMINIFERA: CONKIN 181 LOCALITY K-63 Covered. ll. Siltstone, gray to buff, in single bed. *10. Shale, clayey, slightly silty, gray to drab, with ironstone concretions. . Siltstone, smooth even beds, separated by shaly partings; partly covered. . Shale, clayey; partly covered. 18'6"' . Shale, fissile, black. — . Shale, partly arenaceous, blue gray to BUG = olive gray; intercalated black fissile shales in lower part. . Shale, black, fissile. . Shale, green gray. . Shale, black, fissile. NEW ALBANY SHALE Shale, green gray. Shale, black, fissile; mostly covered. 182 BULLETIN 196 LOCALITY K-66 —-s- * 9, Shale, very silty, light gray; worm markings. Siltstone in smooth even beds up to 3"! thick, gray to drab, separated by shale partings up to l"' thick; Taonurus. Siltstone and shale, clayey, drab; Taonurus. VANCEBURG SILTSTONE Siltstone, drab, evenly bedded, with shale partings. Covered. < O = < > ~ 2 Z g — O eg a, = fa Z Shale, clayey, olive to maroon. SUNBURY}J)71 . Shale, black, fissile; soft, weathered SHALE to gray brown in upper part. BEREA ave aes i . Sandstone, gray to brown; ripple Ss. ———— marks. Shale, sandy in upper 6 feet, in irregular beds, light gray to buff; light to medium gray, soft, sticky, plastic shale in lower part; lower 15 feet covered. BEDFORD SHALE MIssISsIPPIAN SMALLER FORAMINIFERA: CONKIN 183 LOCALITY K-67 ROTHWELL] 6! *8. Shale, clayey, olive gray and SHALE — maroon. FLOYDS |thin —— \*7. Shale, silty, glauconitic, greenish KNOB FM.|streak/@.n ss black to olive gray. e = * 6. Siltstone, limestone lenses, and So amos silty shale, olive gray and maroon; m §} 35! BE fossiliferous; partly covered. 2 aoe ww » . ae a ny n = — 5 bs : 5. Siltstone with shaly zones; = o S 50! Fa IES fossiliferous. ) uv 3 oa) S eA Z © 4, Shale and siltstone, gray to drab; = partly covered. = 105! 2 NALA O ee fy —— Q wisi ttle as . . eS ROOF 3. Siltstone, massive, gray to drab; 5 ooo 8 sampled in lower part. 2 Sioa OO) sagt LAS W — fH a eae aes rs) Se a Saree O a 10! Cs geacees 2. Siltstone, shaly, iron stained; worm markings. . Shale, olive gray, silty, iron stained; ironstone lenses; worm markings. NEW 25! ay <= ea) Zz Zz O c= as S a ne) o, & 184 BuLLETIN 196 LOCALITY K-68 *6, Siltstone and shaly siltstone, blue gray to olive gray, shalier in lower part; Taonurus and worm markings. ail HALDEMAN SILTSTONE 5. Siltstone, massive, buff to drab. * 4, Siltstone, shaly, blue gray to olive gray; Taonurus and worm markings. Z. e) H < 2 oe O fy Q Oc 2 oa — 2 ke its | Ses a — O I Fs — {z] @D a) eS > Jc 5 — pe a, : 3. Shale, hard, gray; no phosphatic = 51 nodules. a) Zi é @@— *2. Shale, green gray, with large oc phosphatic nodules. " qT — 4 8 iad —_— z = 2 QP —_ 1. Shale, black, fissile; not measured. 190 BuLLETIN 196 LOCALITY O-1 3. Shale, fissile, black. *2, Sandstone, buff to tan to light gray, fine grained, evenly bedded, with siltstones and silty shale; some beds micaceous, < 3) io ea) ae) BEDFORD . Shale, black, fissile; covered below, OHIO SHALE MIssISSIPPIAN SMALLER FORAMINIFERA: CONKIN 191 LOCALITY O-2 * 9. Shale, silty, brownish gray. ARRAN RAT * 8: Shale, gray, platy; small ironstones. 7. Siltstone. . foe . . eee cee wpyete’ * 6. Shale, silty, with thin siltstones. * 5. Siltstone, in three beds, with two 2 inch shale breaks. VANCEBURG MEMBER *4, Shale, gray green. —— = ———_—— = — =—=—>—=—s — _—_— — —_—_— — _—_— = —= —— _—_— 3. Siltstone, massive. * 2, Siltstone, shaly, green gray; partly covered. Siltstones and sandstones up to 2.5 feet thick, with intercalated green gray shales up to 6 inches thick. CU YA OGA WORM AW Own 17'6" Ss 192 BULLETIN 196 LOCALITY O-3 *6, Siltstone, blue gray, gray, thin to medium bedded, with silty shale. *5, Shale, blue gray. 4, Covered by slump. *3, Shale, blue gray. Z oO oa < 2 a O fy < O e) a0) < 4 =) 1o) *2. Shale, blue gray, with thin siltstones. LAH ILO RAT EPEA REG ATA PORTO l. Shale, not sampled. MIssIssIPPIAN SMALLER FORAMINIFERA: CONKIN 193 WOCALITY O-4 Sandstone, light gray to blue gray; beds contorted; not measured. 6. Shale, not measured or sampled. 5. Shale, clayey, gray to yellow buff. * 4, Shale, clayey, gray to yellow buff. SAVE a) mG e) fy a) i) ea) * 3, Shale, clayey, gray to yellow buff. * 2, Shale, gray to dark gray; spores; not measured, transition zone. 1. Shale, black, fissile; not measured, OHIO SHALE ee 194 BULLETIN 196 LOCALITY O-5 3. Siltstone, gray; covered above. *2, Shale, blue gray, olive gray, buff, and reddish; clayey; thin siltstones, SHALE A mG O by 2) f] ea) . Covered, River level. MIsSsISSIPPIAN SMALLER FORAMINIFERA: CONKIN 195 LOCALITY O-6 M. 10. Shale, gray to blue gray, clayey, slightly silty. CUYAHOGA F HENLEY SH 9. Shale, black, fissile, becoming more clayey and browner upward. Covered. SUNBURY SHALE 7. Shale, gray, partly covered. 6. Shale, black, fissile 5. Sandstone, massive. 3. Sandstone, massive 2. Shale, thin. ae Tt \ *4. Shale, thin. 1. Sandstone, massive. BEREA SANDSTONE 196 BuLLETIN 196 LOCALITY O-7 *6, Shale, greenish-gray, clayey; ON some maroon shale in upper part; covered above. 30'6"! TMAH . Siltstone, buff to gray; ''Buena Vista". . Shale, gray, yellowish, buff, to reddish, clayey. CUYAHOGA FORMATI AG . Shale, black, fissile; road intersec- tion at base of Sunbury shale. . Sandstone; measurement from well on Lester's Crabtree Farm, i) Z O A WY) A A < wn <, ea ox ea -Q *1, Shale, gray to tan; sample taken 1 ‘mile south of Hiway 50 on Jester Hill Rd. MIssISSIPPIAN SMALLER FORAMINIFERA: CONKIN 197 LOCALITY O-8 *5. Shale, gray, clayey, with a few thin sandstones; covered above. 4. Sandstone, medium grained, red brown. es #3, Shale, gray, silty and clayey. 2. Sandstone, medium grained, reddish brown. l. Shale, gray, clayey with thin sandstones; sample from upper 2 feet. a O cal < = faa) O fy < O O 20) < val =) O 198 BULLETIN 196 STRATIGRAPHIC PALEONTOLOGY COMPOSITION OF THE FAUNAS A complete list of all Mississippian smaller Foraminifera ported in this study follows: Order FORAMINIFERA d’Orbigny, 1826 Family ASTRORHIZIDAE Brady, 1881 Genus CRITHIONINA Goés, 1894 C. palaeozoica, n. sp. Genus THURAMMINOIDES Plummer, 1945 emend. T. sphaeroidalis Plummer, 1945 emend. Family SACCAMMINIDAE Brady, 1884 Subfamily SACCAMMININAE Brady, 1884 Genus PROTEONINA Williamson, 1858 P. cumberlandiae, n. sp. P. wallingfordensis, n. sp. Family HYPERAMMINIDAE Eimer and Fickert, 1899 Subfamily HYPERAMMININAE Cushman, 1910 Genus HYPERAMMINA Brady, 1878 emend. Conkin, 1954 H., casteri, n. sp. H. kentuckyensis Conkin, 1954 H. rockfordensis Gutschick and Treckman, 1959 Family EARLANDITDAE Cummings, 1955 Genus EARLANDIA Plummer, 1930 E. consternatio, n. sp. Family REOPHACIDAE Cushman, 1927 Subfamily REOPHACINAE Cushman, 1927 Genus REOPHAX Montfort, 1808 R. cf. R. arenatus (Cushman and Waters), 1927 R. asper Cushman and Waters, 1928 R. kunklerensis, n. sp. R. cf. R. lachrymosus Gutschick and Treckman, 1959 R. mcdonaldi, n. sp. R. cf. R. minutissimus Plummer, 1945 re- MISSISSIPPIAN SMALLER FORAMINIFERA: CONKIN 199 Family TOLYPAMMINIDAE Cushman, 1929 Subfamily INVOLUTININAE Cushman, 1910 Genus INVOLUTINA Terquem, 1862, emend. Loeblich and Tappan, 1954 I. exserta (Cushman), 1910 I. longexserta Gutschick and Treckman, 1959 I. semiconstricta (Waters), 1927 Genus GLOMOSPIRA Rzehak, 1888 G. articulosa Plummer, 1945 Genus LITUOTUBA Rhumbler, 1895 L. semiplana, n. sp. Subfamily TOLYPAMMININAE Cushman, 1928 Genus TOLYPAMMINA Rhumbler, 1895 T. botonuncus Gutschick and Treckman, 1959 T. cyclops Gutschick and Treckman, 1959 T. jacobschapelensis, n. sp. T. laocoon, n. sp. T. tortuosa Dunn, 1942 Genus AMMOVERTELLA Cushman, 1928 A. cf. A. inclusa (Cushman and Waters), 1927 A. labyrintha Ireland, 1956 A. cf. A. primaparva Ireland, 1956 Genus TREPEILOPSIS Cushman and Waters, 1928 T. glomospiroides Gutschick and Treckman, 1959 T. recurvidens Gutschick and Treckman, 1959 T. spiralis Gutschick and Treckman, 1959 Family LITUOLIDAE Reuss, 1861 Subfamily HAPLOPHRAGMIINAE Cushman, 1927 Genus AMMOBACULITES Cushman, 1910 A. gutschicki, n. sp. Family TEXTULARIIDAE d’Orbigny, 1846 _ Subfamily TEXTULARIINAE d’Orbigny, 1846 Genus CLIMACAMMINA Brady, 1873 C. mississippiana, n. sp. FamilyMILIOLIDAE d’Orbigny, 1846 Genus AGATHAMMINA Neumayr, 1887 A. mississippiana, n. sp. Family OPHTHALMIDIIDAE Cushman, 1927 Genus HEMIGORDIUS Schubert, 1908 H. morillensis, n. sp. 200 BuLLETIN 196 Family TROCHAMMINIDAE Cushman, 1929 Genus TROCHAMMINA Parker and Jones, 1959 T. ohioensis, n. sp. Family PLACOPSILINIDAE Cushman, 1927 Genus STACHEIA Brady, 1876 S. cicatrix, n. sp. S. neopupoides, n. sp. S. trepeilopsiformis, n. sp. The Foraminifera presented in the above faunal list are alloted to twelve families, one of which, the Miliolidae, is new to the Mississippian; to eighteen genera, seven of which are new to the Mississippian: Agathammina, Climacammina, Crithionina, Pro- teontna, Stacheia, Thuramminoides, and Trochammina; to 38 species, 18 of which are described as new species: Agathammina mississip- piana, Ammobaculites gutschicki, Climacammina mississippiana, Crithionina palaeozoica, Earlandia consternatio, Hemigordius moril- lensis, Hyperammina castert, Lituotuba semiplana, Proteonina cum- berlandiae, P. wallingfordensis, Reophax kunklerensis, R. mcdonald, Stacheia cicatrix, S, neopupoides, S. trepeilopsiformis, Tolypammina jacobschapelensis, T. laocoon, and Trochammina ohioensts. GENERA AND SPECIES IMPORTANT IN STRATIGRAPHIC DIVISION HYPERAMMINA Three species of Hyperammina occur in the studied area. Frag- ments of Hyperammina are common to abundant, many identifiable as to species. Specimens with proloculi are not uncommon. The most commonly occuring species is Hyperammina castert, which is especially characteristic of the lower New Providence and lower Cuyahoga where H. kentuckyensis is lacking, but H. castert occurs in lesser numbers at many other levels from the Upper Devonian Portwood formation to the Chesterian Pennington shale, and possibly the Menard limestone. H. casteri ranges higher in the New Providence formation, and is abundant at this level, from southeastern Kentucky to southern Ohio where H. kentuckyensis is absent or present only in the upper part of the New Providence in southeastern Kentucky. In eastern Kentucky the upper part of the New Providence was not sampled and thus the lower range of MISSISSIPPIAN SMALLER FORAMINIFERA: CONKIN 201 H. kentuckyensis and the upper range of abundant H. casteri were not determined in this area. Hyperammina kentuckyensis is highly characteristic of and is restricted to the Osagian of Kentucky and southern Indiana, oc- curring most abundantly in the Floyds Knob and middle and upper New Providence formations. Hyperammina rockfordensts, like H. castert, occurs in the lower New Providence and lower Cuyahoga formations, but less abundant- ly; unlike H. casteri, H. rockfordensis does not occur above the lowest part of the middle New Providence formation (lower Button Mold member); H. rockfordensts ranges downward through the Kinderhookian to the Upper Devonian Blackiston formation. INVOLUTINA In abundance, /nvolutina semiconstricta and J. exserta are characteristic of the Kinderhookian and lowest Osagian. J. long- exserta apparently is restricted to this zone but does not occur abundantly. /nvolutina was not found in the Meramecian, but col- lecting was restricted in this series. /. semiconstricta occurs com- monly, but locally, in western Kentucky and southern Indiana, in the Paint Creek shale and in the shaly part of the Menard limestone (associated with /. exserta); the species is less commonly observed in the Kinkaid limestone. PROTEONINA Of the two species of Proteonina found in this study, P. cwm- berlandiae occurs most commonly in northwestern and southwestern Kentucky and in southcentral Ohio, while P. wallingfordensis occurs mostly from southeastern Kentucky to southern Ohio. Both species are often found together at the same locality, however. | Proteonina cumberlandiae occurs especially in the lower and middle New Providence formation, and in the lower part of the Cuyahoga formation. P. wallingfordensis is most abundant in the lower New Providence and lower Cuyahoga and in the middle Cuyahoga formation. THURAMMINOIDES SPHAEROIDALIS This long-ranging species in the Mississippian of the studied area 1s particularly characteristic of and abundant in, the New 202 BULLETIN 196 Providence and Cuyahoga formations. The species also occurs in moderate numbers in the Brodhead formation. It ranges through- out the Mississippian in the studied area and has been found in the Blackiston formation of Upper Devonian age, T. sphaeroidalis from the Silurian and Devonian of Kentucky was reported by Conkin and Conkin (1960, p. 8). The species was originally des- cribed from the Pennsylvanian of Texas and has been identified in the Permian of Australia (Crespin, 1958). TREPEILOPSIS Three species of Trepeilopsis were found during this study. They had been described by Gutschick and Treckman (1959) from the Rockford limestone of northern Indiana. The most commonly oc- curring of the three species 1s 7. spiralis which is found particularly in the lower part of the New Providence formation of Kentucky and Cuyahoga formation of Ohio, and in the Kinderhookian; however, 1. spiralis ranges up into the Muldraugh formation, and down to the Upper Devonian Portwood formation. 7. recurvidens occurs especially in the lower part of the New Providence and Cuyahoga formations, but it also ranges upward into the Brodhead formation. 1. glomospiroides was found in the Rockford limestone of southern Indiana and in the lower parts of the New Providence and Cuyahoga formations. AMMOVERTELLA Fragments of Ammovertella were found from the Kinderhookian to the middle Chesterian; identifiable species are three: A. cf. A. inclusa, which ranges from the Bedford to Brodhead formations; A. labyrintha, which was found only in the lower part of the New Providence formation; and A. cf. A. primaparva which occurs in the Kinderhookian Eulie shale of Tennessee, the Rockford limestone of southern Indiana, and the lower part of the New Providence and Cuyahoga formations. Thus, Ammovertella is especially common in the Kinderhookian and lowest Osagian. AMMOBACULITES One species of Ammobaculites, A. gutschicki, was found in the studied area. This species represents the third identified species of the genus in the Mississippian of North America. A. gutschicki was MISsSISSIPPIAN SMALLER FORAMINIFERA: CONKIN 203 found in the Kinderhookian Eulie and Falling Run shales. It ranges up through the upper Osagian Brodhead formation and correlatives; however, A. gutschicki occurs commonly only in the lower part of the New Providence formation in eastern and _ northwestern Kentucky. AGATHAMMINA One species of Agathammina, A. mississippiana, was found in this study to occur rarely and in few localities; the species has a stratigraphic range from the base of the Osagian to the top of the middle Chesterian. At present it has not been found commonly enough to have real stratigraphic value, but it does represent the earliest occurrence of the genus in North America, and indeed, of the family Miliolidae. HEMIGORDIUS Henugordius morilensis was found only in the Chesterian beds of the studied area, especially in the shaly beds of the Glen Dean limestone in western Kentucky. The species was also found in the Paint Creek and Kinkaid limestone and the Big Clifty-Cypress sandstones but does not occur in numbers at any sampled locality. EARLANDIA The lowest known Earlandia, E. consternatio, was found in the Chesterian and Meramecian, but not below the Somerset shale member of the Salem limestone. E. consternatio is especially common in the Paint Creek shale in western Kentucky. RANGE CHARTS Charts 3 through 10 show the occurrence of species according to locality number and bed number. The bed number is the same as that on the measured sections. Where no measured section is given, the bed number refers to the bed number in the list of localities. A solid black square indicates that the species occurred commonly to abundantly in that bed. An “X” indicates that a species was found, but not commonly, in that bed. Charts 1] through 21 show the range of species in the various more or less distinct lithologic provinces. A wide range line indicates common or abundant occurrences of that species. A thin line indi- BULLETIN 196 204 STSUSDPIOJSUTTTEM CUTUDIIOIgG ell dc lil awa! a a a lai age ee | ce alee PS Us|) a aL BSS (SURE BASSES GEE XIX) | XLS DX XL XL sjususery stsdojtedary SjJusUuIseIy euTUIUIedATO J, Sjusuisery Cute IadAPy SJUSUISEIT VTTIJIPAOWIWILYY sijeitds ‘7 Saeplortdsowioys stsdojtedai yj “aL ugod0RT “TL stsueTedeyosqooel ‘7 esonji0j sdojoAo ‘JT snounuojoq euturureddjqo JT, StTeproraeyds saproutumureinyy, XTI}JBOID VtayoejS tedsB xeydoay @eIPUeTIaqUIND eUuIUOaJOIg euetdiuras eqnjonziq7 eBYOtI}JsSuOotTuIAS “T eylasxosuol ‘T[ 2J1I9SX9 CUTINTOAUT STISUAPIOJHOOI “PY stsuoAyonjuey “Y Tiajysed eurulmieradAyy Xe an K Koa xD i em ef Pe (ee iste ba 3Gl Ia aca ne aes ~ De 6 ft eAredeutid ‘y "jo ‘Vy esnpout “VY “sO eTTeJTaeAoWMULYy THOIISjns sajtjnoeqoumumy € LUVHO Yee GICAL Iasi wee les t “(P-I-L “9-Z-] SOUTpPeoOTT) aaquinu peq pue AqrIpPeRoo, AQ SatoedsS Jo voUaIAINVVG 5 20 pane MIssSISSIPPIAN ee FORAMINIFERA: SERSE Ss TH DODD Dd age eee oo koe (ats PTT OX SSP RRSEERRR Re ceo eee) SSSRSS Seale e soo Re ees P JUBRUEO OM oe can gee |X DX A | a esa es el pea ie) SHEER AEEERAS em) Rot he BRAT IaA ED a eBay suena ot le rae ala im eS Ammovertella cf. A. inclusa A. labyrintha Glomospira articulosa Hyperammina casteri H, kentuckyensis H. rockfordensis Involutina exserta I. semiconstricta Proteonina cumberlandiae P,. wallingfordensis Stacheia cicatrix fe) a S. neopupoides [ | | S. trepeilopsiformis Thuramminoides sphaeroidalis ae x ix Trepeilopsis recurvidens T. spiralis ie i Ammovertella fragments LI GEM Hyperammina fragments d_| XXX) << | Tolypammina fragments | | Sse | | XK ee Trepeilopsis fragments MX Involutina longexserta G an =: oa | in i “a1 whi a uP & a 7 7 “~ . wa Aa - ae . ; * ; 7 oa th 4 a di 7 i ; P a woe Me ay a 7 y d 7 ‘3 ’ b. a 5 a vi. vrs a) ii i aif A = : a \ t \ 4 . ri > 1 + ‘ ' o i anh = \ o~ ‘ } “ Hh ers VN wv - — ‘1 ' y ¢ ell ‘ - : - « a » 7 _ 4 @ : 4 & 207 SjusUIdeIy CUTUIWIedATO J, H SJUIUISeIT VTTaJIIAOWWIY SJUsUISGeIF CUTUIUIeIAd SITeploreeyds saptoutumei4ny J, SstsudsiIayTyuNY xeydoay BJOTAJSUOIIWIIS ‘JT eJI9SX9 BUTINTOAUT xX Tl9ajseo eulMmUIerTsdAY STSUST[IIOW SNIpIOSIUISyy OTJeUIS{SUOD eIpuelT1ey || | | [| [ [ euerddtsstsstur eutrmureseutyo EERE Si 2aa PURTACATISSTSSIU CUTIE Yes oti eH PCa niGen oly alal Bee 2 eee BES ‘(OF ‘Sh ‘SF ‘18-62 ‘9Z-2S-M ‘T-I SeltTeoo7]) Jequinu peq pure Aypeoo] Aq Soeloeds JO vdUaTINDIO *) WALBUD MIssIsstIpPIAN SMALLER FORAMINIFERA: CONKIN BULLETIN 196 le SjusuIsery stsdottedad yj SjJusUIsery euTUIUIedATOT SJUSUISeIFT CUTIE IAdAP] sijeaiids stsdottadai yj (Tin XK | | XK xX x stjeproreeyds sapourmureany | BEBE See)e ee i eee ee eR alt] a (2 a a eOTISUOSTUMAS BUTINTOAUT TALE aS se eee eee Fe) a SY eS CCC x a x hi A ae a a) eee eS ee Bios JE PEC GG Sia SE ee OS-Ml6F~-S/8h- MILb- SPs STSUDPIOFHOOI “PY StsudAyoOnuUsy “PY I1ejseo eulmUeradApy THOLYOSjnNS Sajit[Nnoeqowuuy vy-s “(OG-LP ‘Sh ‘PP-M SOMIPROOT) J9qunu plod puRY AZITROOT Aq Satoods JO doUaTAINDIO “8 WARY 209 CONKIN MIssiIsstpPIAN SMALLER FORAMINIFERA: euetdtuias eqnjonqty sjuduIseIy stsdojtadai yj, sjusuIsery eutururedATO J sjuauisery PuTUIUTeITadAPT sJUZUIBeI} LTTOJIOAOWIWI YY stjerids 1 SUBPTIAINOII “JT el a 00 saptortdsowioys stsdojteadaiy stjeproraeyds saptoutuiureiny J, XT XXX fea saptodndosu ‘Ss XIIJBITD VIDYOeY SNUITSSTJNUILI xeYydoay STSUDPIOFSOUTTTEM ‘“q aeIpueyTIaquiNnd euIuosj}oOIg ByOTIJSUODIUIAS “T ByLaSKXIdUOCT “J eyI9Sx9 CUTINTOAUT SISUSPIOJYOOI “PY stsuaAyonjuay “HY T1ajseo euIUIUIeIadAT esopTNotj1e VPItdsOUoTY esnpout “VY ‘jo e{TaJI9AOWULY THOTYOS NG SaztTNoeqgowmuy BVURTIGAISSISSIUL BUTUIWIEYESY HEESPER EPH BS EEBREEeE Scar ¥S-s cos GE ral}| USS 2 CUCU aC $9-s €9-Al29- M|19- Hl 09-Mj6S-M] 8S- 4 LS->|\9S-s ‘(F9-TG-M SOTTTROOT) Joqunu poeq pue AI][RO0T Aq Sotdads\ Jo DUIBLINIIO *G§ }LeYO BULLETIN 196 210 q is % m x a Y, eS core arene | oe Pa eee) 4 one ACCES BeBe aie tse { 4 a | — a cca x a f i i i H ik i i i Val ise SnoePEeoREE i HI o [I i El LU X RET HG MBERREEROEA Ht at] A 3 KA Kz aS a ESERIES | | XXX X EDEGRNaS XMM XT ) FERRE PTF L-O]9-O|s-O £-O CaO O] Se 9e si STSUDAYON}JUOW CUTUIUIEIOGATY sjususeiry stsdojtiedeary sjusuIdery ePutururedArfoy sjusuIsery eutUIUTeIadApy SJUaUISeIy VTTaJIaAOWIWY SISUBOTYO BUTUIUIeYIOI J, stjeatas "7 SUAPTAINIGI “fF septoxrtdsouroys stsdojtedery sdojSA5 eutuuedAjqo J, SITeploraeyds saproutmiureiny yj, saptodndosau etaysejs Tpreuopour "Yy snsourAryoey, “Yy “Fo “Y snjeusie “y ‘so xeydoay SISUSPIOJSUTTTEM “q SPIPURTI9qUINS eutuo|a}OIgG nl BjLIVsxe BUTIN[OAUT SIsUePIOJHOOI “YY TI9jsed eurmUeTadATy XTIJBOTQ etayseqig BsOTNotjie eItdsowoTy earedeuitid “vy “jo “Vv "y “JO B]TeJIAAOWMIUTY THIOTYIsINS saytpnoeqouruy BPURICAISSISSIUL BPUIUIUIBUESY BJOIA}SUOOIWIaS esnyour L9-Al99-HIS9- “(TI-T-O “89-G9-M Setyeooy) taquinu pod pue Aypeoo, Aq Sotoads JO voUaIINDDO “OT Wey MISsSISSIPPIAN SMALLER FORAMINIFERA: CONKIN 211 Chart 11. Range of species in southern Indiana (Localities I-2-6). n 2 a od o ne) CY) = iS ) s mle 2 3 ay a o| > :o vw io} i xe) rs) oA c 3) i 5 a} ¢ A g al <) Qo = ‘a 2 o| | & 3 a10 & s : n ts) o Gt AES e i Slab || mls 3 n Ol al wm] go v1 on ice We} Lowe 3] al Hl «| | el a] she] Sly] s/s B=] (= B11 eI GIS] Oo] eC] alo 9 7) 4 ad] ea v0 n Qu) c “4 oO VY] o Ol gi.a o 3} 4 GE] 4) & | S| 8] 2) ].4 Sl mn) 2 o} HI- vo} Oo] a ol || o is Do Q. 3} Gl sisi |X] ofa o}| 2} 0 a] > sl eis Spel ele] si alg ol Zia o| oO BOTs] SM cl of Sa © ho Hl ol ol Sle] 8] Sic] ela] s Sala PS Ig Ol ylH|o| oO] elo| asia] S | 0) a celal art 1si-|*|2 [8] alate : oe ‘ Hilo on) = el8| 3-6 <| )Pennington oe) o » 3 Paint Creek BULLETIN 196 2 Chart 16. Range of species in northern Tennessee (Localities T-1-4). ie eek) anneal a i ol] aa) sjusudeary SUTUIULe LOC A |; TT (eed rss ol ELT CF EAE OT (| SE oe Toad sponge Se -—_ | re au ae eso [NITIaAe Sl meee | auheg 310 q| eouaptaorg MAN] BBoourrzeYyD| MISsSISSIPPIAN SMALLER FORAMINIFERA: CONKIN 2A Chart 17. Range of species in southeastern Kentucky (Localities K-44, 45, 47-50). n . on % s|2 & oO] o 5] 2] cll ee Fd be ElEle Ss 2] ols12| e| ele oe Dia Ele} BPS £1 op | Op n ist) 5 wo] @]°l¢ u 00 SO) al-eal ols ior Slo 13) Dla la Wy o al ¢ = eo ball }o) 2) a/ S| S| El elo]? alec o/s m i) alae] a] = Ela S16 o 3 oD i) 12) 12) Reed se el fo} Ela eI E)s)Ule-q ° ° Olelelolslels|s| Sela O}n o|5}° i) slo Elolgl xla]2 5 aa aS o|*# jon SN ellie ASS 7) AY | SSIs ral h O|# ODDS lo te le tr lee FBanderson | | {| {|} tt spisckiston! TTT TTT ETT ee ae HO 218 BULLETIN 196 Chart 18. Range of species in eastern Kentucky (Localities K-51-64). rH} « 0 = © n e195 a el ie ro al“! oO [ol bial qgvic H}O a om) od n o c Clie _ 5 aya, o n g ui ia ron i) n o al=| |—12 mE a1 0 g o>] . n a Dl » £ fo ort} OF HH a) 2 my Cl m|% n «3 El m| 2 3) ey Y ey el Wey Wary ad fe to . v0 ao) 8) 3) 31 5 S}'e) 5) &) 2g ]2]o |e oI cl-a] a rou ed tS) bed oO} Fl olZlolal2 ¢ al] oO “4 Oo 2 Sela lol a f-alUl a ea ql 3) 2 £|~*< a] & Si RAS OHSS £16 3| © 3 “IO x] 0) 218) S14] ° £] 3] © Els a} Y O15 ols &| 2 AQ] > ajo ) £ \|a w = Sol Oo c & | v]o 1) ) ae a He| Kl € lol ad|eojo]a qj] v S| EE vo) ¥ Qo} o ST Oolelelalsl a : a A —1 7 ° =| 0 of ELE : | SeUSEeE O| & sal sp! “Se 1Floyds Knob _| ds Knob StH itn Fort Branch ee 7 ami CS aaa Farmers | Henley 1A rovidence -—Sunbury MIssIsstpPIAN SMALLER FORAMINIFERA: CONKIN 219 Chart 19. Range of species in northeastern Kentucky (Localities K-65-68), and in southern Ohio (Localities O-1-2). n od = n n G4 3 oo uc} Lomi n os) ) qd s o| 3 H i “NC | = ie y c fs ee alc] 2 <<} S} o celts of ala] & EGS 3 Oo} 1, Oo] nH] od] 0 1 Ol g} 2] oo) ES] 0 S| o|.4] © Otel Ola E/ S/S] | [ays fale Sl] 3] SF) ele) lol] 3/3] 7 Zl al Sl oy Sle? Tlolo]@)c - = setter ela El4l el clatdls12/s ale Slalelseelsicts_lele O oc > RISE SVE/¥IS |e] e iS & c][r o|s pes “al a g HlolS/Elolclolelafolx § Vie ialole/AlElS]Hlalo QO) m}|oO}]o Ylsjoja £ eV HO] -|S ie luls a Hey] papa) Pe WS (cal Rothwell Floyds Knob ome — tt Haldeman | ee HHA 4C reek Perry ] Pees mt 1 BuLLETIN 196 22 Chart 20. Range of species in southern Ohio (Localities O-3-5). setpue,TIaquind euluos}oOIg une PORES | stjeptoraeyds Se prloutuuiesny J, STSUAPIOFSUTTTEM eUuIUOS}OIgG BJDtIJSuOoturas. *T e419Sx9 eUTINTOAU]T SjusuIsery CUuTUIUeIadATY T1ajseo eutmmuesradpy esopnoiy1e ertdsouoyy Berea eae Cuyahoga , H CONKIN MIssISsIPPIAN SMALLER FORAMINIFERA: Chart 21. Range of species in southcentral Ohio (Localities O-6-11). sjusurseay stsdofiedary s}JUSUISeIF PuTUTUTeCATO J, sjudUuIsery PUTUIUIeIAdAT SJUDUISeIF VTTOIIIAOWINUL YY stjeaiids “J, saptortdsowoys stsdojtedei J, sdoyoAdD euturuiedAyo J, sijeptoraeyds soptoutuuresny J XTI}EOTD VIayoeIS Ip[euopour xeydooy snsouAryor, “Yy “yo xeydoay SISUBPIOFSUITTeEM “q seIpPUeTIIqUIND eUuIUos}OIg eyOLIySuOOTUIaS ByIISKO BUTINTOAUT SISUSPIOFAOOI “PY I19jsed euTuUIUIersd esnpout “VY “Fo eTTeJTOAOWIWIY THOIYISjNS sojttnoeqowmumy SVULTACAISSISSIUI CUTWUIUIeUIeEOY cudon | ADU AMAR REE AR SERS RE SAS Ra enna SR e hee =ShhsS mee el eee ee Ree eee ewes Eee cep ee Pe aa esoyedng BULLETIN 196 NS N N ‘uvLddississiyy 9dAé} UROLIOULY YON ay} JO SWI9} UL OLYO [Bi] UeDYINOS pUy ‘vBSsSSoUUA TL Utsey} eUTWIUIeY IOI J, stsdojtedaa yj, eutuiureddqo J, Se9prloulMUIernuy, so}IpnNoeqowmumy eUuIUIW eyed dd al Upper fe Mj uetzra4ysauy lou ‘Ayon|Uy “eueIPUy, Ue NOS UL vIeuUeS Jo a8uevI O1Yydelsqenlsg “EZ WWeYyD oe St uetyooy - Lapury NVIddISSISSIW stsuacTyo eutumueyoory, Se ploatdsou1oy stsdojredaiy esr | sovsoer x1 || | | stsua -jedeyosqooelf "7 saoroco al | | | | snounuojoq euturuteddyjo y, snjeusie “y cyo xeydoay STSUdPIOF -BuryTem “qd aetpuelztequino eutuoesjoig ej1asxa eutyNOAUT Chart 22. Range of species in the Mississippian and uppermost Devonian. esoTNoy1e eatdsouro[y o1yeuraysuod erpuelieq eotozoaeyjed euruoryytt esnjout *‘y ‘so eTazT9AOWMIW THOTYIS NS saqtpnoeqowuuy euetddtsstsstut euIUIUIe Ye vo i) a o ie) $ A kas o) H o| 4 5 : o H a SBS 2c : us} cla. alia o BiemO im op “ Fe Ee) & gl! | & gS EoRo «4 a o BIz/° be) D os 3 al Ee] o piles a ee els 5 Pe ed A & o| o| 5 male aa 5| SO} alo one Siro oO B12) 8) H @)-3] 2] a}a)s £ % AIZ10 ih lien a} 4 a] 8] 8 P= 0 ao o i me Aa ore Oe AlSl eld OSI! oO] al Bl ei e ¢ 2 bal lite! Bod Ww ed td o| of &| 2] o a ; 5 3 Fs i) Elo 2 Gebeetash ets) olol S| x rail el el ee ese alo S SI S| S| S/S) o]4] ets I-s]si gy ol aye é Sy efbass 8| &\-3] Sods} 5] a) .) §| S| oles obs SW} 8} S| | 8] 3} 5] 2] 3]3] 2 aS) Ho tt 2 a] a} O} > i) +3] 0 = | | =) fe foo) (e20 Cecd Ae) ee) Ms) Mw 2 eR E SES : Ol TPO]S |B] a for} 2] ssf co] sl cxf fe Jom [a fo Sia | z nh o pee 2 es Geem.c ors MIssISSIPPIAN SMALLER FORAMINIFERA: CONKIN 223 cates occurrence of that species, but rarely or in small numbers. A given species may occur at only one locality in a particular member or formation; these charts indicate the sum total of occurrences at all the localities on each chart. Chart 22 shows the range of the species in the Upper Devonian and Mississippian formations in which Foraminifera were found. Again the thick lines indicate common to abundant occurrences, and the thin lines, relatively rare ones. The presence of a given species in any formation or member represents the sum total of occurrences of this species at all localities. The range of the genera in terms of the type Mississippian sec- tion is given on Chart 23. In the case of Ammovertella, Hyperam- mina, Tolypammina, and Trepeiopsis, the indicated range is par- tially based on fragments not identifiable as to species. ANALYSIS OF MISSISSIPPIAN AND UPPER DEVONIAN FAUNAS UPPER DEVONIAN Limited sampling of the Upper Devonian shales in connection with the present study of the Mississippian system has revealed the presence of a sparse fauna of smaller Foraminifera in the lenses of green to gray-green to buff-yellow shale which are intercalated in the lower part of the New Albany shale. The fauna consists of the following species: Involutina exserta, I. semiconstricta, Hyper- ammina caster, H. rockfordensis, Proteonina wallingfordensis, Thur- amminoides sphaeroidalis, and Trepeilopsis spiralis. It is now known that the Middle Devonian limestones of Kentucky also contain some smaller Foraminifera. Conkin and Conkin (1960, p. 8) listed the following Foraminifera from the following Devonian formations: New Albany shale: Thuramminoides sphaeroidalis and Hyper- ammuna spp. Portwood formation: Hyperammina spp., Proteonina sp., and Lhuramminoides sphaeroidalis. Beechwood limestone: Rhabdammina? sp. Sellersburg limestone: Litwotuba sp., Psammosphaera sp., In- volutina sp., and Hyperammina spp. i) bo He BuLLETIN 196 KINDERHOOKIAN ‘Twenty-one species of smaller Foraminifera were found to occur in the Kinderhookian, from southern Indiana through Ken- tucky and northern Tennessee to southcentral Ohio (except in southeastern Kentucky where the Kinderhookian was not sampled). Two species, /nvolutina semiconstricta and I. exserta, were found to be abundant throughout this area; associated with these two species, Trepeilopsis spiralis was found in abundance, but at few localities; in addition, fragments of Ammovertella, Tolypammina, and other species of T'repeilopsis occur. Occurring less frequently and at various localities were 18 other species: Ammobaculites gut- schicki, Ammovertella cf. A. inclusa, A. cf. A. primaparva, Glomo- spira articulosa, Hyperammina casteri, H. rockfordensis, Involutina longexserta, Lituotuba semiplana, Proteonina cumberlandiae, P. wal- lingfordensis, Stacheia neopupoides, Thuramminoides sphaeroidalis, Tolypammina botonuncus, T. cyclops, T. jacobschapelensis, T. lao- coon, T. tortuosa, and Trepeilopsis glomospiroides. Notably absent in the Kinderhookian beds is the Osagian form, Hyperammina kentuckyensis; also H. casteri and Thuramminoides sphaeroidalis are only moderately well developed in these beds. LOWEST OSAGIAN The most prolific Mississippian foraminiferal fauna in the studied region is found in the lowest part of the Osagian, below the Fern Glen-Burlington correlative (the Button Mold Knob mem- ber of the New Providence formation). These early beds, perhaps the earliest known Osagian in North America, were recognized and designated as the Coral Ridge member of the New Providence for- mation by Conkin (1957). On the basis of a megafossil fauna, the Coral Ridge fauna of Conkin (1957), the upper part of the Coral Ridge member was determined to be slightly younger than known Kinderhookian beds and slightly older than known Osagian beds. Nonetheless, an Osagian age for the Coral Ridge fauna is proven by the presence of such characteristic Osagian genera as: Orbitre- mites, Beyrichoceras, Merocanites, Pericyclus (Tournaisian of MISSISSIPPIAN SMALLER FORAMINIFERA: CONKIN 225 Europe), and Wachsmuthicrinus. No megafossils (except Scalari- twba) are found in the lower part of the Coral Ridge member so that this unit might be either Osagian or Kinderhookian with age determination based on megafossils; however, information gained from foraminiferal faunas lends some rather tenuous evidence sup- porting a Kinderhookian age for this unit. In the present study, the foraminiferal faunas of the lower New Providence (Coral Ridge, Clay City, Farmers siltstone, and Henley members of Kentucky) contain 26 species of smaller Fora- minifera, while the lower Cuyahoga of Ohio (Henley shale mem- ber of Ohio) contains 18 species. From southern Indiana to eastern Kentucky, and in south central Ohio, lowest Osagian faunas consist of abundant Hyperam- mina casteri, Involutina exserta, I. semiconstricta, and Thurammi- noides sphaeroidalis with more or less abundant occurrence of Am- mobaculites gutschicki, Hyperammina rockfordensis, Trepeilopsis spiralis, and fragments of Tolypammina and Trepeiopsis. Occuring less frequently, and at varying localities, 12 other species were found: Agathammina mississippiana, Ammovertella cf. A. inclusa, A. labyrintha, A. cf. A. primaparva, Crithionina palaeozoica, Glomo- spira articulosa, Hyperammina kentuckyensis, Stacheia cicatrix, S. neopupoides, Tolypammina cyclops, Trepeilopsis glomospiroides, and T. recurvidens, Rarely Lituotuba semiplana, Reophax cf. R. lach- rymosus, R. minutissimus, and Tolypammina jacobschapelensis are found in the lowest Osagian. OSAGIAN Twenty-one species were found in the Osagian (exclusive of the lowest part). In Kentucky, 18 species occur in the middle and upper New Providence, 13 species occur in the Brodhead forma- tion, three in the Floyds Knob formation, seven in the Rothwell and Wildie members of the Muldraugh formation. In Ohio, five species are found in the middle and upper Cuyahoga, and nine in the Black Hand sandstone. Abundant Thuramminoides sphaeroi- dalis and Hyperammina kentuckyensis are especially characteristic of the middle and upper New Providence formation from southern Indiana ‘to southern Kentucky. Proteonina cumberlandiae and In- 226 BuLLETIN 196 volutina semiconstricta occur commonly in northwestern Kentucky. Ammobaculites gutschicki, Glomospira articulosa, Hyperammina castert, Involutina exserta, Proteonina wallingfordensis, and Trepet- lopsis spiralis are of less common occurrence from southern Indiana to southwestern Kentucky. In northeastern Kentucky and southern Ohio, 7hurammuinoides sphaeroidalis and Hyperammina casteri are commonly occurring species in the middle and upper Cuyahoga. Lesser numbers of Glomospira articulosa, Proteonina wallingfordensis, and Trepeilop- sis spiralis also occur in these beds. Hyperammina kentuckyensis is rarely found in northeastern Kentucky, and the species is not found in Ohio and Tennessee. A localized fauna consisting of nine species was found in the thin shales in the lower five feet of the Black Hand sandstone at Armstrong (Locality 0-11) in central Ohio. This Black Hand fauna consists of common T'rochammuina ohioensis, with less common A ga- thammina mississippiana, Ammobaculites gutschickit, Ammovertella cf. A. inclusa, Glomospira articulosa, Involutina exserta, I. semt- constricta, Proteonina cumberlandiae, Reophax mcdonaldi, and Thuramminoides sphaeroidalis; in addition, fragments of Hyperam- mina and Tolypammina occur. The only other know occurrence of R. mcdonaldi is in the Churn Creek member of the New Providence formation of northeastern Kentucky. The Brodhead formation of Kentucky and the Logan forma- tion of Ohio were not extensively sampled, but H/yperammuina caster, H. kentuckyensts, and Thuramminoides sphaeroidalis occur in the Brodhead of northwestern to northeastern Kentucky. The follow- ing species were less commonly observed in the Brodhead of north- western to northeastern Kentucky: Ammobaculites gutschicki, Am- movertella cf. A. inclusa, Glomospira articulosa, Involutina exserta, I. semiconstricta, Proteonina cumberlandiae, P. wallingfordensis, Stacheia cicatrix, Trepeilopsis recurvidens, and T. sptralis. In the Logan formation of Ohio, only Thuramminoides sphae- roidalis and fragments of Hyperammina were found. The Floyds Knob formation is especially characterized by abundant and well-developed Hyperammina kentuckyensts, with lesser H. casteri and Thuramminoides sphaeroidalis. The Floyds Knob formation is not present in Ohio. MIssISSIPPIAN SMALLER FORAMINIFERA: CONKIN 207. In the Muldraugh formation, Foraminifera were found in the Wildie sandstone and the Rothwell shale in eastern and northeastern Kentucky, but nowhere in abundance. Seven species were identified from the Muldraugh: Agathammina mississippiana, Glomosptra ar- ticulosa, Hyperammina castert, H. kentuckyensis, Reophax cf. R. arenatus, Thuramminoides sphaeroidalis, and Trepeilopsis spiralis. MERAMECIAN Only five species of smaller Foraminifera were found in the Meramecian, but this may be due partly to restricted sampling which in turn was due to the abundance of limestone in the series (lime- stones were found not to be significantly productive of smaller Foraminifera). However, among these five species is the oldest known occurrence of EHarlandia, E. consternatio. The Somerset shale member of the Salem limestone in north- western Kentucky yielded Earlandia consternatio, Hyperammina castert, Proteonina wallingfordensis, and Thuramminoides sphaerot- dalis. In the Somerset shale of southwestern Kentucky only 7. sphaeroidalis and fragments of Hyperammina were observed. Smaller Foraminifera are known from the St. Louis limestone at only one locality, in Rockcastle County, Kentucky, where Thur- amminoides sphaeroidalis was found, poorly developed. No Ste. Genevieve smaller Foraminifera were encountered; however, in the Ste. Genevieve correlative in Ohio, the Maxville limestone, one species, Proteonina cumberlandiae, was found in the thin green shales which are intercalated between the limestone layers. CHESTERIAN Nine species of smaller Foraminifera were found in the Ches- terian series, two of which, Climacammina mussissippiana and Hemi- gordius morilensis, were not found in lower beds. Collecting was generally restricted to the shalier formations and as a result the records of occurrences of Foraminifera in the Chesterian are rather scattered stratigraphically. The more commonly occurring species were Earlandia consternatio, Hemigordius morillensis, and Involutina semiconstricta. Less commonly observed species were: Agathammina mississippiana, Climacammina mississippiana, Hyperammina castert, 228 BuLLETIN 196 Involutina exserta, and Thuramminoides sphaeroidalis. Reophax kunklerensis is present only in the shaly portion of the Menard lime- stone in Perry County, Indiana. Fragments of Hyperammuna, Am- movertella, and Tolypammina were found in several formations at various localities in the Chesterian. ZONATION OF THE MISSISSIPPIAN BASED ON SMALLER FORAMINIFERA It has been assumed by many foraminiferalogists, particularly those who have worked on the magnificent Recent, Tertiary, and Mesozoic faunas, or even by those who concentrate upon the fusu- linids, that arenaceous Foraminifera in general are so conservative, slowly evolving, and of such simple makeup, that they would be of little use in stratigraphic paleontology and correlation. It was thought that their usefulness lay primarily in their being indices for types of depositional environment; or in essence, they were strongly controlled by facies. This conservative picture of the arenaceous Foraminifera has been fostered by the provincial nature of the works on Paleozoic smaller Foraminifera. Workers have been overly occupied with the description of faunas from small geographic areas (often one or two outcrops) and usually from small intervals in geologic time, often a member of a formation, or formation. Several faunas of smaller Foraminifera have been described from the Ordovician to the Permian of the United States, but no real effort has been exerted to attempt recognition of the ecological requirements of the faunas in a hori- zontal dimension or the recognition of evolution in a vertical di- mension with time. No broad monographic work has been attempted to correlate the various faunas over different regions of the country, and to cite any stratigraphic significance of the arenaceous Forami- nifera. It is quite true that arenaceous Foraminifera in general are con- servative and slowly evolving forms, and that they are of value in the recognition of facies and interpretation of environment of depo- sition; however, it 1s possible to demonstrate change within arena- ceous Foraminifera in the Mississippian and to recognize species, MIsSISSIPPIAN SMALLER FORAMINIFERA: CONKIN 229 genera, and faunas which are restricted to certain parts of the sys- tem, surely not by facies alone. It can be further shown that the Foraminifera in the Mississippian can be used as a basis for recogni- tion of foraminiferal zones within the system and for stratigraphic division and correlation within a region, if not between regions. Based on the information derived from this study, I introduce a foraminiferal zonation of the Mississippian of the studied area as follows: Stratigraphic Name: Zones (species, genera, faunas) Chesterian: Millerella, Climacammina, Hemigordius, Earlandia, and endo- thyrids. Meramecian: Endothyrids and Earlandia. Osagian: Hyperammina kentuckyensis and Thuramminoides sphaeroidalis - includes all formations from the top of the Muldraugh to the base of the Coral Ridge member of the New Providence; this zone is divided into six more or less locally applicable subzones: 1. Muldraugh—poor development of Hyperammina kentucky- ensis and Thuramminoides sphaeroidalis. 2. Floyds Knob—excellent development of H. kentuckycnsis; rare 7. sphaeroidalis. 3. Brodhead—poor development of H. kentuckyensis and mo- derate development of JT. sphaeroidalis; rare other Fora- minifera; locally a megafossil fauna is present which re- sembles (but is distinct from) that in the New Providence below. 4. Upper Cuyahoga—upper New Providence (Black Hand- Churn Creek members) Reophax mcdonaldi — a possible marker. 5. Button Mold Knob member of the New Providence for- mation; divided into two parts: 5a. Upper Button Mold Knob—common occurrence of short, stubby, H. kentuckyensis; common occurrence of T. sphae- roidalis, sometimes associated with the Button Mold Knob megafossil fauna. 5b. Lower Button Mold Knob—highest occurrence and near absence of H. rockfordensis in lower part; common and large Thuramminoides sphaeroidalis; H. kentuckyensis; general absence of Button Mold Knob megafossil fauna. 6. Coral Ridge member of New Providence formation-Henley shale member of Cuyahoga formation—most prolific smaller foraminiferal fauna in the Mississippian; divided into two parts: 6a. Upper Coral Ridge—rare, short, stubby H. Kentucky- ensis; H. rockfordensis; frequent to common large T. sphaeroidalis; associated in Jefferson, Bullitt, and Nelson counties, Kentucky, and Clark County, Indiana, with the Coral Ridge megafossil fauna of lowest Osagian age. 6b. Lower Coral Ridge member—absence of H. kentucky- ensis; H. rockfordensis; frequent to common occurrence of large T. sphaeroidalis. 230 BULLETIN 196 Kinderhookian: Various faunas with much the same Foraminifera as in the Upper Devonian; abundant occurrence of Jmwvolutina; rare and small JT. sphaeroidalis; common Tolypammina, Ammovertella, and H. rockfordensis; rare occurrence of the land spore Tas- manites. Upper Devonian: Faunas much like the Kinderhookian, but sparser, with fewer species and individuals; fewer T. sphaeroidalis, Involu- tina, Tolypammina, and Ammovertella; frequent Tasmanites and other spores. PALEOECOLOGY Interpretation of ecology of the individual species is attempted in the Systematic Paleontology portion of this paper. More general considerations as to the relationships between the faunas and the lithology of beds is presented here. Lithology represents the fos- silized environment. Ideally then, it may be possible under favorable conditions of preservation to reconstruct the life relations of organ- isms to their chemical, physical, and biological environment. UPPER DEVONIAN The “black shales” of the Upper Devonian contain no Forami- nifera; this is in keeping with the chemical and physical conditions of formation of dark organic muds (stagnant waters, reducing con- ditions, lack of oxygen, low pH, state of incomplete oxidation of organic matter); such extremely restricted environment could be exploited only by forms of life capable of living in a nearly anaerobic state, and either primitive (unspecialized ), or highly specialized for life in such restricted environment. There are, however, small and thin green to green-gray shale layers intercalated between the black shale beds in the lower part of the New Albany shale and in the Olentangy shale; these green shales carry a rather small fauna of arenaceous Foraminifera. In general, the test size is small, and the test is simple in structure, with the exception of Thuramminoides sphaeroidalis. This Devonian foraminiferal fauna consists of a small cosmopolitan group which possessed wide range of tolerance for various kinds of environment. KINDERHOOKIAN The black and brown shales of the Sunbury carry no Foramini- fera, but intercalated small lenses of gray to gray-green shales carry a small fauna of five genera and seven species. MIssISSIPPIAN SMALLER FORAMINIFERA: CONKIN Hd | The Jacobs Chapel shale, soft, clayey, greenish-gray, contains only four genera and six species, but a large number of individual specimens. The small areal distribution, the fine-grained, clayey muds, and the diminutive nature of the megafossils occurring in the formation, may indicate lagoonal conditions which, because of the gentleness of the wave action, might promote the growth of such fragile forms as Zolypammina which are found in this unit in numbers, The Kinderhookian beds generally consist of fine-grained, gray to buff to greenish-gray shales; however, some fine-grained lime- stones are present, such as the Rockford limestone. In these fine- grained sediments, with little fine silt present for the construction of arenaceous tests, some Foraminifera, such as /nvolutina semicon- stricta and J. exserta, built smooth tests with few silt grains and abundant cement (this type of test is herein called Variant 1); in other beds which carry sufficient fine-grained silt, these two species are often present as Variant 2 which has a coarse texture to the tests and only a small amount of cement compared to Variant 1. A typical fine-grained limestone of Kinderhookian age is the Rockford limestone of southern Indiana. The Rockford is a dense, glauconitic, and ferruginous limestone which may have been laid down in a restricted environment of a lagoon; it contains a high concentration of tolypamminids; I have observed that tolypamminids are rather characteristic of fine-grained sediments, particularly dense limestone. The phosphatic nodules of such beds as the Maury shale in Tennessee, the Falling Run of southern Indiana and Kentucky, and even the green glauconitic grains in the Rockford limestone, prob- ably indicate near shore conditions. LOWEST OSAGIAN The Coral Ridge member of the New Providence formation may be (in its lower part) transitional between the Kinderhookian and Osagian; no megafossils, other than the problematic Scalarituba, are found in the lower part. The upper part of the Coral Ridge member contains the Coral Ridge fauna of lowest Osagian age. Associated with the Coral Ridge fauna are small nodules of iron- 939 BULLETIN 196 stone indicating some concentration of carbonates in the muds at the time of deposition. It is interesting to note that the greatest abundance of genera, species, and the greatest number of individual Foraminifera occur in the lowest part of the New Providence forma- tion, in the Coral Ridge member, or in the lower few feet of the New Providence formation where the Coral Ridge member is not recognized. The most abundant foraminiferal fauna in Ohio occurs in the lower few feet of the Henley shale, at the base of Bed 10, at Nipgen (Locality 0-6), and in the lower few feet of the Cuyahoga formation at Jester Hill (Locality 0-7). OSAGIAN The middle New Providence formation contains the next most abundant fauna; in places it contains crinoidal biostromes and fossiliferous shales carrying the Button Mold Knob megafossil fauna. The upper part of the New Providence becomes silty and the Kenwood sandstone and its equivalents are too silty and sandy to promote even moderate numbers of Foraminifera, except in the intercalated shaly beds. The Brodhead formation is in general too sandy to support significant numbers of Foraminifera; however, in some localities the Brodhead may contain shalier beds with a fair development of Foraminifera. The Floyds Knob formation is a variable lithologic unit, ranging from a shell breccia to odlitic limestone to siltstone to silty shale, all glauconitic. The Floyds Knob sediments must have been de- posited in shallow waters with land nearby; minor unconformity is evidenced by the glauconite grains and occasional erosional surfaces, sometimes with a number of limestone pebbles in the basal beds of the formation. Only three species of Foraminifera were found to occur in the Floyds Knob: rare Hyperammina casteri, abundant and well-preserved H. kentuckyensis, and rare Thuramminoides Sphaeroidalis, H. kentuckyensis is beautifully developed and abun- dant throughout the formation, with best development in the lime- stones, but present in some numbers even in the shaly siltstones. MERAMECIAN The limestones of the Meramecian were not extensively exam- MISsSISSIPPIAN SMALLER FORAMINIFERA: CONKIN 233 ined, but evidence derived from the samples studied indicates that the highly calcareous nature of the sediments militates against num- bers of arenaceous Foraminifera having occupied the Meramecian seas. An ideal environment for promotion of arenaceous Foraminifera would be one of clayey muds, with fine-grained silt present in quanti- ties sufficient for the construction of tests. The arenaceous Fora- minifera were not adapted to live in highly calcareous sediments in the absence of fine-grained silts or finesgrained sand. Meramecian seas were dominated by calcareous tests (granular calcareous and compound walled forms; that is, forms like Earlandia and Endo- thyra). These forms lived in the shoal areas of lagoons or shallow seas, where the water was saturated with calcium bicarbonate. Only one species, Thuramminoides sphaeroidalis, has been found in the Harrodsburg (Warsaw) limestone. The granular calcareous Earlandia has its lowest occurrence in the Somerset shale member of the Salem limestone. In the St. Louis limestone (shale) only Thuramminoides sphaeroidalis has been found among the arenaceous forms. In shale streaks in the Maxville limestone (Ste. Genevieve cor- relative) one specimen of Proteonina is reported. It 1s of course true that nearly all Meramecian beds contain endothyrids in greater or lesser numbers. CHESTERIAN The Chesterian beds are dominated by Millerella and the endo- thyrids. Other Foraminifera are rare with only seven genera and nine species here reported from the studied region. One genus, Climacammina, is unknown in the beds below the Chesterian. Hemi- gordius morillensis, C. mississippiana, and Reophax kunklerensis are restricted to the Chesterian. H. morillensis 1s an amorphous cal- careous form; C. misstssippiana is a calcareous form with a com- pound wall. Note that most forms restricted to and characteristic of the Chesterian have calcareous tests or tests with cement dom- inantly calcareous. It seems that the occurrence and distribution of smaller Foram- inifera in the Mississippian beds are not completely controlled by facies, but that evolutionary changes can be observed within the 234 BULLETIN 196 genera of Foraminifera (Hyperammina, for example), and within groups—faunas replacing one another vertically in time. In summary, most Mississippian smaller Foraminifera occur in clayey shales which contain much silt and fine-grained sand or fine-grained sand which is necessary for construction of an arena- ceous test. Beds which best exemplify this type of lithology are in the lower Osagian and Kinderhookian series. Sandstone beds do not carry Foraminifera unless there are shales or clayey siltstones interbedded with them. In the highly calcareous limestone sequences, as in the Mera- mecian, smaller Foraminifera are nearly absent. The best develop- ment of smaller Foraminifera in limestone is in the impure, argil- laceous, and silty limestones. The Chesterian beds of western Kentucky provided a better en- vironment for smaller Foraminifera in their alternation of shales and sands than does the dominantly limestone Chesterian sequence of southeastern and eastern Kentucky; in the Chesterian series, smaller Foraminifera occur mostly in the calcareous shales. WALL STRUCTURE Detailed discussions of problems of wall structure and composi- tion are included under generic and specific descriptions in the Systematic Paleontology portion of this paper (under the genera Hyperammina, Ammobaculites, Reophax, and Earlandia); however, a few general statements are presented here. Primary concern here is with the smaller Foraminifera; 2.e., those Foraminifera which can be identified without sectioning; therefore, wall structure in larger Foraminifera is not considered. A practical classification of wall structure and wall composi- tion of Mississippian smaller Foraminifera is presented here (infor- mation taken partially from Brady, 1878; Plummer, 1930; and Cum- mings, 1955). 1) Arenaceous A) caleareous—extraneous grains in calcareous or ferrugin- ous cement or both B) siliceous—extraneous grains in siliceous cement MIssISSIPPIAN SMALLER FORAMINIFERA: CONKIN 235 2) Granular caleareous—equidimensional grains of calcite em- bedded in crystalline calcite cement (subarenaceous wall of Brady, 1876) A) calcite granules secreted by the protoplasm, embedded in crystalline calcite cement? B) calcite granules derived from a supersaturated limy sea bottom by the selection of extraneous grains of cal- careous material by the protoplasm? 3) Compound wall—inner wall layer of fibrous calcite; outer wall layer of microgranular calcite or aragonite?, or altered from calcite or aragonite? 4) Amorphous calcite, or imperforate calcareous (porcellaneous ) Controversy over wall structure and wall composition revolves around questions of original microstructure of the test wall and composition of the cementing material (whether originally cal- careous, ferrugino-calcareous, siliceous; or whether wholesale re- placement by silica of original calcareous or ferrugino-calcareous tests has taken place). Secondary disputation concerns the source of the grains that are incorporated into and are a part of the test wall, whether the grains may be secreted by the protoplasm, or are chosen by the protoplasm from extraneous particles (organic or in- organic fragments) on the sea bottom, or both. Involved also in these discussions are the questions as to the time of origin of the various types of tests, and which types of tests are primitive and which advanced. Most Paleozoic smaller Foraminifera have been thought to be arenaceous; however, there are a number of Upper Paleozoic smaller Foraminifera with crystalline calcareous tests which possess an inner wall layer of fibrous calcite, such as Nodosinella (Cummings, 1955, p. 224). Perhaps the fibrous wall structure evolved in Devon- ian times; at least I know of no earlier record of this type of wall microstructure. I can not accept the proposition advanced by some workers that all Paleozoic arenaceous Foraminifera are actually the results of secondary replacement by silica of an original crystalline calcite test. Such a proposition seems unsound for several reasons: (1) no Nm os) Oo BuLLeETIN 196 definitive, compelling petrographic work on the test microstructure has been presented which embodies comprehensive thin-sectioning of representatives of all arenaceous families, Recent and fossil, (2) truly arenaceous Foraminifera are represented in the Quaternary, Tertiary, and Mesozoic, and (3) ideas bearing on phylogenetic con- tinuity of genera which obviously have stratigraphic ranges from Paleozoic to Recent (as in Hyperammina) would be hopelessly confused, for the type of Hyperammina (a Recent species) has a truly arenaceous wall. As a basis for clear understanding of wall structure and wall composition of fossil arenaceous Foraminifera, Recent arenaceous forms should first be examined, for much more detail of wall struc- ture can be seen in them than in the Paleozoic forms. Certainly some Paleozoic Foraminifera have had their wall structure and chemical composition altered by weathering and various types of replacement, i.é., silicification, dolomitization. The terminology of the texture of the wall of smaller Foramini- fera is discussed in the Systematic Paleontology portion, but addi- tional notes may be added here as to usage of the term “‘arenaceous”. In opposition to some present workers, but in agreement with H. J. Plummer (1930), I consider the term arenaceous to be a good one to describe the granular nature of smaller foraminiferal tests. Further, I see no objection to the use of the term arenaceous merely because it happens to be a term used in describing grain size in sedimentary rocks. Can not a word have more than one meaning, particularly when the term appears in two rather different disci- plines? A better substitute terminology has not been devised. Cer- tainly such terms as siltaceous, lutaceous, or the like would be sub- ject to the same inexactness as is the term arenaceous. Description of wall texture in numerical terms (measurement of individual grains) is an exercise in preciseness, but such method would have questionable advantage. A detailed study of grain size by precise measurements of individual grains would be a valid line of research, but certainly should not be directed soley for the purpose of in- validating the well-established textural term, arenaceous (which used in the restricted sense of Plummer, 1930, is quite exact). MISSISSIPPIAN SMALLER FORAMINIFERA: CONKIN 237 SYSTEMATIC PALEONTOLOGY Order FORAMINIFERA d@Orbigny, 1826 Family ASTRORHIZIDAE Brady, 1881 Genus CRITHIONINA Goés, 1894 Crithionina Goés, 1894, Kongl. Svensk. Vet. Akad., Handl., vol. 25, No. 9, p. 14; idem, 1896,Mus. Comp. Zool., Bull., vol. 29, p. 24; Rhumbler, 1903, Arch. Protisk., vol. 3, p. 229; Cushman, 1910, U. S. Nat. Mus., Bull. 71, pp. 53-57. Crithionina [?] Moreman, 1930, Jour. Paleont., vol. 1, No. 4, p. 45. Type species, Crithionina mamilla Goés, 1894. The generic definition of Crithionina as given by Cushman (1910, p. 53) follows: Test spherical, lenticular, or variously shaped, interior either labyrinthic or with a single chamber, apertures small and scattered or indistinct, wall thick, composed of sponge spicules or very fine sand, often chalky in appearance. Crithionina seems to be a genus compounded of two distinct test types: one such as C. mamilla Goés, 1894 and C. rotundata Cush- man, 1910 is labyrinthic internally; the other type of test is com- posed of a large to rather large hollow interior surrounded by a relatively thick wall composed of sand, sponge spicules, shells of other organisms, mica flakes, with irregular and intersitial apertures. I have studied the holotype of Crithtonina rotundata and find that the internal labyrinthic structure is not so regular as depicted by Cushman (1910, p. 57, figs. 64, 65). For this reason then, the Paleozoic genus Thuramminoides (with a regularly arranged in- terior) 1s not congeneric with Crithionina. The geologic range of Crithionina has been given as Silurian to Recent (Cushman, 1948, p. 71). Cushman’s record of the Paleozoic occurrence of the genus was based on Moreman’s (1930, p. 45, pl. 5, figs. 7, 11) report of C. rara from the Silurian Chimney Hill lime- stone of Oklahoma and on Parr’s (1942, p. 107, figs. 9, 10) record of C. teichertt from the Permian of Australia. Crithionina rara Moreman, 1930 is in doubt; it may be a species of Thuramminoides, perhaps T. sphaeroidalis; however, inasmuch as the types of C. rara are unavailable for study and no description or figures of the internal structure of the species was given, the generic bo wW oO BULLETIN 196 affinities must remain in question and the present writer can not accept Moreman’s form as congeneric with Crithionina. C. teicherti Parr has been referred to Thuramminoides by Crespin (1958, p. 41, figs. 12, 13). T. teicherti (Parr) is herein considered a junior sub- jective synonym of 7. sphaeroidalis (see discussion of 7. sphaeroid- alts), I have found in this study specimens of a form which fit the generic concept of Crithionina as exemplified by Recent species, in- cluding the type species, C. mamuilla. The new species, Crithionina palaeozoica, is the first undoubted fossil species of Crithionina yet reported, older than Miocene. Crithionina palaeozoica, new species IPL AG), seve, YS aus, il) Description.—Test free, subglobose, a rounded to tumidly ellip- tical mass, with a hollow central chamber the diameter of which is one-third to one-half the diameter of the entire test; test wall is thick and cavernous, about .5 mm thick, consisting of passages, irregularly contorted and progressing from the central cavity to the surface of the test where the passages intersect the surface of the test to form apertures; some passages are large (some up to .34 mm in diameter) and others are small (some as small as .03 mm); viewed from within the central cavity, the proximal ends of the passages appear to form on all sides a network or meshwork, spheri- cal surface; thus, there is some regularity to the internal labyrinthic structure, and the texture of the test wall in cross-section looks like the texture of a bath sponge; the test wall is arenaceous, con- sisting of agglutinated fine siliceous silt grains in siliceous cement (regardless of the original wall composition); the color is white to orange-buff. Measurements.—See Table 1 for measurements of Crithionina palaeozoica and for comparison with measurements of C. rotundata Cushman, 1910. Comparison and affinities —Crithionina palaeozoica is strikingly similar to C. rotundata Cushman, 1910 in that: (1) the labyrinthic structure is arranged to form a regular network, (2) both species possess similar structure (passages extending from the central hol- low to and piercing the surface of the test to form apertures of vari- MISsSISSIPPIAN SMALLER FORAMINIFERA: CONKIN 239 ous sizes), (3) the labyrinthic wall is thick, occupying about one- third of the diameter of the test, and (4) the central chamber wall (the inner margin of the test wall) forms a spherical network surface enclosing the central hollow. Table 1. Measurements of Crithionina palaeozoica, n. sp., in mm. and comparison with C. rotwndata Cushman, 1910 Pl. 19, fig. 9 unfigured C. rotundata, holotype paratypes U.S.N.M. No. 8259 Pl. 19, figs. 10, 11 Max. diam. 1.40 .81-.91 .30-.60 Min. diam. 1.20 .25-.43 Diam. of interior space 34 Diam. of canals .03-.34 .03-.08 Crithionina palaeozoica is also similar to the other species of Crithionina which possess a labyrinthic test wall enclosing a hollow interior, such as C. lens Goés, 1903 and the types species, C. mamulla Goés, 1894. The exterior of the holotype of Crithionina palaeozoica is similar to the exterior of C. rugosa Goés, 1896 while the surface of the para- types of C. palaeozoica is similar to the surface of C. lens Goés, 1903. Crithionina palaeozoica differs from C. rotundata in: (1) being much smaller (C. rotwndata is 2.1 to 4.3 times larger than C. palaeozoica), (2) having the labyrinthic structure of the test wall somewhat more regular than in C. rotundata, and (3) different test composition (the holotype of C. rotundata is only slightly cemented, with minute silt particles, muscovite flakes, and shells of other ani- mals, whereas the test of C. palaeozoica is rather rigid and com- posed of siliceous silt grains in siliceous cement (regardless of the original composition of the cement). Inasmuch as Crithionina rotundata is Recent, and only two species, C’. pisum (Colom, 1945, p. 4) and C. sp. (Parr, 1942, p. 78), both of which are Miocene, are heretofore known in the fossil form, the four above characters are considered of specific importance. Evolution would not have preserved the same species for 200 mil- lions of years inasmuch as mutations occur at rather constance rates 240 BuLLETIN 196 within particular groups of organisms. With such an immense lapse of time, the genetic complex of a species almost certainly would have been transmuted into other species. Type locality—Blue Gap on U. S. Highway 31E, 2.65 miles north of New Haven, Nelson County, Kentucky (Locality K-13). The holotype is from the Coral Ridge member of the New Provi- dence formation, 22 feet to 27 1/2 feet above the Falling Run member of the Sanderson formation (Bed 4), Stratigraphic occurrence—Crithionina palaeoxzoica is known to occur only in the Button Mold Knob and Coral Ridge members of the New Providence formation in Kentucky. (See Charts 4, 12, and 22); Ecology—Crithionina palaeozoica is known to occur only in the olive-gray to blue-gray, soft and plastic shales of the New Providence formation and at localities where these shales do not have megafossil faunas or calcareous beds. Recent species of Crithionina are known from cool to cold waters and from moderately deep waters (Cushman, 1910, pp. 59557): Remarks. —Crithionina palaeozoica derives its name from the Paleozoic sequence of rocks inasmuch as this is the first known species of Crithionina to be reported from the Paleozoic. Genus THURAMMINOIDES Plummer, 1945, emend. Thuramminoides Plummer, 1945, Univ. Texas, Pub. 4401, pp. 218, 219, pl. 15, figs. 4-10; Crespin, 1958, [Australia] Bur. Mineral Res., Geol. and Geophys., Bull. 48, pp. 40-42, pl. 3, figs. 9-13; pl. 31, figs. 1, 2. Type species, Thuramminoides sphaeroidalis Plummer, 1945 (monotypic genus). Thuramminoides was erected by Plummer (1945, pp. 218, 219) on material from the Pennsylvanian (lower Strawn shale) in San Saba County, Texas. Only the type species is known. Plummer’s original definition of Thuramminoides (1945, p. 218) follows: “The external characters of this globose unilocular test are like those of Thurammuina, but internally it is labyrinthic.” MIssISSIPPIAN SMALLER FORAMINIFERA: CONKIN 241 The definition of Thurammina Brady, 1879 (from Cushman, 1948, p. 80) follows: Test typically free, usually nearly spherical, sometimes compressed; cham- bers typically single, occasionally divided; wall thin, chitinous, with fine sand; apertures several to many, at the end of nipple-like protuberances from the surface, occasionally wanting. The original generic definition of Thuramminoides Plummer, 1945 is hereby emended on the basis of topotypes (Plummer’s Station 205-T-148) from the Texas Pennsylvanian and specimens collected from the Mississippian beds herein studied: The original shape of the test was spherical, but most specimens have been distorted into discoidal or lenticular forms, sometimes broken. The biconcave, compressed tests of Thuramminoides often resemble red blood corpuscles. The exterior surface 1s smooth to moderately rough with a thick test wall composed of quartz sand embedded in siliceous cement. There is no evidence of secondary replacement in the siliceous cement or quartz grains of the test wall in any of the hundreds of specimens of Thuramminoides studied, There are no characteristically astrorhizoid apertures present in Lhuramminoides, but there are multiple tubular openings of two sizes in the test wall. A few small protuberances are rarely seen on the exterior of the test; these are not considered to be apertures. The interior of Thuramminoides is not really labyrinthic as originally described. The test wall surrounds a moderate-sized hollow sphere (proloculus? ). The test wall is occupied by centripetal tubes which extend from the boundary of the hollow sphere toward the surface of the test; in some instances, the centripetal tubes pierce the surface of the test. In most cases, however, the centripetal tubes do not perforate the surface of the test. In addition, there are small tubelets in the outer part of the test wall which do not always run perpendicular to the surface of the test wall; these tubelets pierce the surface of the test in a great number of instances. Carbonaceous matter is sometimes observed in the interior of Thuramminoides where the interior centripetal tubular structure is not present. In cases where the centripetal tubular structure is absorbed or de- stroyed, there seems generally to be small to medium-sized, pitlike polygonal to rounded depressions on the interior part of the test wall. 242 BULLETIN 196 Thuramminoides has affinities to the genus Crithionina, a genus which includes the “labyrinthic species” C. lens Goés and C. ro- tundata Cushman, 1910. C. rotundata Cushman (1910, pp. 64, 65) is especially close to Thuramminoides. The description of C. ro- tundata was given by Cushman (1910, pp. 56, 57): Test free, subspherical, composed of loosely agglutinated sand grains; surface with many pores leading by canals through the thick walls to the simple central chamber with many circular or roughly polygonal openings which ramify into canals leading to the surface; wall of the central chamber and canals is firmer than the rest of the test, usually showing in these firmer portions a reddish-brown cement; color dark grayish brown. Diameter 3-6 mm. The interior “labyrinthic” part of the test (irregular tubular structure) of Crithionina is not regular enough for this genus to be congeneric with Thurammuinoides. The centripetal tubular structure in T’huramminoides radiates out equally and regularly in all direc- tions on a definite geometric plan, like a sunburst of tubes from a hollow sphere. Thuramminoides may have affinities to Hauesler’s (1890, p. 69) genus Thuramminopsis from the Jurassic of Switzerland. Thur- amminopsis 1s apparently arenaceous and possesses a network of tubular structures on the interior side of the test wall (this network indicates a “labyrinthic” interior to the test). The centripetal tubular structure of Thuramminoides is singular, and such structure is not observed, nor does the family definition allow inclusion of such forms, within the Saccamminidae. However, Lhuramminoides was referred to the Saccamminidae by Plummer, and later workers have followed her lead; the similarity of the in- ternal structure of Thuwramminoides to Crithionina, a member of the Astrorhizidae, has not been recognized previously. Thus, Thuram- mainoides can not be retained in the Saccamminidae inasmuch as the family does not embrace tests with labyrinthic or centripetal tubular internal structure. Thuramminoides is hereby removed from the Saccamminidae and placed in the Astrorhizidae. The Astrorhizidae includes in its definition those arenaceous genera which have either labyrinthic or centripetal tubular interiors. Stratigraphically Thuramminoides is known in the United States from the rocks of Middle Silurian through Middle Pennsyl- MISsSISSIPPIAN SMALLER FORAMINIFERA: CONKIN 243 vanian periods. In Australia, the only other country in which Thuramminoides has been reported, the genus is known from Permian strata. After Plummer’s erection of the genus from the Middle Penn- sylvanian shales of Texas, Thwramminoides was not reported in any other beds or areas until Conkin (1957, p. 1884) cited a Thuram- minoides-Hyperammina zone from the Osagian rocks of Kentucky and Ohio. Conkin (1958, p. 17) recognized Thurammunoides in the Lower Mississippian New Providence formation (Coral Ridge mem- ber) and the Underwood shale at the Gap-in-Knob section, north of Shepherdsville, Bullitt County, Kentucky. (See Chart 23 for range of Thuramminoides in the Mississippian as determined in this study. ) Crespin (1958, pp. 40-42) demonstrated the presence of Thur- amminoides in the Permian of Australia, recognized T. sphaeroidalts, and placed Crithionina teicherti Parr in Thuramminoides. T. teicherta (Parr) is considered in this work a junior subjective synonym of 7’. Sphaeroidalis. Conkin and Conkin (1960, p. 8) in discussing the discovery of Silurian and Devonian Foraminifera in Kentucky, recognized for the first time the occurrence of Thuramminoides sphaeroidalis in these two systems. It is interesting to recall that Moreman (1930, p. 45, pl. 5, figs. 7, 11) reported a new species of Foraminifera under the name of Crithtonina rara. Moreman’s species may be a true Crithionina, or may be the first reference to a Thuramminoides. Inasmuch as the types of C. rara are not available for study, this species will remain of doubtful generic position. Thuramminoides sphaeroidalis Plummer, 1945, emend. Pilea. tgs. t=O): Pl. 18, figs. 1-4; Pl. 26, figs. 1-3, Fig. 1 Thuramminoides sphaeroidalis Plummer, 1945, Univ. Texas, Pub. 4401, pp. 218, 219, pl. 15, figs. 4-10; Crespin, 1958, [Australia] Bur. Mineral Res., Geol. and Geophys., Bull. 48, pp. 40, 41, pl. 3, figs. 9-11; pl. 31, figs. 1, 2; Conkin and Conkin, 1960, Geol. Soc. America, S. E. Sect., Abstracts, p. 8. Thuramminoides teicherti (Parr), Crespin, 1958, [Australia] Bur. Mineral Res., Geol. and Geophys., Bull. 48, pp. 41, 42, pl. 3, figs. 12, 13. Description (specific emendation).—Test free, unilocular; test shape spherical in life; fossils may retain original sphericity, but 244 BULLETIN 196 usually are preserved as flattened, disk-shaped to lens-shaped masses which range in size from .118 to 2.15 mm. in the Mississippian forms, and up to 2.50 mm. in Crespin’s Australian Permian forms; test arenaceous with fine to medium-sized quartz sand grains embedded in a moderate to large amount of siliceous cement; when in excess, cement gives the test a glossy appearance externally; internally, the species is not labyrinthic, but consists of many centripetal tubes which occupy the test wall and radiate outward from the central hollow sphere toward the surface of the test; some of the centripetal tubes pierce the surface, most of the tubes do not; in the outer portion of the test wall much smaller tubelets are disposed at various angles to the surface of the test; many of these tubelets pierce the surface but others do not; the test wall is moderately thick to thick; carbonaceous material is sometimes observed in the interior of tie test when the centripetal tubular structure has not been preserved; in such instances, there are vestiges of this centripetal tubular struc- ture on the interior surface of the test wall in the form of small to medium-sized, pitlike polygonal to rounded depressions; distinct astrorhizoid apertures are lacking; rarely a few, small protuberances are present but these are not regarded as necks of apertures; the two sets of tubes (the centripetal tubular structures and the smaller, erratically oriented tubelets) apparently functioned as multiple apertures; no evidence of dimorphism is indicated as microspheric and megalospheric forms are not distinguishable; color of test 1s variable, ranging from white to gray to buff to orange and brown. A summary of the essential elements of the emendation of Thuramminoides sphaeroidalis follows: Topotypes of Thuramminoides sphaeroidalis were found not to be labyrinthic in the interior as described by Plummer (1945, p. 219); the interior of the test is hollow, surrounded by a thick test wall which possesses centripetal tubular structure identical to that possessed by the Mississippian specimens of the species; these large tubes may or may not pierce the surface of the test, In addition, the outer part of the test wall contains many smaller tubelets which are irregularly arranged, but most pierce the surface of the test. No typical astrorhizoid apertures present, but apertures are multiple. Measurements —See Table 2 for measurements of present specimens of Thuramminoides sphaeroidalis and ‘Vable 3 for range MISSISSIPPIAN SMALLER FORAMINIFERA: CONKIN 245 in measurements of 7°. sphaeroidalis and for comparison of the range of measurements of Plummer’s Pennsylvanian and Crespin’s Permian specimens. Comparison and affinities—The Mississippian specimens of Thuramminoides sphaeroidalis agree in all respects with topotypes collected by me, and exhibit all features shown in Plummer’s pub- lished figures. In general, the Mississippian specimens are much better preserved than Plummer’s Pennsylvanian material. The Mississippian collections contain many well-preserved spherical specimens (Plummer postulated an original spherical shape for her specimens although none was close to this). Most of the Mississip- pian examples are flattened as were Plummer’s and Crespin’s. All presently known Silurian and Devonian forms of the species agree with the Mississippian ones and also with Plummer’s type figures and topotype material. Crespin’s new name, Thuramminoides teicherti (Parr), based on Crithtonina tetcherti Parr, 1942, (Crespin, 1958, pp. 41, 42, pl. 3, figs. 12, 13) is invalid inasmuch as this species is conspecific with 1. sphaeroidalis. T. teicherti exemplifies every characteristic of 7’. Sphaeroidalis as shown by examination of topotypes of 7. sphaer- oidalis and by the Mississippian specimens of the species, as well as the features that are shown by Plummer’s published figures of the types of 7. sphaeroidalis; in addition, 7. teicherti fits the emendation of T. sphaeroidalis as presented here. Stratigraphic occurrence —The stratigraphic range of the species Thuramminoides sphaeroidalis is the same as that of the genus: Middle Silurian to Permian. (See Charts 3-18 and 22 for occurrence of T’. sphaeroidalis in the Mississippian. ) Ecology—The smallest examples of Thuramminoides sphaer- oidalis occur in the Devonian part of the New Albany shale. The species generally increases in size with decreasing geologic age al- though there are exceptions due to the nature of the enclosing sedi- ments. [The largest forms of the species are found in the Permian of Australia (Crespin, 1958, p. 40) where the largest specimen is re- ported to be 2.5 mm in diameter. The Pennsylvanian forms of Plummer exhibited a maximum size of 1.6 mm. (Plummer, 1945, p. 219). The largest Mississippian specimens of the species occur in 246 BuLLeETIN 196 the Coral Ridge and Button Mold Knob members of the New Provi- dence formation in which beds the species rarely reaches a diameter of 2.15 mm, Above the Brodhead formation, however, the size of the test diminishes with decrease in geologic age. The most favorable environment for growth and _ proliferation of Thurammuinoides sphaeroidalis in the Mississippian existed during deposition of the fine silt-bearing, plastic shales of the Coral Ridge and Button Mold Knob members of the New Providence formation in Kentucky and southern Indiana. The absence of megafossils in the outcrops of the lower part of the Coral Ridge member indicates that 7. sphaeroidalis could flourish in environmental conditions which were not condusive to the promotion of prolific invertebrate life in general. Yet, 7. Sphaeroidalis was tolerant of calcareous mud and muddy water en- vironment as is shown by its abundance in the calcareous shales of the Button Mold Knob member of the New Providence formation. In Ohio, the Cuyahoga formation contains much smaller forms of 1. sphaeroidalis; this smallness of test and poor development of the species in the Cuyahoga formation is correlated with more and coarser silt and sand grains on the east side of the Cincinnati arch in Ohio. The New Providence beds in eastern Kentucky, all along the strike of the Mississippian beds, again show smaller test and much more meager development of 7. sphaeroidalis due to deposition of sediments under environmental conditions much like those of the shales in the Ohio Cuyahogan sequence. Thuramminoides sphaeroidalis has not been found in the strictly sandstone beds; the species is present in the Black Hand sandstone of eastern Ohio only in the thin intercalated plastic shale units. Thus, 7. sphaeroidalis “preferred” clayey shales in which there were sufficient small silt grains to allow construction of an arenaceous test. MIssISSIPPIAN SMALLER FORAMINIFERA: CONKIN 247 Table 2. Measurements of Thuramminoides sphaerotdalis Plummer, 1945, in mm. specimen and min. max. locality number, formation, type number diam. diam. thickness and bed number ia ties ll .70 .70 55 K-13, New Providence, bed 2 IAG WG, ane 37 39 a O-11, Black Hand, bed 1 Pl. 17, fig. 3 47 49 34 K-13, New Providence, bed 8 Bla hig A7 52 .10 K-9, Brodhead, bed 1 Pl. 17, fig. 5 90 90 25 K-15, Clay City, bed 5 PI figs 6 US TS sy I-6, Button Mold Knob, bed 8 1A 7s, suse 7/ 81 82 42 K-36, New Providence, bed 4 JA alee aie t3 .60 .70 IY) K-13, New Providnce, bed 10 Il IAS saya, 1.20 1.85 45) I-2, Button Mold Knob, bed 1 IPL Ak, aee, AUC) 85 .86 25 K-63, Henley, bed 8 Pls. fish 1 1.50 1.55 40 K-36, Brodhead, bed 5 RES ties 2 85 90 25 O-8, Cuyahoga, bed 5 IPL, TS, Sure 1.65 1.65 45 K-19, New Providence, bed 3 Pl. 18, fig. 4 .98 1.00 19 I-6, Button Mold Knob, bed 8 Table 3. Range in diameter of Thurammuinoides sphaeroidalis Plummer, 1945, in mm. Permian (Australia) .39-2.50 Pennsylvanian (Texas) .70-1.60 Big Clifty sandstone .403-.550 (3 specimens) Glen Dean limestone 1.00 (1 specimen) Paint Creek limestone .118-.210 (4 specimens) Brodhead formation .369-.487 (4 specimens) Black Hand sandstone .377-.993 (8 specimens) Cuyahoga formation .487-.900 (8 specimens) Henley shale -650-.850 (2 specimens) Button Mold Knob member and equivalents .218-2.00 plus (44 specimens) Coral Ridge member and equivalents .235-2.15 (27 specimens) Sunbury shale .244-.420 (5 specimens) Falling Run member .235-.900 (4 specimens) New Albany shale .235-.285 (4 specimens) Family SACCAMMINIDAE Brady, 1884 Subfamily SACCAMMININAE Brady, 1884 Genus PROTEONINA Williamson, 1858 Proteonina Williamson, 1858, Rec. Foram. Great Britian, London, p. 1; Cush- man, 1948, Foraminifera, Cambridge, p. 78. Reophax Montfort, Brady, 1879, (pars), Quart. Jour. Micros. Sci., vol. 19, p. 51, pl. 4, figs. 3a, 3b; idem, 1884, Rept. Voyage Challenger, Zool., vol. 9, p. 289, pl. 30, figs. 1-5; Rhumbler, 1895, Kon. Gesell. Wiss. Gottingen, Nachr., p. 82. (non Reophax Montfort, 1808, Conch. Syst. vol. 1, p. 331) 248 BULLETIN 196 Difflugia Lamark, Egger, 1895, (pars), Kon. bay. Akad. Wiss. Munchen, vol. 18, p. 251. (non Difflugia Leclerc, 1815, Mus. Hist. Nat., Mem., v. 2, p. +74) Saccammina Sars, Eimer and Fickert, 1899, (pars), Zeitschr. Wiss. Zool., vol. 65, pp. 671, 672. (non Saccammina Sars, 1869, Foérh. Vidensk.-Selsk. Christiania, p. 248, (momen nudum) Type species, Proteonina fusiformis Williamson, 1858, (original designation. Recent, Great Britian). The generic definition of Proteonina was given by Cushman (1948, p. 73): Test free, a fusiform or flask-shaped undivided chamber; wall a _ thin chitin layer on which are cemented sand grains, mica flakes, other tests, efc.; aperture usually circular, often with a slight neck which may become elongate. The Mississippian species of Proteonina have tests composed of siliceous grains in siliceous cement (regardless of the composition of the original test wall). The affinities of Proteonina Williamson, 1858, Lagenammina Rhumbler, 1911, and Saccammina Sars, 1869 are obscure. Lagenam- mina and part of Saccammina (the free, single chambered forms) may belong to the genus Proteonina. The genus Proteonina ranges stratigraphically at least from the Silurian to the Recent (see Chart 23 for the range of Proteonina in the Mississippian). The genus is undoubtedly primitive and con- servative in its evolution. Proteonina cumberlandiae, new species Pl. 19, figs. 1-3: Pl. 26, figs. 4, 5:3) Biss) 2593 Description.—Test consists of a single chamber with a tapering neck which is broken off some specimens; aperture circular, at open end of neck; chamber teardrop to avocado-shaped, from 1.3 to 2.5 times longer than broad; test more or less compressed in present specimens so that original proportions of test were more slender; neck rather slender and from about one-third to one-half the length of the chamber; wall of fine siliceous grains in siliceous cement; color of test light gray to yellowish gray. Measurements.—See Table 4 for measurements of Proteonina cumberlandiae, Table 5 for range in measurements in the species, and Table 8 under P. wallingfordensis for comparison of this species with those to which it is similar. MIssISSIPPIAN SMALLER FORAMINIFERA: CONKIN 249 Comparison and affinities—See discussion under Proteonina wallingfordensis. Type locality —Hill side along road on side of Fishing Creek, Lake Cumberland, near Somerset, Pulaski County, Kentucky (Lo- cality K-32). The holotype is from the New Providence formation, 8.5 to 25 feet above the Falling Run member of the Sanderson forma- tion (Bed 2). Stratigraphic occurrence-—Proteonina cumberlandiae occurs in the Sunbury shale of eastern Kentucky, the Kinderhookian Falling Run member of the Sanderson formation, throughout the Osagian New Providence formation in Kentucky and southern Indiana, sparingly in the Brodhead formation, and in the Osagian Cuyahoga formation of Ohio, including the Henley, Vanceburg, and Black Hand members; one specimen was found in a shale break in the Mera- mecian Maxville limestone. (See Charts 3-6, 9-13, 18, 21, and 22 for details of occurrence. ) Table 4. Measurements of Proteonina cumberlandiae, n. sp., in mm. specimen and length length diam. diam. diam. locality number, type number of of of of of formation, and test chamber chamber base end bed number of neck of neck 12M, WG, sehen gs 460 352 218 -067 .050 O-9, Maxville, bed 1 PAL WG) oseey al 806 806 545 118 118 O-11, Black Hand, bed 1 Ak, WG), save, Y 436 PHT P2o 2, .075 .067 K-31, New Provi- holotype dence, bed 2 Table 5. Range in measurements of 25 specimens of Proteonina cumberlandiae, n. sp., in mm. Length of test -235-.806 Length of chamber .168-.806 Diam. of chamber -151-.545 Diam. of base of neck .067-.168 Diam. of end of neck .033-.134 Ecology.—Proteonina cumberlandiae undoubtedly had much the same ecological requirements as did P. wallingfordensis. The species is known to occur only in silt-bearing shales and shale breaks in sandstone and limestone. Thus P. cuwmberlandiae “preferred” 250 BULLETIN 196 muddy sea bottoms with silt and fine-grained sand, in which there was generally an absence of calcareous-rich sediments. Proteonina wallingiordensis, new species Pl. 19, figs. 4-8; Pl. 26, fig. 6; Figs. 4, 5 Description—Test consists of a single chamber with a tapering neck; test shaped like a Florence flask, with chamber originally nearly spherical (compressed in most specimens), or in instances slightly oblate; neck about one-sixth to one-half the length of the chamber, and about one-fourth to two-fifths the diameter of the chamber at the apertural end of the neck; wall of fine siliceous grains in siliceous cement; color of wall white to light gray to yellowish- gray. Measurements—See Table 6 for measurements of Proteonina wallingfordensis, Table 7 for range in measurements of the species, and Table 8 for comparison of the species with those to which it is similar. Comparison and affintties—The two species of Proteonina found in this study are distinguished from each other as shown on Table 8. Inasmuch as Proteonina is a simple form even among smaller Foraminifera, it is in instances difficult to distinguish various species. Furthermore, the genera Lagenammina and Saccammina in- clude some species which are not clearly distinguishable from Pro- teonina, All three genera have been reported from the Silurian to Recent. The relationship of these genera is obscure, as noted by Dunn (1942, p. 327). Lagenammina and the single-chambered and free forms of Saccammina may belong in Proteonina; such Paleozoic forms of these two genera from the United States all are composed of siliceous grains in siliceous cement, and apparently, in their fossilized state are without the chitinous base of Recent forms. Table 6, Measurements of Proteonina wallingfordensis, n. sp., in mm. specimen and length length diam. diam. diam. locality number, type number of of of of of formation, and test chamber chamber base end bed number of neck of neck Pl. 26, fig. 6 .762 521 554 ae 134 K-2, New Provi- dence, bed 3 Pl. 19, fig. 4 586 436 436 .201 168 K-63, Farmers, bed 9 On font MISSISSIPPIAN SMALLER FORAMINIFERA: CONKIN ju ilk, WG), says 7 BS 269 319 118 .067 K-63, Farmers, holotype bed 9 Pl. 19, fig. 6 436 Sle 352 193 101 K-63, Farmers, bed 9 Wels WG Tate 369 302 319 118 088 O-7, Cuyahoga, bed 4 IL, WG) aed! 5 1.000 720 .840 360 240 O-1, Bedford, bed 2 Table 7. Range in measurements of 39 specimens of Proteonina wallingfordensts, n. sp., in mm. Length of test -235-1.000 Length of chamber .201-.720 Diam. of chamber .201-.840 Diam. of base of neck .059-.360 Diam. of end of neck .047-.240 Table 8 gives a comparison of the present species of Proteonina and of several Paleozoic species of Proteonina, Lagenammina, and Saccammina which are somewhat similar to the two species of Proteonina herein described, As seen on Table 8, P. wallingfordensts and P. cumberlandiae are distinct from the species with which they are compared. P. wallingfordensis with its spherical chamber is similar to Lagenammina sphaerica, Saccammina aspera, P. cervici- fera, and S. moremani. However, the neck of P. wallingfordensis dif- fers from the neck of all these other species in that it is broader than the neck of S. aspera“ind L. sphaerica, longer than the neck of S. moremani, and more slender and more tapering than the neck of P. cervicifera. Proteonina cumberlandiae differs from Lagenammina stila in having a broader and longer neck, and from L. sphaerica, the neck of which is similar, in not having a spherical chamber but rather a teardrop to avocado-shaped chamber. Proteonina cumberlandiae and P. op ohion cpp differ from each other in that the chamber of P. wallingfordensis is spherical rather than teardrop or avocado-shaped and its neck is shorter and stockier. Type locality—One mile northeast of Wallingford, along hill road leading to Poston School, Fleming County, Kentucky (Locality K-63). The holotype is from the Farmers siltstone (Bed 9). Stratigraphic occurrence—Like Proteonina cumberlandiae, P. wallingfordensis occurs in the Kinderhookian Falling Run member BULLETIN 196 N wy Lon | BWOYP[YO ‘UBTINIIS LLX98° 8/T BUBIPU] ‘UBTINIIS TE XES 9/1 eWOYe|Y¥O ‘URLINIIS BEX $/C PWOYLYO ‘URLINIIS 8OXtt +/T SBX9 |, 9° X6" ‘uetuealAsuuad apply Buoy TT OF S° $/Z 9} +/T S+5°X908" Ayonjuay ‘uRIBes—Q) OF TST'XSEz Z/T OF £/T +8°X00'T Ayonjuay ‘uersesQ 0} [07 xSEz Z/T 9} 9/T agddjojoy fo MU UL SO] AIGUDY U01]0)0] puv abd f{O 4ojouvip {0 YOu] puv yjhua) [you f{O YjOur] +/T 6/1 6/1 cl/t G/N OTS e/a £/1 9} 9/1 S/o 9% b/T AIGQUDY I {o “ULDIp / YIU {0 “ULDIP MINE }10Ys [eorsrayds MOIIBU aye [qo Jaoys ‘jeottayds-qns Japuays [eotsayds ‘ayeduoja Apjoaziad ysowye pajurod 19yjer jeprosdiya Joys Ssay Io 910W Pa}OII}suod ‘jNO}js ‘[Bo1ipuryAo ynoys ‘papuno. Japuo]|s podeys OPpBIOAR ‘Suo] Jaye 0} doipiea} Suo| Ajajetapow yeorayds Aj.eau ‘Surtodey 0} jeortayds yoou fo ogvys LI qQuUioy fo odvys ‘ds ‘u ‘sisuapsofsuyjoa ‘q pue ‘ds ‘u 6£61 ‘puelaI] mpWII0W “Ys I+6r ‘Applid pue WEMIIS ViIgsD DUIULUDIIVYE O€6T ‘URWIAIOJY DIIMIDYgS “7 OfL6T ‘URWOIOJA, DIPS DUIMUDUIDDT 8Z6T “S1OIE AA pue ueWwysny dvsafto1a1I) “dq IDIPUD] AI Gund ‘d SISUIPAO{HU1]]VA VUIUOIJOA ‘QDIpUD]LIQuUNd ‘d U IM DUIMUDIIVIE pue “‘DUNUUWDUA SD] ‘DUIU09104L J jo satoods [B19A9S jo uostivdwoy as a9e | U1 WN MIssISSIPPIAN SMALLER FORAMINIFERA: CONKIN Dp: of the Sanderson formation, throughout the Osagian New Providence formation of Kentucky and southern Indiana, and throughout the Osagian Cuyahoga formation of Ohio. Above the Osagian, P. walling- fordensis was found in the Somerset shale member of the Salem lime- stone. Unlike P. cwmberlandiae, P. wallingfordensis occurs also in the Blackiston, Bedford, and Maury shales, as well is in shale in the Berea sandstone. (See Charts 3-6, 8-13, 17-22 for details of occurrence. ) Ecology—Recent species of Proteonina are rather widely dis- tributed in cool to cold and rather deep to deep waters. Proteonina is not restricted to cold and deep water or both, for species of the genus are found in other environmental situations where particulate material (generally siliceous sand and silt) is available for con- struction of tests. | have recovered Recent specimens of Proteonina from bay bottom muds in Corpus Christi Bay, Nueces County, Texas, associated there with silt or sand-bearing muds or both. Proteonina wallingfordensis occurs most often in the area from southeastern Kentucky to southern Ohio in the silty shales of the New Providence and Cuyahoga formations, while P. cumberlandiae is more abundant in northwestern and southwestern Kentucky and in southcentral Ohio in the less silty shales of the New Providence and lower Cuyahoga formations. This “preference” for the less silty shales by P. cumberlandiae is perhaps reflected in its more slender test, while P. wallingfordensis with its stockier test seemingly was able to live in a more silty environment. Family HYPERAMMINIDAE Eimer and Fickert, 1899 Subfamily HYPERAMMINAE Cushman, 1910 — Genus HYPERAMMINA Brady, 1878, emend. Conkin, 1954 Hyperammina Brady, 1878, Ann. Mag. Nat. Hist., ser. 5, vol. 1, pp. 433, 434, pl. 20, figs. 2a, 2b; idem, 1884, Rept. Voyage Challenger, Zool., vol. 9, pp. 257-260, pl. 23, figs. 4, 7-10; Cushman and Waters, 1930, Univ. Texas, Bull. 3019, p. 33; Plummer, 1945, Univ. Texas, Pub. 4401, pp. 219, 220; Conkin, 1954, Cushman Lab. Foram. Research, Contr., v. 5, pt. 4, pp. 167, 168; Cummings, 1955, Micropaleontology, v. 1, No. 3, pp. 233, 234. Nodosinella Brady, Cushman, (pars), 1927, Cushman Lab. Foram. Research Contr., vol. 3, pt. 3, p. 147, pl. 26, figs. 4, 5a, 5b. (mon Nodosinella Brady, 1876, Pal. Soc. Mon., v. 30, p. 102). BULLETIN 196 bo nm ee Hyperamminella Cushman and Waters, 1928, Cushman Lab. Foram. Re- search, Contr., vol. 4, pt. 2, p. 36, pl. 4, figs. 3, 4. (zon Hyperamminella de Folin, 1881, Soc. Hist. Nat. Toulouse, Bull. année 15, p. 140. nomen nudum). Hyperamminoides Cushman and Waters, 1928, Cushman Lab. Foram. Re- search, Contr., vol. 4, p. 112. (New generic name substitution.) Type species, Hyperammina elongata Brady, 1878 (original designation. Re- cent, Atlantic Ocean). Conkin (1954, p. 167) summarized Brady’s generic concept of Hy perammina: H. B. Brady (1878, pp. 433, 434, pl. 20, figs. 2a, 2b) first defined Hyperam- mina with H. elongata as the genotype, and in 1884 (pp. 257-260, pl. 23, figs. 4, 7-10) emended his original definition . . . Brady considered Hyperammina to have: an arenaceous test , free or adherent, [attached tests have since been referred to other genera] with an elongate tubular, singular or branching, second chamber; aperture open or only slightly constricted; interior smooth; exterior roughly or smoothly finished with test tapering toward the aperture; and a proloculus of varying bulbosity and shape. The generic concept of Hyperammina and its relationship with Hyperammunoides Cushman and Waters, 1928 were discussed by Conkin (1954, pp. 167, 168); this discussion amounted to a generic emendation of Hyperammina although no formal statement of emendation was made in the 1954 paper. I now formally propose that the 1954 (pp. 167, 168) discussion of the generic concept of Hyperammina be recognized as constituting generic revision of Hyperammina. To this end, I repeat the essential elements of my generic emendation, which added to Brady’s defini- tion, bring Hyperammina up-to-date and capable of embracing all species of Hyperammina and Hyperamminoides, as informally stated in 1954 (pp. 167, 168’): (1) the second chamber may be nontapering, may taper towards the proloculus, or in a few species taper toward both the aperture and the proloculus (‘hourglass tapering’) ; (2) aperture may be moderately or strongly constricted; and (3) exterior may be marked by transverse constrictions of varying strength. . . No clear generic definition is possible for either Hyperammina or Hyperamminoides as long as Hyperamminoides is accepted as a valid genus. Hyperamminoides, therefore, should be suppressed in favor of Hyperammina. The three characters considered diagnostic of Hyperamminoides by Cushman and Waters (constricted aperture, siliceous test, and tapering shape of test) and the one character considered diagnostic of Hyperamminoides by Plummer (the rapidly expanding nature of the second chamber) are here considered only of specific value. All the above characters are exhibited in varying degrees by species of Hyperammina. MIssSISSIPPIAN SMALLER FORAMINIFERA: CONKIN 255 Considerable misunderstanding as to the nature of the test wall in Hyperammina has arisen. Cushman’s treatment of the test wall is vague and his terminology is not precise. Generally, in de- scribing species of Hyperammina, Cushman referred to the test wall as “arenaceous” or “agglutinated”. Arenaceous, or agglutinate, to Cushman meant extraneous grains in a secreted cement; the cement could be ferruginous, calcareous, or rarely siliceous, usually with an interior chitinous lining. Thus, when Cushman used the term arenaceous without comment, he tacitly assumed that the test wall contained either ferruginous or calcareous cement. When Cushman dealt with Paleozoic Hyperammina, as well as with many other Paleozoic genera, his tacit assumption as to the nature of the test wall was not always well founded, as in all instances he apparenetly made no real determination as to the chemical nature of the cement, and in many instances did not describe the chemical composition of the agglutinated grains. Cushman and Waters described several faunas from the Penn- sylvanian of Texas (1927, 1928, 1930) in which the test wall com- position was stated to be arenaceous; these statements by Cushman and Waters were assumptions based on preconceived ideas as to the test wall composition. However, Cushman and Waters (1928, p. 36) based their generic definition of Hyperamminoides on the fact that it had siliceous cement (which cement they considered to be original). Plummer clearly understood the unnecessary difficulties at- tending lack of precision in the nomenclature and description of the nature of the test wall in smaller Foraminifera, Among Plum- mer’s contributions to the nomenclature of arenaceous forms was the proposal to adopt (1930, p. 7): . the word ‘adventitious’ as a satisfactory comprehensive term to describe all shells composed of an extraneous material bound by cement. The term ‘arenaceous’ will be employed strictly according its etymology, that is, for tests composed of mineral grains obviously selected from their surroundings and cemented into a firm investment by a protoplasmic secretion. Plummer (1945, p. 219) described the test wall composition in Pennsylvanian Hyperammina: The shell of the Texas Pennsylvanian species in this generic group [Hyperammina] consists of siliceous grains bound by an insoluble siliceous cement, which is generally subordinate enough to leave the surface distinctly dull and rough but commonly of fine texture. . . bo on On BULLETIN 196 The true nature of the wall composition of the type species of Hyperammina, H. elongata Brady, a Recent species, was not known until Cummings (1955, pp. 233, 234) examined the type material in the British Museum (Natural History) and reported that this material has a calcareous or ferrugino-calcareous cement, whereas the wall of Hyperamminoides is stated to have a siliceous cement. Such a fundamental difference of secretory activity in the cytoplasm can not be regarded as mere specific variation, as Conkin would suggest. However, tests of Hyperammina often undergo secondary alteration by silicification in Paleozoic sediments. This has been noted in several populations of Hyperammina neoglabra Conkin from different localities in the British Carboniferous. Hyperamminoides is therefore included within the genus Hypferammina, in the present work, on the grounds that the former is based on secondarily silicified specimens of the latter. Conkin (1956, p. 193) attempted to clarify Cummings’ misun- derstanding of his concept of the wall structure in Hyperammina and its junior subjective synonym Hyperamminoides: ... I would not suggest that cement secreted by the protoplasm of a foram- inifer is of mere specific value. Until Dr. Cummings’ announcement, I knew of no reference to [Paleozoic] Hyperammina possessing calcareous or ferrugino- calcareous cement secreted by the cytoplasm; indeed, the generic definition of both Hyperammina and Hyperamminoides [here the writer was following Plummer’s description of the chemical nature of the cement in Hyperammina inasmuch as Brady had not defined it precisely] had clearly required that these two genera possess siliceous cement. Therefore, the specific variation to which I referred was not a variation between siliceous cement [regardless or origin: original or altered] and calcareous or ferrugino-caleareous cement, but was a variation in the proportion of siliceous cement [regardless of origin: original or secondary] to cemented grains. Crespin (1958, p. 35), in a study of the Permian hyperamminids of Australia, discussed the relationship between Hyperammina and Hy peramminoides, and concluded: After studying innumerable tests, I agree with Conkin in using Hyperam- mina rather than Hyperamminoides, for the following reasons: (1) The dif- ference in the shape of the proloculus is neither a definite generic nor a specific character. . . The amount of increase in width of the test is surely specific rather than a generic character, (2) Plummer (1945) remarks that the tests of Hyperammina are mostly much longer than those of Hyperam- minoides. Evidence against this view is shown in the two species described by Parr (1942) from Western Australia. The tests of ‘Hyperamminoides’ acicula are up to 20 millimetres long; the greatest length of Hypferammina coleyi is given as 9 millimetres, and (3) Cummings (1955) found that the test of Hyperammina had calcareous or ferrugino- calcareous cement, but no species with calcareous cement were found during the present investigation. The tests were presistently siliceous, as found by Conkin (1956). As already com- mented here, there seems to be little or no evidence of secondary silicification of arenaceous tests in the Australian Permian or in the rocks in which the foraminifera are found. MIssISsIPPIAN SMALLER FORAMINIFERA: CONKIN Lh Plummer (1945, p. 223) placed considerable importance on the proportion of cementing material to arenaceous grains in the constitution and texture of the test of the two genera; thus in dis- cussing Hyperamminoides Plummer remarked: The strong shell wall is composed of fine, siliceous cement. . . Most of the species exhibit such an abundance of siliceous cement in the shell wall, that the surface is very smooth and even glossy, but sufficient variation exists in both genera to render this feature too unstable to serve as a generic character. I reiterate here my belief that the amount of cement (whether originally ferrugino;calcareous or siliceous) is at most of only specific value. In many instances it 1s doubtful whether the proportion of cement to cemented grains is of any taxonomic value. The cement is considered ito be secreted by the protoplasm and the kind of cement should not vary within a species or genus. Actually it is considered that genera in any subfamily, and perhaps the genera of a family, should possess the same kind of cementing material. Some families of Foraminifera as presently conceived do not have the same test composition displayed in all the genera within the family. Many families undoubtedly contain unnatural groupings of genera. It is known that some Protozoa do secrete siliceous test material and I can see no inherent difficulty in believing that some Paleozoic Foraminifera may have used silica as cement. Actually Miliammina, and others of tthe Silicinidae (Cretaceous and Recent), possess siliceous cement, although admittedly such truly siliceous genera in post-Paleozoic rocks are few and rarely encountered. Cummings (1955, p. 234) reported: “Usually, representatives of the genus Hyperammina are found in the British Carboniferous in an unaltered condition.” However, in the Pennsylvanian of Texas (Plummer, 1945, p. 261), unaltered ELarlandia (with calcareous ce- ment) occur in the same beds and at the same localities as does Hyperammina. The presence of Hyperammina (with siliceous ce- ment) and unaltered Earlandia (with calcareous cement) in the same beds at the same localities lends support for the possession of an original siliceous cement by Hyperammina. If there has been secondary replacement of the Hyperammina then the silicification would have been extremely selective, leaving Earlandia completely unaltered. 258 BULLETIN 196 St. Jean (1957, p. 41) expressed the following suspicion: Because of the transversely fibrous type of wall found in the diverse species of the fauna [Pennsylvanian Stanton fauna from Dubois Co., Indiana], it is suspected that all Paleozoic Foraminifera referred to the genus Hyperammina are actually Earlandia. If all Paleozoic Hyperammuna originally possessed a calcareous test as has been advocated by St. Jean (1957), then Hyperammina would become a junior subjective synonym for Earlandia Plummer, 1930 only if Hyperammina and Earlandia both possess granular cal- cite tests, as St. Jean believed (1957, p. 41). However, it is not yet established whether Earlandia was “arenaceous” in the sense of Plummer (1930 p. 7); that is, whether the calcareous granules were “selected” from the calcareous material on the sea bottom in warm, shallow seas, highly charged with carbonates, or whether the cal- careous granules in the calcite cement were secreted by the proto- plasm of the foraminifer. If we were to entertain hypothetically the assignment of Hy- perammina to the granular calcareous Earlandiidae Cummings, 1955, then what is the phylogenetic relationship of the Paleozoic Hyperam- mina and the Recent Hyperammina? Even the most ardent advo- cate of original crystalline calcareous wall constitution could hardly maintain the restriction of the genus Hyperammina to the Recent. In essence, St. Jean advocated just such restriction of Hyperammina when he suspected that Paleozoic Hyperammina are actually Earlandia. St. Jean (1957, p. 41) recognized the type species of Hyperammina, H. elongata Brady, 1878 to be a Recent arenaceous form, but took no notice of Cummings’ work (1955, p. 233) which demonstrated that the type species has an arenaceous test of quartz sand grains in calcareous or ferrugino-calcareous cement. Inasmuch as the type species of Hyperammina is arenaceous, there may well be, in the Paleozoic beds, silicified Harlandia which thus come to “mimic” Hyperammina, but the arenaceous Hyperam- mina can not be secondarily calcified to “mimic” Earlandia (which genus possessed a granular calcareous wall). Further, I believe that St. Jean (1957, p. 41) made a funda- mental misinterpretation of evolutionary thought in his discussion of his Farlandia bulbosa (which in reality is most likely a new species of Earlandia, not Hyperammina bulbosa): MIssISSIPPIAN SMALLER FORAMINIFERA: CONKIN 259 As it seems unlikely that this genus [Hyferammina] would be so far ranging, the Pennsylvanian Hyperammina bulbosa is placed under the genus Earlandia. Although the exact zoological relationships between Paleozoic and Recent Hyperammina are unknown, primitive and simple forms of life possessing wide tolerances for and potentialities for adaptation to various chemical, physical, and biological factors of environment, should have long geologic ranges, especially if the life forms are adapted to live in an environment which has persisted basically un- changed throughout immense lengths of geologic time. A further difficulty may be involved in the correct interpreta- tion of wall structure and composition as Cummings mentioned (1955; p-.234): As Plummer (1945) noted, complete specimens of Hyperammina are rare, and fragments are difficult to distinguish from members of the Rhizamminidae. Some records of the latter group in the Upper Paleozoic may be the result of incomplete preservation of Hyperamminidae. Fragments of some of the members of the Rhizamminidae occasionally may be mistaken for fragments of Hyperammina; many species of Hyperammina are described from fragmental material (lacking the proloculus). It is interesting to note that at least some of the species of the Rhizamminidae are reported to have an outer calcareous layer (Cushman, 1948, p. 73). The foregoing discussion of possible silicification and original calcareous test composition and structure has not convinced me that all Ordovician, Silurian, Devonian, Mississippian, and Pennsylvanian Hyperammina in the United States and all Australian Permian Hyperammina are secondarily silicified. Much more work needs to be done on the wall structure of Paleozoic Foraminifera along the lines of Cummings’ contribution. Not enough faunas have been described, and not enough concern has been given to the composition of the test wall; perhaps silicifi- cation has been extremely selective in replacing only certain types of Foraminifera, or environmental conditions differing so much in various areas have promoted silicification in one area and not in another. At present state of knowledge of wall structure and composition of Paleozoic smaller Foraminifera, no sweeping conclusions should 260 BuLLETIN 196 be attempted which bear upon the nomenclature of genera and ideas of phylogeny. Assumptions as to wall structure, as yet unverified, can not be used as guides in systematics. I believe that problems of wall composition and structure are much more complex than gen- erally recognized and that the foundation of foraminiferal systema- tics is weakened by our lack of exact knowledge, most particularly among arenaceous Foraminifera. Hyperammina casteri, new species Pl. 20) figs. 113) Ved PADS ISS fy tein LSE (OT) Description—Megalospheric form: Test consists of a proloculus of varying shape (oblate to spherical to somewhat pointed prolate to rounded prolate) and a straight to nearly straight second cham- ber which gradually and more or less regularly expands from a diameter less than that of the proloculus to a diameter greater than that of the proloculus; in a few instances, the test tapers toward the aperture after having expanded slightly in that direction; most tests show faint to moderate external constrictions at irregular in- tervals; test size varies greatly, with some specimens as much as three times larger than others and with all sizes between represented by yet other specimens; nearly all specimens are flattened so that measurements other than length are exaggerated about one and one- third times their original size; aperture formed by slightly to moder- ately constricted end of tube; apertural end of most specimens broken; test wall opaque to translucent and generally rather smooth with large proportion of siliceous cement, but wall may be rather granular with a lesser proportion of cement; color of wall varies from white to cream to gray. Microspheric form: Test consists of a tiny pointed proloculus and a rather rapidly expanding second chamber which ceases to expand after achieving considerable length; the general shape of the test is that of an elongated cone; the proloculi of some speci- mens are extremely long and pointed; the pointed tips of the tiny proloculi are broken off of many specimens; aperture formed by slight constriction of open end of cone; however, the apertural end is usually broken; nearly all specimens are flattened as in the megalospheric form; measurements of test corrected for distortion MIsSsISSIPPIAN SMALLER FORAMINIFERA: CONKIN 26) show that the test was about three times to six times longer than broad; a few tests show less expansion of the second chamber and have the length about seven times longer than the width; in other respects the microspheric form closely resembles the megalospheric form. Measurements —See Vable 9 for measurements of the megalo- spheric form and Table 10 for measurements of the microspheric form of Hyperammina castert. Table 11 shows the range in measure- ments of H/. casteri, a comparison in the ranges of the measurements of H. casteri and H. glabra, and the ranges of the measurements of the tests of H. castert which have been hypothetically restored to their original dimensions, before flattening occurred. Comparison and affinities—The megalospheric form of /Hy- perammina casteri is somewhat similar to the megalospheric form of H. glabra Cushman and Waters (1927, p. 146); however, H. castert is proportionally broader, with a maximum diameter (for a given length) attaining nearly three times that of //. glabra and a proloculus diameter ranging to nearly two and one-half times greater than that of H. glabra. The microspheric form of Hyperammina casteri is distinct from all forms of Hyperammina in the present study because of its conical shape; however, the microspheric form is similar in its conical shape to H. expansa (Plummer) (1945, pp. 223, 224). H. expansa expands at a much faster rate than does H. casteri and in g..eral has a larger proloculus. Plummer did not give measurements for the proloculus of H. expansa, but the proloculi of three topotypes (from Plummer’s Locality No. 128) range from .042 to .067 mm. in diameter. Also, the microspheric form of H. casteri resembles H. johnsvalleyensis Harl- ton (1933, p. 8). The microspheric form of H. casteri superficially resembles Reophax buccina Gutschick and Treckman (1959, pp. 239, 240), but R. buccina has a much larger proloculus (.08 to .10 mm.), and its test is partially constricted internally. The generic position of R. buccina is in doubt. 262 BuLLeETIN 196 Table 9. Measurements of Hyperammuina casteri, n. sp., megalospheric form, in mm. diam. length locality number, Specimen and of of max. min. formation, and bed type number proloc. test diam. diam. number BS 20s figs es 335 2.100 420 .302 K-13, Brodhead, bed 10 Pl; 20; fig. 5 193 .704 193 m3 )8 K-38, New Providence, bed 7 PZ Oreos s 450 = 1.625 450 350 K-31, New Providence, bed 2 IL AO, aoe, 117) 225 Oe 10) 300 190 K-31, New Providence, bed 2 PZ0N ties 7 120 840 Biles .080 K-36, New Providence, bed 5 Pl. 20, fig. 9 244 1.126 .270 .210 K-16, New Providence, bed 3 PIS 26. tig 7, 22 eS) 300 .200 K-12, New Providence, bed 2 PIS2Z0 fies 3 134 924 .164 109 K-36, New Providence, bed 2 Pl20) fie. 12 .670 134 088 K-5, Falling Run, bed 1 Table 10. Measurements of Hyperammuina casteri, n. sp., microspheric form, in mm. diam. length locality number, specimen and of of max. min. formation, and bed type number proloc. test diam. diam. number Pl. 20, fig. 6 .025 .780 218 025 K-34, New Providence, bed 7 1A Ae capes, Ilf6 1.260 425 .142 I-3, New Providence, bed 1 AB VALS sabes 604 168 025 K-16, New Providence, bed 3 BIS 20 etre. 1 .077 806 E252, .075 K-16, New Providence, bed 3 P20 ties 10 .746 319 168 K-16, New Providence, bed 3 P20" figs 1, .033 =: 1.140 265 .033 I-4, New Providence, holotype bed 3 IAB PANE aye 7 050 772 302 050 I-4, New Providence, bed 3 Pl. 20, fig. 4 .570 302 .067 K.-36, New Providence, bed 1 P20 tiga .018 586 201 018 K-5, Falling Run, bed 1 MIssISSIPPIAN SMALLER FORAMINIFERA: CONKIN 263 Table 11. Range in measurements of Hyperammuna castert, n. sp., in mm., and comparison with H. glabra Cushman and Waters H. casteri H. glabra megalospheric microspheric megalospheric 34 specimens 38 specimens Diam. of proloc. .120-.450 .018-.075 150 Length of test up to 2.30 up to 1.26 up to 3.00 Max. diameter .134-.650 .105-.470 .120-.200 Min. diameter .080-.350 .018-.075 Restored ranges Diam. of proloc. .120-.360 .015-.060 Max. diameter .107-.520 -084-.380 Min. diameter .080-.280 .015-.060 The megalospheric and microspheric forms of Hyperammina castert taken together are roughly similar in appearance to the megalospheric and microspheric forms of H. elegans (Cushman and Waters) (1928, p. 36). However, H. elegans is much larger (up to 5 mm. long and 1 mm. in diameter) and is more strongly constricted. Type locality—One mile west of Jacobs Chapel, Clark County, Indiana (Locality I-4). The holotype is from the lower three feet of the New Providence formation (Bed 3). Stratigraphic occurrence-—Hyperammina castert has a longer stratigraphic range than do the other species of the genus encount- ered in this study. The species ranges in Kentucky from the Upper Devonian part of the New Albany black shale upward and through- out the Kinderhookian and Osagian; in the Meramecian the species has been found only in the Somerset shale member of the Salem limestone; in the Chesterian, H. casteri occurs in the upper part of the Pennington shale, while questionable specimens of H. casteri were found in the shaly part of the Paint Creek and Menard lime- stones. The species occurs in the Kinderhookian and Osagian of southern Indiana. In Ohio, H. casteri has been found in the Osagian Cuyahoga formation, H/. casteri occurs rather often (in the Kinder- hookian and lower Osagian) in association with H. rockfordensis, and less often in association with H. kentuckyensis, within the Osagian sequence. See Charts 3-22 for details of occurrence of /H. castert in the Mississippian. Ecology—Hyperammina casteri occurs in a wide variety of shales (calcareous and noncalcareous), shaly siltstones, and shaly 264 BuLLETIN 196 sandstones; thus, like /nvolutina semiconstricta, the species was tol- erant of a wide range of environmental conditions. There is no gradual change in size with decreasing geologic age, nor apparently any other change in the morphology which can be correlated with stratigraphic level. Various sized specimens are found even in the same sample. The great variety in size and shape assumed by H. castert may indicate that polymorphism existed within the species rather than the species having had simple alternation of micro- spheric and megalospheric generations. Remarks.—Vhis new species is named in honor of Dr. K. E. Caster, Professor of Geology at the University of Cincinnati. Hyperammina kentuckyensis Conkin, 1954 Pl. 21, figs. 1-9): Pj. 26, fiz. 9s Bie s Hyperammina kentuckyensis Conkin, 1954, Cushman Found. Foram. Research, Contr., vol. 5, pt. 4, pp. 166, 167, pl. 31, figs. 1-6. Description —Conkin gave this specific description of Hyperam- mina kentuckyensts: Megalospheric form shows an oblate proloculus and a moderately curved, undivided second chamber, tapering initially toward the aperture, then ex- panding toward the aperture the remainder of the test, producing a necking at the position of reversal of direction of tapering (this double tapering of the early part of the second chamber is herein termed ‘hourglass tapering’) ; test moderately constricted externally at irregular intervals; part of test between last constriction and moderately constricted aperture, slightly inflated forming a distinct lip which ranges up to 16 percent of the total length of the test; wall cream colored and smoothly finished, consisting of minute siliceous grains in siliceous cement; rarely a specimen approaches a cylindrical shape, ... but this is merely an individual abberation within the species. Microspheric form shorter, stouter, and less curved than megalospheric form; proloculi of microspheric forms broken off; very early part (less than 10 percent of total length of second chamber) narrow, and very gradually expanding, followed by a rapid expansion, and thereafter approaching a cylindrical shape, but always retaining a definite expansion; . . . aperture slightly constricted; lip as in megalospheric form; wall same as in megalo- spheric form, but thicker. Measurements—See Conkin (1954, p. 166) for measurements of type specimens, Table 12 (this paper) for measurements of topo- types and hypotypes, and Table 13 for range in the measurements. Comparison and affinities—Hyperammina kentuckyensis was originally compared to H. glabra Cushman and Waters, 1927, as fol- lows (Conkin, 1954, p. 167): The megalospheric form of Hyperammina kentuckyensis differs from the megalospheric form of H. glabra in having: (1) numerous moderately de- MIssISSIPPIAN SMALLER FORAMINIFERA: CONKIN 265 veloped, though distinct, external constrictions, (2) pronounced ‘hourglass’ tapering of the early part of the second chamber, (3) distinct lip structure, and (4) oblate proloculus The microspheric form of Hyperammina kentuckyensis has no close affinities to any known microspheric form of Hyperammina. Gutschick and Treckman (1959, p. 238) described a new species, Hyperammina rockfordensis, as having close affinities to H. elegans Rauser-Cernoussova and Reitlinger, 1937 and to H. kentuckyensis Conkin, 1954. Table 12. Measurements of Hyperammina kentuckyensis Conkin, 1954, in mm. diam. length locality number, specimen and of of max. min. formation, and bed type number proloc. test diam. diam. number Pl. 21, fig. 2, 101. .781.~—S—.118-~S— «084. ~Ss K-5, Floyds Knob, topotype bed 1 IAL. Pil aaee, al 1067) e208 .087 .050 K-5, Floyds Knob, topotype bed 1 PAG AL aaten hp 092 SSIS alll .084 K-5, Floyds Knob, topotype bed 1 PL Aik, sates © 126 .858 .109 .075 1-2, Button Mold Knob, bed 1 Plo All infer, 7 .604 allay .060 I-2, Button Mold Knob, bed 1 PAL Ail, wis, 120 850 118 .084 K-32, New Providence, bed 5 IPL Ale sayy, 1.083 134 .055 K-32, New Providence, bed 5 Jeb Alls anes, GE 1.100 .134 .067 K-32, New Providence, bed 5 TPA Al savers 126 .704 105 .069 K-6, Button Mold Knob, bed 5 Table 13. Range in measurements of 29 specimens of Hyperammina kentuckyensis Conkin, 1954, in mm. Diameter of proloculus .067-.176 Length of test .436-1.629 Maximum diameter of test .092-.252 Minimum diameter of test .050-.120 Diameter of lip .087-.244 Diameter of aperture .025-.134 In the present paper (under Hyperammina rockfordensis) I document the derivation of H. kentuckyensis from H. rockfordensis (or stated another way, the transformation in time of H. rock- fordensts into H. kentuckyensis), Although the two species are intimately related and Hyperam- 266 BULLETIN 196 mina kentuckyensis is derived from H. rockfordensis, H. kentucky- ensts differs from H. rockfordensis in having: (1) distinct hourglass tapering, (2) the second chamber expanding more rapidly, (3) dis- tinct constrictions, and (4) rather less granularity to the test wall. Type locality —This species was described by Conkin (1954, pp. 166, 167) from the Mississippian (upper Osagian) Floyds Knob formation (Bed 1) on the north side of Mitchell Hill in southwestern Jefferson County, Kentucky (Locality K-5). Stratigraphic occurrence—Hyperammina kentuckyensis is re- stricted to beds of Osagian age in Kentucky and southern Indiana; the species is not known from the Mississippian of Ohio or Tennessee. (See Charts 3-6, 8, 9, 11-13, 17.19, and 22 for details of occurrence. ) Ecology.—Hyperammina kentuckyensis is best developed and most abundant in the coquinas (crinoid, bryozoan, and brachiopod breccias) of the Floyds Knob formation as presented at the type locality. The nature of the Floyds Knob formation has never been studied in detail except for tracing of its distribution and significance as a datum within the Osagian rocks of Kentucky and southern Indiana (Stockdale, 1931). The universal presence of glauconite grains or pellets, coupled with the presence in some places of rounded to angular pebbles of limestone near the base or within the forma- tion, strongly suggests unconformity, or certainly near shore deposi- tion. [his conclusion is further supported by the coquina of abundant brachiopod fragments and other invertebrate fragmental remains. Significant portions of the formation are in places composed of beds of odlitic limestone. The origin of and the chemical and physical environment of deposition of odlitic beds is well known. Oolites today are formed in marine waters that are of high alkalinity (and thus supersaturated with calcareous salts), high pH, tropical temperature, and shallow depth, as in shoal areas where agitation of water by waves causes the formation of concentric bands of calcium carbonate around some foreign particle as a nucleus, (For ecological signifi- cance of odlitic limestones, see Henson, 1950, pp. 215-238, and Con- kin and Conkin, 1958, p. 151.) In most areas, the Floyds Knob formation is a glauconitic lime- stone or siltstone or both. Where the limestone is absent or poorly developed, tests of Hyperammina kentuckyensis are distorted in MIsSISSIPPIAN SMALLER FORAMINIFERA: CONKIN 267 appearance and generally smaller in size. Among these apparently depauperate forms there is occasionally found a “giant”. Hyperammina kentuckyensis is known to be well developed, but of smaller size, in the New Providence formation (particularly in the calcareous shales of the Button Mold Knob member); the species is rare in the Coral Ridge member of the New Providence formation in which beds the transformation from H. rockfordensis to H. kentuckyensts occurred. The species is less well developed in the slightly calcareous siltstones of the Brodhead formation. Un- doubtedly the water was colder in New Providence and Brodhead times than in Floyds Knob time. Remarks—Hyperammina kentuckyensis was probably the first species of smaller Foraminifera to be described from the Lower Mississippian of North America. Only a few specimens of the several hundred examples studied of Hyperammina kentuckyensis exhibit slight effervescence with strong hydrochloric acid. This effervescence may indicate the original presence of calcareous material in the test of H/. kentuckyensis. The types of H. kentuckyensis described from the limestone of the Floyds Knob formation in Jefferson County, Kentucky, were recovered from acid residues. Any calcareous material originally present in the test would have been dissolved before the specimens were recovered, However, it may be noted that in washed shale samples which have not been treated with acid, specimens of H. kentuckyensts (siliceous ) occur with calcareous megafossils which are not replaced by silica. The rare effervescence in H. kentuckyensis mentioned above prob- ably is due to calcareous material in the main cavity of the test or m tiny spaces which may occur between siliceous grains. Hyperammina rockfordensis Gutschick and Treckman, 1959 JBL, Palle renee ORs Ik AG, iis, IOS lis, &) Hyperammina rockfordensis Gutschick and Treckman, 1959, Jour. Paleont., vol. 33, No. 2, p. 238, pl. 34, figs. 1-5, text-figs. 1A-1C. Description—Test consists of a prolate to spherical proloculus, the diameter of which is equal to or greater than the maximum diameter of the second chamber, and a straight or nearly straight undivided second chamber which enlarges only slightly distally so 268 BULLETIN 196 that the apertural region of the second chamber is only slightly larger in diameter than the initial portion of the second chamber; a slight amount of hourglass tapering is noted on some tests; test slightly constricted externally; apertural end is broken off of all present specimens; wall constructed of fine siliceous grains in siliceous cement; wall color white to buff to gray. Measurements—See Table 14 for measurements of present specimens of Hyperammuina rockfordensis and Table 15 for range in measurements of the species. Table 14. Measurements of Hyperammina rockfordensts Gutschick and Treckman, 1959, in mm. diam. length locality number, specimen and of of max. min. formation, and bed type number proloc. test diam. diam. number PI26) tig 0 -105 521 .059 .050 K-17, New Providence, bed 3 il, Ail, anes 1% .160 .670 118 109 K-13, New Providence, bed 2 PAL alo sehen, 318} 118 554 .084 .067 K-57, New Providence, bed 8 PALA s oregs 10) .118 .738 101 084 K-13, New Providence, bed 2 il, Al aiyed. I .092 E822 088 .062 K-13, New Providence, bed 2 Table 15. Range in measurements of 24 specimens of Hyperammina rockfordensis Gutschick and Treckman, 1959, in mm., and comparison with the original types As measured Restored Original types Diam. of proloculus .092-.160 .092-.128 .110-.130 Max. diam. of test .050-.118 .040-.094 .090-.110 Min. diam. of test .050-.109 .040-.087 .070-.090 Comparison and affinities—Hyperammina rockfordensis has its closest affinities to H. kentuckyensts, but H. rockfordensts differs from H. kentuckyensts in having: (1) only slight hourglass tapering in some specimens, (2) the second chamber expanding only slightly from the proximal to the distal end so that the proloculus possesses the greatest diameter observed in the whole test (or at least a diameter equaled only by the greatest diameter of the second chamber), (3) a test only slightly to moderately constricted (if at all), and (4) rather more granularity to the test wall. It appears that Hyperammina rockfordensis is the ancestral MISSISSIPPIAN SMALLER FORAMINIFERA: CONKIN 269 stock from which H. kentuckyensis was derived. This belief is based on several considerations. H. rockfordenstis has its closest affinities to H. kentuckyensis and is directly succeeded in time by H. kentucky- ensis (H. kentuckyensis does not occur below the Osagian and //. rockfordensts is typically a Kinderhookian species known only from the lower Osagian). The transition from H. rockfordensis to H. kentuckyensts occurred in Coral Ridge time inasmuch as few speci- mens of H. rockfordensis were noted in the lower part of the Button Mold Knob member and H. kentuckyensis is rarely encountered in the lower part of the Coral Ridge member of the New Providence formation. The morphological features of Hyperammina rockfordensis could be, with moderate exaggeration, made to correspond on a specific level with the morphological features of H. kentuckyensts. Indeed, rarely a specimen seems to fit in either species and can be identified only by its association with distinctive forms of one or the other species. Thus, I believe that the material presented in the Kinder- hookian H. rockfordensis and the lower Osagian forms of H. ken- tuckyensis exhibits as well as can be hoped for among Paleozoic simple arenaceous Foraminifera the transformation of one species into another, The geologic range, the time of first appearance of H. kentuckyensis, the time of last occurrence of H. rockfordensis, and the morphological affinities of the two species are consistent with the interpretation of the evolution of H. kentuckyensis from H. rockfordensts. Stratigraphic occurrence —Hy perammina rockfordensis is known from the Kinderhookian Rockford limestone of northern Indiana (Gutschick and Treckman, 1959). The species is herein recognized from the Upper Devonian Blackiston formation; in the Kinder- hookian, from the Eulie and Maury shales of Tennessee, the Falling Run member of the Sanderson formation and the Jacobs Chapel shale of southern Indiana. H. rockfordensis was found to occur especially in the Coral Ridge member of the New Providence for- mation and in the lower few feet of the New Providence formation where the Coral Ridge member is not recognized, The species occurs rarely in the lower part of the Button Mold Knob member of the New Providence formation and in the Henley shale of Ohio. The age of the lowest beds (lower Coral Ridge member) of the New 270 BULLETIN 196 Providence formation is in doubt. The lower part of the Coral Ridge member does not contain a megafossil fauna and may be partially Kinderhookian in age. Conkin (1957) adequately demonstrated a low Osagian age for the megafossil fauna from the upper part of the Coral Ridge member in Jefferson and Bullitt counties, Kentucky, and Clark County, Indiana. (See Charts 3-6, 8-13, 16-18, 21, and 22 for details of occurrence of H. rockfordensis in the Mississippian. ) Ecology—In Kentucky, nearly all specimens of Hyperammina rockfordensis are found in the Coral Ridge member of the New Provi- dence formation, or equivalent parts of the New Providence forma- tion; the characteristics of the Coral Ridge member were given by Conkin (1957, p. 116): upper part: Shale, green-gray to blue-gray, with ironstone lenses, ironstone cone-in-cones, flat, variously shaped, dark gray to blue-gray, small ironstone nodules, some phosphatic nodules, rare and thin ferruginous and fossiliferous limestone lenses; pyritized, marcasitized, silicified, Coral Ridge fauna. lower part: Shale, green-gray, virtually free of ironstones of even the smallest size, with worm markings; no megafossils noted. Inasmuch as Hyperammina rockfordensis occurs in the Coral Ridge member of the New Providence formation and in the Rock- ford limestone, we must consider the ecological conditions existing during the deposition of the Coral Ridge member and the Rockford limestone in order to hope to present something of the ecology of the species. The fossils of the Coral Ridge fauna are pyritized, marcasatized, and some individuals are replaced partially by silica; the fauna is associated with a large number of small lens-shaped ironstone nodules and beds of ironstone cone-in-cone layers; phosphatic-fer- ruginous thin lenses are present at Kenwood Hill (Locality K-3). It seems as if the Coral Ridge fauna is a biocoenosis in that (1) most species present complete growth series from young to adult individuals, (2) fragmentary specimens are rare, (3) no real evi- dence of currents is preserved in the fine, clayey, plastic shales, and (4) the pelecypods are preserved with both valves tightly closed. The great amount of iron sulphide in the sediments may indicate the sudden death of the fauna en masse because of reducing conditions and the release of poisonous sulphides. The presence of abundant coprolite-like structures may also indicate conditions of incomplete oxidation, but the presence of the large number of impure calcareous MIsSISSIPPIAN SMALLER FORAMINIFERA: CONKIN 271 ironstones and the absence of carbonaceous material in the sediments would seem to indicate shallow water deposition; nevertheless, the presence of several goniatite genera (Merocanites, Pericyclus, and Beyrichoceras) does not restrict the environment to shallow water. Hyperammina rockfordensis is present in the lower part of the Coral Ridge member where no megafossils (except Scalarituba) are known. In all events, it is demonstrated that H. rockfordensis “preferred” muddy bottoms in which there were sufficient amounts of fine silt to allow construction of a fairly thick arenaceous test. The Rockford limestone lithology was characterized by Gut- schick and Treckman (1959, pp. 230, 231) as a: . . yellow-grey fine-grained argillaceous crinoidal limestone with small black rounded phosphatic pebbles in its basal part. There are also 1 to 2 inch interbeds of calcareous fossiliferous shale. The HCl acid residues are largely made up of fine silty granular siliceous porous aggregates, undoubtedly argilla- ceous, and arenaceous Foraminifera in abundance. There are some quartz sand grains, silicified fragmental fossil material, pyrite, rare glauconite, and oc- casional radial aggregates of fine needle-like crystals of millerite. Gutschick and Treckman continued by discussing the fauna of the Rockford limestone, mentioning the several cephalopods which apparently were found in the shale units, . Other large fossils are scarce because of limited exposures, but include both large and diminutive forms of brachiopods, corals, bryozoans, gastropods, trilobites, abundant echinoderm debris and fish fragments. The microfaunas include conodonts, holothurian sclerites, microcrinoids, ostracodes, worm tubes, and other material. Most, if not all, are calcareous or phosphatic and are found in the water washings of the calcareous shale inter- beds. ... The major portion of the fauna of the Rockford is diminutive which suggests some restrictions in general normal marine conditions. The acid residues of the Rockford limestone of southern Indiana consist of fine muds, plus arenaceous grains, fossils, and fossil frag- ments. The presence of glauconite and pebbles of phosphate must indicate near shore environment. The possibility that the Rockford limestone represents lagoonal deposits should at least be considered. ‘The fine-grained muds, the presence of diminutive elements of the fauna, the thinness of the Rockford limestone, and its position in an unstable framework of sedimentation (fairly quick changes in environments as presented by various different lithologies in rather thin beds below and above) may indicate deposits laid down near a fluctuating sea shore. In conclusion, it can be remarked that Hyperammuina rockford- ensis was well adapted to fine-grained sediments where soft muddy 272 BULLETIN 196 bottoms were the rule, but where there were sufficient amounts of fine silt to allow construction of a fairly thick arenaceous test. Family EARLANDIITDAE Cummings, 1955 Genus EARLANDIA Plummer, 1930 Nodosinella Brady, 1876, (pars), Paleont. Soc., vol. 30, p. 66. Earlandia Plummer, 1930, Univ. of Texas, Bull. 3019, pp. 12, 13; Cushman, 1948, Foraminifera, Cambridge, p. 86; Cummings, 1955, Micropaleontology, WOl- 1 No! 3.5p) 228: Type species, Earlandia perparva Plummer, 1930 (original designation by Plummer, 1930). Description—H. J. Plummer (1930, pp. 12, 13) described Earlandia from the Pennsylvanian Brownwood shale at Bridgeport, Wise County, Texas. Test free, very elongate, composed of a globular or subglobular proloculus and an elongate, nonseptate, second chamber; shell wall of minute crystalline calcareous granules bound by a calcareous cement, imperforate, smoothly fin- ished; aperture a broad circular opening at the end of the tube. ... The salient distinguishing character of Earlandia n. gen. is the constitution of the shell wall, which is identical with that of Endothyra and Nodosinella. Hyperam- mina is its morphological equivalent with a typically adventitious test (aren- aceous in Pennsylvanian strata). Hyperamminoides [synonym of Hyperammina Brady, 1876] another very closely allied structure is composed of fine siliceous sand grains smoothly finished with much siliceous cement and is especially characterized by the constricted aperture at the end of the enlarging second chamber. Cummings (1955, p. 227) erected the new family Earlandtidae to embrace those genera which are, “Tubular or uniserial tests in which the wall is composed of equidimensional granules of calcite bound by calcium cement.” Cummings placed Harlandia Plummer, 1930, Earlandinella Cummings, n. g. (1955, p. 230), and Lugtoma Cummings, n. g. (1955, p. 231) in the Earlandiidae, In Europe, Earlandia ranges stratigraphically from the Middle ‘Yournaisian into the Lower Permian (Cummings, 1955, p. 235, text- fig. 10). In Australia Earlandia is reported from the Permian (Cres- pin, 1958, pp. 58, 59). Earlandia has been recorded from North America only in the Pennsylvanian; however, this paper extends the stratigraphic range of Earlandia downward into the Middle Mississippian. The relationship of Earlandia and Paleozoic species of Hyper- ammina in regard to general morphology and wall structure is dis- cussed in this work under the genus Hyperammina. Some workers, MIssISSIPPIAN SMALLER FORAMINIFERA: CONKIN 273 as Plummer (1930, 1945) and Conkin (1954), have held (or tacitly assumed) that Paleozoic species of Hyperammina are congeneric with Recent Hyperammina; but others, as St. Jean (1957) believed that all Paleozoic species of Hyperammina are in reality species of Earlandia which have been secondarily replaced and recrystallized. The latter group of workers hold that Paleozoic Hyperammuina are not congeneric with Recent Hyperammina. I admit that some Paleozoic Hyperammina may eventually prove to be Earlandia; nevertheless, I can not accept the thesis that all Paleozoic Hyperam- mina are merely replaced and recrystallized Farlandia. Earlandia consternatio, new species Pl. 2a" fies! 14-16); Tk, AG. sales, lS Mee IM) Description —Test moderate-sized, elongate; proloculus (broken off of all specimens) followed by an undivided tapering and slightly arcuate second chamber; test constricted at rather regular intervals; test wall of calcium carbonate particles in crystalline calcite cement; wall imperforate; aperture formed by slightly constricted open end of second chamber; prominent lip present; test smooth with texture of unglazed porcelain; color, pastel gray. Measurements—See Table 16 for measurements of Farlandia consternatio and Table 17 for range in measurement of £. conster- natio and comparison with £. perparva Plummer, 1945. See Table 13 for comparison with Hyperammina kentuckyensis. Comparison and affinities—Earlandia consternatio is similar to the type species of Earlandia, E. perparva, but E. consternatio has a more constricted aperture, is less elongate (rather more cylin- drical than E. perparva), and is larger. Earlandia consternatio is similar to Hyperammina kentuckyensts in its morphology, but the test of E. consternatio is less prominently constricted; furthermore, the test of E. consternatio is completely calcareous. Type locality —Outcrop on slope west of farm off of Sand Lick Road, Caldwell County, Kentucky (Locality K-24). The holotype is from shale in the Paint Creek limestone (Bed 1). Stratigraphic occurrence.—Earlandia consternatio is known only from two Chesterian formations, the Paint Creek and Glen Dean 274 BULLETIN 196 limestones, and one Meramecian formation, the Somerset shale mem- ber of the Salem limestone. (See Charts 5, 7, 14, 15, and 22 for de- tails of occurrence of £. consternatio in the Mississippian. ) Ecology —Earlandia consternatio was found only in calcareous and fossiliferous shales. Seemingly then, the species required an en- vironment in which the water was charged with calcium bicarbonate. Remarks—TVhe remarkable similarity which exists between Earlandia consternatio and Hyperammina kentuckyensis seems to indicate the perfection of isomorphism between analogous genera of Foraminifera. The specific name is proposed because of the surprising similar- ity which exists between Earlandia consternatio and Hyperammina kentuckyensts. Table 16, Measurements of Earlandia consternatio, n. sp., in mm. length locality number, specimen and minus max. min. formation, and bed type number proloc. diam. diam. number PL AL. aayes, A1(65 1.700 190 100 K-24, Paint Creek, bed 1 PAL, Alla spe Wid 1.200 180 .080 K-24, Paint Creek, holotype bed 1 AL Ale aaner aS 800 .120 .050 K-24, Paint Creek, bed 1 Table 17. Range in measurements of six specimens of Earlandia consternatio, n. sp., in mm. and comparison with E. perparva Plummer, 1945 E. consternatio E. perparva Length of test .61-1.70 1.00 Max. diameter .10-.19 08 Min. diameter .03-.10 Diam. of proloculus .030 Family REOPHACIDAE Cushman, 1927 Subfamily REOPHACINAE Cushman, 1927 Genus REOPHAX Montfort, 1808 Reophax Montfort, 1808, Conch. Syst. vol. 1, p. 331; Brady, 1884, (pars), Rept. Voyage Challenger, Zool., vol. 9, p. 289; Chapman, 1902, (pars), The Foraminifera, London, p. 137; Cushman, 1930, Uniy. Texas, Bull., No. 3019, p. 37; idem, 1948, Foraminifera, Cambridge, p. 90, pl. 3, figs. 27, 28; Cummings, 1955, Micropaleontology, vol. 1, No. 3, pp. 234, 235, pl. 1, figs. 7, 8, 13, 16, 18, text-figs. 8, 9. (non Reophax, Rhumbler, 1895, Nachr. K. Gesell. Wiss. Gottingen, p. 82 MIssISSIPPIAN SMALLER FORAMINIFERA: CONKIN 275 Haplostiche Schwager, 1865, Ver. Vaterl. Nat. Wiirttemburg, Jahresh., vol. 21, p. 92, figs. 2a-2c. (non Haplostiche Reuss, 1861, K. Béhmen Gesell. Wiss., Sitzber., vol. 1, p. 15) Nodulina Rhumbler, 1895, K. Gesell. Wiss. Gottingen, Nachr., pp. 85, 86. Protoshista [?] Eimer and Fickert, 1899, Zeitschr. Wiss. Zool., vol. 65, pp. 677, 678, text-fig. 21. Lugtonia [?] Cummings, 1955, Micropaleontology, vol. 1, No. 3, p. 231, pl. 1, figs. 9-12, 20, text-fig. 6; Crespin, 1958, [Australia] Bureau Mineral Res., Geol. and Geophys., Bull. 48, pp. 65, 66, pl. 7, figs. 6, 7. Type species, Reophax scorpiurus Montfort, 1808. The generic definition of Reophax as given by Cushman (1930, p. 37) follows: Test free, elongate, composed of several undivided chambers, ranging from overlapping to remotely separated ones connected by stolon-like necks, in a straight or curved linear series; wall single, of agglutinated material, firmly cemented, sand grains, mica scales, sponge spicules or other foraminifera; aperture simple, terminal, sometimes with a slight neck. Cushman’s generic definition for Reophax (1948, p. 90) differs essentially from his 1930 generic definition only in the mention of a chitinous base for the test wall. Cummings (1955, pp. 231, 232) divided Reophax into two gen- era. Reophax was retained by Cummings for those forms which are agglutinate and possess stolon-like necks, while a new genus, Lug- tonta, based on Nodosinella concinna Brady, 1876 as the type species, was erected with the purpose of embracing those forms which have succeeding chambers overlapping preceding chambers and a test wall of original granules of calctum carbonate in calcareous cement. Cummings placed Lugtona in his new family Earlandiidae which he defined in the following manner (1955, p. 227): “Tubular or uniserial tests in which the wall is composed of equidimensional granules of calcite bound by calcareous cement.” Cummings’ basis for the genus Lugtonia was some 450 speci- mens from the British Lower Carboniferous, all of which are silicified. Thus, in reality, Lwgtonia was erected only on the basis of its pos- session of overlapping chambers in contrast to the presence of stolon- like necks connecting the chambers in the genus Reophaw s.s.; Cum- mings noted (1955, p. 231) that, “[Lugtonia] must be distinguished on the basis of chamber form,” . . . “original microstructure of wall unknown. . .” Cummings has assumed without conclusive evidence that the wall of Lugtonia is secondarily silicified from an original wall of calcareous granules in calcareous cement. 276 BULLETIN 196 While discussing his specimens of Hyperammina, Cummings (1955, p. 234) noted: “Usually, representatives of the genus Hyper- ammina are found in the British Carboniferous in an unaltered state.” It seems strange that in the British Carboniferous all Lug- tonia, and Reophax to a varying degree, should be completely secondarily replaced by silica while the Hyperammina of that region are usually unaltered, agglutinate test with ferrugino-calcareous cement. It becomes singular when we remember that North Amer- ican Mississippian and Pennsylvanian, and Australian Permian Hy- perammina are reported to possess siliceous cement, Further, I am not convinced that all reophacids with overlapping chambers are or were originally composed of calcareous granules in calcareous ce- ment. Reophax with overlapping chambers described in the present paper are composed of quartz grains in siliceous cement, not of calcareous granules in calcareous cement. Crespin’s (1958, p. 65) new species which was referred to Lugtonia, L. thomast, does not fit Cummings’ generic definition in that L. thomast Crespin was described as: “Wall thick, finely aren- aceous, composed chiefly of regular sized quartz grains in consider- able cement, giving the test a smooth, polished appearance.” Crespin recognized the difficulties in referring her new species to Lugtonta; she noted (1958, p. 35): Tests of certain foraminifera from Western Australia have been referred to the new genus Lugtonia of Cummings (1955). All features are similar to this form, but the wall of the test though polished is definitely arenaceous, quartz grains of varying size being set in a siliceous cement. Cummings placed the genus in his new family Earlandiidae as he regards the present siliceous test as secondary to granular calcareous structure. However, for the present the Western Australian specimens are included in the Reophacidae. Further, Crespin (1958, p. 35) noted in her discussion of the genus Hyperammina: As already commented here, there seems to be little or no evidence of secondary silicification of arenaceous tests in the Australian Permian or in the rocks in which the foraminifera are found. It is certain that the only basis for differentiation of Lugtoma as a distinct genus is in the lack of stolon-like necks which connect the chambers in Reophax, s.s. and the possession of overlapping chambers in Lugtonia. The overlapping of the preceding chambers by succeeding chambers may or may not be of generic significance. MIssIsSIPPIAN SMALLER FORAMINIFERA: CONKIN Diff) Until the Reophax, s.1. of the world are studied as to wall structure, and the forms with overlapping chambers are found to invariably possess original calcareous granules in calcareous cement, I have no course but to use Reophax, s.J. and to consider Lugtonia as of doubtful generic status. If it be found that the overlapping nature of the chambers is truly of generic value, then Lugtonia could be considered a valid genus only if it be removed from the family Earlandidae and placed in the Reophacidae, a family of arenaceous Foraminifera. Cummings indicated in text-figure 10 (1955, p. 235) that Lugtonia is known in the British Isles from the upper part of the Viséan and Namurian, with some species restricted to the Namurian. However, he records Reophax, s.s. (in the upper Paleozoic) through- out the Carboniferous and Permian. In the rest of the world, true Lugtonia has not yet been recognized, but Reophax, s.1. with over- lapping chambers is found almost universally in the geologic column from Paleozoic to Recent. Thus, seemingly, Lugtonia has no wide stratigraphic significance. (See Chart 23 for stratigraphic range of Reophax, s.J. in the Mississippian as determined in this study. ) Reophax cf. R. arenatus (Cushman and Waters), 1927 Bl Fal. ie 12 1211, PADS ialee, IS aes, al Nodosinella arenata Cushman and Waters, 1927, Cushman Lab. Foram. Research, vol. 3, p. 147, pl. 26, figs. 2, 3. Nodosinella? arenata, Warthin, 1930, Okla. Geol. Sur., Bull. 53, p. 28, pl. PBS AG ee he Reophax arenatus, Plummer, 1945, Univ. Texas, Pub. 4401, pp. 225, 226, pl. 17, figs. 1-3. Description—Test stocky, consisting of a globular proloculus and a second distinctly pyriform chamber of a greater diameter than the proloculus; aperture at open end of tapering neck of second chamber; wall composed of fine quartz grains in a moderate amount of siliceous cement. Measurements —See Table 16 for measurements of Reophax cf. R. arenatus. Comparison and affinities—The present specimens closely re- semble Plummer’s figured specimens of Reophax arenatus (1945, pl. 17, figs. 1, 3). Only two specimens were found in the present study; 278 BULLETIN 196 thus the range of variation of Reophawx cf. R. arenatus in the Missis- sippian system is not known. Stratigraphic occurrence.—Reophax cf. R. arenatus has been found only in the Rothwell shale member (Bed 8) of the Muldraugh formation at Garrison, Lewis County, Kentucky (Locality K-67). Ecology—The specimens of Reophax cf. R. arenatus are from a soft, clayey, plastic when wet, olive-gray to maroon shale. This shale contains only small amounts of fine to medium-sized grains. No macrofossils were observed. Brady (1884, p. 289) noted the wide depth tolerance of Reophax: The genus Reophax is cosmopolitan and its bathymetrical range extends from almost the deepest portion of the sea-bottom yet explored [as determined by the Voyage of the Challenger 1873-1876] to the shallow waters of the Laminarian zone. Reophax asper Cushman and Waters, 1928 Veal, Pal, wees, GALOIS Reophax asperus Cushman and Waters, 1928, Cushman Lab. Foram. Re- search, Contr., vol. 4, p. 37, pl. 4, fig. 7. Reophax asper Cushman and Waters, 1930, Univ. Texas, Bull., No. 3019, 5 SR yo A save IN): Description—Test elongate, coarse grained, consisting of five chambers which are somewhat obscure in outline due to rugosity of test wall; chambers oblate and gradually expanding in diameter; last chamber roughly pyriform; wall composed of angular quartz grains in a small amount of siliceous cement. Measurements—See Table 19 for measurements of Reophax asper. Comparison and affinities —The present specimen is remarkably similar to the figured type of Cushman and Waters (1930, pl. 2, fig. 10) but is slightly smaller and apparently has one less chamber. Reophax asper is distinctive among the species of Reophaw consid- ered in this paper because of the rugosity of the test. Table 18. Measurements of Reophax cf. R. arenatus (Cushman and Waters), 1927, in mm. length length specimen and of max. of last no. of diam. of type number test diam. chamber chambers proloculus Pls 215 fig: 19 .746 403 453 2 369 Pl. 26, fig. 12 658 302 403 2 201 MISsSISSIPPIAN SMALLER FORAMINIFERA: CONKIN 279 Table 19. Measurements of Reophax asper Cushman and Waters, 1928, in mm. Pl. 21, fig. 24 Length of test 570 Max. diameter .226 Length of last chamber e252 Number of chambers 5 Diameter of proloculus 084 Stratigraphic occurrence —The figured specimen was found in the Button Mold Knob member (Bed 2) of the New Providence formation at the Louisville Cement Company Quarry, Clark County, Indiana (Locality I-3). The species was originally reported by Cushman and Waters, 1930, from the Upper Pennsylvanian of Texas. Ecology —Reophax asper probably had ecological requirements similar to the other species of Reophax of this study, but Rk. asper apparently “preferred” a muddy bottom in which there were suf- ficient quartz silt grains available for construction of a test. High concentrations of calcareous salts certainly were not required inas- much as the species occurs in the lower part of the Button Mold Knob member of the New Providence formation which at this lo- cality is not significantly calcareous and does not contain calcareous megafossils. Reophax kunklerensis, new species Pl. 21, figs. 20-23; IPL PAG, tales webs Teaiees, lz; Description—Test small, slender, straight to gently curved, consisting of small proloculus and a succession of seven to nine moderately inflated chambers which expand in diameter evenly until the last chamber; last chamber is as broad as or only slightly broader than preceding chamber, and up to three to six times broader in diameter than the first chamber; last chamber longer than pre- ceding chambers due to the tapering neck of the aperture and 1s of pyriform shape; last chamber as broad as long or nearly so, while preceding chambers are about 1.5 to 1.6 times broader than long; wall composed of rather coarse quartz grains in a small amount of siliceous cement; no dimorphism is evident. Measurements —Table 20 gives the measurements of Reophax kunklerensis, and Table 21 the range in measurements of the species. bo oo) =) BULLETIN 196 See Table 25 under description of R. minutissimus for comparison of R. kunklerensis with that species. Comparison and affinities —Reophax kunklerensts is similar to R. minutissimus Plummer, 1945; however, R. kunklerensis is shorter and more slender and has more chambers than does R. minutissimus. Reophax kunklerensis differs from R. mcdonaldi in that R. kunklerensts is shorter, has more chambers (and these chambers less rounded ), is more slender, and expands more from the proloculus to the last chamber. Type locality—Kunkler Quarry, on hill side, south side of U.S. Highway 460, 1.3 miles west of Uniontown Post Office, Perry Coun- ty, Indiana (Locality I-1). Types are from the upper shale ( Bed 7) of the Menard limestone. Stratigraphic occurrence—Reophax kunklerensis is known to occur only in the lower three feet of the upper shale portion of the Menard limestone, just above the nine-and-one-half foot quarried limestone. The limestone units were merely spot checked for Fora- minifera by acidization. Ecology—The upper shale of the Menard limestone is a marine, soft, plastic when wet, buff to tan to brown, calcareous and fossili- ferous, thin-bedded unit. This fossiliferous shale, lying immediately above the main limestone unit of the formation and lying immedi- ately below more than 10 feet of dark gray, nonfossiliferous shales, represents a depositional environment perhaps transitional from typical marine waters to quiet muddy waters of lagoons. Reophax kunklerensis has a moderate amount of cement (at present siliceous, regardless of its original chemistry) and a con- siderable amount of silt particles in its test. R. kunklerensis was adapted to live in fine-grained calcareous muds which contained only small amounts of silt. The invertebrate fauna of the upper shale is restricted in the number of animal groups present. The dominant groups recovered from the shale are the crinoids (many wing plates of Pterotocrinus menardensis), the brachiopods (thin valved Derbya), fenestrate bryozoans, and rare solitary lophophyllid corals. The invertebrate fossil shells are mostly complete (7. e., both valves of thin-shelled brachiopods are commonly intact), Some fragmentation occurred MISSISSIPPIAN SMALLER FORAMINIFERA: CONKIN 281 perhaps as a result of post-depositional compaction of the shale; little breccia 1s present; thus, wave action was not pronounced. The foraminiferal fauna of the Menard limestone (shale) con- sists of a small array of arenaceous genera which characteristically live in silty or sandy muds: Hyperammuina, Involutina, and Reophax. Remarks.—Reophax kunklerensis derives its name from the Kunkler Quarry, west of Uniontown Post Office, Perry County, Indiana. Table 20. Measurements of Reophax kunklerensis, n. sp., in mm. diam. of length proloculus Specimen and length max. of last no. of (or of first type number of test diam. chamber chambers chamber) Pi 2 etis: 20! -503 .143 118 US) .050 holotype Pl. 26, fig. 14 .529 .130 101 8 (.042) VAG ABI aetee, ZY .570 .134 134 9 .037 JA Ail, saver, We} 590 134 .134 9 .042 I, All, iater, Ail 420 118 118 hk .033 ‘Table 21. Range in measurements of eight specimens of Reophax kunklerensis, n. sp., 1m mm. Length of test 420-.590 Max. diameter -118-.151 Length of last chamber .101-.143 Number of chambers 7-9 Diam. of proloculus -033-.050 Reophax cf. R. lachrymosus Gutschick and Treckman, 1959 PI. 21, fig. 18; IG AO. ie. WBS Janes ie Reophax lachrymosa Gutschick and Treckman, 1959, Jour. Paleont., vol. 33, No. 2, pp. 240, 241, pl. 34, figs. 20-25, text-fig. 2A, 2B. Description —This species is represented in the present material by only two fragmentary specimens which consist of two chambers each; these chambers are elongate and pyriform; the last chamber has a length of 1.36 and 1.4 times greater than the breadth; present specimens are flattened on one side; surface of test finely granular, of fairly small quartz grains in a moderate amount of siliceous ce- ment; color of test white and gray. Measurements—See Table 22 for measurements of Reophax cf. R. lachrymosus. 282 BULLETIN 196 Table 22. Measurements of Reophax cf. R. lachrymosus Gutschick and Treckman, 1959, in mm. length diam. length diam. locality number, specimen and of first of first oflast oflast formation, and type number chamber chamber chamber chamber bed number 4G Al oayen ah 268 180 235 185 K-58, New Providence, bed 3 P26 retical s 235 168 sa 52 168 O-7, Cuyahoga, bed 4 Comparison and affinities —The present specimens are similar to the last two chambers of Gutschick and Treckman’s paratype of Reophax lachrymosus (1959, pl. 34, fig. 23), but the present speci- mens are proportionally slightly broader. R. lachrymosus is similar to R. bendensis Plummer, 1945, as Gutschick and Treckman pointed out (1959, p. 240); however, R. bendensts is generally much larger. Plummer (1945, pl. 17, fig. 8) shows a youthful specimen of a size nearly that of R. lachrymosus; however, the present specimens are somewhat broader than R. bendensis which has chambers 2.3 times longer than broad, Stratigraphic occurrence.—Reophax cf. R. lachrymosus is herein recorded from the lower New Providence formation of Kentucky and the lower three feet of the Cuyahoga formation of Ohio. This species was originally described from the Rockford limestone of northern Indiana. See Charts 10, 21, and 22 for details of occurrence of R. cf. R. lachrymosus in the studied area. Ecology.—The specimens of this species were found only in soft, plastic when wet, shales. Thus, the species was adapted to live in muddy environments with only small amounts of silt grains present. Table 23. Measurements of Reophax mcdonaldi, n. sp., in mm. diam. of length proloculus specimen and max. of last no. of (or of first type number length diam. chamber chambers chamber) Pl. 21, fig. 25, 640 269 235 5 ASA Pl. 21, fig. 26 .678 .269 jie) 3 5a Pl. 21, fig. 30 738 302 302 3-4 (.151) Pl. 21, fig. 28 658 235 235 4-5 (.118) Pl. 21, fig. 29 704 319 470 3 (.226) VEAL PAL, Gate, PAN) -622 Pas .285 3 (.134) 9 MISsSISSIPPIAN SMALLER FORAMINIFERA: CONKIN 283 Table 24. Range in measurements of 13 specimens of Reophax mcdonaldi, n. sp., in mm. and comparison with R. tumidulus Plummer, 1945 R. mcdonaldi R. tumidulus Length of test .554-.840 1.05 Max. diameter .201-.369 40 Length of last chamber -185-.470 No. of chambers 3-5 4 Diam. of proloculus ltSil .030 Reophax medonaldi, new species Pl. 21, figs. 25-30; LIL, PAD, IDR, Alig Jaa Wee IG Description.—Test small, rather stocky, straight to slightly curved, with a fairly large proloculus and a succession of up to five moderately inflated chambers which enlarge in diameter only slightly in some specimens, but which in most specimens enlarge gradually up to twice the diameter of the first chamber; chambers about 1.2 to 1.5 times broader than long, except the last chamber which 1s as long as it is broad or nearly so, due to the tapering neck of the aper- ture whch gives the last chamber its broad pyriform appearance; test coarse textured, composed of quartz grains in a moderate amount of siliceous cement. Measurements —See Table 23 for measurements of Reophax mcdonaldi and Table 24 for range in the measurements of the species, and for comparison with R. twmidulus Plummer. Comparison and affinities—Reophax mcdonaldi most closely resembles R. tumidulus Plummer (1945, p. 231, pl. 17, fig. 31). How- ever, R. mcdonaldi has more chambers, is shorter, less broad, and expands more than R. twmidulus. R. mcdonaldi differs from R. kunklerensis in being larger, broader, and expanding less and having fewer chambers. Type locality.—Road cut along Vanceburg-Tannery Road, 1.25 miles south of Vanceburg, Lewis County, Kentucky (Locality K-66). Holotype and all figured measured specimens on Table 23 are from the Churn Creek shale member of the New Providence formation (Bed 9). Stratigraphic occurrence.—Reophax mcdonaldi is apparently re- stricted to the Osagian, occuring only in the Churn Creek shale member of the New Providence formation in Kentucky and in shale in the Black Hand sandstone member of the Cuyahoga formation 284 BULLETIN 196 of Ohio. (See Charts 10 and 19-22 for details of occurrence. ) Ecology.—Reophax mcdonaldi is known only in shaly siltstone and shale in sandstone. The nature of the test reflects this species’ “preference” for silty or sandy environments by having its wall con- structed of moderate to coarse-grained silt or sand, with a small to moderate amount of siliceous cement. No megafossils are present in the enclosing sediments except for “worm markings” (poorly preserved specimens of Scalarituba). Thus, R. mcdonaldi was cap- able of living in muddy, sandy, waters where animals other than “Worms” were apparently unable to establish themselves, Remarks. —This new species of Reophax is named for Mr. Don- ald McDonald, Curator of the Geology Museum at the University of Louisville. Reophax cf. R. minutissimus Plummer, 1945 VEAL Ail, wines aliy/ Reophax minutissimus Plummer, 1945, Univ. Texas, Pub. 4401, pp. 230, 231, pl. 17, figs. 25-30. Description—TVest small (proloculus missing), consisting of four evenly and rather rapidly expanding chambers; first three chambers are moderately inflated and 1.7 to 2.7 times broader than long; last chamber as long as broad and pyriform; length of test is 1.94 times longer than width; test coarse grained, of quartz grains in silic cement. Measurements—Table 25 gives measurements of Reophax cf. R. minutissomus. Table 25. Measurements of Reophax cf. R. minutissimus Plummer, 1945, in mm. Pl. 21, fig. 17 Length 487 Max. diameter 25, Min. diameter 084 Length of last chamber 252 Comparison and affinities—This specimen closely resembles Plummer’s figured paratype (1945, pl. 17, fig. 26) of Reophax minutissimus. The present specimen is somewhat broader than Plummer’s figured specimens, but this may be due to incompleteness of the present specimen (only four chambers are preserved) and certainly one specimen could hardly exemplify a species. MIsSISSIPPIAN SMALLER FORAMINIFERA: CONKIN 285 A single specimen of Reophax cf. R. Stratigraphic occurrence. minutissimus was found in the basal part of the Henley shale mem- ber (Bed 2) of the Cuyahoga formation (New Providence forma- tion), one to two feet above the Sunbury shale at Locality K-61 (south of Hilda Post Office, Rowan County, Kentucky ). Ecology.—The Henley shale member of the Cuyahoga forma- tion is a soft, plastic when wet, olive-gray shale with small amounts of fine to medium-sized silt grains. The absence of megafossils in the basal portion of the Henley shale at Locality K-61, and the re- covery of only one specimen of Reophax cf. R. minutissimus may indicate that environmental conditions were far from optimum even for this species. Family TOLYPAMMINIDAE Cushman, 1929 Subfamily INVOLUTININAE Cushman, 1910 Genus INVOLUTINA Terquem, 1862, emend. Loeblich and Tappan, 1954 Ammodiscus Reuss, 1862, (pars), Akad. Wiss. Wien., Sitz., math-natu. Cl., Jahrg. 1861, 44, Abt. 1, p. 365. Involutina Yerquem, 1862, Acad. Imp. Metz, Mem., ann. 42 (ser. 2, ann. 9), 1860-1861, pp. 450, 451. Involutina Terquem, emend. Loeblich and Tappan, 1954, Washin Acad. Sci., Jour., vol. 44, No. 10, pp. 308-310, figs. 2a, 2b. vj Type species, Involutina silicea Verquem, 1862 (monotypic genus). The emended generic definition of /nvolutina Terquem, 1862 as given by Loeblich and Tappan (1954, pp. 308, 309) follows: Test free, discoidal, with proloculus followed by an undivided planispiral tubular chamber, which slightly overlaps preceding whorls at the lateral mar- gins; occasional irregular surficial constrictions possibly denoting stages of growth, but without internal septa; wall finely agglutinated, of sand grains with considerable cement; aperture at the open end of the tube. Loeblich and Tappan (1954, p. 308) showed that Ammodtscus Reuss, 1862 is a junior synonym of Spirillina Ehrenberg, 1843 and that the generic name Ammodiscus should be suppressed. The type species of Involutina, I. silicea Terquem, 1862, was found to be an agglutinate form, completely undivided internally, and thus capable of embracing all species formerly relegated to the genus Ammodtscus, other than those forms which possess a hyaline calcareous test. 286 BULLETIN 196 The emended definition of Jnvolutina by Loeblich and Tappan did not make a definite reference to those forms of “Ammodiscus” which, in addition to being aggiutinate and undivided internally, possess a final rectilinear portion (neck) such as /nvolutina (form- erly Ammodiscus) exserta. | believe that such meaning was implied when Loeblich and Tappan (1954, p. 308) concluded: “Thus the species previously considered as Ammodiscus will fall in the same genus [nvolutina.” Loeblich and Tappan (1954, p. 308) removed the genus Involutina Terquem, 1862 from the family Silicinidae and relegated it to the family Tolypamminidae Cushman, 1929 and the subfamily Involutininae Cushman, 1910. Chart 23 gives the range of /nvolutina in the Mississippian as ' determined in this study. Inyolutina exserta (Cushman), 1910 Pl. 22, figs. 4-6, 8; Pl, 26, figs. 16, 17, 19; Fig. 21 Ammodiscus exsertus Cushman, 1910, United States Nat. Mus., Bull. 71, pt. 1; pp. 75, 76, figs. 97a, 97b (in text). Involutina exserta (Cushman), Gutschick and Treckman, 1959, Jour. Paleont., vol. 33, No. 2, p. 241, pl. 35, figs. 8, 9. Description——Test biconcave, consisting of a small proloculus and a second chamber planispirally coiled, of two to six volutions, becoming uncoiled and aligned at nearly a right angle to preceding whorls, and in the same plane as preceding whorls; aperture formed by open end of tubular second chamber; test rough, with medium- sized grains in a moderate amount of cement (Variant 2, see Com- parison and affinities); in a few cases the test is clear and glossy and made up largely of cement (Variant 1); color of test, white to gray- white to rusty. Measurements. exserta and Table 27 for the range in measurements of this species. See Table 26 for measurements of /nvolutina Table 26. Measurements of /nvolutina exserta (Cushman), 1910, in mm. locality no., specimen and thick- no. of diam. formation, and type number diam. length ness whorls proloc. bed number PInZ6 tie e19 .604 .622 118 3 K-6, New Provi- dence, bed 4 EZ Z tions 50 521 101 ae K-1, New Provi- dence, bed 2 MIsSISSIPPIAN SMALLER FORAMINIFERA: CONKIN 287 Pl. 26, fig. 16 269% 5 3695) 2042) 3 122016 — 2 O26. Henley, bed 10 P22 hho 4 335 562 .067 3 .017 K-14, New Provi- dence, bed 6 Pl. 22, fig. 5 igae SO2N) SeOGTe 22:5 K-14, New Provi- dence, bed 6 JPA, BA, waver, 6 386 521 .067 3 K-14, New Provi- dence, bed 6 Pl. 26, fig. 17 S70 8G ALORA SES O-4, Bedford, bed 3 Table 27. Range in measurements of 22 specimens of Involutina exserta (Cushman ), 1910, in mm. Diameter of proloculus .012-.025 Diameter of test .235-.386 Length of test .319-.622 Thickness of test .033-.118 Comparison and affinities—By reference to Tables 27 and 31 it will be seen that the infraspecific variation is as great within Involutina exserta as it is within J. semiconstricta. The forms in the present study resemble some of those found in the Rockford limestone by Gutschick and Treckman (1959, p. 241, pl. 35, figs. 8, 9); nevertheless, most of the present forms vary considerably from the Rockford specimens in having more rugged, coarser grained tests and larger size (herein called variant 2). The whorls in the present material are usually partly or completely ob- scured by the rough wall texture. A comparison of two morphological features of several present specimens of /nvolutina exserta and of several of Gutschick and Treckman’s forms (1959, p. 241) from the Rockford limestone follows: length diameter of test of test Present specimens: 430 mm. 362 mm. Rockford specimens: 410 mm. 330 mm. One variation of the species (herein called variant 1) is com- posed largely of cement with little agglutinated matter. Stratigraphic occurrence—Involutina exserta is known from: the Silurian (Moreman, 1930, p. 58; Dunn, 1942, p. 338); the Missis- sippian Kinderhookian Rockford limestone of Indiana (Gutschick and Treckman, 1959, p. 241); and the Recent (the holotype is from the sea off Japan). 288 BULLETIN 196 From the stratigraphic information collected in this study, Involutina exserta appears to be especially abundant in the Kinder- hookian and lower Osagian beds. No specimens were found in the Meramecian. With the exception of an isolated occurrence in the brown, plastic shaly part of the Menard limestone, no specimens were found in the Mississippian above the Osagian Brodhead forma- tion of Kentucky, nor above the middle Osagian Black Hand sand- stone member of the Cuyahoga formation of Ohio. Variant 1 has been found only at the following localities and in the following stratigraphic units: Nipgen, Ohio (Locality O-6), Cuyahoga formation, Henley shale member, lower one foot and from three to 4.5 feet (Bed 10). Jester Hill, Bainbridge, Ohio (Locality O-7), Cuyahoga forma- tion, Henley shale member, lower 11 feet (Bed 4). Armstrong, Ohio (Locality O-11), plastic shale in lower 5 feet of the Black Hand sandstone (Bed 1). (See Charts 3-7, 9-14, 16, and 18-22 for details of occurrence. ) Ecology.—Apparently Involutina exserta had much the same ecological requirements as J. semiconstricta inasmuch as the two species are in some instances associated with one another in the same beds, but J. exserta generally occurs in more arenaceous sedi- ments where fine to medium silt grains are available in sufficient quantity to construct the rather stout agglutinate test (variant 2). InvOlutina longexserta Gutschick and Treckman, 1959 PIS 22) fie staneeos Pl. 26, fig. 18; Fig. 22 Involutina longexserta Gutschick and Treckman, 1959, Jour. Paleont., vol. 33, No. 2, pp. 241, 242, pl. 35, figs. 10-14. Description—Test planispiral becoming uncoiled; coiled por- tion circular to oblately elliptical; second chamber coiled for a few volutions and then uncoiled at right angles to the preceding whorls, but still in the same plane; proloculus obscured by the coarse texture of the test; length of uncoiled portion of test is greater than or equal to the minimum diameter of the coiled portion; number of whorls varies from more than two to more than three; aperture circular, formed by open end of tube; wall structure arenaceous with medium MIssISSIPPIAN SMALLER FORAMINIFERA: CONKIN 289 coarse-grained silt and a moderate amount of insoluble cement (vari- ant 2); color of test, white to gray. Measurements—See Table 28 for measurements of /nvolutina longexserta and Table 29 for range in measurements of the species. Comparison and affinities—I have studied paratypes of Jn- volutina longexserta and am convinced of the validity of the species; however, some difficulty is experienced in deciding whether partic- ular specimens are complete tests of J. exserta or fragments of J. longexserta. | have followed the practice of referring to J. longex- serta only those specimens which are undoubtedly comparable to the types of the species. The present specimens possess fewer whorls than do the studied paratypes or figured types, and most present specimens have more coarsely arenaceous wall structure with less cement than do the types. In the present material, the internal coiled portion is almost completely obscured, but enough can be observed to ascertain the presence of only a small number of whorls. As to the general shape of the test in the present material, the coiled portion is less circular in outline than that of the types, although two specimens do re- semble three of the Rockford types (Gutschick and Treckman, 1959, pl. 35, figs. 12-14) including the holotype. None of the forms in the present material attains the maximum length of the Rockford specimens (.91 mm.); however, some of the present material closely approaches this dimension. On the other hand, the diameter of the coiled portion of the present specimens varies from .269 to .470 mm. while the diameter of the coiled portion of the original types of J. longexserta ranges only from .210 to .270 mm. The range of variation within /nvolutina longexserta can readily be appreciated from the above statements and by reference to Table 29: Stratigraphic occurrence.—Involutina longexserta was originally described from the Rockford limestone of northern Indiana (Gut- schick and Treckman, 1959). As determined in this study, J. longexserta has a stratigraphic range from the Upper Devonian New Albany shale to the lower New Providence formation. (See Charts 3, 5, 6, 9, 11-13, 16, 18 and 22 for details of occurrence. ) 290 BuLLETIN 196 Ecology—Apparently Involutina longexserta required much the same type of environment as did both J. exserta and I. semicon- stricta. The species occurs more frequently in the fine- to medium- grained, silt-bearing New Providence shales than in the less silty Kinderhookian shales; this, coupled with the observation that the present tests of 7, longexserta are of medium coarse arenaceous tex- ture with a moderate amount of cement, seems to indicate an in- herent “preference” for an arenaceous environment. Gutschick and Treckman’s types of Jnvolutina longexserta possess a clearer and more glossy test than do the specimens ob- served in this study. The fine-grained texture of the Rockford tests is probably due to the more calcareous and less silty nature of the sediments in the Rockford limestone. Table 28. Measurements of /nvolutina longexserta Gutschick and Treckman, 1959, in mm. locality number, specimen and thick- no.of formation, and type number diam. length ness whorls bed number PI Z6 etic. Ls 3/3) .739 109 2? K-13, Coral Ridge, bed 2 Pls 22) fie.9 404 -720 .084 2? K-13, Coral Ridge, bed 2 PAL ZN yee 7/ .269 554 .067 2? K-57, Bedford, bed 6 Table 29. Range in measurements of 12 specimens of Involutina longexserta Gutschick and Treckman, 1959, in mm. Diameter .269-.470 Length .394-.899 Thickness .033-.134 Involutina semiconstricta (Waters), 1927 Pla 22 tie stele Pl. 26, fig. 20; Wig. 20 Ammodiscus semiconstrictus Waters, 1927, Jour. Paleont., vol. 1, p. 132, pl. 22 tipeels Ammodiscus semiconstrictus var. regularis Waters, 1927, Jour. Paleont., vol. ae US) aL AZ say Be Cornuspira semiconstrictus, Harlton, 1933, Jour. Paleont., vol. 7, pp. 9, 10, pla Ztics, 2a. 2b: Involutina semiconstrictus (Waters), Loeblich and Tappan, 1954, Washing- ton Acad. Sci., Jour., vol. 44, No. 10, p. 306. Description—Test planispiral, circular, biconcave; test in some MISsSISSIPPIAN SMALLER FORAMINIFERA: CONKIN 291 instances elliptical as a result of secondary distortion; diameter of test .210 to .594 mm.; proloculus small, .008 to .028 mm. in diameter, spherical to elliptical in form; second chamber tubular, planispiral, of three to eight whorls, and moderately constricted externally; aper- ture circular in cross-section, formed by the open end of tube; medium-sized specimen has an apertural diameter of .37 mm.; wall composed of siliceous grains in siliceous cement; color of wall, gray to orange-buff to white. Two general variations in test composition are recognized in the Mississippian forms of Jnvolutina semiconstricta: Variant 1, clear and glossy and dominantly of cement with little agglutinate material; Variant 2, more robust test with much more agglutinate material and less cement. These variants are discussed under ecology, Measurements—See Table 30 for measurements of several Mississippian specimens and Table 31 for range in measurements and comparison with Pennsylvanian forms. Comparison and affinities—I have examined specimens from Plummer’s Pennsylvanian localities in Texas and agree with her (1945, p. 232) in considering /nvolutina semiconstricta var. regularis (Waters) to be synonymous with J. semiconstricta (Waters). How- ever, I am not convinced that J. semiconstricta var. regularts is a juvenal form of J. semiconstricta; rather, I believe that the relation- ships between the diameter of test, thickness of test, number of whorls, and size of proloculus indicate wide individual variation in adult forms in regard to these anatomical features. The wide infra- specific variation in J. semiconstricta can be appreciated by refer- ence to Table 31. By measurement and study of the various anatomical features of Involutina semiconstricta attempts were made to uncover evi- dence of change within the species with time. There seems to be a trend toward increase in the test diameter with decreasing geologic age. The Devonian beds were found to yield the smallest known tests of J. semiconstricta; the largest recorded tests of the species are found in the Pennsylvanian. Within the Mississippian sequence, the Chesterian J. semiconstricta are the smallest, with the Kinder- hookian next largest and the Osagian forms still larger, but smaller than the Pennsylvanian forms. The small average size of the Chester- 292 BULLETIN 196 ian specimens presents the exception to the gradual increase in size, and may be the result of insufficient sampling of Chesterian beds; the Chesterian beds sampled in this study yielded few smaller Foraminifera. As regards the number of whorls per test, the Pennsylvanian forms possess the largest number (as many as 10 whorls). In the Mississippian materials studied, the Kinderhookian forms of Jn- volutina semiconstricta have the greatest number of whorls (up to eight ); this number of whorls is comparable to that which I observed in medium-sized specimens of J. semiconstricta from Plummer’s Pennsylvanian material. The Chesterian forms possess the least number of whorls (up to 5) while the Osagian and Devonian forms possess less (up to 6% and 7) than the Kinderhookian forms, but more than the Chesterian forms. . Stratigraphic occurrence—lInvolutina semiconstricta has a rather wide stratigraphic distribution in the North American Upper Paleozoic sequence. The species was first described from the Pennsyl- vanian of Oklahoma (Waters, 1927); Plummer (1945) reported the species from the Pennsylvanian of Texas; Gutschick and Treck- man (1959) found it in the Kinderhookian Rockford limestone of northern Indiana. Involutina semiconstricta is herein recognized from Upper De- vonian, Kinderhookian, Osagian, and Chesterian beds. It is especially abundant in the Kinderhookian and lower Osagian beds. The highest known Osagian examples of /. semiconstricta are in the fine-grained, olivesgray shale streaks in the Black Hand sandstone of Ohio. No Meramecian forms were found. (See Charts 3-14 and 16-23 for de- tails of occurrence. ) Ecology.—Involutina semiconstricta is recorded dominantly from soft, fine-grained, plastic shales which have fine to medium- sized silt grains; these beds usually have a paucity of marine mega- fossils. J. semiconstricta is in some instances (as in the Bedford shale) found in association with carbonaceous matter and chitinized land spores of the genus 7'asmanites and other spores, J. semicon- stricta is also known to the writer from the semilithographic lime- stone of the Louisiana limestone at Louisiana, Missouri. Thus, it seems well established that the species “preferred” fine-grained sedi- ments. MISsSISSIPPIAN SMALLER FORAMINIFERA: CONKIN 293 The variation in the composition of the agglutinated test is be- lieved to be due to ecological conditions present on the sea bottom at the time of deposition of the sediments. For example, in the Up- per Devonian part of the New Albany shale of Kentucky, the Eulie shale (New Albany equivalent) of Tennessee, the Kinderhookian Rockford limestone and Jacobs Chapel shale of southern Indiana, the Bedford and Sunbury shales of eastern Kentucky, the basal few feet of the Osagian Henley shale of Ohio, and the shale in the Black Hand sandstone of Ohio, /nvolutina semiconstricta is present in the form of Variant 1, a clear and glossy test with a great proportion of cement and little agglutinated material. In these aforementioned sediments only small amounts of small grain-sized material are available for building an agglutinate test. For these reasons, the cement secreted by the protoplasm makes up most of the test, thus producing a depauperate skeleton. Two specimens of Variant | were also recovered from the dark, soft shales of the Chesterian Kinkaid formation. In a study of the Upper Pennsylvanian (Virgilian) microfauna of the Deer Creek formation of Kansas and northern Oklahoma, Involutina semiconstricta was the only species of Foraminifera found in the strictly black fissile shale member (Larsh-Burroak shale ) (Conkin, B., 1954, p. 16); these black shales in the Pennsylvanian cyclothems are seemingly similar lithologically to the Devonian black shales. The occurrence of Involutina semiconstricta in the Mid-Con- tinent Pennsylvanian black shales and in the small gray-green shale lenses within the Devonian “Black shale” demonstrates the ability of this species to live under unfavorable environmental conditions. Reducing conditions, low pH (with consequent unavailability of calcareous and ferruginous-calcareous salts for cementation of aren- aceous grains to make an agglutinate test) would militate against support of all life except the most hardy and unspecialized forms (or forms particularly specialized to live in stagnant reducing con- ditions ). In more arenaceous beds and in better aerated waters, such as those found in the Osagian, the tests of Jnvolutina semiconstricta are found to be more robust, to have a more granular appearance, 294 BuLLETIN 196 and to have a smaller percentage of cement compared to arenaceous material. Thus, the occurrence of /nvolutina semiconstricta in various kinds of sediments (fissile black shale; sublithographic limestone; green gray, blue gray, and buff plastic shales; gray and spore-bearing carbonaceous shales; silty shales; and soft, plastic, green-gray shales within black fissile shales) demonstrates eloquently the versatility of the species in adapting to various ecological conditions existent in diverse sites of sedimentary deposition. The more conservative, the more unspecialized nature of the species would also account for the geologic longevity of 7. semiconstricta. Table 30. Measurements of Involutina semiconstricta (Waters), 1927, in mm. locality number, specimen and max. thick- no.of diam.of formation, and type number diam. ness whorls proloc. bed number PI 225 tie Si .090 5 .021 K-23, Paint Creek, bed 1 Pla 22 tise 420 033 8 .016 I-4, Jacobs Chapel, bed 1 PliZ6; itl 2 0 .330 -067 6 .016 I-4, Rockford, bed 2 PIS 22 tice 5 D2 .033 6.5 .016 T-2, Eulie, bed 2 Table 31. Range in measurements of 21 specimens of Involutina semiconstricta (Waters), 1927, in mm. Present specimens Pennsylvanian forms Maximum diameter .210-.594 .393-1.525 Thickness -017-.101 -059-.166 No. of whorls 3-8 5-10 Diam. of proloculus .008-.050 -008-.055 Genus GLOMOSPIRA Rzehak, 1888 Trochammina Jones and Parker, 1880, (pars), Quart. Jour. Geol. Soc., v. 61, p. 304. Glomospira Rzehak, 1888. Verb. k.k. Geol. Reichs.. p. 191; Cushman, 1928, Cushman Lab. Foram. Research, Special Publ. No. 1, p. 102. Gordiammina Rhumbler, 1895, Nachr. Ges. Wiss. Gottingen, p. 84. Type species, Trochammina gordialis Jones and Parker, 1860 (monotypic genus). Cushman’s (1948, p. 96) generic definition of Glomospira fol- lows: Test free, with a proloculum and long, tubular, undivided, second chamber MISSISSIPPIAN SMALLER FORAMINIFERA: CONKIN 295 winding about its earlier coils in various planes; wall arenaceous with much cement; aperture at the end of the tube. All specimens studied in this paper were composed of quartz grains in insoluble silica cement. Chart 23 shows the range of Glomospira in the Mississippian as determined in this study. Glomospira articulosa Plummer, 1945 1 EAs PAR pkey aD) IPAL, BAT, sealer, ILS Jeiee alr Glomospira articulosa Plummer, 1945, Univ. Texas, Pub. 4401, p. 233, pl. 16, figs. 21-25; Ireland, 1956, Jour. Paleont., vol. 30, No. 4, p. 847, text- fig. 4, figs. 7-10; Gutschick and Treckman, 1959, Jour. Paleont., vol. 33, No. 2, pp. 242, 243, pl. 35, figs. 17-19. Description —Test consists of a proloculus (usually not visible ) and a gradually expanding tubular second chamber which coils around itself in a haphazard manner so as to form a tightly wound knot of varying, but always compact, shape; aperture at open end of tube; wall fine grained with siliceous grains in siliceous cement; color of wall, white to gray to yellow gray. Measurements —See Table 32 for measurements of Glomospira articulosa. Comparison and affimties—Because of variability within the species no two specimens look exactly alike; however, the present specimens are conspecific with the specimens figured by Plummer (1945, p. 233) and by Gutschick and Treckman (1959, pp. 242, 243). The present examples of Glomospira articulosa are in general of the same size as those figured by Gutschick and Treckman (1959) and by Plummer (1945), but a few specimens are larger than most members of the species; Ireland’s (1956, text-fig. 4-7-10) figured specimens are generally smaller. Stratigraphic occurrence —Glomospira articulosa was recorded by Plummer (1945, p. 233) from the Lower and Middle Pennsyl- vanian of Texas; the species was reported from the Upper Pennsyl- vanian of Kansas by Ireland (1956, p. 847). Gutschick and Treck- man (1959, p. 242, 243) reported the species from the Rockford limestone of northern Indiana. In the present work, Glomospira articulosa was found in the 296 BULLETIN 196 Kinderhookian and Osagian beds, but not stratigraphically above them. (See Charts 4, 6, 9-13, 16 and 18-22 for details of stratigraphic occurrence. ) Ecology.—Glomospira articulosa occurs in the Mississippian of the studied region primarily in clayey, plastic shales without signifi- cant carbonates. However, G. articulosa was adapted to live in the calcareous mud environment that existed on the sea bottom during deposition of the Rockford limestone. The possibility of the Rock- ford limestone having been deposited in a lagoon is discussed in the section on Hyperammina rockfordensts. Cushman noted (1928, p. 102) that Recent species most com- monly occur in cool water. Perhaps the shape (coiled like a ball of twine, the “Gordian Knot” of Plummer, 1945) was an adaptation (mot in Lamarckian sense) which afforded considerably more strength and resistance to breaking of the test in moderately agitated waters. Table 32. Measurements of Glomospira articulosa Plummer, 1945, in mm. locality number, specimen and max.diam. max.diam. formation, and bed type number of test of tube number PAR AYA saves 10 520 150 K-23, New Providence, bed 3 Pla 27, figs 1 470 200 O-7, Cuyahoga, bed 4 16 specimens .310-.806 .080-.370 Genus LITUOTUBA Rhumbler, 1895 Lituotuba Rhumbler, 1895, Nachr. Kongl. Gesell. Wiss. Gottingen, p. 83. Trochammina Brady, 1879, Quart. Jour. Micros. Sci., (N.S.), vol. 19, p. 59, ple, shies 6: Type species, Trochammina lituiformis H. B. Brady, 1897 (designated by Cushman, 1910). Rhumbler’s (1895, pp. 83, 84) description of the genus Litwo- tuba follows: Ich vereinige in diesem Genus alle diejenigen biformen Arten der von Butschle und Neuwage schon als chaotisch erkannter Ordnung Trochammina, deren Anfang spiral eingerollt, deren Ende aber noch gerade gerstrecht ist. Hierher also; Lituotuba (Trochammina) filum Schmid; Lituotuba centrifuga (Brady); L. lituiformis (Brady). Fossil in Kohlenkalk. Chart 23 shows the stratigraphic range of Litwotuba in the Mississippian of the studied area. MIssISsIPPIAN SMALLER FORAMINIFERA: CONKIN 297 Lituotuba semiplana, new species IPL Ope salary lik Tas JPAle 727s sess DAS Rite, TES Description.—Test free, consisting of a spherical proloculus and tubular undivided second chamber which coils in nearly the same plane for 2% to 2% whorls, then uncoils and becomes rectilinear, with the rectilinear portion in nearly the same plane and directed at right angles to the preceding part of the second chamber; aper- ture circular, somewhat constricted; wall of second chamber with slight constrictions externally; wall of fine siliceous grains in siliceous cement; color white to gray. Measurements—See Table 33 for measurements of Litwotuwba semtplana and comparison with L. exserta Moreman, 1930. Comparison and affinities —Lituotuba semiplana has close af- finities to L. exserta Moreman, 1930 but differs from L. exserta in having (1) nearly planispiral coils, (2) lesser number of whorls (about 2% in L. semiplana, but 4 to 5 in L. exserta), (3) slight ex- ternal constrictions, and (4) smaller size. Type locality —North of Garrett Creek Church, north of West- moreland, Sumner County, Tennessee (Locality T-2). The holotype is from the Eulie shale (Bed 4). Table 33. Measurements of Lituwotuba semiplana, n. sp., in mm. and comparison with L. exserta Moreman, 1930 diam. max. length max. max. min. diam. of diam. of diam. diam. diam. of specimen and proloc. of test of of of aperture type number tube test neck neck RleZ2 ates Li: .02 .08 .269 .20 08 .07 .03 holotype Pl. 22, fig. 12 03 07 290 20 10 06 03 IEA, te 05 .07 .290 24 10 07 03 L. exserta 34- 48 Stratigraphic occurrence. — Lituotuba semiplana has been re- covered from the Kinderhookian Eulie shale of Tennessee (Locality T-2, Bed 4) and the lower Osagian New Providence formation in Kentucky (Locality K-52, Bed 8; Locality K-6, Bed 2). Ecology. — Lituotuba semiplana occurs in the noncalcareous parts of the Eulie and lower New Providence shales, where inverte- brate megafossil assemblages are absent. The species required a sediment with fine siliceous grains with which to construct its test. 298 BULLETIN 196 Subfamily TOLYPAMMININAE Genus TOLYPAMMINA Rhumbler, 1895 Hyperammina Brady, 1879, (pars), Quart. Jour. Micr. Sci., vol. 19, p. 33; idem, 1884, (pars), Rept. Voyage Challenger, Zool., v. 9, pp. 260, 261. Tolypammina Rhumbler, 1895, Nachr. Kon. Ges. Wiss. G6ttingen, p. 83; Cushman, 1910, United States Nat. Mus., Bull. 71, p. 66; idem, 1928, The Foraminifera, Cambridge, p. 98. Serpulella Eimer and Fickert, 1899, Zeitschr. Wiss. Zool., vol. 65, p. 674. Type species, Hyperammina vagans Brady, 1879 (original designation, by Rhumbler, 1895, p. 83). Description—Rhumbler’s (1895, p. 83) original description of Zolypammina follows the definition of his subfamily Girvanellinae (now obsolete ): Gehause mehr oder weniger festgewachsen, mit kugliger oder ovaler Anfangskammer, sonst eine gleich weite ROhre darstelland, welche sich in unregelmassigen Hin-und Herwindungen aufknauelt. The generic definition of T’olypammina as given by Cushman (1910, p. 66) follows: Test typically adherent by its under surface, but may become free, con- sisting of an elongate oval proloculum and a long irregular tube, unbranched, composed of sand grains and reddish brown cement. There has been some doubt as to the relationship between Toly- pammina and Ammovertella. The salient generic characteristics of the two genera have been critically reviewed and commented upon by Ireland (1956, p. 838): The test of Tolypammina is generally a free tube circular in cross-section and attached only in the initial stage and at various points in the later stage where support of the long tube is needed. Growth of the tube is always in random directions. The lower wall of the tube, where attached, is generally of agglutinated particles, though in some cases the surface of the object of attachment is used as part of the lower wall. The initial stage may be straight, slightly coiled, or with one or two whorls . . . Ammovertella is generally attached throughout the length of the tube, but the terminal portion may be unattached and circular in outline. Growth from the proloculus is sinuous, back and forth in a plane with test generally enlarging in the same direction. In the final stage the tube may make a partial or complete encirclement of the early portion of the test. A lower wall is not found because the surface of attachment serves as the bottom of the test; and the cross-section of the tube is semi-circular, flat on the bottom and convex on top. Tubes bent back over the top of the test use the older portions of the tube as a bottom surface. Ireland apparently overlooked that part of Cushman’s de- scription of Ammovertella (1928, p. 98) in which the early plani- MISsSISSIPPIAN SMALLER FORAMINIFERA: CONKIN 299 spiral portion of the tube is mentioned. Thus, like Tolypammuna, Ammovertella may or may not be planispirally coiled initially. Generic differentiation between Tolypammina and Ammover- tella usually has been made upon the basis of summation and analysis of the nature of: (1) attachment (or nonattachment or degree of attachment), (2) winding of the second chamber, (3) presence or absence of lower wall (and method of construction), and (4) cross- sectional shape of the proloculus and second chamber; nevertheless, there are instances of gradation between the two genera, and in some cases it has been difficult to make generic allocation of doubt- ful species. Gutschick and Treckman (1959, p. 241) recognized the prob- lems involved in differentiation of species of Tolypammina and Am- movertella as follows: We are following the diagnosis outlined by Ireland (1956, p. 838) for the characteristics of this genus [Tolypammina]. It must be recognized that such vermicular adnascent tests show great variation which makes it difficult taxo- nomically. We find that some Rockford tolypamminids contradict some of Ireland’s criteria for distinguishing between Tolypammina and Ammovertella. The semi-circular cross-section of the tube is like Ammovertella; the presence of an agglutinate floor wall is like Tolypammina. Coiling in the early stages is characteristic of Tolypammina; [Here, as Ireland, Gutschick and Treckman make no mention of the planispiral nature of the early portion of Ammovertella as originally described by Cushman] however when the forms have one or two whorls in the early stage, a semi-circular second chamber, and may or may not have a wall along the surface of attachment, it is difficult to decide to which genus they belong. The attached tests, early development of coiling, and the late uncoiling into simple tube, not writhing, seems to favor their assignment with Tolypammina. A practical method, and I believe the best means, of differentia- tion between T'olypammina and Ammovertella is offered here, The basis for generic differentiation lies primarily in the configuration of the second chamber with other characters considered of secondary significance. The second chamber of Tolypammina is sinuous and tortuous but does not wind in the same general plane, and the windings of the second chamber do not fuse into a planoconvex unit. Tolypam- mina is more or less free of attachment, with the tubular second chamber rounded in cross-section where free, and semicircular in cross-section where attached. In contrast to Tolypammina, Ammovertella exhibits a sinuous, tortuous, (back and forth) maze of windings of the second chamber 300 BULLETIN 196 in the same general plane; this maze of windings is fused into a planoconvex unit. The floor of the test (if present) is more or less flat, depending on the nature of the surface to which it is attached; the sides and top of the test are convex. The latter portion of the second chamber may utilize the earlier portions as bases for at- tachment. in summary then, the principle generic characteristic of Am- movertella is considered to ‘be the winding back and forth of the second chamber in the same general plane with the fusion of the winding tube into a planoconvex unit; initial portion of the tube may be planispiral. Inasmuch as little is known concerning the test wall of are- naceous Foraminifera, I am unwilling to undertake a detailed specu- lation on the original wall composition of Paleozoic Tolypammuina and Ammovertella. The present specimens are arenaceous, consist- ing of siliceous grains in siliceous cement (regardless of original composition). A more or less detailed consideration of the original wall composition and structure would follow the lines of the dis- cussions of wall composition and structure of Hyperammina (Conkin, 1954; Cummings, 1955; and Conkin, 1956); such course, at present state of knowledge of wall structure of Paleozoic Foraminifera, most likely would be unfruitful. Chart 23 shows the stratigraphic range of Tolypammina in the Mississippian as determined in this study. Lolypammina botonuneus Gutschick and Treckman, 1959 1d AS elle AS levee 24! Tolypammina botonuncus Gutschick and Treckman, 1959, Jour. Paleont., VOL S35 NOs Zaps 245. plessOsrlo silo) los Description—Test attached, consisting of a bulbous proloculus, followed by a tubular, undivided, second chamber (with a thin floor wall); second chamber coils around and closely embraces the pro- loculus for about 3/4 whorl, then narrows and bends almost at a right angle, then finally uncoils to form a straight tube which expands gradually; proloculus only moderately elevated above the level of the 3/4 planispiral whorl of the second chamber; cross- section of the second chamber rather triangular (controlled by MISSISSIPPIAN SMALLER FORAMINIFERA: CONKIN 301 mode of attachment); wall finely arenaceous with siliceous silt in siliceous cement (regardless of original composition of the test wall); color of test, gray to white-gray. Measurements—See Table 34 for measurements of present specimen of Tolypammina botonuncus and comparison with Gut- schick and Treckman’s types of the species. Comparison and affinities—Gutschick and Treckman (1959, p. 245) discussed the species Tolypammuna botonuncus: The species is characterized by its button-hook shape with less than one whorl of the second chamber, constrictions at the bend, and linear portion of the mature part of the test. It is similar to Tolypammina cyclops, n. sp., but does not have the complete coil around the proloculus, is smaller, and more unidirectional. The present specimen compares well with the orginal descrip- tion of the species by Gutschick and Treckman, the only differences noted were that the present hypotype has generally smaller size, less height to the proloculus (not projecting much above the level of the 3/4 planispiral whorl), a triangular cross-section of the second chamber, and a small irregular wedging to the second chamber. Stratigraphic occurrence.—T olypammuna botonuncus is recorded only from the Kinderhookian Rockford limestone of northern Indi- ana (Gutschick and Treckman, 1959, p. 245) and in this study from the Rockford limestone of southern Indiana (Locality I-4, Bed 2). Ecology.—Apparently Tolypammina botonuncus had much the same ecological requirements as the other species of Tolypammuna. Remarks——Only one specimen of this species was found in this study. Tolypammina cyclops Gutschick and Treckman, 1959 PI. 22, figs. 14, 15; 12d Att iat, Be adales, Why Tolypammina cyclops Gutschick and Treckman, 1959, Jour. Paleont., vol. 33, No. 2, pp. 245, 246, pl. 36, figs. 1, 2, 4, 6, 7, 10-14. Description.—Test attached, composed of a spherical proloculus and a tubular second chamber, semicircular in cross-section; second chamber coils a little more than one time around the proloculus be- fore uncoiling; uncoiled portion describes a sinuous path; height 302 BULLETIN 196 of proloculus greater than the second chamber and projects above the level of the coiled portion; second chamber partially floored with a thin layer of arenaceous material of siliceous grains in siliceous cement; wall of test composed of siliceous grains in siliceous cement; color of test, white to light gray. Measurements—See Table 35 for measurements of hypotypes of Tolypammuna cyclops. Comparison and affinities—The three present measured speci- mens closely resemble Gutschick and Treckman’s species and two of them fit well within the range of measurements given for the types of Tolypammina cyclops. The third specimen of the present material however, is much larger than those figured by Gutschick and Treck- man (1959, pl. 36, figs. 1, 2, 4, 6, 7). The figures 10-14 on plate 36 of Gutschick and Treckman are of large size; nevertheless, the third specimen of the present material is still larger. Stratigraphic occurrence.—T olypammina cyclops was originally described from the Rockford limestone of northern Indiana. 7. cyclops was found sparingly in the Rockford limestone and Jacobs Chapel shale in southern Indiana, and in the lower New Providence and Cuyahoga formations. (See Charts 3-5, 10-12, 21, and 22 for details of occurrence. ) Table 34. Measurements of 7'olypammina botonuncus Gutschick and Treckman 1959, in mm. and comparison with holotype and paratype PI; 22, fig. 13 Holotype Paratype Length of test 1.02 85 1.20 Diam. of proloculus sz 35 14 Diam. of whorl 18 24 22 Min. diam. of tube 07 08 08 Max. diam. of tube 16 14 13 Table 35. Measurements of Tolypammina cyclops Gutschick and Treckman, 1959, in mm. diam. length diam. diam. of of of of locality number, specimen and proloc. test coiled end of formation, and type number portion tube hed number Pie s2/ee tious 084 403 .168 .092 I-4, Rockford, bed 2 Pli22 tical: 101 =1.450 252 15 I-4, Rockford, bed 2 Pi 22 tices 235 .692 .570 .252 I-4, Jacobs Chapel, bed 1 MISSISSIPPIAN SMALLER FORAMINIFERA: CONKIN 303 Ecology.—This species undoubtedly had much the same eco- logical requirements as 7'olypammuna jacobschapelensis. Tolypammina jacobschapelensis, new species Pl. 22, figs. 16-21; Tell, PAG sues 5 Lele 28 Description—Test consists of an attached proloculus and a second chamber in the form of a long, aimlessly sinuous tube, semi- circular in cross-section, and attached throughout its length, or be- coming unattached near its end; proloculus in the shape of half an egg and usually somewhat pointed at the initial larger end, though in some instances the initial end is rounded; apertural end broken off all specimens; the surface of attachment of the proloculus and the tubular second chamber may be partially or entirely covered with a thin floor, or the floor may be absent altogether; tube usually enlarges gradually but may maintain its initial diameter which is from about one-half to three-fourths the diameter of the proloculus, or rarely the tube may diminish in diameter; wall finely granular, composed of quartz grains in siliceous cement; color of test white, rarely reddish-orange. Measurements—Measurements of Tolypammuina jacobschapel- ensis are given in Table 36, and the range in the measurements of this new species and comparison with 7’. cyclops are given in Table a: Comparison and affinities —Tolypammina jacobschapelensts is somewhat similar to 7. cyclops Gutschick and Treckman, 1959, from the Rockford limestone of northern Indiana, but the second chamber of T. jacobschapelensis does not coil around the proloculus, and the proloculus of 7. jacobschapelensis is usually pointed at its tip rather than being completely spherical; furthermore, the proloculus of 7. jacobschapelensts is attached, while that of 7. cyclops is unattached. Type locality —Campbell’s (1946, p. 856) type locality for the Jacobs Chapel shale, one mile west of Jacobs Chapel, Clark County, Indiana (Locality I-4). The holotype and paratypes are from the Rockford limestone (Bed 2). Stratigraphic occurrence.—T olypammina jacobschapelensis has been found only in the Rockford limestone in southern Indiana and in the lower New Providence formation in northwestern Kentucky. (See Charts 3, 4, 11, 12, and 22 for details of occurrence. ) 304 BULLETIN 196 Table 36. Measurements of Tolypammina jacobschapelensis, n. sp., In mm. diam. of diam. length specimen and diam.of length of tube near of end of type number proloculus proloculus proloculus of tube test Plie22 tipss 084 101 .050 2 2.000 jel, Weavers ly “Sul 185 .084 .134 1.500 Pie 22 5 ties 16 134 .201 101 .193 1.500 holotype PIS 22 shies 20 .269 .285 118 .134 -800 Pla 22enie 2 252 386 .201 285 2.100 Pl. 27, fig. 5 .134 .193 .088 Sit 950 Pl. 22, fig. 19 193 201 101 151 650 Table 37. Range in measurements of 22 specimens of Tolypammina jacobschapelensis, n. sp., in mm. and comparison with T. cyclops Gutschick and Treckman, 1959 T. jacobschapelensis T. cyclops Diameter of proloculus .084-.269 .075-.150 Length of proloculus .101-.285 .09-.15 Diam. of tube near proloc. -050-.201 — Diam. of end of tube .084-.285 .06-.20 Length of test up to 2.10 up to ca. 2.0 Ecology—The environment of deposition of the sediments of the Rockford limestone is discussed in the present work under the ecological portion of Hyperammuina rockfordensts. The Jacobs Chapel calcareous shale bears a diminutive macro- fauna of rather varied groups of organisms, including microblastoids, brachiopods, and snails; however, the ostracodes and Foraminifera do not show signs of “dwarfing”. Both the Rockford limestone and the Jacobs Chapel shale have diminutive faunal elements which are reminiscent of the “dwarf” macrofauna of the Louisiana limestone of Missouri; thus, it seems clear that the Rockford limestone and Jacobs Chapel shale present evidence of somewhat restricted environmental conditions of deposi- tion, perhaps sedimentation in calcareous muddy lagoons, or deposi- tional sites closely associated with such lagoons. In lagoonal environ- ments, water depth would be shallow and the water should be slightly agitated. The land close at hand could act as a source for the green phosphatic substance which mottles the Rockford lime- stone. MIsSISSIPPIAN SMALLER FORAMINIFERA: CONKIN 305 I have observed that Mississippian species of TJ olypammina are found mostly in dense (fine-grained to semilithographic) lime- stones, sometimes associated with algal limestones. In some beds, such as the Greenbrier limestone of West Vir- ginia, Tolypammina is present almost to the exclusion of other Foraminifera and thus presumedly was able to live under environ- mental conditions unfavorable to other Foraminifera. Only one other genus of Foraminifera, Climacammina, has been reported from the Greenbrier limestone of West Virginia (Flowers, 1956, p. 10). Near White Sulphur Springs, Greenbrier County, West Virginia, I collected Tolypammina in abundance from dense limestone in the upper and middle parts of the Greenbrier limestone. The association of Tolypammina at this locality with well-preserved dasycladacean algae is proof of shallow water, Odlites are abundantly present which indicates at least slightly agitated water. It follows necessarily from the limestone lithology of odlites and the green calcareous algae, that the sea water was alkaline and supersaturated with calcium bicarbonate. The mostly attached and encrusting nature of the Tolypammuina may account for the ability of such animals with seemingly deli- cate, sinuous, long, and tubular tests to maintain themselves in shallow, somewhat agitated water. Tolypammina is thus seen to be characteristically associated with calcareous shales and argillaceous limestones, in near shore warm waters of shallow depth. The associated diminutive faunal elements lend evidence for a somewhat restricted environment, not promoting development of macrofossil assemblages of robust or even normal-sized individuals; the depositional site may have been a lagoonal or shoal area. Remarks —This new species is named for the type locality of the Jacobs Chapel shale and thus is based on a geographic name. Tolypammina laocoon, new species Pl, 22, fic. 23:5 Mics 26 Description—Test free in its early portion, consisting of a large spherical proloculus followed by a tortuously coiled, glomo- spiroid, undivided, rather tightly embracing, second tubular chamber; the coiling in the holotype is in this manner: from the proloculus the second chamber describes a small and tight U-shaped loop 306 BULLETIN 196 which turns back toward the proloculus and passes beneath the proloculus and a part of the U-shaped loop; the second chamber then continues in a tight coil around the proloculus for the distance of one whorl (nearly planispirally coiled), the first formed loop being used as part of the attachment; the loop and end of the spiral chamber are in, or nearly in, conjunction one with another; the coil then abruptly bends downward and progresses to the other side of the test (or left), then continues across the diameter of the cross-section of test; the remaining portion of the second cham- ber then abruptly bends downward and finally turns upward to form a gradually enlarging linear and rounded tube; test rather robust; test wall finely arenaceous, of siliceous grains in siliceous cement (regardless of original composition); apertural end of tube broken off; color of wall, white to gray-white. Measurements —See Yable 38 for measurements of T'olypam- mina laocoon. Table 38, Measurements of 7'olypammuina laocoon, n. sp., in mm. Pl. 22, fig. 23, holotype Length of test .76 Diam. of proloculus 10 Diam. of coiled portion 23 Length of coiled portion Yi Min. diam. of tube .08 Max. diam. of tube als Comparison and affinities —Tolypammina laocoon has no close affinities to any know Tolypammina. Although superficially some- what similar to 7. botonuncus, T. laocoon differs from T. botonwn- cus in that it: (1) is free (unattached) in early portion, (2) has a rounded tubular second chamber, and (3) has a glomospiroid con- figuration in the initial portion of the second chamber. Type locality —Jacobs Chapel, southern Indiana (Locality I-4); type locality for Jacobs Chapel shale; holotype is from the Rockford limestone (Bed 2). Stratigraphic occurrence—Tolypammina laocoon is recorded only from the Rockford limestone. Ecology.—Tolypammina laocoon apparently “preferred” fine- grained shales and calcareous muds. The tortuously coiled earlier portion of the test may have been an adaptation to strengthen the MISSISSIPPIAN SMALLER FORAMINIFERA: CONKIN 307 test and may have acted as a substitute for the Selly of a more attached living habit. Remarks —Tolypammina laocoon is named because of the serpentine-like coiling of the early portion of the second chamber. Tolypammina tortuosa Dunn, 1942 Pl. 22, fig. 22; JEG AG, Wale G28 Malas PAT) Tolypammina tortuosa Dunn, 1942, Jour. Paleont., vol. 16, No. 3, p. 341, pl. 4, figs. 19-21, 32. Description—Test mostly attached (some portions are free and are rounded and tubular); proloculus large, elevated above height of second chamber; proloculus is surrounded by the second chamber for three-fourths of a whorl, then the second chamber coils and bends in a tortuous manner, not always in the same plane; test generally with a floor wall, occasionally not; tubes often crowded and some- what intertwined; the overall shape of the test is determined by the mode of attachment; test wall of fine siliceous grains in siliceous cement; color of test, white. Measurements—See Table 39 for measurements of T'olypam- mina tortuosa. Comparison and affimties—The present specimens seem to be conspecific with Tolypammina tortuosa Dunn, 1942, from the Silur- ian Brassfield limestone of Missouri. Table 39. Measurements of Tolypammina tortuosa Dunn, 1942, in mm. locality number, Specimen and diam. of min. diam. max. diam. formation, and type number proloculus of tube of tube bed number unfigured .07 .10 ziL5 I-4, Rockford, specimen bed 2 BIN 22s ties 22 .08 05 siz! I-4, Rockford, bed 2 Stratigraphic occurrence.—T olypammina tortuosa is known to occur in the Middle Silurian and the Lower Mississippian. The species was found in the Kinderhookian Rockford limestone (Bed 2) at Jacobs Chapel, Indiana, (Locality I-4) and in the Eulie shale (Bed 2) near Westmoreland, northern Tennessee, (Locality T-2). 308 BULLETIN 196 Ecology—Tolypammina tortuosa undoubtedly lived in much the same environment as did the other tolypamminids. Remarks.—Five specimens of the species were recovered. Genus AMMOVERTELLA Cushman, 1928 Psammophis Schellwien, 1895, Palaeontographia, vol. 44, pts. 5, 6, p. 265. (non Psammophis Boie, 1827, fide Cushman, 1948, Foraminfera, Cambridge, DoS) Ammovertella Cushman, 1928, Cushman Lab. Foram. Research, Contr., vol. 4, p. 8; idem, 1948, Foraminifera, Cambridge, p. 98. Type species, Psammophis inversa Schellwien, 1898. Description —tThe generic definition of Ammovertella was given by Cushman (1948, p. 98): Test attached, with proloculus and long, tubular second chamber, early portion planispiral, later and larger portion bending back and forth but progressing forward in one general direction; wall clearly arenaceous with much cement; aperture at end of the tube.—Pennsylvanian to Recent. Schellwien proved the arenaceous character of the wall by test with polarized light. The salient features of the genus Ammovertella as I conceive of them have already been given in the section devoted to the genus Tolypammina. A summary of the generic characters of Ammovertella will suffice here: Ammovertella presents a sinuous, tortuous (back and forth) maze of windings of the second chamber in the same general plane; this maze of windings is fused into a planoconvex mass. The floor of the test (if present) is more or less flat; the sides and top of the test are convex. The later portion of the second chamber may utilize the earlier portions as bases for attachment. The initial portion of the second chamber may or may not form itself into one or a few planispiral coils, In essence then, the princi- pal generic character of Ammovertella is considered to be the winding back and forth of the second chamber in the same general plane with fusion of the winding tube into a planoconvex mass. All tests of Ammovertella in the present material are composed of siliceous grains in siliceous cement (regardless of original wall composition ). Chart 23 shows the range of Ammovertella in the Mississippian as determined in this study. MISSISSIPPIAN SMALLER FORAMINIFERA: CONKIN 309 Ammovertella cf. A. inelusa (Cushman and Waters), 1927 Pl. 23, fig. 8; Pl. 27, figs. 6-9; Fig. 29 Psammophis inclusa Cushman and Waters, 1927, Cushman Lab. Foram. Re- search, Contr., vol. 3, p. 148, pl. 26, fig. 12. Ammovertella inclusa (Cushman and Waters), 1930, Univ. Texas, Bull. 3019, pp. 44, 45, pl. 7, fig. 13; Ireland, 1956, (pars), Jour. Paleont., vol. 30, No. 4, pp. 853, 854, text-fig. 5-12. (non Ammovertella inclusa [Cushman and Waters], Ireland, 1956, Jour. Paleont., vol. 30, No. 4, pp. 853, 854, text- fie 56-1 13,, 14), Description—Test attached, consisting of a proloculus and a gradually expanding tubular second chamber which is planispirally coiled for one or two volutions in the present specimens, then me- anders in the same general plane back and forth and partially em- braces the coiled portion; in some specimens the tube laps back on top of previous portions of the test; cross-section of tube semicir- cular; tubular portion fused together to form a planoconvex mass; wall of test composed of fine siliceous grains in siliceous cement; color of wall, white to gray to yellowish gray. Measurements—Vable 40 gives measurements of Ammovertella cf. A. inclusa; Table 41 gives the range in measurements of the spe- cies and the measurements of Cushman and Waters’ holotype. Comparison and affinities—TVhe present specimens are only compared to Ammovertella inclusa inasmuch as the illustration given by Cushman and Waters (1930, pl. 7, fig. 13) shows only the upper convex side of the test; however, Cushman and Waters’ description of the test allows comparison of the present material with A. inclusa. The form which Ireland described (1956, pp. 853, 854, text-fig. 5— 6-11, 13, 14) as Ammovertella inclusa does not seem to be con- specific with A. zmclusa inasmuch as Ireland’s specimens apparently lack the planispirally coiled early portion of the second chamber; only one figure (text-fig. 5— 12b) shows a planispiral coil, In other respects these forms closely resemble the figure of the holotype of A. inclusa. Stratigraphic occurrence —Cushman and Waters (1930, pp. 44, 45, pl. 7, fig. 13) described Ammovertella inclusa from the Upper Pennsylvanian of Texas. Ireland (1956, pp. 853, 854, text-fig. 5— 12) reported the species from the Upper Pennsylvanian of Kansas. The present specimens were found as rather scattered occur- rences from the Bedford shale to the lower part of the Brodhead 310 BULLETIN 196 formation. (See Charts 3, 4, 6, 9-13, 16, 18, 19, 21, and 22 for details of occurrence. ) Ecology—Ammovertella cf. A. inclusa is recorded in this work only in soft, blue-gray to olive-gray, plastic when wet shales which contain fine-grained silt, and are in instances, calcareous with well- developed megafossil faunas (such as the Button Mold Knob mem- ber of the New Providence formation which carries the Button Mold Knob fauna). No specimens of Ammovertella have been observed in strictly siltstone or sandstone beds in the studied area. Thus, it seems that Ammovertella cf. A. inclusa, and probably Ammovertella in general, “preferred” a soft, muddy sea bottom. This species could live in calcareous or noncalcareous sediments, with or without a well- developed megafauna. Where megafaunas were present, the species would utilize the living organisms or hard fragmental parts of dead organisms as objects of attachment. The habit of attachment may have been an adaptation to an agitated environment of deposition. A moderately shallow-water en- vironment is evidenced by the association of the species with the Button Mold Knob fauna and the stratigraphic proximity of the dominantly molluscan Coral Ridge fauna. The alkalinity of the water must have been fairly high in order to allow formation of the calcareous shales and crinoidal bioherms within the Button Mold Knob member. Table 40. Measurements of Ammovertella cf. A. inclusa (Cushman and Waters), 1927, in mm. length width min. max. locality number, specimen and of of diam. diam. formation, and bed type number test test of tube of tube number Pe 235 tiles 480 440 033 .092 K-2, New Providence, bed 2 Leip nat. (6 5/4) Biss .033 101 K-2, New Providence, bed 2 PZ tlen 7, 554 420 118 K-32, New Providence, bed 2 PI 27 tigen & P5Si7, 403 033 084 K-32, New Providence, bed 2 Pl. 27, fig. 9 503 420 033 101 K-32, New Providence, bed 2 MIssISSIPPIAN SMALLER FORAMINIFERA: CONKIN bi Table 41. Range in measurements of 13 specimens of Ammovertella cf. A. inclusa (Cushman and Waters), 1927, in mm. and comparison with the holotype holotype (all but length are estimated from original figure) Length of test .302-.710 .850 Width of test .252-.453 540 Pi Min. diam. of tube .025-.033 .063 (earliest part not visible) Max. diam. of tube .067-.134 .220 Ammoyertella labyrintha Ireland, 1956 Pipe23e hics9: LENE PATS wae UNS Veniess 2Fs5 Ammovertella labyrintha Ireland, 1956, Jour. Paleont., vol. 30, p. 854, text- fi Ga I Ot Description—Test consists of a tortuous, labyrinthic maze of intertwining tubes, partially attached at the base of the fused unit to a substratum, and partially free or attached to other tubes; pres- ent specimens only fragmentary; test wall gray to dull tan. Measurements —See Table 42 for measurements of Ammover- tella labyrintha. Table 42. Measurements of Ammovertella labyrintha Ireland, 1956, in mm. Pile Zi, oye) Diam. of proloculus 084 Diam. of tube .05-.08 Diam. of test 79 Comparison and affinities—Present specimens seem to fit well the descriptions and figures given for Ammovertella labyrintha by Ireland (1956, p. 854). Stratigraphic occurrence——Ammovertella labyrintha is known to occur in the Pennsylvanian and Permian of Kansas. Herein the species is reported from the lower part of the New Providence forma- tion, 11 to 16.5 feet above the New Albany shale, near Atherton- ville, Larue County, Kentucky, (Locality K-13) and in the lower 2.5 to 5.5 feet of the New Providence formation at Fishing Creek near Somerset, Pulaski County, Kentucky, (Locality K-32). Ecology.—Apparently Ammovertella labyrintha had much the same ecological requirements as other ammovertellids. 312 BULLETIN 196 Ammovyertella cf. A. primaparya Ireland, 1956 IPTG PAG tas, WE TEAL Ath, tees, AILS Tees Bil Ammovertella primaparva Ireland, 1956, Jour. Paleont., vol. 30, No. 4, p. 834, text-fig. 6— 8-12. Description —Test attached, consisting of a tiny proloculus and a gradually expanding tubular second chamber which meanders back and forth in a plane and usually progresses roughly in the same direction; adjacent walls are fused so that the whole test forms a planoconvex mass; tube makes up to eight crossings, making four complete meanders in the present specimens; cross-section of the tube semi-circular; as noted by Ireland (1956, p. 854), the later more randomly winding portion of the second chamber is readily broken off, and it is not preserved in the present specimens; wall composed of siliceous grains in siliceous cement; color of wall, white to light yellowish-gray. Measurements—Table 43 gives the measurements of Ammover- tella cf. A. primaparva; Table 44 gives the range in measurements of A. cf. A. primaparva and measurements of Ireland’s types of the species. Comparison and affinities—The present specimens are frag- mentary, and for this reason are compared with Ammovertella primaparva; however, the specimens of this paper closely resemble text-fig. 6— 8, 9, and 11 as given by Ireland (1956). Ammovertella primaparva is similar in the meandering manner of its second chamber to the type species of Ammovertella, A. in- versa (Schellwien), 1898, but A. primaparva does not possess the planispirally coiled initial portion of the second chamber. A. prima- parva differs from A. inclusa (Cushman and Waters), 1927 in lacking the planispirally coiled early portion of the second chamber and in having the earlier portion of the test less embraced by the meander- ing of the second chamber. Stratigraphic occurrence.—Ireland (1956) described Ammover- tella primaparva from the Upper Pennsylvanian of Kansas. The present specimens are from the Kinderhookian Eulie shale of Ten- nessee and the Rockford limestone of southern Indiana, the lower part of the Osagian Henley shale member of the Cuyahoga forma- tion of Ohio, and the lower part of the Osagian New Providence MIssISSIPPIAN SMALLER FORAMINIFERA: CONKIN 313 formation of Kentucky. (See Charts 3, 4, 10, 12, 16, 21, and 22 for details of occurrence. ) Ecology —Ammovertella cf. A. primaparva likely had ecological requirements similar to those of Ammovertella cf. A. inclusa, except A. cf. A. primaparva has been found in the Rockford limestone. As discussed under Hyperammina rockfordensis and Tolypammuina jacobschapelensis, the Rockford limestone may represent deposition in a lagoonal environment. Table 43. Measurements of Ammovertella cf. A. primaparva Ireland, 1956, in mm. width length no. of min. locality number, specimen and of of cross- diam. formation, and type number test test ings of tube bed number Pl. 23, fig. 10 335 386 7 033 0-6, Henley, bed 10 Pl. 27, fig. 11 352 386 7 063 I-4, Rockford, bed 2 Table 44. Range in measurements of five specimens of Ammovertella cf. A. primaparva Ireland, 1956, and measurements of the holotype, in mm. Present specimens holotype Width of test .294-.453 .25 (lower part) Length of test .269-.386 (lower part) .60 (whole test) No. of meanders up to four three Min. diam. of tube .017-.067 .020 Genus TREPEILOPSIS Cushman and Waters, 1928 Turritellella Cushman and Waters, 1927, Cushman Lab. Foram. Research, Contr., vol. 3, p. 38. (non Turritellella Rhumbler, 1903, Archiv. Prot., vol. 3, p. 283) Trepeilopsis Cushman and Waters, 1928, Cushman Lab. Foram Research, Contr., vol. 4, p. 38. Type species, Trepeilopsis grandis (Cushman and Waters), 1928 (original designation). Cushman’s generic definition (1948, p. 99) of Trepeilopsts is as follows: Test attached to Productus spines, with a proloculus and long, tubular, second chamber, early portion spirally coiled, later bending back and making nearly a straight tube over the earlier whorls; wall finely arenaceous with much cement; aperture at the end of the tube. 314 BuLLETIN 196 There is some question as to the relationship between Trepetlop- sis Cushman and Waters, 1928, and Twrritellella Rhumbler, 1903. I would broaden the generic definition of Trepedopsis more than did Cushman and Waters. The generic definition of Trepeiopsts, as I view it, should require that species of Trepeilopsis be attached to some object, brachiopod spine, sponge spicule, or such; the final portion of the second chamber may or may not recoil backward over the earlier part of the second chamber. Turritellella would have generic characters similar to Trepeiop- sis except the test must be free (unattached) and may not have the later portion of the second chamber recoil backward over the earlier part of the second chamber, Among the trepeilopsids there are some species, such as Trepeiopsis spiralis Gutschick and Treckman which seemingly fit the generic definition of Twrritellella; however, Gutschick and Treck- man (1959, p. 244) interpret their Rockford T. spiralis as a Tre- peilopsis which was wound around a calcareous cylindrical spine which has been dissolved leaving a hollow enclosed by windings. Such solution of a calcareous spine would make the test superficially like Turritellella. It may be added here that a test in question must show definite evidence of attachment on the inner side of the second chamber or the example should not be placed in Trepeilopsts. Chart 23 shows the range of Trepeilopsis in the Mississippian as determined in this study. Trepeilopsis glomospiroides Gutschick and Treckman, 1959 edb PRY rales lp Qe il eye wie. Wei eae Bis" Trepeilopsis glomospiroides Gutschick and Treckman, 1959, Jour. Paleont., vol. 33, No. 2, pp. 243, 244, pl. 35, figs. 29-31. Description.—Test attached to a spine, spicule, or similar object; test consists of a proloculus (broken off of all present specimens ) and a gradually enlarging tubular second chamber which winds tightly and spirally around the object of attachment for about five to six coils (in present specimens) and then winds in a glomospiroid fashion over the latest coils and the end of the object of attachment; MIssISSIPPIAN SMALLER FORAMINIFERA: CONKIN 315 aperture formed by open end of tube; wall of fine siliceous silt in siliceous cement; color of wall white to yellowish-gray. Measurements—See Vable 45 for measurements of present specimens of T'repeilopsis glomospiroides and Table 46 for range in measurements of the species. Comparison and affinities—The present specimens are in gen- eral slightly smaller than Gutschick and Treckman’s types of the species but otherwise are identical with them. Stratigraphic occurrence —Trepetlopsis glomospiroides was originally described from the Rockford limestone of northern In- diana. 7. glomospiroides was found in this study to occur in the Rockford limestone of southern Indiana, the lower New Providence formation of Kentucky, and the lower Cuyahoga formation of Ohio. (See Charts 3, 9-11, 18, 21, and 22 for details of occurrence. ) Table 45. Measurements of T'repeilopsis glomospiroides Gutschick and Treckman, 1959, in mm. locality number, specimen and no.of max. formation, and bed type number length coils diam. number IPL) 2S sate I .650 7 302 K-51, New Providence, bed 6 P23 etice 2 452 7 5235 I-4, Rockford, bed 2 AL Ay sates, se 550 5 226 I-4, Rockford, bed 2 Table 46. Range in measurements of five specimens of Trepeilopsis glomospiroides Gutschick and Treckman, 1959, in mm. Length .425-.650 No. of coils 5-7 Max. diam. .218-.302 Ecology—T repeilopsis glomospiroides is known to occur only in dense (fine-grained) limestone and in fine-grained, calcareous or noncalcareous plastic shales. T. glomospiroides has not been ob- served in medium to coarse-grained limestones. It is believed that the species lived on an argillaceous or calcareous-argillaceous bottom, in quiet waters; the Rockford limestone has already been interpreted as possibly lagoonal (see discussion under Hyperammina rockford- ensis ). 316 BULLETIN 196 Trepeilopsis recurvidens Gutschick and Treckman, 1959 Ply 23, figs, 3, 47 Bl 2 ties Ace eae Trepeilopsis recurvidens Gutschick and Treckman, 1959, Jour. Paleont., vol. 33, No. 2, p. 244, pl. 35, figs. 25, 26. Description.—Test attached to a spine, spicule, or similar object; test consists of a proloculus (broken off of present specimens) and a gradually enlarging tubular second chamber which spirals tightly around the object of attachment for six to eight coils, then uncoils and turns back over the preceding coils in a broadly winding path directed toward the proloculus; aperture at open end of tube; wall finely grained, of siliceous silt in siliceous cement; color of test, light gray. Measurements—See Table 47 for measurements of T'repeilopsis recurvidens. Comparison and affinities—The present specimens closely re- semble the figured specimens of Trepeidopsis recurvidens Gutschick and Treckman (1959, pl. 35, figs. 25, 26) and unfigured paratypes of this species in my possession. Gutschick and Treckman give .90 mm. as the length of the holotype. Unfigured paratypes of the species measure .60 to .75 mm. in length. Trepeilopsis recurvidens differs from A. mississt~ppiana Cooper (1947, p. 87, pl. 20, figs. 34-41) in being more regularly coiled. Stratigraphic occurrence —Trepeiopsis recurvidens was origi- nally described from the Rockford limestone of northern Indiana. The species was found to occur, in the present study, in the Cuya- hoga formation undifferentiated and in the Henley shale member of the Cuyahoga formation in Ohio; in Kentucky the species occurs in the Button Mold Knob member of the New Providence forma- tion and in the Haldeman siltstone member of the Brodhead for- mation. (See Charts 4, 6, 9, 10, 12, 13, 18, 21, and 22 for details of occurrence. ) Ecology.—Trepeilopsis recurvidens was found only in clayey shales of the lower part of the Cuyahoga formation, the plastic Hen- ley shale, in the calcareous shales of the Button Mold Knob member, and in the olive-gray to drab-gray shale breaks in the Haldeman siltstone member. 7. recurvidens seems to have lived on soft, cal- careous or noncalcareous muddy sea bottoms. This species, and Trepeiopsis in general, have not been observed in strictly siltstone or MIsSsISSIPPIAN SMALLER FORAMINIFERA: CONKIN 7 sandstone beds. Species of Trepeidopsis in general were attached to and coiled around spines or spicules, or other elongate organic frag- ments. Sponge spicules are often used for support and attachment. Although, ecologically, the sponges today are most abundant in water just below tide level, representatives of the Porifera are known to be widely distributed even at great depths of the ocean. Table 47. Measurements of Trepeidopsis recurvidens Gutschick and Treckman, 1959, in mm. locality number, Specimen and no.of max. formation, and bed type number length coils diam. number Jes Aye sot .675 7 420 K-56, Haldeman, bed 2 Pl. 23, fig. 4 .625 6 33119) O-7, Cuyahoga, bed 6 IDG Zs anes, 9S) .700 7-8 269 O-7, Cuyahoga, bed 6 Trepeilopsis spiralis Gutschick and Treckman, 1959 TPL, PA MUS, i, WE Pl 27; fis. 145 Wig, 34 Trepeilopsis spiralis Gutschick and Treckman, 1959, Jour. Paleont., vol. 33, No. 2, pp. 243, 244, pl. 35, figs. 20-24. Description—Test attached to a spine, spicule, or similar ob- ject; test consists of a proloculus (broken off of present specimens ) and a tubular second chamber which winds tightly and _ spirally around the object of attachment, gradually enlarging, and consisting in present specimens of about 6 to about 12 coils; aperture formed by open end of tube; wall of fine-grained silt in siliceous cement; color of wall, white to gray to rusty. Measurements—See Table 48 for measurements of Trepeilopsis spiralis and Table 49 for range in measurements of the species. Comparison and affinities —The present specimens are identical with Gutschick and Treckman’s figured specimens and with un- figured paratypes in my possession. Table 48. Measurements of Trepeilopsis spiralis Gutschick and Treckman, 1959, in mm. locality number, specimen and no.of max. formation, and bed type number length coils diam. number Pl. 27, figs 14 950 WAG .302 K-32, New Providence, bed 2 PiES235 figs 7 1.050 8 386 K-12, New Providence, bed 4+ IAL, Wei, sine, 470 6-7 126 I-4, Rockford, bed 2 P23) tig) 6 .750 10 235 T-2, Eulie, bed 2 318 BULLETIN 196 Table 49. Range in measurements of 19 specimens of Trepeilopsts spiralis Gutschick and Treckman, 1959, in mm. Length of test .500-1.100 Number of coils 6-12 Maximum diameter of test .151-.386 Stratigraphic occurrence —Trepeilopsis spiralis occurs in the Eulie shale of Tennessee; the Rockford limestone and Jacobs Chapel shale of southern Indiana; the Bedford shale, the New Providence formation, the Conway Cut and the Haldeman siltstone members of the Brodhead formation, and the Rothwell shale member of the Muldraugh formation of Kentucky. (See Charts 3-6, 8-13, 16-19, 21, and 22 for details of occurrence. ) Ecology.—Trepeiopsis spiralis occurs in soft, plastic shales, in shale breaks within siltstone, and in fine-grained limestone, possibly lagoonal. The ecological requirements for the species were probably much like those of 7. recurvidens and T. glomospiroides. Family LITUOLIDAE Reuss, 1861 Subfamily HAPLOPHRAGMIINAE Cushman, 1927 Genus AMMOBACULITES Cushman, 1910 Spirolina d’Orbigny, 1846, (pars), Foram. Foss. Bass. Tert. Vienne, p. 137. Haplophragmium Brady, 1884, (pars), Rept. Voyage Challenger, Zool., vol. 9, pp. 301, 302. Ammobaculites Cushman, 1910, United States Nat. Mus., Bull. No. 71, pp. $14 e015: Type species, Spirolina agglutinans d’Orbigny, 1846 (original designation, by Cushman, 1910. Miocene, Austria). The generic definition of Ammobaculites was given by Cushman (1910, p. 114) as follows: Test free, chambered, early portion close coiled in one plane, latter portion uncoiled and made up of a more or less linear series of chambers; wall coarsely arenaceous, fairly thick; aperture single at the center of the terminal face of the uncoiled portion, but in the coiled portion at the base of the apertural face. Gutschick and Treckman (1959, pp. 247-249) described the oldest known Ammobaculites, A. leptos, A. pyriformis, and A.? sp. from the Kinderhookian Rockford limestone of northern Indiana. The species described in the present study, A. gutschickt, is, there- fore, the third known species from the Mississippian system. Chart 23 shows the range of Ammobaculites in the Mississippian as deter- mined in this study. MIssISSIPPIAN SMALLER FORAMINIFERA: CONKIN 319 Gutschick and Treckman (1959, p. 249) noted concerning Ammobaculites? sp.: Specimens recovered from acid residues are vesicular and indicate that the animal must have formed its test of agglutinate lime sand grains cemented together with a siliceous paste. It is the siliceous material which is preserved. Again quoting Gutschick and Treckman (1959, p. 249) con- cerning wall composition: Composition and nature of wall structure have become important criteria for classification of Foraminifera. If we are to regard these as important generic characteristics and recognize isomorphism as valid (Ireland, 1956; Cummings, 1955), then the Rockford form would become a new genus related to the agglutinate silica grained Ammobaculites and the calcareous test Endothyranella. Again, in Ammobaculites the spector of wall structure and wall composition arises. Some workers on Paleozoic Foraminifera would hold to strict isomorphism in Foraminifera. Thus, it has been con- ceived that Ammobaculites and Endothyranella are isomorphs. Ac- cording to some workers, Ammobaculites would be considered to have siliceous grains in siliceous cement while Endothyranella would be considered to have calcareous grains (whether extraneous or se- creted by the protoplasm) in calcite cement; others consider /ndo- thyranella to have a completely fibrous calcite structure and compo- position. However, Cushman in his original generic definition of Ammobaculites (1910, p. 114) described the wall as coarsely arena- ceous (arenaceous to Cushman presumedly meant grains of various composition embedded in ferruginous, calcareous, or ferrugino- calcareous cement). I believe that the crux of the wall problem lies primarily in the nature of the cement. If all Foraminifera (save a minute number, as in the family Silicinidae) had originally calcareous, ferruginous, or ferrugino-calcareous cement, and if nearly all siliceous cement repre- sents secondary replacement of original ferruginous, calcareous, or ferrugino-calcareous cement, then I can not accept the principle of isomorphism; that is, I would be quite hesitant to say that genera of Foraminifera are so selective in the type of extraneous particles which they incorporate into their test wall that such selection of extraneous particles would constitute a valid basis for generic dif- ferentiation. ~~ bo ad —- BULLETIN 196 St. Jean (1957, pp. 18, 19) disavows the possession of an aren- aceous test by any Paleozoic Foraminifera. In line with this assump- tion, St. Jean (1957, p. 41) suspected that: . . . all Paleozoic Foraminifera referred to the genus Hyperammina are actually Earlandia. The type of Hyperammina, H. elongata Brady (1878, p. 433, pl. 20, fig. 2) is a Recent arenaceous form from the Arctic Sea. Thus, St. Jean assumed the granularity in the tests of Paleozoic Hyperammina to be due to secondary recrystallization of an original calcite test. What are the relationships between Paleozoic Hyperam- mina and Recent Hyperammina (which are undoubtedly aren- aceous)? I should think that the phylogeny of Recent Hyperammuina extends back to the Paleozoic Hyperammina, although such a propo- sition is difficult of proof, as is also (it may be noted) the negation of the statement. After all, no one seriously believes the genus Lingula among the inarticulate brachiopods does not have a strati- graphic range from Cambrian to Recent. Certainly it is admitted that the smaller Foraminifera have relatively simple test shapes, and thus there are not a great number of structures which can be used for specific and generic criteria. In another vein, if arenaceous (agglutinate) or adventitious (in the sense of Plummer, 1930, p. 7) Foraminifera are known in the Paleozoic (a proposition nearly all workers in the past have agreed to), then the cement in any given genus may have been: (1) orig- inally ferruginous, calcareous, or ferrugino-calcareous, (2) siliceous, or (3) originally ferruginous, calcareous, or ferrugino-calcareous and secondarily replaced by silica. If all Paleozoic arenaceous tests were originally calcareous, ferruginous, or ferrugino-calcareous, then I would disavow isomorphism; thus Ammobaculites would be con- generic with Endothyranella (the chemical nature of the extraneous grains is not here considered of generic importance). If some Paleozoic Foraminifera originally possessed siliceous cement (se- creted of course by the protoplasm), then I would admit the prin- ciple of isomorphism and then Paleozoic Ammobaculites (at present with siliceous cement) and Endothyranella would be distinct genera. I can see no reason to believe that the nature of the extraneous particles in arenaceous Foraminifera (in the sense of Plummer, 1930, p. 7) would of necessity constitute a criterion for generic, or even MIssISsSIPPIAN SMALLER FORAMINIFERA: CONKIN 321 specific differentiation. It has been manifestly demonstrated that arenaceous genera can use particles of many materials to incorporate into their test wall in instances where the “preferred” particles are not available. Of course, some Foraminifera are more selective than others in their “choice” of extraneous particles to incorporate into their test wall; some species are extremely “demanding” in their selection of particles for test construction. In conclusion, until the Quaternary, Tertiary, Mesozoic, and Paleozoic Foraminifera have been thoroughly monographed as to their wall structure and composition (with basic investigation di- rected at adequate redescription of the available types of smaller Foraminifera, as well as study of ecology of Recent Foraminifera and paleoecology of fossil Foraminifera), most statements con- cerning the nature of wall structure of smaller Foraminifera are conjectural. Indeed, we know very little about wall structure and wall composition of Foraminifera in general. The obscure references to arenaceous tests, without clear statements as to the true nature of the cementing material, and to lesser extent the nature of extran- eous particles (in adventitious tests) have served magnificently to confound and delude present workers in their study of the Fora- minifera. Currently, the nature of the test wall in Foraminifera is so beclouded that no worker can remain unconfused when discoursing on wall structure and chemical composition, and their relationships to elements of taxonomy, classification, and phylogeny of the Fora- minifera. Ammobaculites gutschicki, new species Pl. 28, figs. 11-22: IDL ATG wes, US Iie, Bs Description.—Test consists of planispiral and rectilinear por- tions; planispiral part indistinct in inner portion, but outer whorl composed of three to five-and-one-half gradually enlarging inflated chambers; rectilinear portion consists of as many as five slightly enlarging oblate and inflated chambers; final chamber of rectilinear series, subequally long as broad and pyriform due to tapering neck of aperture; test wall moderately coarse-grained with moderate amount of siliceous cement; test generally somewhat compressed; color of test, white to reddish-orange. >) bo bo BULLETIN 196 Measurements—See Table 50 for measurements of Ammobacu- lites gutschicki and Vable 51 for range in measurements of the species and comparison with A. pyriformis Gutschick and Treckman, 1959. Comparison and affinities—Ammobaculites gutschicki has its closest affinities to A. pyriformis Gutschick and Treckman (1959, pp. 248, 249, pl. 37, figs. 14-17, 19, 21-25), especially in the nature of the coiled portion of the test, but A. gutschicki differs markedly in that the rectilinear portion has fewer chambers (up to five) than A. pyriformis (which has six or more rectilinear chambers); in addi- tion, the rectilinear chambers of A. gutschicki are oblate rather than prolate as are the rectilinear chambers in A. pyriformis. Type locality—Blue Gap, 2.65 miles north of New Haven, Nelson County, Kentucky, (Locality K-13) on U.S. Highway 31E. Holotype from the New Providence formation, 44 to 49.5 feet above the Falling Run member of the Sanderson formation (Bed 10). Table 51. Range in measurements of 27 specimens of Ammobaculites gutschicki, n. sp., in mm. and comparison with A. pyriformis Gutschick and Treckman, 1959 A. gutschicki A. pyriformis Length of test .386-.688 -750-1.050 Diam. of coiled portion .176-.440 .250-.280 No. of chambers in outer whorl 3-5.5 4-6 Length of rectilinear part .277-.658 Diam. of rectilinear part .092-.252 No. of rectilinear chambers 1-5 6 or more Stratigraphic occurrence—Ammobaculites gutschicki is found in the Falling Run member of the Sanderson formation, in the New Providence formation, especially in the lower part (Coral Ridge member and equivalent beds) in Kentucky and southern Indiana, in the Brodhead formation in Kentucky and less frequently in the Cuyahoga formation in Ohio. The species also occurs in the Eulie shale of northern Tennessee. Thus, A. gutschicki is known to occur only in the Kinderhookian and Osagian. (See Charts 3-6, 8-13, 16-18, 21, and 22 for details of occurrence. ) Ecology—Ammobaculites gutschicki occurs especially in the soft, plastic when wet, blue-gray and olive-gray shales of the New Providence, and, in the somewhat more silty shales of the Brodhead G25 CONKIN MISsSISSIPPIAN SMALLER FORAMINIFERA peq ‘aouaplAoIg MaN peq ‘souaprAoIg MaN ‘FT-¥ peq ‘souaplAolIg MaN Z peq ‘Asjuay ‘T9-y peq ‘s0uaptaAoig MAN ‘EI[-¥ peq ‘aouapraorg MAN ‘ZI-¥ peq ‘aouaprAoig MaN ‘ZI-¥ 9 peq ‘edoyednyd ‘2-0 peq ‘auaplAoig MAN ‘E[-y OT paq ‘aouaprAolg MAN ‘EI[-¥ peq ‘s0uaplAolg MAN ‘EI-¥ daqunu Pq puv ‘uo1pmsof ‘4aquinu &71]090] £ Sia 06° Cc £6. 69C° c 16) LLO £ $8" Oct c SLT 697° £ OTC £0 £ CSC OLY $-& $8" 98E° £ 81d OLY C 100° £0" SI QUloyd qivd jivd ADIUIJIJIIA ADIUIPIJIIA ADIUIPIYIIA UL S4aqguivyd f{O “WoIP {0 ‘ou fo-wpip fo 4j6ua] SY $'S SY $ ]4O0YO JSD] fo ‘Ou CSC See Sst CSC 097 CSC LLO Ott 9LV ttc 695° 1109 985° Tes" 9Et +09" 98e° $09" 889° LES” OL9 OL9 YjOuI] “UU ul SaSavur ‘Ly vyIsIns SIJUNIVG OU Wp jo SJUIWIIINS V9 [A] ‘OS Ie | OC alge ec. Id IZ ‘SIF “EZ ‘Id Bi ole toeald adAjoloy II “SIF “2 ‘Id St ‘SIF ‘EZ ‘Id LE ‘SIF “£2 ‘Id 9I “SIF “2 ‘Id cz SIF “EZ ‘Id €l “SI} “£¢ ‘Id +I “SIF ‘EZ ‘Id cl “SIF “EZ ‘Id daquinu aga pun uauiags 324 BULLETIN 196 and Cuyahoga formations; there are rather small to moderate amounts of silt in these beds and the silt is usually of small to medium size. Remarks.—This new species is named for Dr. Raymond C. Gutschick, Head of the Dept. of Geology at the University of Notre Dame, in recognition of his pioneering work on Lower Mississippian smaller Foraminifera. Family TEXTULARIIDAE d’Orbigny, 1846 Subfamily FEXTULARIINAE d’Orbigny, 1846 Genus CLIMACAMMINA Brady, 1873 Textularia Defrance, Brady, 1871, (pars), Geol. Soc. Glasgow, Trans., vol. 3, suppl., p. 13. (nomen nudum) Climacammina Brady, 1873, Geol. Sury. Scotland, Mem., Expl. Sheet 23, p. 94; idem, 1876, Paleont. Soc. Mon., vol. 30, pp. 67, 68; Cushman, 1948, Foraminifera, Cambridge, p. 120. Bigenerina d’Orbigny, Brady, 1884, (pars), Rept. Voyage Challenger, Zool., iro Bh joes SIAL sige Type species, Textularia antiqua Brady 1871, (monotypic genus). Cushman’s (1948, p. 120) generic definition of Climacammina follows: Test free, early portion biserial, later uniserial; wall arenaceous, mostly of fine fragments but including coarser ones, cement calcareous; aperture in the biserial portion textularian, in the uniserial portion irregularly cribrate, terminal ... IJ have examined Brady’s specimens of Climacammina antiqua as well as duplicates which have been treated with acid. The cement is calcareous, but the arenaceous fragments are of various sorts and sizes. The test is truly arenaceous as stated by Brady in his original description of the genus. The original specimens show the characteristic distortion and collapsing so fre- quently seen in the Textulariidae. The stratigraphic range of Climacammina was considered by Cushman (1948, p. 120) to be Carboniferous to Permian. However, Cushman (1928, p. 120) reported the range of the genus to be “Carboniferous to Permian... Tertiary and Recent(?)”, and noted: The Bigenerina robusta H. B. Brady (Rep. Voy. Challenger, Zoology, vol. 9, p. 1884, p. 371, pl. 45, figs. 9-16) and some Tertiary species have essentially the characters of Climacammina, but there seems to be a very wide gap where no representatives of the genus are known if these are the same as the Paleozoic forms. Chart 23 shows the range of Climacammuna in the Mississippian as determined in this study. There has been some doubt as to the relationships between Climacammina and Bigenerina. Brady (1876, pp. 371, 372) rejected MISsSISSIPPIAN SMALLER FORAMINIFERA: CONKIN 325 the genus Climacammina; however, Climacammina was considered valid by Cushman (1948, p. 120). The specific definition of the Recent Bigenerina robusta Brady (1881, p. 53) was given as follows: Test elongate, compressed in its earlier (biserial) portion, cylindrical in its later (uniserial) growth. Uniserial segments numerous, short, somewhat irregular, often ventricose at their periphery. Aperture simple and Textularian in the biserial segments, becoming multiple and porous in the uniserial portion, the pores either arranged in a ring or irregularly distributed in the central part of the exposed face of the terminal chamber. Interior non-labyrinthic. Length, about 1/5 inch (4.8 mm.). The original generic definition of Bigenerina by D’Orbigny (1826, p. 261) requires Bigenerina to possess a single terminal aper- ture in the uniserial portion, the figures of the type species, B. nodosaria dOrbigny, 1826 (p. 11, figs. 9-12) demonstrating beyond doubt the single terminal aperture of the genus Bigenerina. It seems reasonable that Bigenerina robusta Brady, 1881, be relegated to Climacammina in that it fits well within the generic concept of Climacammina, except its interior is not labyrinthic. The type species, C. antiqua (Brady), 1871 is labyrinthic (Brady, 1876, p. 68), but not all species which have been referred to Clhmacammina are labyrinthic. The lack of examples of Climacammuina between the Tertiary and Permian is no evidence that they did not exist. Ulti- mate knowledge concerning the geologic range of any fossil is deter- mined empirically and therefore is rather fortuitous. Climacammina often occurs in hard limestones and its presence there would have to be determined from thin sectionings. In any event, stratigraphic discontinuity can not be given preference over biologic evidence (identical morphology) in dis- cerning the geologic ranges of species, or any taxon above the species. The paleontologic record is supreme; it is the measure for ascer- taining the time-stratigraphic ranges of all taxa of higher or lower catagories. Climacammina mississippiana, new species Pl. 24, figs. 1-6; Figs. 41-43 Description—Test elongate, approximately five times longer than broad; test consists of two portions, the earlier portion con- sisting of about 11 biserial textularian chambers, followed by a series of three uniserial chambers; the textularian series has inflated 326 BULLETIN 196 chambers taking on a rounded wedge shape; the uniserial series has nearly cylindrical chambers; the last (or third) uniserial chamber becomes rounded and only slightly bluntly pointed at the middle of the apertural face; the uniserial chambers possess cribrate apertures; the apertural face of the uniserial chamber is pierced by eight or possibly slightly more, partially triangular apertures (the two present specimens are imperfectly preserved); ‘sutures originally distinct and depressed, but both specimens exhibit evidence of wear; internally the test wall is seen to be composed of two layers, both calcareous, the inner layer is crystalline calcite completely secreted by the protoplasm of the foraminifer, while the outer layer is aren- aceous with calcite cement (see Fig. 43). Measurements —Table 52 gives the measurements of Climacam- mina mussissippiana and a comparison with the measurements of C. cylindrica Cushman and Waters, 1928. Table 52. Measurements of Climacammina mississippiana, n. sp. in mm. and comparison with C. cylindrica Cushman and Waters, 1928 C. mississippiana, 0. sp. C. cylindrica holotype, Pl. 24, paratype, Pl. 24, figs. 1, 2, 6 figs. 3-5 Length of test 971 554 2.000 Length of uniserial chambers 3- 193 .210 2- 118 118 1- Lif 118 Diameter of uniserial chambers 3- 462 436 .600 2- 470 369 1- 403 360 Length of biserial chambers 5- 185 4- 101 3- 084 2- .075 1- .068 Diameter of biserial chambers 5- L252 4- .252 3- .160 2- 134 1- 118 Diameter of proloculus 118? Thickness of outer wall .080 Thickness of inner wall .050 MIssISSIPPIAN SMALLER FORAMINIFERA: CONKIN 527 Comparison and affinities—Clmacammina mississippiana has its closest affinities to C. cylindrica; however, C. mississippiana dit- fers from C. cylindrica in having: (1) smaller number of biserial chambers, (2) smaller number of uniserial chambers, (three instead of four as in C. cylindrica), and (3) size only about one-half that of C. cylindrica. Type locality —Clark’s Station Quarry, 2.4 miles south of Morill on Highway 421, Jackson County, Kentucky, (Locality K-46). Holotype is from the horizon of the Big Clifty sandstone (Bed 1). Stratigraphic occurrence—Climacammina has been reported from the Permian of Texas, the Pennsylvanian of Texas (Cushman and Waters, 1930, p. 56), and the Pennsylvanian of Oklahoma ( War- thin, 1930, p. 31). The only record of Climacammina in the Missis- sippian of North America is the report of a Climacammina? zone in the Greenbrier limestone (top of the Reynolds limestone) in West Virginia (Flowers, 1956, pp. 7, 8). The species of Climacam- mina? of Flowers is a true Climacammina; | have collected samples and prepared thin sections of the Greenbrier limestone which yielded specimens of Climacammina along with Tolypammina spp. and dasycladacean algae in the pisolitic limestone portions of the upper Greenbrier in Greenbrier County near White Sulphur Springs, West Virginia. In Europe, Climacammina is known to range from the Permian downward into the Lower Carboniferous. In Russia, Climacammina antiqua (Brady), 1876 has been reported from the Lower Carboni- ferous around Leningrad ( Mikhailov, 1939, p. 62, pl. 4, figs. 17, 18). In the present study Climacammina was found in the lower Chesterian Paint Creek limestone and Big Clifty sandstone; thus, the geologic range of Climacammina is extended downward to the Upper Mississippian in North America. Ecology.—Of the two specimens of Climacammina misstssip- piana found in this study, one is from the calcareous, clayey, and fossiliferous shale of the upper portion of the Paint Creek limestone (Bed 1), south of Mt. Vernon in Rockcastle County, Kentucky, (Locality K-42) and the other specimen is from a marine shale at the horizon of the Big Clifty sandstone (Bed 1) at Morill, Jackson County, Kentucky, (Locality K-45). These two localities are about 17 miles apart. 328 BULLETIN 196 Flowers commented on the sediments within which the Climacammina zone occurs in the Greenbrier limestone of West Virginia (1956, p. 8): The Climacammina? faunal zone can nearly always be found in wells having little clastic material in the upper part of the Greenbrier limestone. In southeastern West Virginia where there is a large increase in clastic material at the location of this zone, both the Greenbrier and the Mauch Chunk are universally thick in this area, making it difficult to locate with any cer- tainty, either the stratigraphic position of the Reynolds limestone or the top of the Greenbrier limestone. Where this is the case, the position of the Climacammina? zone cannot always be determined. The occurrence of Climacammina mississippiana in the calcar- eous shale of the Paint Creek limestone is in keeping with the cal- careous nature of the test, but the occurrence of C. mississippiana in the less calcareous shales at the horizon of the Big Clifty sand- stone raises questions as to whether the Big Clifty specimen might have been reworked from one of the lower limestones or calcareous shales. Climacammina in general flourished in the warm and shallow seas of high carbonate alkalinity as evidenced by its occurrence in the Greenbrier limestone in association with the characteristically warm and shallow water sedimentary structures, the oolites and pisolites. Nevertheless, Climacammina mississtppiana occurs, so far as 1s known, in calcareous shales in Kentucky, demonstrating that the species of Climacammina are not restricted to the odlite-pisolite limestone facies. Remarks.—The cribrate aperture and the labyrinthic interior of Climacammina mississippiana clearly distinguishes it from any superficially similar species of Bigenerina d’Orbigny, 1826. Thus, C. mississtippiana becomes the first Mississippian species of the genus to be described from North America. Family MILIOLIDAE d’Orbigny, 1846 Genus AGATHAMMINA Neumayr, 1887 Serpula Geinitz, 1846, (pars), Verstein. Deutsch. Zechsteingebirge und Roth- liegenden, Heft 1, p. 6, pl. 3, figs. 3-6 (fide Cushman, 1948, Foraminifera, Cambridge, p. 177). Agathammina Neumayr, 1887, Sitzber. K. Wiss. Wein, Math.-Naturiv. Cl., vol. 95, pt. 1, p. 171; Cushman, 1927, Cushman Lab. Foram. Research, Contr., vol. 3, pt. 4, p. 188; idem, 1928, Cushman Lab. Foram. Research, Spec. Pub. No. 1, pp. 145, 146. MIssISSIPPIAN SMALLER FORAMINIFERA: CONKIN 329 Type species, Serpula pusilla Geinitz, 1846 (subsequent designation by Cushman, 1927, p. 188). The type description of Agathammina was given by Neumayr GI887Z,.p. 171): Ich fasse unter diesum Namen Formen zusammen mit unregelmassig miliolides Aufrollung, unvollkommender Kammerung und Sandiger Schale mit kalkigens cement. Vorwiegend carbonische und permische Arten. Cushman’s (1928, p. 146) generic definition of Agathammina follows: Test tubular, undivided, winding about an elongate axis; wall imperforate, calcareous, with arenaceous material at the surface; aperture formed by the open end of the tubular chamber. The miliolid genus Agathammina has been reported from the Recent (Cushman, 1929, p. 21), the Tertiary (Grzybowski, 1896, p. 282), the Pennsylvanian (Cushman and Waters, 1930, p. 59; Galloway and Ryniker, 1930), and the Permian (Cushman and Waters, 1928, p. 43). Agathammina mississippiana is the first Mississippian species of the genus to be reported. (See Chart 23 for the range of Agatham- mina in the Mississippian. ) All specimens of Agathammina mississippiana are composed of fine-grained siliceous silt in siliceous cement. The problem of test wall composition again looms, In one specimen of the present ma- terial, I concede that there must have been siliceous replacement of the original arenaceous test inasmuch as the test is composed com- pletely of chalcedony. None of the present specimens effervesces with acid. Inasmuch as the tubular second chamber of the present speci- mens is not divided, the specimens can not be referred to the family Silicinidae. A possible course of action would be to erect a new genus, the generic essence of which might be expressed as a form with a proloculus followed by a tubular and undivided second chamber which winds about an elongate axis, and is composed of siliceous silt grains in siliceous cement. This temptation is resisted inasmuch as the structure of the test wall of Paleozoic arenaceous Foramini- fera is insufficiently known to allow conclusive judgement as to the questions of original wall structure versus replacement, and the real nature of isomorphism among Foraminifera. 330 BULLETIN 196 Agathammina mississippiana, new species Pl. 23, figs. 23-25; Pl, 27; fis. 18 ies 3b Description—Test configuration varies from narrowly spindle- shaped in the early one coil stage to broadly oval (shaped like a Quinqueloculina or Spiroloculina) in the mature two-coil stage; test compressed; test consists of a spherical proloculus, followed by an undivided, tubular second chamber disposed in two coils; whorls nearly planispirally coiled around the proloculus producing the milio- line appearance of the mature test; the ends of the elongate axis are slightly pointed and are formed by the sharp bending of the second chamber around the ends of the axis; length of test attains a size as much as 2.9 times the width, but the average ratio of length to width is slightly less than 2 to 1; aperture terminal, rounded to elliptical, formed by the constricted open end of the tubular second chamber; test opaque to translucent, white to gray to orange-buff in color; test wall composed of fine-grained siliceous silt in siliceous cement. Comparison and affimties—Agathammina mississippiana is similar to A. protea Cushman and Waters, 1928 in that: (1) the measurements of A. protea given by Cushman and Waters (1928, p. 43) fall well within the range of dimensions of A. mississippiana, (2) a prominent milioline shape is possessed by the mature forms of both species, (3) ratio of length to width of test is about 2 to 1 in both species, (4) both species have forms which vary from nar- rowly elongate to broadly elongate shape, and (5) both species are nearly planispirally coiled. Although Agathammina mississippiana has closest affinities to A. protea, A. mississippiana differs specifically from A. protea in having (1) less number of coils (two in A. mississippiana compared to five or six in A. protea) and (2) a more rounded to elliptical aperture than the subtriangular aperture of A. protea. Agathammina mississippiana is also somewhat similar to A. pusilla, the type species of the genus. Galloway and Ryniker (1930, p. 8) believed that A. protea Cushman and Waters, 1928 is con- specific with A. pusilla. However, I consider A. protea to vary signi- ficantly, and certainly specifically, from A. pusilla in having much more regular and planispiral coiling. MISSISSIPPIAN SMALLER FORAMINIFERA: CONKIN 331 Measurements——See Table 53 for measurements of Agatham- mina mississtppiana and for comparison with A. protea. Type locality—Road cut along U. S. Highway 31F, .5 miles southwest of Balltown, Nelson County, Kentucky, (Locality K-12). The holotype is from the lower 2 to 5.5 feet of the New Providence formation (Bed 4). Stratigraphic occurrence —Agathammina mississippiana occurs in the Osagian of Kentucky in the lower New Providence formation and the Rothwell shale member of the Muldraugh formation; in the Chesterian, it occurs in the Glen Dean formation. In Ohio, the species is recorded from only the Osagian Black Hand sandstone member of the Cuyahoga formation. (See Charts 5-7, 9, 10, 13, 14, 18, 21, and 22 for details of occurrence.) This is the first known reference to Agathammina in the Mis- sissippian System. Thus the time of origin and the lineage of the family Miliolidae is extended backward in time one geologic period. Table 53. Measurements of Agathammina mississippiana, n.sp., 1 mm. locality number, specimen and thick- formation, and bed type number length width NeSS number Pl. 23, fig. 24, .657 420 185 K-25, Glen Dean, holotype bed 1 JEN Pah, fea VAS 924 503 193 O-11, Black Hand, bed 1 PZ o eile. 23 453 .260 176 K-35, New Providence, bed 7 Ecology —Agathammina mississippiana with only one known exception is restricted ecologically to soft, plastic shales, dominantly with no large amount of carbonates present. Thus the species was apparently best adapted for life on a muddy sea bottom where fine silty grains were available. The members of the family Miliolidae are characteristic of shallow water. The strictly calcareous imperforate (porcellaneous ) forms, such as the genus Miliola, where they appear in plethora are characteristically associated with reefs, as in shallow water environ- ment of lagoons, fore-reef shoals, or bank reefs. The ecology of the eS) iS) bo BULLETIN 196 Eocene Muiliola limestones of the Middle East was considered by Henson (1950, p. 230): Typical Miliola limestones occur in shallows of barrier-reef lagoons and in littoral shoal areas of fringing-reefs. Along flat, foreland shores and in analogous shallow-water environments where reef development is in patches rather than belts, the reef and back-reef facies may be intricately intermingled. .. . Miliola limestones, recognizably modified by mixture with other material, may also be formed in open littoral zones. Futher, Conkin and Conkin (1956, p. 895) discussed the eco- logical significance of the Nuwmmoloculina limestones from the lower Cretaceous of the Sierra Madre Oriental of Mexico, southwest and east Texas, Louisiana, and central Florida as follows: There is excellent evidence for a lagoonal origin of some of the subsurface Lower Cretaceous limestones of southwest Texas and the other areas as noted above in that they: (1) are dense, gray to dark-colored, organic limestones containing carbonaceous matter, hydrogen sulphide gas, and in some places anhydrite, with frequent to abundant miliolids (to the near exclusion of other fossils) and (2) alternate with reef nucleus rocks and fossils (algae, reef foraminifers, rudistids and other mollusks with smaller amounts of corals and bryozoans. . . . From consideration of their ecology it is clear that miliolids occuring in abundance are facies foraminifers characteristic of back-reef and inter-reef environments. I do not, of course, imply that reef conditions existed in areas where the present specimens were found (in fact it is clear that no reefs were present), but it is desirable to establish the fact that miliolids have a propensity for shallow water environments. It is well known that miliolids are frequently found in sandy, littoral zones. I have observed the dominance of miliolids in the Recent beach and very near shore sand, seaward from Padre Island in Nueces County, near Corpus Christi, Texas. Again, it 1s well estab- lished that miliolids live in the shallow and somewhat brackish water of bays. Family OPHTHALMIDIIDAE Cushman, 1927 Genus HEMIGORDIUS Schubert, 1908 Cornuspira Howchin, 1895, Roy. Soc. South Australia, Trans., vol. 19, p. 195, pl. 10, figs. 1-3 (non Cornuspira Schultze, 1845, Organismus Polythal., Leipzig, p. 40). Hemigordius Schubert, 1909, Jahrb. K. K. Geol. Reichs., 1908, vol. 58, p. 381; Cushman, 1928, Cushman Lab. Foram. Research, Spec. Pub. No. 1, p. 161. Type species, Cornuspira schlumbergeri Howchin, 1895. MIssISSIPPIAN SMALLER FORAMINIFERA: CONKIN 333 Cushman’s generic definition (1948, p. 192) of Hemigordius follows: Test free, early coils not entirely planispiral, later planispiral and com- pletely involute, but not umbonate; wall calcareous, imperforate; aperture formed by the open end of the tube——Carboniferous and Permian. I have topo- types of the type species, and it is certainly close to Cornuspira. Chart 23 shows the range of Hemigordius in the Mississippian as determined in this study. Hemigordius morillensis, new species Pl. 23, fig. 26; Pl. 27, fig. 17; Fig. 30 Description—Test free, discoidal, circular in outline; juvenar- ium consists of a proloculus and two to three non-planispiral whorls; diameter of juvenarium making up as much as 45 percent of the diameter of the tubular, undivided second chamber; juvenarium succeeded by as many as four planispiral whorls; megalospheric form may be completely planispiral; test not completely involute, with portions of preceding whorls visible; exterior of test rarely possesses secondary deposits which obscure the nature of the internal coiling; aperture rounded; wall calcareous and imperforate. Measurements.—See Table 54 for measurements of Hemigordius moriulensts and for comparison with H. calcarea Cushman and Waters, 1928. Table 54. Measurements of Hemigordius morilensis, n. sp., in mm. and comparison with H. calcarea Cushman and Waters, 1928. Pl. 23, fig.26, unfigured holotype paratypes H. calcarea Diam. of juvenarium .10 02, .07 14 Diam. of test 30 MG, 55 35 Axial width of test .08 03 Diam. of proloculus .03 EOueO2 No. of whorls in juvenarium 2 OQ, 8 3 No. of planispiral whorls 2.5 1.75, 4 1.5 Comparison and affinties—Hemigordius morillensis seems to be similar to H. calcarea Cushman and Waters, 1928; unfortunately the figures of H. calcarea are poor. The only original measurement given for H/. calcarea was the diameter, I have prepared the measure- ments of H. calcarea in Table 54 from examination of PI. 6, figs. 1-2 of Cushman and Waters, 1928. 334 BULLETIN 196 Hemigordius morillensis seems to differ from H. calcarea in having: (1) whorls more planispirally arranged, (2) lesser number of whorls in the juvenarium, and (3) a pronounced microspheric form. Lype locality —Clark Station Quarry, Morrill, Jackson County, Kentucky, (Locality K-46). The holotype is from the shale at the horizon of the Big Clifty sandstone (Bed 1). Stratigraphic occurrence —Hemigordius morillensis is herein re- ported only from the Chesterian beds, occuring in Kentucky in the calcareous shales of the Paint Creek limestone, basal shales of the Big Clifty-Cypress sandstone, the calcareous shale of the Glen Dean limestone and in the Kinkaid shale. (See Charts 7, 14, 15, and 22 for details of occurrence. ) Ecology—Hemuigordius morilensis occurs primarily in cal- careous shale. The test is completely calcareous crystalline. The species displayed a definite “preference” for limy mud bottoms. Remarks.—There is no evidence of replacement of the calcareous crystalline test, Family TROCHAMMINIDAE Cushman, 1929 Genus TROCHAMMINA Parker and Jones, 1859 Nautilus Montagu, 1808, (pars), Testacea Britania, Suppl., p. 81, pl. 18, fig. 3. Rotalina d’Orbigny, Williams, 1858, (pars), Foraminifera Great Britain, Fol., London, p. 50, pl. 4, figs. 93, 94 (on Rotalina d’Orbigny, 1846, Foraminiferes fossiles du Bassin tertiarie de Vienne, Paris, p. 149). Trochammina Parker and Jones, 1859, Ann. and Mag. Nat. Hist. (ser. 3), No. 4, p. 347; Brady, 1879, Quart. Jour. Micros. Sci., vol. 19, p. 54. Lituola Lamarck, Parker and Jones, 1865, (pars), Philos. Trans., p. 325. (non Lituola Lamarck, 1804, Ann. Mus., vol. 5, p. 243). Haplophragmium Reuss, Siddall, 1879, (pars), (fide Cushman, 1948, Fora- minifera, Cambridge, p. 106); (non Haplophragmium Reuss, 1860, Akad. Wiss. Wien, Sitz., vol. 40, p. 218). Type species, Nautilus inflatus Montagu, 1808 (monotypic genus). Brady (1879, p. 54) presented a complete and clear account of the vicissitudes of the genus 7'rochammina and gave the generic definition of Trochammina Parker and Jones, 1859 in the restricted sense of Brady: The genus Trochammina was established by Messrs. Parker and Jones (Annals and Mag. Nat. Hist., 1859, ser. 3, vol. LV, p. 347), for a group of MISsSISSIPPIAN SMALLER FORAMINIFERA: CONKIN 335 arenaceous foraminifera characterized primarily by their thin, smooth finely- cemented tests. Although the name was originally applied to a rotalid shell (Nautilus inflatus Montagu, 1808, Test. Brit., Suppl., p. 81, pl. 18, fig. 3—Rotalina inflata Williamson, 1858, Rec. For. Gt. Br., p. 50, pl. 4, figs. 93, 94), the author prefers to regard the trochoid, often adherent variety (Tr. squamata J. and P.), as the type of the genus. The tenuity and fine texture of the arenaceous investment rather than the mere general contour has very properly been accepted as the essential distinction, and fresh forms possessing this character have one by one been added to the genus until it has come to include a series having a very wide range of morphological variation. Not only have we trochoid and rot- aliform, but nautiloid, milioline, spirilline, and as we shall presently see, lageniform and nodosarian modifications of the type. In addition to these there are certain simple adherent organisms, described by d’Orbigny under the name Webbina (Foram. Canaries, p. 125), whose natural affinity is with the same group; in point of fact the term Trochammina, with these repeated additions, has come to comprehend an assemblage of forms having the dimen- sions of a family rather than a genus. The series is now altogether too bulky and diverse to be zoologically convenient, and it is necessary to consider whether it may not be subdivided with advantage. Prof. von Reuss makes a distinct genus of the spirilline non-septate forms to which he gives the name Ammodiscus, and their term has been generally adopted by German authors. If we accept Webbina to distinguish the simple adherent varieties and Am- modiscus for the free, non-septate forms, and limit the application of Trocham- mina to the well differentiated septate modifications of the type, to which it was first applied, there only remains the Nodosaria-like species to be provided for, and for these the term Hormosina (from opHos, a necklace) would be a suitable generic or subgeneric appellation. Trochammina ohioensis, new species IDL Wey lee, We PASS 1 Ay, walls. TGR Lies, Sys) Description—Test trochoid, moderately compressed, earlier chambers more globose, chambers of last whorl moderately inflated and the largest in size; test of three whorls. The last whorl consists of three to four chambers; sutures on both dorsal and ventral sides nearly straight, or slightly curved; aperture on the ventral side of test, extending to mid-point of the apertural face, at the base of the last chamber; aperture slitlike and rather rectangular, .084 mm. in length and .025 mm. in height; test usually somewhat distorted, crushed; wall coarsely arenaceous of siliceous grains in siliceous ce- ment. Measurements —See Table 55 for measurements of T'rocham- mina ohioensis and Table 56 for range in the measurements and for comparison with 7. arenosa Cushman and Waters, 1927. 336 BULLETIN 196 Table 55. Measurements of Trochammuina ohioensts, n. sp., in mm. specimen and maximum maximum no. of chambers in type number diameter width outer whorl : dorsal ventral Pl. 23, fig. 27, 50 24 3 3 holotype Pl. 23, fig. 28 60 28 4? 3? Table 56. Range in measurements of nine specimens of Trochammina ohioensis, n. sp. in mm. and comparison with T. arenosa Cushman and Waters, 1927 T. ohioensis T. arenosa Maximum diameter .37-.60 65 Maximum width .13-.29 18 No. of chambers in outer whorl: dorsal 3-4 4 ventral 3-4 + Comparison and affinities—Trochammina ohtoensis is similar to T. arenosa, but T. ohtoensis differs from 7. arenosa in having more inflated chambers, much coarser quartz sand grains in siliceous cement, and generally smaller test. Unfortunately the shape and dimensions of the aperture in Trochammina arenosa are unknown. T. arenosa is based on one specimen; however, the species is reported (Cushman and Waters, 1927, p. 152) as being “common” in the Pennsylvanian of Texas. Thus, presumably a characteristic form was figured; nevertheless, the range of individual variation remains unknown. Type locality—All specimens are from shale streaks in the Black Hand sandstone (Bed 1), at Armstrong, Ohio, (Locality O-11). Stratigraphic occurrence——Trochammina ohioensis is known only from the Osagian Black Hand sandstone of Ohio. Ecology.—The occurrence of Trochammina ohioensis only in the silty and sandy shale of the noncalcareous Black Hand sandstone and its absence elsewhere may indicate the “preference” of 7. ohioensis for a muddy sand environment. Remarks —Trochammina ohtoensis is the first species of Lrochammina reported from the Mississippian of the studied area. MIssISSIPPIAN SMALLER FORAMINIFERA: CONKIN 337 Family PLACOPSILINIDAE Cushman, 1927 Subfamily POLYPHRAGMINAE Rhumbler, 1913 Genus STACHEIA Brady, 1876 Stacheia Brady, 1876, Paleont. Soc. Mon. 30, p. 107; Cushman, 1927, Cushman Lab. Foram. Research, Contr., vol. 3, pt. 1, p. 42; idem, 1927, Cushman Lab. Foram. Research, Contr., vol. 3, pt. 4, p. 189; idem, 1928, Cushman Lab. Foram. Research, Spec. Pub. No. 1, p. 178. Stacheia Brady, emend, Chapman, 1895, Ann. and Mag. Nat. Hist., ser. 6, vol. 16, p. 321. Type species, Stacheia marginuloides Brady, 1876, first species (subsequent designation by Cushman, 1927). Brady’s (1876, p. 107) definition of Stacheia follows: Test (normally) adherent, composed either of numerous segments sub- divided in their interior, or of an acervuline mass of chamberlets, sometimes arranged in layers, sometimes confused. Texture subarenaceous, imperforate. Chapman (1895, p. 321) emended Stacheia Brady, 1876: Test adherent or free; composed of numerous segments subdivided in their interior, or of an acervuline mass of chamberlets, sometimes arranged in layers, sometimes confused, or of a thick-walled test with acervuline or labyrin- thic structure and with the interior subdivided into numerous elongate sinuous cavities (the latter characters especially applying to the Rhaetic representatives of the genus). Aperture simple, but irregular, terminal or scattered over the surface of the test. Texture subarenaceous, composed of fine sand, sometimes admixed with coarser material, and with a calcareous or chitinous cement; imperforate ... In his ‘Monograph of the Carboniferous and Permian Foramini- fera’ Dr. Brady lays particular stress upon the fact that in the Carboniferous strata Stacheia is always parasitic (adherent); and such is undoubtedly the case with specimens from that formation. In the Rhaetic assemblage the tests are more often perfectly free in their mode of growth. The flat complanate or fron- dose form (S. dispansa) is by far the best represented species, in point of num- bers, in the Rhaetic washings; and this form appears to have flourished on the sea-bottom, spreading horizontally and growing so numerously as to make a separation band at frequent intervals in the clay deposits. Most of the present Stacheia are adherent, usually either to sponge spicules or bryozoan fragments. Apertures are usually not observed; openings at the distal portion of the elongate forms may contain the apertures. The test is smooth or moderately smooth, containing fine siliceous grains in much siliceous cement. Perhaps the silica cement in these arenaceous forms indicates replacement of original calcareous cement. Most species of Stacheia exhibit rather wide latitude of individual variation; the specific characteristics are not strongly pronounced. Many of the specimens are adherent and thus the configuration of the test is somewhat controlled by 338 BULLETIN 196 their mode of attachment and by the shape of the object to which they are attached. The free living forms also exhibit irregularity in the shape of their tests. The adherent mode of life and the arenaceous nature of the test would seem to cause the species of Stacheia to be provincial in their distribution. Wider geographic distribution might have been attained if the genus had been adherent to floating algal masses; however, the arenaceous nature of the test would seem to restrict the genus to the benthos. Stratigraphically, Stacheia has been reported from the Silurian and the Pennsylvanian of North America. This is the first record of the genus in Mississippian rocks. Chart 23 shows the range of Stacheia in the Mississippian as determined in this study. Stacheia cicatrix, new species ‘ Pl. 25, figs: 1-3) Pl. 27, figs. 20, 21) Bice 37 Description—Test adherent, forming medium to _ large-sized irregularly to poorly rounded, compressed, semiglobular to discoidal, or less often irregular, masses, all fused into a unit; attached gen- erally to sponge spicules and bryozoan fragments; test arenaceous with siliceous grains in siliceous cement; color of test gray to buff- white. Measurements—See Table 57 for measurements of Stacheia cicatrix and Table 58 for range of measurements of S. cicatrix and comparison with S. acervalis. Comparison and affinities —Stacheia cicatrix resembles S. acer- valis Brady, 1876 in general appearance. Inasmuch as little internal structure is discernable in thin sections of the present specimens or in the original material of Brady (1876, p. 16, pl. 9, figs. 6-8) and inasmuch as Stacheia is a generalized genus, the precise definition of species of Stacheia is difficult. S. cicatrix differs from S. acervalis in having: (1) more regularly rounded individual masses fused into a unit, (2) stronger amalgamation of the individual rounded masses, and (3) a larger size to the fused mass. Type locality—Northwest side of Kenwood Hill, southern Louisville, Jefferson County, Kentucky, (Locality K-2), The holo- type is from the Coral Ridge member (Bed 2) of the New Provi- dence formation. MISSISSIPPIAN SMALLER FORAMINIFERA: CONKIN 339 Stratigraphic occurrence.—Stacheta cicatrix has been found only in the Osagian New Providence and Brodhead formations and in the Meramecian Somerset shale member of the Salem limestone in Kentucky. The species is most abundant below the Brodhead forma- tion, especially in the lower and middle parts of the New Providence formation. In Ohio, the species is known only from the Osagian Hen- ley shale member of the Cuyahoga formation. (See Charts 3-6, 9-13, 18, 21, and 22 for details of occurrence.) Table 57. Measurements of Stacheia cicatrix, n. sp., in mm. specimen and locality number, formation, type number length diameter and bed number Jey Ab savers I 1.70 82 K-2, Button Mold Knob, bed 4 Pip 25. ties 2 1.30 1.20 I-2, Button Mold Knob, bed 3 IPL 5, siee; 3}, 1.60 84 K-2, New Providence, holotype bed 2 IPL 7h, sates, 2A 1.10 89 K-4, Coral Ridge, bed 2 Table 58. Range in measurements of 10 specimens of Stacheia cicatrix, n. sp. in mm. and comparison with S. acervalis Brady, 1876 S. cicatrix S. acervalis Maximum length .84-2.5 .80 Maximum diameter .35-1.4 Ecology.—Stacheia cicatrix apparently was restricted to shaly beds which contain megafossil remains, inasmuch as the species was primarily adherent in its living habit (to sponge spicules or bryo- zoan fragments). The generic definition of Stacheia requires that its species possess calcareous cement. S. cicatrix contains no calcareous cement. It is possible that the tests of S. cicatrix have been replaced by siliceous material. In any event, I am unwilling to erect a new genus based on this species inasmuch as our lack of precise infor- mation concerning original wall structure and chemical composition of Paleozoic Foraminifera and processes of possible replacement of these ancient forms precludes such action, Remarks —The trivial name for this new species is derived from the resemblance of the test to a scar. 340 BULLETIN 196 Stacheia neopupoides, new species PI25, fies. 4 be is 40 Description.—Yest adherent, elongate, small to moderate-sized; externally the test appears as a mass, cylindrical to somewhat taper- ing, composed of an irregular series of indistinct, curved chambers; test delicate, usually attached to a sponge spicule; test texture fine- grained or smooth; test wall of fine siliceous grains in siliceous ce- ment; color, gray to yellow-gray. Measurements—See Table 59 for measurements of Stacheia neopupoides and for comparison with S. pupoides Brady, 1876 and S. congesta Brady, 1876. Table 59. Measurements of Stacheia neopupoides, n. sp. in mm. and comparison with available measurements of S. pupoides Brady, 1876 and S. congesta Brady, 1876 Specimen and locality number, formation, type number length diameter and bed number IG by sites, Bh, 89 30 K-4, New Providence, holotype bed 6 PIS 27 petics 19 66 30 K-32, New Providence, bed 3 1A AG, aatreds at 94 45 K-61, New Providence, bed 2 3 unfigured paratypes .50-.97 .25-.37 S. congesta .7-1.5 Carboniferous, Scotland S. pupoides 1.0 Carboniferous, Scotland Comparison and affinities—Stacheia neopupoides has closest affinities to S. pupoides Brady, 1876 and S. congesta Brady, 1876. It is with some reluctance that a new species is erected in view of the similarities between the present specimens and S. congesta and S. pupoides. However, inasmuch as S. congesta and S. pupoides are primarily European species (S. pwpoides has been reported by Cush- man and Waters, 1930, p. 73, figs. la, lb; pl. 12, fig. 8 from the Pennsylvanian of Texas) and the genus Stacheia was undoubtedly an arenaceous and encrusting or attached form, I feel that the pres- ent material is not conspecific with either S. congesta or S. pupoides. Stacheia neopupoides seemingly has closest affinities to S. pupoides but differs from S. pupoides in having more prominent sutures and less fusiform test, MIssISSIPPIAN SMALLER FORAMINIFERA: CONKIN 34] Type locality —East Quarry of the Coral Ridge Brick and Tile Corp., at Coral Ridge, southwestern Jefferson County, Kentucky, (Locality K-4). Holotype is from the Button Mold Knob member (Bed 6) of the New Providence formation. Stratigraphic occurrence—Stacheia neopupoides occurs in the lower Osagian beds of Kentucky and eastern Ohio and in the Kinder- hookian Bedford shale. See Charts 4, 6, 9, 13, 18, 19, 21, and 22 for details of occurrence. Ecology—Stacheia neopupoides seems to have been adapted to live in fine-grained, slightly calcareous muds. Remarks. —Stacheia neopupoides receives its trivial name from its similarity to S. pupoides. Stacheia trepeilopsiformis, new species Pl. 25, figs. 6, 7; Big: 39 Description—Test adherent to spines, rods, or other cylindrical objects; early portion apparently consisting of a series of uniserial or nearly uniserial (perhaps slightly trochoid), moderately inflated segments (two to three) which are fused into a broad cone-shaped mass, the proximal portion of which is pointed; no evidence of at- tachment found at the base; the fused mass succeeded by three nearly rectilinear large segments, the last of which exhibits over- lapping of segments at right angles to the section sutures; object of attachment missing, leaving a rounded or oval opening; wall aren- aceous with calcite cement; no evidence of replacement. Measurements —See Table 60 for measurements of Stacheia trepeilopsiformis and for comparison with S. pupoides Brady, 1876. Comparison and affinities—Stacheia trepeilopsiformis has its closest affinities to S. pupoides Brady, 1876, but S. trepeidopsiformis differs from S. pwpoides in having lesser number of segments per test length, and in addition, the test of S. trepeidlopsiformts is general- ly less rapidly expanding distally proximally than S. pupoides; how- ever, this is not always the case (Brady, 1876, pl. 8, figs. 20, 26). Type locality —F ishing Creek, Lake Cumberland, west of Som- erset, Pulaski County, Kentucky, (Locality K-32). Holotype is from the upper part of the New Providence formation, 167% to 175 feet above the Falling Run member of the Sanderson formation (Bed 10). 342 BULLETIN 196 Stratigraphic occurrence ——Stacheia trepeilopsiformis has been found only as a single specimen in the upper part of the New Provi- dence formation in southern Kentucky in an area where the New Providence formation probably contains beds younger than Fern Glen-Burlington. Table 60. Measurements of Stacheia trepeilopsiformis, n. sp., in mm. and comparison with S. pupoides Brady, 1876 pl 25) figss 6.) 7 holotype S. pupoides Length of test 1.00 1.00 Distal diameter 35 Proximal diameter 12 Ecology —Stacheia trepeilopsiformis is an arenaceous, calcareous form and is found in calcareous shales intercalated between siliceous siltstones. It is difficult to present much concerning the ecological requirements of a species from observation of one specimen; never- theless, the sediments in which the specimen occurs indicate the existence of a calcareous, marine mud environment in close proximity to sites of silt and sand deposition; the paucity of fossils in the sedi- ments may indicate restricted marine environment in near shore shallow water where shaly beds were interspersed within deltaic silts, REFERENCES Brady, H. B. 1876. A monograph of Carboniferous and Permian Foraminifera (the genus Fusulina excepted). Paleontogr. Soc. Monogr., vol. 30, pp. 1-166, 12 pls. 1878. On the reticularian and radiolarian Rhizopoda (Foraminifera and Polycystina) of the North-Polar Expedition of 1875-76. Ann. Mag. Nat. Hist., ser. 5, vol. 1, pp. 425-440, pls. 20, 21. 1879. Notes on some of the reticularian Rhizopoda of the Challenger Expedition, Quart. Jour. Micrs. Sci., vol. 19, pp. 20-63, 261-299, pls. 3-5. 1881. Notes on some of the reticularian Rhizopoda of the Challenger Ex- pedition. Pt. III, Quart. Jour. Micrs. Sci., vol. 21, pp. 31-71. 1884. Report on the Foraminifera dredged by H. M.S. Challenger during the years 1873-1876. Rept. Voyage Challenger, Zoology, vol. 9, pp. 1-814, pls. 1-115. Browne, R., Conkin, J., Conkin, B., and MacCary, L. M. 1958. Sedimentation and stratigraphy of Silurian and Devonian rocks in the Louisville area, Kentucky. Geol. Soc. Kentucky Field Trip, pp. 1-46, 18 figs. 3 tables. Campbell, G. 1946. New Albany shale. Geol. Soc. America, Bull., vol. 57, pp. 829-908, 3 pls., 7 figs. wd MISSISSIPPIAN SMALLER FORAMINIFERA: CONKIN 34: Chapman, F. 1895. On Rhaetic Foraminifera from Wedmore, in Somerset. Ann. Mag. Nat. Hist, ser. 6, vol. 16, pp. 305-329, pls. 11-12. Colom, G. 1945. Los Foraminiferos de “concha arenacea” de las Margas burdigali- enses de Mallorca. Instit. Invest. Geol., Estudios Geologicos, Num. 2, pp. 1-33, 12 pls. Conkin, B. 1954. Microfossils of the Virgilian Deer Creek formation of Kansas and northern Oklahoma. Unpublished Master’s Thesis, Univ. of Kansas. Conkin, J. E. 1954. Hyperammina kentuckyensis, n. sp. from the Mississippian of Ken- tucky, and discussion of Hyperammina and Hyperamminoides. Cush- man Found. Foram. Res., Contr., vol. 5, pt. 4, pp. 165-169, pl. 31. 1956. “Nodosinella Brady, 1876, and associated Upper Paleozoic genera’— A comment. Micropaleontology, vol. 2, No. 2, p. 193. 1957. Mississippian smaller Foraminifera of East-Central United States (abstract). Geol. Soc. America, Bull., vol. 68, p. 1889. 1957. Stratigraphy of the New Providence formation in Jefferson and Bullitt counties, Kentucky, and description of the Coral Ridge fauna. Bull. Amer. Paleont., vol. 38, No. 168, pp. 109-157, 3 charts, 5 tables, 2 text-figs., 4 pls. Conkin, J. E., and Conkin, B. 1956. Nummoloculina in the Lower Cretaceous of Texas and Louisiana. American Assoc. Petr. Geol., Bull., vol. 40, No. 5, pp. 890-896, 4 text- figs. 1958. Revision of the genus Nummoloculina and emendation of Nummo- loculina heimi Bonet. Micropaleontology, vol. 4, No. 2, pp. 149-158, pl. 1, text-figs. 1-25, tables 1-5. 1960. Arenaceous Foraminifera in the Silurian and Devonian of Kentucky. Geol. Soc. America, S. E. Sect., abstracts, p. 8. Coryell, H. N., and Rozanski, G. 1942. Microfauna of the Glen Dean limestone. Jour. Paleont., vol. 16, No. 2, pp. 137-151, pl. 23, 24. Cooper, C. L. oa 1947. Upper Kinkaid (Mississippian) microfauna from Johnson County, Illinois. Jour. Paleont., vol. 21, pp. 81-94, pls. 19-23. Crespin, I. 1958. Permian Foraminifera of Australia. [Australia] Bur. Min. Res., Geol. and Geophys., Bull. No. 48, pp. 1-207, 33 pls. Cummings, R. H. j 1955. Nodosinella Brady, 1876, and associated Upper Paleozoic genera. Micropaleontology, vol. 1, No. 3, pp. 221-238, pl. 1, text-figs. 1-10. Cushman, J. A. 1910. A monograph of the Foraminifera of the North Pacific Ocean. United States Nat. Mus., Bull. 71, pt. 1, pp. 1-134, 203 figs.; pt. 2, pp. 1-108, 156 figs.; pt. 3, pp. 1-125, 47 pls. 1928. Foraminifera. Their classification and economic use. Cushman Lab. Foram. Res., Spec. Pub., No. 1, Sharon, Massachusetts, pp. 1-401, 59 pls. 1948. Foraminifera. Their classification and economic use. Cambridge, pp. 1-605, 9 text-figs., 31 text-pls., 55 key pls. 344 BULLETIN 196 Cushman, J. A., and Waters, J. A. 1927. Arenaceous Paleozoic Foraminifera from Texas. Cushman Lab. Foram. Res., Contr., vol. 3, pt. 3, pp. 146-153, pls. 26, 27. 1928. Some Foraminifera from the Pennsylvanian and Permian of Texas. Cushman Lab. Foram. Res., Contr., vol. 4, pt. 2, pp. 31-56, pls. 4-7. 1930. Foraminifera of the Cisco Group of Texas. Univ. Texas, Bull. No. 3019, pp. 22-81, pls. 2-12. Dawson, J. W. 1868. Acadian Geology. 2d. ed., London, pp. 1-694, text-figs. 1-23. Dunn, P. H. 1942. Silurian Foraminifera of the Mississippi Basin. Jour. Paleont., vol 16, No. 3, pp. 317-342, pls. 42-44. Flowers, R. R. 1956. A subsurface study of the Greenbrier limestone in West Virginia West Virginia Geol. Sur. Rept. Inv., No. 15, 17 pp. Galloway, J. J.. and Ryniker, C. 1930. Foraminifera from the Atoka formation of Oklahoma. Oklahoma Geol. Sur., Circ. No. 21, pp. 1-27, pls. 1-5. Grzybowski, J. 1896. Otwornice czerwonych ixow z Wadowic. Akad. Umiej. Krakowie, Wydz. Mah.-Przyr., Rozpr., Krakow, ser. 2, tom 10, pp. 261-308, tables 8-11. (fide Cushman, J. A., 1950, Card Catalogue Foraminifera. United States Geol. Sur., Washington) Gutschick, R. C., and necked J. F. 1959. Arenaceous Foraminifera from the Rockford limestone of northern Indiana. Jour. Paleont., vol. 33, No. 2, pp. 229-250, pls. 33-37, 3 text-figs. Hauesler, R. 1890. Monographie der Foraminiferen-fauna der schweizerischen Trans- versariuszone. Schweiz. Pal. Ges., Abhandl., v. 47, art. 1, pp. 1-134, Mat; 1-15 Harlton, B. H. 1933. Micropaleontology of the Pennsylvanian Johns Valley shale of the Ouachita Mountains, Oklahoma, and its relationship to the Mississippian Caney shale. Jour Paleont., vol. 7, No. 1, pp. 3-29, pls. 1-7. Henson, F. R. S. 1950. Cretaceous and Tertiary reef formations and associated sediments in the Middle East. American Assoc. Petrol. Geol., Bull., vol. 34, No. 2, pp. 215-238, 14 figs., 1 table. Hyde, J. E. 1953. The ees aa ee of central and southern Ohio. Ohio Div Geol. Sur. Bull. pp. 1-355, 54 pls., 19 figs. (edited by M. F. Marple) Ireland, H. A. 1956. Upper Pennsylvanian arenaceous Foraminifera from Kansas. Jour. Paleont., vol. 30, No. 4, pp. 831-864, 7 text-figs. Loeblich, A, R., Jr., and Tappan, H. 1954. Emendation of the foraminiferal genera Ammodiscus Reuss, 1862, and Involutina Terquem, 1862. Washington Acad. Sci., Jour., vol. 44, No. 10, pp. 306-310, 2 text-figs. MecGrain, P. 1952. Outcrop of the Chester formations of Crawford and Perry counties, Indiana, and Breckenridge County, Kentucky. Geol. Soc. Kentucky Chester Field Excursion, pp. 1-20, 10 figs. MISssISSIPPIAN SMALLER FORAMINIFERA: CONKIN 345 Mikhailoy, A. 1939. To the characteristics of the genera of Lower Carboniferous Fora- minifera, In: Maliavkin, S. F. (Ed.), The Lower Carboniferous deposits of the north-western limb of the Moscow Basin. Leningrad, Geol. Admin., Symposium (Sbornik), No. 3, pp. 47-62, 4 pl. Moreman, W. L. 1930. Arenaceous Foraminifera from the Ordovician and Silurian lime- stones of Oklahoma. Jour. Paleont., vol. 4, No. 1, pp. 42-59, pls. 5-7. Neumayr, A. 1887. Die Natiirlichen Verwandtschaflsverhdltnisse der schalentragenden Foraminiferen. K. Akad. Wiss. Wien., Math.-Naturw. cl., Sitzber., Wien, Bd. 95, abh. 1, pp. 156-186. Orbigny, d’, A. 1826. Tableau methodique de la classe des Cephalopodes. Ann. Sci. Nat., Paris, ser. 1, tome 7, pp. 96-314, pls. 10-17. Parr, W. J. ; 1942. Foraminifera and a tubiculous worm from the Permian of the northwest division of Western Australia. Roy. Soc. Western Australia, Jour., vol. 27, pp. 97-115, 2 pls. Plummer, H. J. ; 1930. Calcareous Foraminifera in the Brownwood shale near Bridgeport, Texas. Univ. Texas, Bull. No. 3019, pp. 1-21, pl. 1. 1945. Smaller Foraminifera in the Marble Falls, Smithwick, and the lower Strawn strata around the Llano Uplift in Texas. Univ. Texas Pub. 4401, pp. 209-271, pls. 15-17, 16 figs. Rhumbler, L. 1895. Entwurf eines Natiirlichen Systems der Thalamophoren. Nachr. k. Gesellsch. Wiss. Gottingen, Math.-Nat. Cl. 1895, pp. 51-98. St. Jean, J. : 1957. Ad middle Pennsylvanian foraminiferal fauna from Dubois County, Indiana. Indiana Dept. Consery. Geol. Sur., Bull. No. 10, pp. 1-66, pls. 1-5. Stockdale, P. B. 1931. The Borden (Knobstone) rocks of southern Indiana. Indiana Dept. Conserv., Div. Geol. Sur., Pub. No. 98, pp. 1-330. 1939. Lower Mississippian rocks of the East-Central Interior. Geol. Soc. America, Sp. Paper, No. 22, pp. 1-237, 26 pls., 2 figs. Thomas, R. N.,, et al. 1955. Exposures of producing formations of northeastern Kentucky. Geol. Soc. Kentucky Field Trip, pp. 1-32, 11 figs. Warthin, A. S. 1930. Micropaleontology of the Wetumka, Wewoka, and Holdenville for- mations. Oklahoma Geol. Sur., Bull., No. 53, pp. 1-95, pls. 1-7. Waters, J. A. 1927. d group of Foraminifera from the Dornick Hills formation of the Ardmore Basin. Jour. Paleont., vol. 1, pp. 271-276, pl. 22. PLATES FIGURES 348 BULLETIN 196 Explanation of Figures Figures 1-19 1. Thuramminoides sphaeroidalis Plummer; 2, 3, Proteonina cumber- landiae, n. sp.; 4, 5, Proteonina wallingfordensis, n. sp.; 6, 7, Hyperam- mina casteri, n. sp.; 8, Hyperammina kentucKyensis Conkin; 9, Hyperam- mina rockfiordensis Gutschick and Treckman; 10, Earlandia consternatio, n. sp.; 11, Reophax cf. R. arenatus (Cushman and Waters); 12, Reophax kunklerensis, n. sp.; 13, Reophax cf. R. lachrymosus Gutschick and Treckman; 14, 16, Reophax medonaldi, n. sp.; 15, Reophax asper Cushman and Waters; 17, Glomospira articulosa Plummer; 18, Lituotuba semiplana, n. sp.; 19, Crithionina palaeozoica, n. sp. s 1-19 FIGURE ULL. AMER. PALEONT., VOL. 43 we idt es BULL. AMER. PALEONT., VOL. 48 FIGURES 20-36 CoN ai tys MISsSISSIPPIAN SMALLER FORAMINIFERA: CONKIN 349 Explanation of Figures Figures 20-36 20, Involutina semiconstricta (Waters); 21, Involutina exserta (Cush- man); 22, InvOlutina longexserta Gutschick and Treckman; 23, Tolypam- mina jacobschapelensis, n. sp.; 24, Tolypammina botonuncus Gutschick and Treckman; 25, Tolypammina cyclops Gutschick and Treckman; 26, Tolypammina laocoon, n. sp.; 27, Tolypammina tortuosa Dunn; 28, Ammovertella labyrintha Ireland; 29, Ammovyertella cf. A. inclusa (Cush- man and Waters); 30, Hemigordius morillensis, n. sp.; 31, Ammovyertella ef. A. primaparva Ireland; 32, Trepeilopsis recurvidens Gutschick and Treckman; 33, Trepeilopsis glomospiroides Gutschick and Treckman; 34, Trepeilopsis spiralis Gutschick and Treckman; 35, Ammobaculites gut- schicki, n. sp.; 36, Agathammina mississippiana, n. sp. 350 BULLETIN 196 Explanation of Figures Figures 37-43 37, Stacheia cicatrix, n. sp.; 38, Trochammina ohioensis, n. sp.; 39, Stacheia trepeilopsiformis, n. sp.; 40, Stacheia neopupoides, n. sp.; 41-43, Climacammina mississippiana, n. sp. ULL. AMER. PALEONT., VOL. 43 FIGURES PLATE 1° 9 v PALEONT., VOL. 4: oR. ULL. AME » }D Figure 1-10. Thuramminoides sphaeroidalis Plummer 1. 2. 3. 4, a MIsSISSIPPIAN SMALLER FORAMINIFERA: CONKIN Explanation of Plate 17 All figures X 50 Page Spherical test showing surface configuration of centripetal tubes. No. 628628 UISNM. Spherical test with outer wal] destroyed, showing casts of tube ends. No. 628629 UISNM. Spherical test, slightly crushed, showing ends of large centripetal tubes. No. 628625 UISNM. Broken specimen showing interior of test. Tube structure destroyed. No. 628617 USNM. . Broken test showing rounded pits on interior wall where tubes pierce surface. No. 628624 UISNM. . Flattened test with internal tubular structure Visible through translucent outer wall, No. 628621 USNM. . Small collapsed test with shape like a red blood corpuscle. No. 628618 USNM. . Flattened test with several protuberances, not taken to be apertural necks. No. 628620 USNM. . Large flattened test with protuberances. No. 628619 USNM. . Test of the most common variation, with a low protuberance. No. 628626 USNM. 352 BuLLETIN 196 Explanation of Plate 18 Figure All figures X 50 Page 1-4. Thuramminoides sphaeroidalis Plummer ........................220.....-------- 243 1. Large test of typical appearance. Dark filling visible through translucent outer wall. No. 628616 USNM. 2. Test with large low protuberances. No. 628623 USNM. 3. Large broken test with internal structure destroyed. No. 628627 USNM. 4. A typical flattened test. No. 628622 USNM. ULL. AMER. PALEONT., VOL. 438 PLATE 18 PLATE 19 PALEONT., VOL. 43 > \e AME! BULL. MissIssIpPIAN SMALLER FORAMINIFERA: CONKIN 353 Explanation of Plate 19 Figure All figures X 50 Page 1-3. Proteonina cumberlandiae, n. sp. -.-.........220..20cccccecceeeceecececcceeeeeeee 248 1. Large specimen with neck missing. No. 628634 USNM. 2. Holotype, showing teardrop shape. Test compressed. No. 628632 USNM. 3. Test more elongate than usual. No. 628633 USNM. 4-3) Proteonina wallingfordensis; nn. -Sp. 222-0222 ool eos ecceesececccceee 250 4, 6, 8. Tests showing typical round to oblate chamber and stocky tapering neck. Nos. 628638, 628640, 628641 USNM. 5. Large specimen of typical shape. No. 628642 USNM. 7. Holotype. No. 628637 USNM. 9} Crithioninapalaecozoicas ms Sp. 2 ese 238 Holotype, showing spongy texture of test wall. No. 638653 USNM. Ode Crithionma, rotundata’ Cushman 222s ce 239 Fragments of the holotype. Shows less regularity to test wall than does Crithionina palaeozoica, n. sp. Figure 1-18. Hyperammina casteri, n. sp. BULLETIN 196 Explanation of Plate 20 All figures X 50 Page 1. Holotype, microspheric form, Test broken at apertura] end, bo but well developed otherwise. No. 628644 USNM. . Microspheric form, broken at apertural end. No. 628650 UISNM. . Megalospheric form, slightly constricted. No. 628662 UISNM. . Microspheriec form, slightly constricted, with proloculus missing, No. 628651 USNM. , 7, 12. Megalospheric forms with apertural ends broken off. Nos. 628655, 628658, 628659 USNM. . Microspheric form with extremely long and pointed tip. Apertural end broken off. No. 628645 USNM. , 11. Microspheric forms, less conical than most. Nos. 628647, 628648 USNM. . Megalospheric form, apertural end broken. Proloculus some- what pointed. No. 628660 UISNM. . Microspheric form showing apertural end with slightly con- stricted aperture. No. 628649 USNM. .Microspheric form, A typical small specimen. No. 628652 USNM. , 15. Fragments of a large megalospheric form. No. 628654 USNM. . Large microspheric form; proloculus missing. No. 628646 USNM. . Large megalospheric form; apertural end partly broken. No. 628657 USNM. . Large megalospheric form with oblate proloculus; apertural end broken. No. 628656 USNM. PLATE 20 ULL. AMER. PALEONT., VOL. 43 PLATE 4 PALEONT., VOL. 43 AMER. BULL. = co gs kamn . a Bea Ea ee oa had, Seiek eee oe ee ea MISsSISSIPPIAN SMALLER FORAMINIFERA: CONKIN 35 Explanation of Plate 21 Figure All figures X 50 Page 1-9. Hyperammina kentuckyensis Conkin ..............22.20000000002222222.--- 264 10-13. 14-16. Ife 18. iY). 1. Topotype showing slender, constricted test, hourglass taper- ing of early part of second chamber and oblate proloculus. No. 628664 USNM. 2,3. Topotypes. Nos. 628663, 628665 USNM. 4-9. More or less well-developed specimens, all showing char- acteristie constriction of test and development of lip at aper- tural end. Proloculus missing on figures 4, 6, and 7. Nos. 628669, 628670, 628668, 628667, 628671, 628666 USNM. Hyperammina rockfordensis Gutschick and Treckman ........ 267 Tests showing rather cylindrical second chamber with few faint constrictions. Nos. 628674, 628675, 628672, 628673 UISNM. BParlandiay CONStEERAMO STH. Sp) 2k ee ee 273 14. Holotype, proloculus missing. Shows tapering nature of test. Constrictions less prominent than in Hyperammina kentuckyensis, but otherwise shape of test is similar. No. 628677 USNM. 15, 16. Small and large specmens. Proloculi missing. Nos. 628679, 628678 USNM. Reophax cf. R. minutissimus Plummer ................00..00..0..-..-....... 285 No. 628698 USNM. Reophax cf. R. lachrymosus Gutschick and Treckman ............ 282 Broken specimen. No, 628689 USNM. Reophax cf. R. arenatus (Cushman and Waters) _.........0.00.....-.. 278 No. 628681 USNM. - Reophax kumkleremsis,, n.. spy 2ccicc0)20e ence eee ees. 280 20. Holotype, showing typical slender test with oblate over- lapping chambers. No. 628684 USNM. 21-23. Nos. 628687, 628685, 628686 UISNM. 4. Reophax asper Cushman and Waters ................---------.--tee---e---- 279 Specimen showing rugose wal] of angular quartz grains. No. 628683 USNM. PIRCODNAx mMmemOMAlaN, sm.) Spyies es eee ee es ee ee 2 284 25. Holotype. Shows typical stocky test with inflated, oblate, overlapping chambers, and pyriform last chamber. No. 628691 USNM. 26-30. Tests showing variation of form within the species. Nos. 628692, 628696, 628694, 628695, 628693 USNM. BuLLETIN 196 Explanation of Plate 22 Figure All figures X 50 Page 1-3. Involutina semiconstricta (Waters) ...........000.0-0-cccccc-ceeeceeeeceeeeeee 291 1. Variant 1. Delicate test composed of much cement. No. 628710 USNM. 2. Variant 2. Robust test composed of much silt and relatively small amount of cement. No. 628709 USNM. 3. Variant 1. No. 628712 USNM. -Inyvolutina, exserta (Ci usiamtam)) se ee err ee 287 All specimens are Variant 2, with large proportion of silt and little cement. Nos. 628701, 628705, 628703, 628699 USNM. 5. Specimen with neck broken off. . Inyolutina longexserta Gutschick and Treckman .|....................... 289 Nos. 628708, 628706 USNM. . Glomospira articnulosa Plummer 2 ee 296 No. 628713 USNM. / Lituotuba-semiplana,:n.~ spi 2 2) a ee eee 297 11. Holotype, microspheric form. No. 628715 USNM. 12. Megalospheric form. No. 628716 USNM. . Tolypammina botonuneus Gutschick and Treckman .................... 301 No. 628718 UISNM. .Tolypammina cyclops Gutschick and Treckman WWW... 302 14. No. 628719 USINM. 15. Fragment of exceptionally large specimen. No. 628720 USNM. . Tolypammina jacobschapelensis, n. sp. .............---.-------------0--------- 304 16. Holotype, showing partially walled floor of test, and pro- loculus shaped like half an egg with a pointed end. No. 628722 USNM. 17, 18. Specimens with pointed proloculi. Nos. 628724, 628723 UISNM. 19, 20. Specimens with rounded proloculi. Fig. 19 shows under- side of test with attached proloculus. Nos. 628728, 628725 USNM. 21. Large specimen with pointed proloculus. No. 628726 USNM. . RBolypammina, tortiiosa unm? 2... 2.22.25. 2: 25s onseeceee ee eee 308 No. 628730 USNM. Poly pamininn-ThOCOON, Tl. Sp.) 2c a 8 ee eee 307 Specimen showing winding of early portion of second chamber. No. 628729 USNM. PLATE 22 9 3) ULL. AMER. PALEONT., VOL. 4: AMER. PALEONT., VOL. 438 BULL. wat ™N MIssSISSIPPIAN SMALLER FORAMINIFERA: CONKIN 3 Explanation of Plate 23 Figure All figures X 50 except where noted Page 1, 2. Trepeilopsis glomospiroides Gutschick and Treckman .......... 315 Specimen showing glomospiroid winding of last portion of second chamber. Nos. 628740, 628742 USNM. 3. 4. Trepeilopsis recurvidens Gutschick and Treckman .................... 316 11-22. 23-25. 26. 27, 28. Specimens showing last portion of second chamber returning toward proloculus. Nos. 628745, 628743 USNM. . Trepeilopsis spiralis Gutschick and Treckman ........................ 318 Nos. 628747, 628748, 628746 USNM. . Ammovertella cf. A, inelusa (Cushman and Waters) —............. 309 Specimen showing underside of test, early planispiral portion, and later embracing windings of second chamber. No. 628734 UISNM. . Ammovertella labyrintha Ireland ~...................-----.-------22--2.e-e eee 312 Specimen showing maze of fused windings of second chamber. No. 628736 UISNM. . Ammovertella cf. A. primaparva Ireland ............................--......---- 313 Specimen showing rather regular meandering of earlier portion of test. Later more irregularly winding portion is missing. No. 628738 USNM. Ammobaculites gutschicki, n. sp. 2.2.2.2 eee 322 11. Holotype, showing oblate rectilinear chambers and pyriform last chamber. No. 628750 USNM. 12-21. Specimens showing variation within the species. Nos. 638623, 638625, 638624, 638630, 638628, 638629, 638631, 638627, 638633, 638632 USNM. 22. Broken test of unusually large size. No. 638626 USNM. Agathammina mississippiana, n. sp. ................------------0----+se0------ 331 23. X 28. No. 638637 UISNM. 24. Holotype. No. 638635 UISNM. 25. X 31. No. 638636 UISNM. Hemigordius morillensis, n: sp. Holotype, showing rather irregularly winding early portion and planispiral later portion of tubular chamber. No. 638639 USNM. Trochammina OhiG€nsis, n. Sp. -...---------<<--c--ccececeeeecceecceccceeeeeeeeeee~ 336 27. Dorsal view of holotype. No. 638641 USNM. 28. Ventral view of flattened specimen. No. 638642 USNM. ~~ on CO BuLLETIN 196 Explanation of Plate 24 Figure All figures approximately X 90 1-6. Climacammina mississippiana, n. sp. —.......2200.....20...-eeeeeeeeeeeeeeeeees 326 1, 2. Holotype. Apertural and lateral views, No. 638654 USNM. 3-5. Broken specimen showing only uniserial portion. No. 638655 USNM. 6. Polished section of holotype showing biserial-uniserial cham- ber arrangement, ULL. AMER. PALEONT., VOL. 43 PLATE 24 PLATE 25 9 vo AMER. PALEONT., VOL. 4 BULL. MIssISsIPPIAN SMALLER FORAMINIFERA: CONKIN 359 Explanation of Plate 25 Figure All figures X 50 Page leo LACK ELA CICALDEX, is (SP iiat<-c ch ol es ele ee eet ie ee 339 1, 2. Nos. 638645, 638646 UISNM. 3. Holotype. No. 638644 USNM. Pes ACUeia NEOPUPOLUES Nl. SPs ioe te 3. ox... ee 341 4. No. 638651 UISNM. 5. Holotype. No. 638649 UISNM. 6, 7. Stacheia trepeilopsiformis, n. sp. -.....-......-2..0-.-c-c-.s-2000s-0ceeeeeeeoeeeeeoos 342 Two Views of holotype. No. 638652 USNM. 360 BULLETIN 196 Explanation of Plate 26 Figure All figures X 50 Page 1-3. Thuramminoides sphaeroidalis Plummer 16, 1, 2. Thin section showing centripetal tubes, cut longitudinally near edge of test and transversely near center. Nos. 628630, 628631 USNM. 3. Dark material in center appears chitinous. No. 628639 USNM. 5. Eroteonina cumberlandiaes mn spy ee Thin section. Nos. 628635, 628636 UISNM. 6. Proteonina wallingfordensis, n. sp. Thin section. No. 628643 UISNM. 8: Hyperammina.casteri mm: *Sp: <2. 4 eee 7. Thin section of megalospheric form. No. 628661 USNM. 8. Thin section of microspheric form with proloculus missing. No. 628653 USINM. 9. Hyperammina kentuckyensis Conkin ...................000....2-2------2--- Thin section of specimen in fig. 5, Pl. 5. No. 628670 UISNM. 10. Hyperammina rockfordensis Gutschick and Treckman ............ Thin section showing thickening of wall at junction of pro- loculus and second chamber. No. 628676 USNM. 141.Barlandia ‘consternation, (Sp), 3. eee Thin section of specimen with proloculus missing. No. 628680 USNM. 248 250 12. Reophax cf. R. arenatus (Cushman and Waters) ....................-.-- 278 Thin section. No. 628682 USNM. 13. Reophax cf. R. lachrymosus Gutschick and Treckman ................ 282 Thin section. No. 628690 USNM. 14. Reophax kunkleremsis, nm: sp. 2:.222.:..4-0--3 eee 280 Thin section showing overlapping nature of chambers. No. 628688 USNM. 15: Reophax mcdonald, n: sp. -2-.2.225-. 2 eee 284 Thin section showing overlapping chambers. No. 628697 USNM. 17, 19. Involutina exsSerta (Cushman) ----22 se nee 287 Thin sections. Nos. 628702, 628704, 628700 USNM. 18. Involutina longexserta Gutschick and Treckman ........................ 289 Thin section. No. 628707 USINM. 20. Invyolutina semiconstricta (Waters) ............----...-----.-------cc-2e---eceeeeee 291 Thin section, Variant 1. No. 628711 USNM. PLATE 26 ULL. AMER. PALEONT., VOL. 43 5a! ra iets) a BULL. AXIERS PALEONT:. VoL. 43 PLATE 3 MISSISSIPPIAN SMALLER FORAMINIFERA: CONKIN 361 Explanation of Plate 27 Figure All figures X 50 Page 6-9. 10. if 12. 13. 14, 15. llGe WY 18. U8). 20, 21. . Lituotuba semiplana, n. sp. . Tolypammina cyclops Gutschick and Treckman . Tolypammina tortuosa Dunn Glomospira articulosa Plummer ................... 296 Thin section, megalospheric form, showing nearly planispiral coiling. No. 628717 USNM. Thin section. No. 628721 USNM. Thin section showing intertwining of tubular chamber. No. 628731 USNM. . Tolypammina jacobschapelensis, n. sp... 304 Thin section showing pointed tip of proloculus and partial floor wall. No. 628727 USNM. Ammovertella cf. A. ineclusa (Cushman and NWiaters) eee 309 Ammovertella labyrintha Ireland ..................... Slt Thin section showing complicated maze of windings of second chamber, No. 628737 USNM. Ammovertella cf. A. primaparva Ireland _.................. 313 Thin section showing regular meandering of tubular second chamber. No. 628739 USNM. Trepeilopsis recurvidens Gutschick and Treckman Thin section. No. 628744 USNM. Trepeilopsis glomospiroides Gutschick and Treckman _...... ILg: Thin section showing irregular winding about upper end of spiral. No, 628741 USNM. Trepeilopsis spiralis Gutschick and Treckman _........ 318 Thin section showing spine or spicule about which tube is wound. No. 628749 USNM. Ammobaculites gutschicki, n. sp. 322 Thin section showing planispiral coiling of early portion and rectilinear arrangement of later portion. No. 638634 USNM. epee ee 316 REGCUAMMila, ONIOCMNIS,. no gps o eM a 336 Thin section. No. 638643 USNM. Hemigordins morillensis, masp. 2 2... ee 334 Thin section showing planispiral coiling of outer whorls. No. 638640 USNM. Agathammina mississippiana, n. sp. _......................--. 331 Thin section showing coiling; test much altered. No. 638638 USNM. Sincheia neopupoidess 1m .cp. a0) he a erie ek eee 341 Thin section. No. 638650 USNM. Strchelaacicatrix: mt sgp. ee eee ty eae ee 980 Thin sections. Nos. 638647, 638648 USNM. INDEX Light face figures before bold face figures refer to Figure numbers; bold face to Plate numbers; light face to pages. A acervalis, Stacheia ___. acicula, ‘“Hyperam- minoides”’ Agathammina agglutinans, SPiLOlina eee Ammobaculites .......... Ammobaculites? Ammodiscus Ammovertella antiqua, Climacam- 00 tra epee eat ees ane eae ee Rexiilarias arenata, Nodosinella arenatus, Reophax .... Reophax CLS ees 11, 19, 26 arenosa, Trocham- Madi itee ea ee eee articulosa, Glomo- Spitaw IG VPRO asper, Reophax 15, 21 aspera, Saccam- mina Bath County, Ment Ckyas = eee Bedford shale Beechwood limestone bendensis, Reophax .. Berea sandstone ........ Bernhagen, Ralph .... Beveridge, Thomas .. Beyrichoceras 338, 339 256 135, 199, 200, 203, 328, 329, 331 318 199, 202, 234, 318, 319 318-320 285, 286, 335 199, 202, 223, 224, 228, 230, 298-300, 308, 310 327 325 217 277 324, 198, 227, 277, 278 335, 336 199, 224-227, 295, 296 198, 278, 279 251, 252 145 137, 147, 202, 253, 293, 309, 318, 341 223 282 253 139 139 224, 271 Big Clifty Sandstonien 144, 203, 327, 328, 334 Bigenerina .......-:..------ 324, 325, 328 Black Hand sand- stone member ........ 14 225 220% 229, 246, 249, 284, 288, 292, 293, 331, 336 Blackiston formation 201, 202, 253, 269 botonuncus, Tolypam- INNA wae 24,22 199, 224, 300- 302, 306 Boyle County, Kent ksysee sees 143 Brady, His Biss 135, 234, 235, 254, 256, 278, 324, 325, 334, 337, 341 Brassfield limestone 307 Breckenridge County, Kent chivas eee 142 Brodhead formation... 141-143, 202, 203, 225, 226, 229, 232, 246, 249, 267, 288, 309, 316, 318, 322, 339 Brownwood shale .... 272 buccina, Reophax .... 261 bulbosa, Earlandia .-. 258 Hyperammina ........ 258, 259 Bullitt County, Kentucky == 140, 141, 229, 243, 270 Button Mold Knob MGM CMe secs eee 140, 146, 201, 224, 229, 232, 240, 246, 267, 269, 279, 310, 316, 241 C calearea, Hemigordius 333, 334 Caldwell County, IRGC Keyan eens ae 142, 273 Campbell, Guy .......... 144, 146-148, 303 Caney Creek member Carboniferous Foraminifera ........ Carter County, Kentucky .............-.- Casey County, Kentucky Caster, Kenneth E. .... casteri, Hyper- ammina ..6, 7, 20, 26 cervicifera, Proteonina ............ (Ghapniane Hy 2 Chimney Hill limestone Churn Creek member cicatrix, Stacheia ..37, 25, 27 Clark County, Indiana Clark County, Kemntuekiye --2:...-.-...- Ciay City siltstone MmeMbDeHee—--- Clay County, Tennessee coleyi, Hyperammina (@olomiy Gat ee concinna, Nodosinella congesta, Stacheia .... Conisini Bi.) S. Conkin, J. E. Conkin, J. E. and Conkins eB. = consternatio, Ear- landia ...... 10, 21, 26 Conway Cut siltstone 1 0\E5 001] ge Oy aaa eee ee CGOoper Ci Mis ae Coral Ridge member 141 256, 257, 275- 277, 327, 340 145 142, 143 138, 264 198, 200, 223- 227, 232, 260- 264 251, 252 337 237 226, 229, 283 200, 225, 226, 338, 339 146, 229, 263, 270, 279, 303 144 225 147 135, 136, 199, 200, 229, 233, 305, 324, 325, 327, 328 256 239 275 340 139, 293 135, 137, 224, 243, 254, 256, 264, 266, 270, 273, 300 202, 223, 243, 266, 232 198, 200, 203, 227, 273, 274 144, 318 137 146, 224, 225, 229, 231, 232, 240, 248, 246, 267, 269-271, 322, 338 Cormuspinay ee Coryell, H. N. and Rozanski, G. Crespinsiees 2 Crithionina Cumberland County, Kentucky, 22. cumberlandiae, Pro- teonina 2, 3, 19, 26 Cummings, R. H. -.:.. Cushman, J. A. Cushman, J. A. and WiatkerSs: dee eee Cuyahoga formation cyclops, Tolypam- mine), 2b, 22, 20 cylindrica, Climacam- OAT GIs Me ena Oa Cypress formation .... D Davidson County, Tennessee .............. Dawson, J. W. ......------ Deer Creek formation Derbya RET ak: ok oe ey oe JOB a OA cee Dubois County, Indiana DWN, IES ISL Seek 363 332, 000 137 135, 202, 238, 243-245, 256, 272, 276 135, 198, 200, 237-240, 242, 243 142 198, 200, 201, 224-227, 248, 249, 251-253 135, 234, 235, 256-259, 272, 275-277, 300 237, 240-242, 248, 255, 259, 275, 294, 296, 298, 308, 313, 319, 324, 325, 329, 333 255, 278, 279, 309, 327, 329. 336, 340 147, 200-202, 225, 226, 229, 232, 246, 249. 253, 263, 282, 284, 285, 288, 302, 312, 315, 316, 322, 324, 331, 339 199, 224, 301- 303 326, 327 . 142, 203, 334 146 137 293 280 223, 230, 235, 291 248 258 250, 287 E Eariandia. 136, 198, 2038, DOT 229 oo), 234, 257-259, OAT) CATs, BAY Earlandinella ...........- 272 elegans, Hyperammina 263, 265 elongata, Hyperammina ........ 254, 256, 258, 320 Bingo enacs ea T36. 13.2305 272 Endothyranella ........ 319, 320 Estill County, Kentucky, 22s 144 Eulie shale 202, 203, 269, 293, 297, 307, 312, 318, 322 expansa, Hyperam- 10.015 110 ee Hope saan Seed OS ys 261 exserta, Involu- el) os Wen eee 21, 22,26 199, 201, 223- 226, 228, 231, 286-290 THLOLU Dae eee 297 EF Pairfield County, Ohio 147 Falling Run member 141, 203, 231, 249, 251, 269, 322, 341 Farmers siltstone member = 22. 145, 225, 251 Fleming County, Kembtehkiyages eee 145, 251 Wlonyyssesy lst, day.) ceeeeane Fioyd County, Indiaman ee Floyds Knob formation 305, 327, 328 146 138, 140-143, 146, 201, 225, 226, 229, 232, 266 Franklin County, Ohi Oe 2 ee 147 Frenchburg freestone 145 fusiformis, Proteouina: =--2--.-.-- 248 G Galloway, J. J. and Ryniker, ©) -222.2 329, 330 Gazins oeCwis se 139 glabra, Hyperammina Glen Dean limestone 261, 263-265 137, 142, 203, 273, 331, 334 Glomospira 1B3(h, ME), ae 295 glomospiroides, Tre- peilopsis ..33, 23,27 199, 202, 224, 225, 314, 315, 318 Golconda limestone -. 142 gordialis, Trocham- TON ales Ne eee EO 294 Gordiammiinay) 2 294 Graham, Chas. H. -....- 139 grandis, Trepeilopsis 313 Grayson County, Kemnitucksy: 22 ee 142 Greenbrier County, West Virginia ......-- 305, 327 Greenbrier limestone Greenup County, 305, 327, 328 Keemitckcya ee 146 Grzybowski, Ji. ------.--- 329 Gutschick] R. Cy 137, 139, 324 Gutschick, R. C. and Treckman, J. F. ..... 269, 271, 282, 287, 289, 314, 316, 318, 319 gutschicki, Ammobacu- ites ee 35,23,27 199, 200, 202, 203, 224-226, 318, 321-323 H Haplophragmium ...... 318, 334 Haplostiche) y--s----.-- 275 Haldeman siltstone .. Harding County, 145, 316, 318 UMNO See 137 Hardinsburg shale .... 142 Samad SLOMeG yees- see eaeee 144 Harrodsburg limestone 233 Hemigordius ......-------- 136, 199, 203. DO) BBVA. Box} Henley shale member 225, 232, 249, 269, 285, 288, 293, 312, 316, 339 ElenisOne Gewese 266, 332 EIOMMOSiMAy co ees ee oeeeee 335 Hotehkisse Ac = 2s 139 ELV. Jig Hee eee 147, 148 Hyperammina 135-138, 198, 200, 223, 226- 228, 234, 236, 243, 253-259, 261, 265, 272, 273, 276, 281, 298, 300, 320 nee: 254 254-257, 272 Hyperamminella Hyperamminoides __. I inclusa, Ammovertella GiacAr --- 29, 23,27 199, 202, 224- 226, 309-313 Psammophis .......... 309 inflatus, Nautilus —.. 334, 335 inversa, Ammovertella 312 Psammophis .......... 308 MV OUT NN ee ee 136, 199, 201, 223, 230, 281, 285, 286 Irelands Eh Ave 295, 298, 299, 0), Bul J Jacobs Chapel shale.. 146, 231, 269, 293, 302-304, 306, 307, 318 jacobschapelensis, Toly- pammina 23, 22,27 199, 200, 224, PVA AX, 8318} HAVENS OD ID), a 139 Jackson County, Keniticky, 22.2 144, 327, 334 Jefferson County, Kempe ksyie pee 137, 140, 229, 266, 267, 270, 338, 341 johnsvalleyensis, Hyperammina __.... 261 K kentuckyensis, Hyperam- TPUETN ee eee 8,21,26 136-138, 198, 200, 201, 224- 221, 229; 22, 263-269, 273 274 Kenwood sandstone 100KS)001] 6s show oS 140, 232 Kinkaid formation... 137, 142, 201, 203, 293, 334 kunklerensis, Reophax 12, 21,26 198, 200, 228, 233,-279-281, 283 L labyrintha, Ammover- tela 225. 28, 23,27 199, 202, 225, 311 Ww ON On lachrymosa, Reophax lachrymosus, Reophax Cs Eee aeeee 13, 21,26 198, 225, 281, 282 281, 282 lagenammina ._... 248, 250-252 laocoon, Tolypammina 26,22 199, 200, 224, 305-307 Larsh-Burroak shale 293 Larue County, Kentucky: 141, 311 lens, Crithionina ___. 23 leptos, Ammobacu- UEC Sire eaeee a beeen ee 318 Lewis County, iKentuckyaee 145, 146, 278. 283 Lincoln County, Kemituie Ksyareee eee 143 GOA st ake 334 TOMUASVONGUIOM), seca 199, 223, 296 lituiformis, Trocham- 13.002 OE VA en ele Mesa Be Soe 296 Loeblich, A. R., Jr. and IPAOWO RN. JE see 285, 286 Logan formation ...... 226 longexserta, Involutina 22, 22,26 199, 201, 224, 288, 290 Louisiana limestone... 292, 304 JOA HOUOIE) sie ee UB, A, DArls= 277 M Macon County, Tennessee .............. 146 Madison County, Keemtickayaae ee 143, 144 mamilla, Crithionina 237-239 marginuloides, Stachelay == en : 337 Marion County, Kwemibui@ksyae- ee 141 WETHEAY GINeWIe- 146, 231, 253, 269 Maxville limestone.... 147, 227, 233, 249 McDonald, Donald .... 139, 284 McDonald, Mrs. Donald 139 micdonaldi, Reophax 14, 16, 21,26 198, 200, 226. 229, 280,283 MehanlanncAe Cesare 139 McKinney Knob silt- stone member 142, 143 366 Menard formation .... menardensis, Pterotocrinus Menifee County, Kentucky Merocanites Metcalfe County, Kentucky Mikhailov, A. Miliammina Miliola Millerella minutissimus, Reophax 142, 200, 201, 228, 263, 280- 284, 288 280 145 224, 271 142 327 257 331, 332 136, 137, 229, 233 284 Reophax cf. R.....21 198, 225, 280. 284, 285 mississippiana, Agatham- mina 36, 23, 27 Climacammina 41, 42, 43, 24 Trepeilopsis Montgomery County, Kentucky Noremant Wr 2. moremani, Saccammina morillensis, Hemi- gordius ....30, 28, 27 Muldraugh formation Nautilis® 2 eee Nelson County, Kentucky, 22> neoglabra, Hyperam- j00UN Ohba Ope eM ge neopupoides, Stacheia 40, 25, 27 NeumayretA: 222222052: New Albany shale... 1£9, 200, 208, 225-227, 329- 331 199, 200, 227. 233, 325-328 316 144 237, 243, 287 251, 252 199, 200, 203, 227, 233, 333. 334 143, 202, 225, 227, 229, 278, 318, 331 334 141, 229, 240, 322, 331 256 200, 224, 225, 340, 341 329 145, 223, 230, 245, 2638, 289, 293, 311 New Providence formation Nodosaria nodosaria, Bigenerina INGO Gosnell aes ee Nodulina ....... See Nueces County, Texas Nummoloculina obduxa, Spirillina _.. Ohio shale ohioensis, Trocham- MONEY eo 38, 23, 27 Olentangy shale Orbitremites Paint Creek formation 140-146, 200- 208, 224-226, 229, 231, 232, 240, 243, 246, 249, 2538, 263, 267, 269, 270, 279, 282, 283, 289, 290, 297, ° 302, 303, 310- 312, 315, 316, 318, 322, 331, 338, 339, 341 342 335 325 235, 253, 272 275 332 332 200, 226, 335, 336 230 224 142, 143, 201, 2038, 263, 273, 327, 328, 334 palaeozoica, Crithionina 19, 19 Paleotextularia Parr swe ee Pennington marine limestone shale Pennsylvanian For- aminifera Pericyclus perparva, Earlandia 198, 200, 225, 238-240 137 237, 239, 256 143 142, 200, 263 202, 240, 241, 243, 245, 252, 255, 257, 259, 272, 276, 291- 293, 295, 309 311, 312, 327, 329, 338,340 224, 271 272-274 Perry County, JGnlienaen: Soon eee ss 146, 228, 280, Sil Pike County, Ohio .... 147 pisum, Crithionina .... 239 leAhiuaawoaleyes Veda Spee 3b, 204, 200, 241-245, 255- 259, 261, 272, 213, 211, 282. 291, 292, 295 296, 320 Portwood formation 144, 200, 202, 223 Powell County, Weemitieky; 222. 144 primaparva, Ammovertella GisgrAG ee: 31, 23,27 199, 202, 224, PAS. Bl, BB} priscilla, Earlandinita 137 protea, Agathammina 330, 331 Proteonina .............-.- 135, 198, 200, 201, 223, 247. 248, 250-253 Erotoshista: 222..--2..-- 275 Psammophis .............- 308 Psammosphaera ____.. 223 Pulaski County, Nentucky.) 22s. 1s Pa) Balas 341 pupoides, Stacheia ___. 340-342 pusilla, Agathammina 330 Serpilla 22h are 329 pyriformis, Ammobaculites 318, 322 Permian Foraminifera Of Australia, 2222. 202, 237, 243, 245, 256, 259, 272, 276 R rara, Crithionina ...... 237, 243 Recent Foramini- PETA) renee er 236, 238, 239, 253, 256-259, 287, 320, 329 recurvidens, Trepeilop- Sisvees 32, 23,27 199, 202, 225, 226, 316-318 Renault limestone _.. 142 Reop hax ts 198, 234, 247, 274-278, 281 Rhabdammina? .......... 223 Isloyinan) oie Ves oe 296, 298 robusta, Bigenerina.. 325 367 Rockeastle County, Kentuchya 2-2. Rockford limestone 1435 220 ola 137, 138, 146, 202, 231, 269- PALA PAS yA INST 289, 290, 292- 296, 301-304, 306, 307, 312, Sls, S3s)y Bull. 318 rockfordensis, Hyperam- TMOMUME senha 9 21.26 136,198, 201, 223-225, 229, 230, 263, 265- 271, 296, 304, Sula}, Se Ross County, Ohio .... 147 FUO Cayman ee 334 Rothwell shale IMeMD Cree 145 220) 22s 278, 318, 331 rotundata, Crithionina 237-239 Rowan County, Get Kayne eee 145, 285 rugosa, Crithionina.... 239 S Saccammina -.2..---..--- 248, 250-252 Sie di@enale ge Is. Man 258, 273, 320 St. Louis limestone .. 221, 230 Ste. Genevieve limestone -........-..-.< Za, Zoo Salem limestone ...... 141, 142, 203, 221, 233, 200, 274, 339 Sanderson formation 141, 249, 253, 269, 322, 341 Sealarituba WpAR,, Masile AU 284 schlumbergeri, ‘COLRNUspina ee 332 Scioto County, Ohio.. 147 scorpiurus, Reophax 275 Sellersburg limestone 223 semiconstricta, Involu- Cia 20, 22,26 199, 201, 223- MPa PAI. PARE 287, 288, 290- 294 semiplana, Lituotuba 18, 22,26 199, 200, 224 225, 297 Senpuilar ak oa ee 328 Serpulelilae eee 298 368 silicea, Involutina .... 285 Silurian Foraminifera 252, 287, 307, 338 Silurian and Devonian Foraminifera 202, 243, 245, 259 Somerset shale member 141, 142, 203, 22, Zoo, 2Dd5 2638, 274, 339 sphaerica, Lagenam- AINA eaten eee eee ese sphaeroidalis, Thuram- minoides 1, 17, 18,26 135, 136, 198, 201, 202, 223- 230, 232, 200, 237, 238, 243- 247 251, 252 spiralis, Trepeilopsis 34, 23,27 199, 202, 223- 227, 314, 317, 318 SUE ina ae 285 Spirolina 2.2 eRe on 318 Stachiciav == ae 135, 200, 337- 340 stilla, Lagenammina PAIL, PASE) Stockdale, P. B. _._..... 140-146, 148, 266 Strawn shale ........._.. 240 Summerson, Chas. _.. 139 Sunbury shale .......... 147, 230, 249, 285, 293 Sumner County, Tennessee 22:22 146, 297 T Nasmanites =. 230 Taylor County, Kentucky 142 teicherti, Crithionina 243, 245 Thuramminoides 135, 238, 243, 245 Textlariay > =. eee 324 thomasi, Lugtonia _.. 276 Abolbbeshaahoanboey oe Thuramminoides 240, 241 135, 137, 198, 200, 237, 240- 243 ana 242 199, 223-226, 228, 230, 231, 298-301, 305, Thuramminopsis Tolypammina 308, 327 tortuosa, Tolypam- TANITA note 27, 28,27 199,224,307, 308 trepeilopsiformis, Stacheia ....39, 265, 27 Trepeilopsis 200, 341, 342 137, 199, 202, 223-225, 313. 314, 316, 317 135, 200, 294, 296, 334-336 Trochammina .....-.-...- Trousdale formation 144 tumidulus, Reophax.. 283 Arwen pole, oe ee 313, 314 U Underwood shale........ 243 V vagans, Hyperam- OU Ole epee ee eae ee, Oe ere 298 Vanceburg member -. 249 W Wachsmuthicrinus _.. 225 wallingfordensis, Pro- teonina ..4,5,19,26 198, 200, 201, 223, 224, 226, 227, 248-253 \Wreielolrials AN Sy Sea 327 WriatterstJierAvg ar ee 292 Wayne County, Ohio 147 \Wirelbibiimas ve e-e- eee 335 Wildie siltstone member ......-....M:-.- 143, 225, 227 Wise County, Texas.. 272 XXXII. XXXVI. XXXVII. XXXVI. XXXIX. XLil. XLIii. Volume 1 II. IV, (NOS. 129-183) 294 pps; |. 89 DIS. so socez pi. c Sos ecto seee be cllewe 10.00 Silurian cephalopods, crinoid studies, Tertiary forams, and Mytilarca. (N08. 354-189) ." (448° pp, BL Wl ihecag aces aponesecetieRinecge Devonian annelids, Tertiary mollusks, Ecuadoran stratigraphy and paleontology. (Nos.:140-445)5 400 p.519 pls h sce es ceyenacnns Trinidad Globigerinidae, Ordovician Enopleura, Tas- manian Ordovican cephalopods and Tennessee Or- dovician ostracods, and conularid bibliography. C08.) 946-154). S86 pps. /S1. psa acc te scan dich oneptenee G. D. Harris memorial, camerinid and Georgia Paleo- cene Foraminifera, South America Paleozoics, Aus- tralian Ordovician cephalopods, California Pleisto- cene Eulimidae, Volutidae, Cardiidae, and Devonian ostracods from Iowa. CN 053, 1556160).! 4127 pps, 53° ‘pis, peg To a ee ee ae etch Type and Figured Specimens P.R.I. (NO8s- 185-392). “738i ppd 35 DIB tet en tek sok appee Australian Carpoid Echinoderms, Yap forams, Shell Bluff, Ga. forams. Newcomb mollusks, Wisconsin mollusk faunas, .Camerina, Va. forams, Corry Sandstone. (No. 193). In press. (Nos. 194-198). Ordovician stromatoporoids, Indo-Pacific camerinids, Mississippian forams, rudists notes } 12.00 13.50 15.00 16.00 16.00 20.00 16.00 PALAEONTOGRAPHICA AMERICANA (Nos, 1-5). 519 pp., 75 pls. Monographs of Arcas, Lutetia, rudistids and venerids. (Nog, 6-18).. 631 po: 37 plist ON re ae 21.00 Heliophyllum halli, Tertiary turrids, Neocene Spon- dyli, Paleozoic cephalopods, Tertiary Fasciolarias and Paleozoic and Recent Hexactinellida. (Nes. 18-26)5 2 518" pp, GE) pls: cack. ci Lae Nees 25.00 Paleozoic cephalopod structure and phylogeny, Paleo- zoic siphonophores, Busycon, Devonian fish studies, gastropod studies, Carboniferous crinoids, Creta- ceous jellyfish, Platystrophia, and Venericardia. (Nos. 26-25). 128-pp.\-b8/ ples oe ye Rudist studies, Busycon 6.50 K CONDENSED TABLE OF CONTENTS OF BULLETINS OF AMERICAN ; PALEONTOLOGY AND PALAEONTOGRAPHICA AMERICANA ie BULLETINS OF AMERICAN PALEONTOLOGY E, Vols. I-VI. See Kraus Reprint Corp. ; VEE. (0.282)6780-pp-y 90 “ples ssn ie eee 15.00 — Claibornian Eocene scaphopods, . gastropods, and ' cephalopods. . ViUll-XV. See Kraus Reprint Corp. ) 16 Bast 46th St. New York 17, N.Y. XVI... -€Nos. 59-61).. 140 ppy, 48) pls.c <2. ee Venezuela and Trinidad Tertiary Mollusca. \\4 MVULy CNO8. C2968) 28S. Dy SS DIS yey. sskc seks Sw Verda Ginaghnctactentes hil 00 Peruvian Tertiary Mollusca. J RVI. :CNos, 64-67)... 286 ppi,-29) PIB. 05 Soe es eonllcee eoctbeae 11.00. G Mainly Tertiary Mollusca and Cretaceous corals. a RIX... (NO, 08) << 272 Dp},/ 24 pls oh 3 le et SE 10.00 Tertiary Paleontology, Peru. XX: (Nos. 69700)... 266 ‘pp. 26.'pisi/ cs a eae 10.00 Cretaceous and Tertiary Paleontology of Peru and Cuba. XT, ~ (Nos. 28-72) 0) -824e pp. ! 2: PISA sik enccnects eo eo 11.00 — Paleozoic Paleontology and Stratigraphy. . XX. (0s. 73-76). <856\ py,; 81 ple, nh ee 12:00 | Paleozoic Paleontology and Tertiary Foraminifera. XXII... (Nos.-77-79)-'* 2b1 'pp., 85 pls. 2c eee 10.00 Corals, Cretaceous microfauna and biography of Con- rad. d XXIV. «€Nos; 80-87). 334 -pp.,: 37 Dips as cele eee 10.50 Mainly Paleozoic faunas and Tertiary Mollusca. KXV.- (Nos. 88-94B) "306 \‘pp., 30 Dis... ke ee 10. 00 Paleozoic fossils of Ontario, Oklahoma and Colombia, Mesozoie echinoids, California Pleistocene and Mapy> land Miocene mollusks. XXXVI. (Nos. 95-100). ° 420 ‘pp., 58 ple, aa 11.00 Florida Recent marine shells, Texas Cretaceous fos- sils, Cuban and Peruvian Cretaceous, Peruvian Eo- gene corals, and geology and paleontology of Ecua- dor. XXXVI. (Nos. * 102-108). B76 Lp, SG) PIB. Sin cwccccsiesasdeculesstVoevedheaptone 12.00 Tertiary Mollusca, Paleozoic cephalopods, Devonian fish and Paleozoic geology and fossils of Venezuela. a4 XX VIEL .QW08,-109-114)., "423 “Dp. S408; occ Fits adele 12.00 Paleozoic cephalopods, Devonian of Idaho, Cretaceous and Eocene mollusks, Cuban and Venezuelan forams, XXX. .(Nos.116-146)..- 738 pp:,"'52 Dbsa 1e.,0s5 a ahs 18.00 Bowden forams and Ordovician cephalopods. WK. CONG. 117)3 563" py; 6B, Diss wasn eer eee pace oaeeer 15.00 Jackson Eocene mollusks. XE, .(NOa, 118-188) y. 458 pos BT papa sors cases nce sosedceastaseaente 12.00. Venezuelan and California mollusks, Chemung and Pennsylvanian crinoids, Cypraeidae, Cretaceous, Miocene and Recent corals, Cuban and Floridian forams, and Cuban fossil localities. BULLETINS OF AMERICAN — PALEONTOLOGY TE SE I ad eg * EEE EN AE A VOL. XLII NUMBER 197 1961 Paleontological Research Institution Ithaca, New York UiiS? A: PALEONTOLOGICAL RESEARCH INSTITUTION 1961-62 PRESIDENGT | sic cnsct Sosy ingctee ceo ah PA fea oad Yass os Haid ove eK atenhedy Muar eben JOHN W. WELLS VICE-PRESIDENT 1.4 Re A TPES ie ToT AXEL A. OLSSON SECRETARY- DREASURER 22.3) fart) ale ccothe sooty btede LAR Masa Sd eM REBECCA S. HARRIS DIRECTOR Fea NN le Po KATHERINE V, W. PALMER COUINSRE eS RICAN SS hee eS A erie ee GSD a te I ARMAND L. ADAMS REPRESENTATIVE AAAS COUNCIL (012 56cf.)lslleclectaieeteecebec th antont KENNETH E. CASTER Trustees KENNETH E. CASTER (1960-1966) KATHERINE V. W. PALMER (Life) DoNALD W. FISHER (1961-1967) RALPH A. LIDDLE (1956-1962) REBECCA S. Harris (Life) AXEL A. OLsson (Life) SOLOMON C. HOLLISTER (1959-1965) NORMAN E. WEISBoRD (1957-1963) JoHN W. WELLS (1958-64) BULLETINS OF AMERICAN PALEONTOLOGY and PALAEONTOGRAPHICA AMERICANA KATHERINE V. W. PALMER, Editor Mrs, Fay Brices, Secretary Advisory Board KENNETH E. CASTER HANS KUGLER A. Myra KEEN Jay GLENN MARKS Complete titles and price list of separate available numbers may be had on application. All volumes available except vol. I of Paleontographica Americana. Subscription may be entered at any time by volume or year, with average price of $16.00 per volume for Bulletins. Numbers of Paleontographica Americana in- voiced per issue. Purchases in U.S.A. for professional purposes are deductible from income tax. For sale by Paleontological Research Institution 109 Dearborn Place Ithaca, New York USS.A. BULLETINS OF AMERICAN PALEONTOLOGY Vol. 43 No. 197 AN ANALYSIS OF CERTAIN TAXONOMIC PROBLEMS IN THE LARGER FORAMINIFERA By W. Storrs COLE Cornell University November 10, 1961 Paleontological Research Institution Ithaca, New York, U.S.A. Library of Congress Catalog Card Number: GS 61-304 HARVARD UNIVERSITY Printed in the United States of America CONTENTS Page iN SSE Shae epee ee oe CRY me ee Ames Are eR oe eee 373 SHAG GIG UG VA Sane cece cad ee ere MR Senne aa eee oie ore ee 373 LOCA ENES - te Susan cteeno acautaac ues bl Soegeanee eee erences MSE eA CRO Meee eta aa Bene ea gee 376 CCOVETEDISSTo7avat Fo lsrs (eli Bho =e 2 oc cy D1 (MPa RSIS ee EP ae = ee Pe ene ee ee 377 WAR IAC OMBIntAds PECIESTOLa GANZCrT7A nee meee a esomneeser ate eee Reese ee 383 Variation in Lepidocyclina canellei Lemoine and R. Douvillé ..0.0..0.000..000000... 383 Pi reas CIN GNIAR Sw tae, oe ec orc ecg. eee Aik Secon nt een teas ex, dace Reasveuate eeaeaehe 383 WIE TSS alee a ae eR ato ec ea ae ner cole re mc One ee OMe cide 386 MihesspEGieSmIlIStrated scares tenes aes tec cee enc cte ter eave dais noe ae sea Se ye oo cee 389 Ralececologicaleam plications jas scseccs erases ee eee ee kee eran 391 BEES RARETERGITC Gt ectle ese tarrceerd ferk ra ee ae ere Redhead a 392 | PUES oo hm Ree Oa Oe SUR OE nee A 2 oN i SRN LE a SPR Tepe OR Seen oe 395 AN ANALYSIS OF CERTAIN TAXONOMIC PROBLEMS IN THE LARGER FORAMINIFERA* W. STorRs COLE Cornell University, Ithaca, N. Y. ABSTRACT Although the major thesis of this discourse is variation in species of larger Foraminifera, two separate, but interrelated problems are discussed. Certain defini- tions which have been published for genera of camerinids with undivided median chambers are analyzed. The conclusion is that these definitions are not valid because the types of these genera are species whose structures are the same as species upon which other generic names have been based. Variation in Lepidocyclina (Lepidocyclina) canellei Lemoine and R. Douvillé is shown, and four formerly recognized species are considered to be variants of this species. Certain inferences are drawn concerning the possible influence of environment on the variation in the struc- ture of the test of L. (L.) canelle7, Illustrations are given of most of the species which are discussed. INTRODUCTION In an earlier study (Cole, 19572) Lepidocyclina (Lepidocyclina) supera (Conrad) 1865 was demonstrated to be a synonym of L. (L.) man- telli (Morton), 1833, and L. (L.) parvula Cushman, 1919 was placed in the synonomy of L. (L.) giraudi R. Douvillé, 1907. Although L. (L.) mantelli is considered to be a valid species, proof will be given that L. (L.) giraudi is a synonym of L. (L.) canellez Lemoine and R. Douvillé, 1904. The conclusion reached is more sweeping than indicated above as several species which have become entrenched in the literature are assigned also to the synonomy of L. (L.) canellez. They are L. (L.) asterodisca Nuttall, L. (L.) miraflorensis Vaughan, and L. (L.) waylandvaughani Cole. These species are invalidated with considerable regret as they have been cited in many publications and certain of these species have been assigned either restricted geographic or stratigraphic ranges. In the interval since Vaughan (1933, p. 6) wrote “The amount of variation in many species of orbitoids is bewildering,’ evidence has accum- ulated to prove the correctness of his observation. Species of larger For- aminifera are variable! Specific names have been given to supposedly recognizable species, but new data have shown that these names have been based upon the variable form and structure of a limited number of speci- mens rather than upon a complete analysis of the available specimens which ‘should be included in the species. As many specific names designate a ‘form’ group within a variable species, they do not express a natural relationship. It is entirely possible to *The cost of the printed plates has been contributed by the William F. E. Gurley Foundation for Paleontology of Cornell University. 374 BULLETIN 197 identify these ‘form’ groups of individuals to which specific names are given. However, the problem arises that another group of specimens may have characteristics which are intermediate between two species. The tendency is to assign another specific name to such specimens, and, finally the literature contains so many specific names that one becomes bewildered. The difficulties inherent in any classification in which variability in the species is not recognized is compounded by the use of a “‘form’’ species as the type of a genus. Several generic names may be given, each of which is supposed to distinguish at the generic level either one species or a group of species from all other species. Yet, these supposedly distinct genera are based upon ecologically or otherwise controlled ‘“‘form’’ species which in reality represent only one kind of a variable species. The proliferation of generic names which have been applied to the camerinids with undivided median chambers is an example of the lack of recognition of the variability which occurs in the species of Camerima. Although the synonyms of Camerina have been discussed (Cole, 1960), additional evidence for the suppression of the superfluous generic names will be given in another section of this discourse. In the preliminary study of the larger Foraminifera entirely too much emphasis has been placed upon the concepts that the species are limited in time and space by rapid evolution and that a species can be distingushed by relative comparisons with other species. Lepidocyclina mantelli and L. supera were maintained as distinct spec- ies because L. mantelli was assumed to be restricted to the Marianna lime- stone, whereas L. swpera was supposed to be a marker for the Byram marl and related formations. Cole (19574, p. 38) demonstrated that L. supera was a synonym of L. mantelli. Previous to this he (19530, p. 6) wrote “If these localities represent the lower Oligocene, as it is known in Florida, such species as Lepidocyclina mantelli and Operculinoides dius might be expected to occur instead of Eocene species.” Later, he (19574, p. 34) could state “the L. (L.) mantelli and the L. (Eulepidina) zones should be combined.” Although the zonation of the American Oligocene proposed by Gravell and Hanna (1938, p. 987) was modified by the recognition that the stratigraphic range of L. (L.) mantelli was more extensive than had been assumed, the appreciation of variability in a species warns of the possible errors which may occur in developing zonation which is based upon ‘‘form” species. LARGER FORAMINIFERAL TAXONOMY: COLE 375 Until this study was undertaken, L. (L.) miraflorensis has been cited as a species restricted to the La Boca marine member of the Panama forma- tion (lower Miocene). If the concept developed in this discourse that L. (L.) miraflorensis is one of the synonyms of L. (L.) canellez is accepted, the supposed unique stratigraphic position of this species as the only American species of Lepidocyclina restricted to the lower Miocene will be destroyed. This is regrettable! However, in the end the problem of stratigraphic correlation may be assisted as other evidence will be sought and a zonation based on the supposed restricted occurrence of L. (L.) miraflorensis will not become entrenched in the literature. Moreover, some of the difficulties in the identification of the species will be eliminated. Under the influence of superficial appearance species have been de- fined, and, thereby, supposedly separated from other species by such state- ments as ‘Lateral chambers short . . . L. camellei’’—'‘Lateral chambers long... L. miraflorensis” (Cole, 1957a, p. 33). On the other hand a plea of convenience is often made in statements such as the following: ‘“These species certainly cannot be separated generically since their specific in- dependence is in question, but one resembles Operculina while the other resembles Assilina. The latter name is nowadays reserved for Paleocene and Eocene species which form a distinct lineage, so it is convenient to assign both Recent species to Operculina’ (Smout and Eames, 1960,p.111). Such statements as those quoted which were selected for illustrative purpose from a multitude of similar expressions must be baffling indeed to anyone attempting taxonomic and stratigraphic research. Are not those of us who are engaged in this kind of research defeating our purpose when we attempt to separate species on preconceived ideas of how much 1n- dividuals within a species vary, or by a defense of some long established generic or specific name? Although it has been logical to define species and genera in relative terms when our data were limited, this condition no longer exists with the progress that has been made in the study of larger Foraminifera. There will be some who object in a serious and conscientious manner that the thesis of this discourse is incorrect, and that the combinations of species proposed is absurd. To some the stellate pattern of L. (L.) astero- disca far overbalances the internal structure of these specimens, Therefore, they will maintain L. (L.) asterodisca, as I have done in the past, is a separ- ate species characterized by its stellate outline. 376 BULLETIN 197 Others, however, will agree that the internal structure of L. (L.) asterodisca and L. (L.) waylandvaughani is so similar that these two species should be united, the more so because some topotypes of L. (L.) wayland- vaughant have an irregular outline (see: Cole, 1928, fig. 1, pl. 35) al- though these irregular specimens occur infrequently in collections from the vicinity of Tampico. But, these same persons who accept the identity of L. (L.) asterodisca and L. (L.) waylandvaughani will object to combining these names under L. (L.) canellei. ‘The superficial appearences of the vertical sections of L. (L.) waylandvaughani are indeed different from those of L. (L.) canellez on first inspection. But, detailed study of the illustrations given here and elsewhere should demonstrate that the fundamental internal structures are the same. One is influenced at first by the thinner floors and roofs of the lateral chambers in the so-called typical specimens of L. (L.) canellez. However, as the specimens are studied in detail these thinner floors and roofs become insignificant and the overall structural similarity becomes apparent. It is more impressive to have a long list of species from a given locality than to have one with few species. There is no objection to this except one begins to believe that identifications can be made with certainty and, therefore, assigns certain species, at least, to restricted geographic or stratigraphic positions. Such may be the case with regard to some species and some genera. It is not implied here that the time tested and well- known species and genera are not restricted geographically and_ strati- graphically. But, until species and genera are evaluated rather completely, caution must be used. Above all the natural relationships should be established by a consideration to the limit of our data regarding variability which may occur in individuals because of environmental conditions or because of genetically controlled plasticity. The specimens used in this study are deposited in the Cole collection at Cornell University and eventually will be transferred to the U. S. National Museum. LOCALITIES Cuba Loc. 1—Northwest of Cienfuegos, one kilometer on Palmira road at Pueblo Grifo, Santa Clara Province (Palmer sta. 336-see: Palmer, LARGER FORAMINIFERAL TAXONOMY: COLE ST 1948, p. 299) ; gift of the late Mrs. D. K. Palmer. St. Lucia, Windward Islands, West Indies 2—La Titance, Lavoutte (sta. 6138); P. H. Martin-Kaye, collector. Mexico (Tampico Embayment area) 3—Five miles west of La Laja on the road to Ozulama at Bajada de Chichimeca, State of Vera Cruz (Huasteca Petroleum Company no. J 24-1462) ; W. S. Cole, collector. 4—Between kilometer posts 17-18 on the Aguila Petroleum Company’s narrow-gauge railroad between Potrero and Tanhuijo, State of Vera Cruz (sta. S. C. M-S 1); W. S. Cole, collector (reference: Cole and Gillespie, 1930). 5 —Quarry on the Huasteca Petroleum Company’s golf course opposite Tampico, State of Tamaulipas; bed of sandy clay overlying massive sandstone (sta. SC 3ABA); W. S. Cole, collector (ref- erences Coley 1928" pP221-223.pl.4) 6—Cut on the Panuco River side of a street below the Palacio Penal in Tampico (sta. SC 1000) ; W. S. Cole, collector. 7—About 700 feet from the station Andonegui on the electric trolley line between Tampico and Miramar (sta. SC 111); W. S. Cole, collector. 8—Arbol Grande near Tampico (sta. SC 1C) ; W. S. Cole, collector (reference: Vaughan, 1933, p. 15, 25, 26). Panama Canal Zone 9—Low garden islet 0.25 miles northeast of landing at Barro Colorado Island; soft sandy calcareous siltstone (sta. 53) ; S. M. Jones and W. P. Woodring, 1947, collectors (reference: Cole, LO530, ps 6): CONFUSION IN DEFINING A GENUS In a review of certain genera of the camerinids Cole (1960, p. 190) wrote” ... there are only two valid genera of all those that have been pro- posed for camerinids with undivided chambers. They are Camerina and Miscellanea.’ He (Cole, 1960, p. 196) emphasized that “.. . There are no structural differences which may be used to distinguish between Camerina, Planocamerinoides (=Assilina of authors), Operculina, Operculinoides, Ranikothalia and Paraspiroclypeus. These genera have been defined in terms of intergradational features which are specific rather than generic diflerences.”’ 378 BULLETIN 197 In 1953 Eames (p. 390) had defined Operculinella Yabe (1918, p. 126) as follows: “. . . miniature Nuwmmulites-like forms of small size, with a very small megalospheric nucleoconch, with little difference in size between the two generations, with or without a tendency to flare in old age.” Later, Eames ef al (1960, p. 448) wrote “Palaeonummutlites Schu- bert 1908 (type species Nwmmulina pristina Brady 1874) is regarded as a prior synonym of both Operculinella Yabe 1918 and Operculinoides Han- zawa 1935.’ Finally, Smout and Eames (1960, p. 112) stated: “. . . The genus represented by Operculinella is, however, an important one.” If the genus Palaeonummulites (=Operculinella and Operculinoides) is to be maintained to include certain species of camerinids with undivided chambers, the species included in this genus should conform to the defini- tion of the genus, and it should be possible to separate this group of species from other groups of species. The critical criteria given in the definition of Operculinella cited are: 1. Miniature Nwmmulites-like forms; 2. The small size of the embryonic chambers; 3. The size relationship between the megalospheric and micro- spheric generations; and 4. The tendency to develop a flange in the terminal whorl. These criteria to be valid must stand against data from different species. Four species are chosen for the analysis although others could be added or substituted for those selected. The type species of Operculinella is “Nummulites” cumingii (Carpenter) [—Camerina venosa (Fichtel and Moll) }. Operculinoides was based on “Nummulites’” willcoxi Heilprin. Therefore, these two species were selected. The American species ““Operculinella’ cojimarensis D,. K. Palmer (1934, p. 259) from the Cuban Miocene is one of the species which most nearly resembles the type of Operculinella, therefore it was chosen. Finally, Camerina pengaronensis (Verbeek) from the Eocene of the Indo- Pacific region was selected as this species has been assigned traditionally to Nummulites (=Camerina). The comparison can be made best in tabular form (Table 1) in which the critical statements in the definition of Palaeonummulites (=Opercu- linella) are contrasted with data from the selected species. As all the species are “minute Nwmmulites-like forms’ this statement is not used in the table. The species cojimarensis does not conform to the definition given of Palaconummutlites because the microspheric specimens are at least twice the 379 COLE LARGER FORAMINIFERAL TAXONOMY: "€8z ‘d ‘ZE61 “YuruIoog :¢¢Z ‘d ‘gLC6L ‘AJOD JV + gi "PLz “4 “98C6L SICC6L “JOD JaIFV *87 ALI _q UO payensny]i suaumdads '6¢7 ‘d ‘peel ‘Iawyeg Yq TIAV z ‘ZOE “d “6C6L ‘JOD Joisy 1 asury asury asury yno aduvy yno jNOyW A oy A “YIM JO YU “YM JO UWA [FoyM [euTWIS 0°6-0°9 0'9-1'S 71-6 OE WU rss (suaumdads disaydsoisrw) sJajawerq OCE-0€ET OLTZ-OF1 OZ O€ 1-06 Dag gies a ec sJaquivy> dtuoAIguIa dJadsoyesau Y}OG ssOIdv adUL}sIP [PUIO}UT O'b-O'¢' 65-97 GiGia Pr-O? wu (suaurads dtraydsoyesau) Joyoweiq gSiSuauowwsuad eiXOI ppm esesuadspultlor wsouad DULAQUD Saprournasad o) (OG O yjournssedO UOT}IUYSpP UT s}UIUID}e}g 20} pausisse AjIaWwIOJ sardadg sprurtawed Jo sardads payzdajas Jo uostsedwioy— T 2[quy, 380 BULLETIN 197 size of megalospheric specimens, yet in other respects it is similar to the type species of Operculinella, However, some megalospheric specimens do have a diameter greater than any specimens of “Operculinella’ venosa which I have examined. Therefore, this species may be so large that it can not be considered ‘‘miniature.”’ “Operculinoides” willcoxi, the type species of Operculinoides which is stated to be a synonym of Palaeonummulites, more nearly resembles Camerina pengaronensis than it does “Operculinella’ venosa or “O.” cojimarensis. This brief analysis is indicative of the problems which arise in attemp- ting to group the species of camerinids into genera when the definition of the genus is stated in relative terms. It should be reemphasized that “These genera have been defined in terms of intergradational features which are specific rather than generic differences’ (Cole, 1960, p. 196). From the data available it seems impossible to develop definitions bas- ed upon distinctive structures of the test which would serve to separate these four species into readily recognizable genera. Therefore, it would seem reasonable to include them in one genus, a grouping which would em- phasize the relationship of the species to each other and which would separ- ate this group of species from all other groups of species whose tests had different structures. Drooger (1960, p. 312) in reinstating the genus Ranikothalia Caudni, 1944, attempted to demonstrate that the test of species which he assigned to this genus did have structures which were different, if only in degree, than those of other species of camerinids. Although this approach is the sound one, it may lead to serious error unless it can be demonstrated that the structures differ sufficiently to be distinctive. Cole (1953c, p. 32; 1960, p. 192) demonstrated that the struc- ture of the test of species assigned to the genus Rankothalia was similar to that of species referred to Camerina. ‘Therefore, he placed Ranikothalia among other generic names in the synonomy of Camerina. Drooger (1960, p- 312) in reinstating Ranikothalia wrote (p. 314): “Cole (1953, p. 10) is perfectly right in stating that the difference between Ranikothalia and other nummulitic genera is one of degree.” Drooger (1960, p. 314) advanced the argument that ‘.. . the pres- ence of the coarse canal system, completely open to the exterior both of the marginal cord and through the double row of coarse pores along the sutures...” as well as the stratigraphic distribution of the species assigned LARGER FORAMINIFERAL TAXONOMY: COLE 381 to Ranikothalia were additional reasons for recognizing this genus. As Lrooger (1960, p. 314) pointed out “. . . such sutural openings, though of much thinner structure, were described and figured already by Carpenter (1862, p. 259, pl. 17) for recent Operculina specimens.” Barker (1939, p. 309) obtained “. . . Canada-balsam preparations of Camerina variolaria (Lamarck) that show excellently developed vertical canals in the bosses of clear shell material in the umbonal area. . .” Cole (1953c, fig. 10, pl. 2) has shown that the marginal cord of Camerina variolaria (Lamarck) 1s as coarse and as completely open to the surface as that of Camerina planulata (Lamarck) (Cole, 1960, fig. 4, pl. 23), a species which he (1960, p. 195) decided was the same as “Nawmmu- lites’ nuttalli Davies. He placed “Nummutlites” nuttalli in the synonomy of C, planulata. In Europe C. planulata occurs in the lower Eocene, whereas C. vario- laria is found in the upper Eocene. As the structure of C. variolaria is so similar to that of C. planulata, it would seem reasonable, if the genus Ranikothalia is to be maintained, to assign both of these species to that genus. Another of the arguments for retaining the generic name Ranikothalia given by Drooger (1960, p. 314) was “. . .the species are restricted in time (Paleocene—? Early Eocene) and space (southern Asia, Togoland, Caribbean)”’. However, it would appear that C. variolaria belongs to the same group of species as does C. planulata. If this is accepted, the range of this group of species would be Paleocene to upper Eocene at the minimum, thus the argument that Rankothalia is confined to the lowermost Tertiary would be invalidated. If criteria, such as the size of the embryonic chambers, the number of nepionic chambers, the total size of the test, the size relationships of the megalospheric and micospheric specimens and similar relationships were to be applied to the species of the genus Cycloclypeus, this genus would have to be split into several genera. In so doing a subjectively derived, artificial set of generic names would result which would destroy the unity given by one generic name. Moreover, many species would have to be assigned arbitrarily to one or the other of the genera defined in such artificial and relative terms. Two subgenera of the genus Cycloclypeus have been proposed, but these subgenera have been defined as possessing different structures than BULLETIN 197 o>) CO bo those of Cycloclypeus (Cycloclypeus). Radiocycloclypeus was based upon stellate specimens and Katacycloclypeus was defined as possessing con- centric, anrular, thickened rings upon the surface of the test. It may be questioned, however, whether these structures are of sufficient magnitude to warrant subgeneric rank as the internal structure of these specimens is identicial to that of specimens assigned to the subgenus Cycloclypeus. These superficial modifications could be considered to be specific characteristics rather than subgeneric ones. Tan (1932, p. 71) in discussing Cycloclypeus (Cycloclypeus) indo- pacificus stated ‘These annuli appear to be either rows of large pillars (Pl. XX, fig. 6) or irregular folds (vide Douvillé’s fig. 6 on Pl. V) which never attain the same regularity and continuity as with Katacycl. annulatus.” In studies (unpublished) which I have made of Cycloclypeus collected on Guam, I had difficulty in attempting to separate certain specimens on the presence or absence of the annular folds into subgenera and had to rely on thin sections by which Cycloclypeus annulatus could be recognized readily and distinguished from other species. As Cycloclypeus annulatus 1s a typical representative of the subgenus Katacycloclypeus, the presence or absence of the annular folds should be so constant that specimens could be identified subgenerically without the difficulties encountered. Cole (1960, p. 198) suggested that in genera, such as Camerina and Cycloclypeus, the phylogenetic relationships are best expressed by indicating lineages within the genera rather than attempting to use either subgeneric or different generic names for species which differ in degree, but not in fundamental structure, from other species. If this suggestion is followed, a natural, but flexible, classification results, and the confusion entailed by arbitrarily assigning species to genera which have been defined in relative terms is eliminated. Stratigraphic correlation based upon species is not only more accurate but also less liable to error than that based upon generic ranges. Although it is accepted that genera have longer stratigraphic ranges than do species, it is not appreciated by many stratigraphers that certain of the so- called index genera are recognized by subjectively determined definitions. Therefore, a certain supposedly stratigraphically restricted genus may have a longer range in geologic time than implied because species which should be included in this genus are assigned to another genus. It is easier to recognize species such as Camerina catenula (Cushman and Jarvis) (Cole, 19584, p. 270) than to decide to which genus this LARGER FORAMINIFERAL TAXONOMY: COLE 383 species should be referred if multiple generic names for camerinids with un- divided median chambers are maintained. This species has been assigned by competent authorities to Miscellanea, Operculinoides, Pellatispirella, and Camerina. It is remarkable that specimens of this species of the kind illustrated by Cole and Herrick (1953, figs. 6, 15, 16, pl. 4 among others) have not been assigned by someone to Operculina, If this had happened, C. catenula would have been assigned at one time or another to three genera which are synonyms of Camerina as well as to two genera which are not synonyms of Camerina, VARIATION IN A SPECIES OF CAMERINA Although variation in species of Camerina has been discussed recently by Cole (1961: see also papers listed in this reference on p. 123, 124) additional illustrations are given of Camerina dia (Cole and Ponton) on Plate 29 as individuals of this species vary greatly especially as viewed in transverse section. The specimen illustrated by figure 4, Plate 29 is compressed, whereas the specimen illustrated by figure 5, Plate 29 is inflated. If only these two specimens were available, it is easy to understand how they could be assum- ed to represent two distinct species. However, the specimen illustrated by figure 2, Plate 29, is intermediate between the other two specimens. If time had been available, it would have been possible to prepare a series of illustrations which would form a completely integrated series. However, the evidence as presented here and elsewhere seems to sub- stantiate the synonomy given for this species (Cole, 19584, p. 270). VARIATION IN LEPIDOCYCLINA CANELLEI LEMOINE AND R. DOUVILLE THE SPECIFIC NAMES Lepidocyclina (Lepidocyclina) canellei Lemoine and R. Douvillé (1904, p. 20) was described from specimens collected at Pefa Blanca, Panama Canal Zone. This locality on the Rid Chagres was submerged by Gatun Lake, but abundant specimens of this species can be obtained from many localities in this area which are above the level of the lake (Wood- ring, 1958, p. 24). The type locality of this species is assigned by Wood- ring (1957, p. 29, 117) to the middle member of the Caimito formation of Oligocene age. Recently, Cole (19534, p. 18) redescribed and illustrat- ed this species. 384 BULLETIN 197 L. (L.) canellei has been reported elsewhere from Venezuela (Gravell, 1933, p. 24), Jamaica (Vaughan, 1928, p. 290; Cole, 1956, p. 213) and Trinidad (Vaughan and Cole, 1941, p. 70). Vaughan (1933, p. 15) re- ported a “dwarf variety of L. canellei at Arbol Grande station, near Tampico.” Vaughan (1928, p. 292) named specimens from Jamaica L. (Lepido- cyclina) matleyi, a species which Cole (1956, table 3) considered to be a synonym of L. (L.) canellez, Vaughan and Cole (1932, p. 510) gave the name L. (L.) pancanalis to small specimens from U. S. G. S. loc. 6025, a locality formerly known as Bohio Ridge Switch, Panama Canal Zone. They reported that L. pancanalzs occurred also in Antigua (Vaughan and Cole, 1932, p. 511) and in Trinidad (Vaughan and Cole, 1941, p. 71). Later, Cole (19534, p. 18) decided that L. (L.) pancanalis was based on small specimens of L. (L.) canellei and was another synonym of L. (L.) canellez. R. Douvillé (1907, p. 307) described L. (L.) giraudi from specimens obtained from the Oligocene of Pointe Macabou and vicinity, Martinique, French West Indies, where it was associated with Spiroclypeus bullbrooki Vaughan and Cole (1941, p. 54), the only species of Sproclypeus known to date from the Americas. Vaughan and Cole (1941, p. 71) found L. (L.) gzraudi in Oligocene sediments in Trinidad where it was associated with Spiroclypeus bullbrookt. In Trinidad these two species are associated with Heterostegina antillea Cushman, Lepidocyclina (Eulepidina)tempanii Vaughan and Cole (=—L. (E.) tournoueri Lemoine and R. Douvillé), L. (E.) wndosa Cashman and L. (E.) yurnagunensis Cushman. Vaughan and Cole (1941, p. 120) noted that certain specimens from Trinidad which they referred to L. (L.) giraudi “might without great impropriety be referred to L. parvula Cushman.” Cushman (1919, p. 58) described a species from the Oligocene of Antigua to which he applied the name Lepidocyclina parvula. Vaughan (1933, p. 16) discussed this species in detail and described (1933, p. 17) from Arbol Grande near Tampico, State of Tamaulipas, Mexico, and several other Mexican localities, a variety which was named L. parvula crassicosta Vaughan and Cole. In 1928 Cole (p. 21) named specimens found in a quarry on the golf course of the Huasteca Petroleum Company opposite Tampico L. (L.) waylandvaughani, Naaghan wrote Cole (1928, p. 22) concerning these specimens: “It appears to me to be more closely related to L. parvula LARGER FORAMINIFERAL TAXONOMY: COLE 385 Cushman, but that species is usually thicker through the center, even to being inflated and the papillae are coarser. However, there is a tremendous amount of variation. Since I have not yet reached a positive decision regarding what to do with the form I hesitate to advise you. Because of the two differences above mentioned, I should hesitate to apply the name parvula to it, but the form runs very close to the flatter varieties of parvula.” At this same locality Cole (1928, p. 22) found microspheric speci- mens in association with L. (L.) waylandvaughani which he identified as Lepidocyclina aff. L. morgani Lemoine and R. Douvillé. Vaughan (1933, p- 16) assigned these specimens to L. (L.) parvula, but at the same time he (1933, p. 13) accepted L. (L.) waylandvaughani as a valid species. Cole (1945, p. 30) accepted this revision by Vaughan in which the megalospheric specimens from this locality at Tampico were assigned to L. (L.) waylandvaughani, whereas the associated microspheric specimens (Cole, 1945, fig. 9, pl. 7) were referred to L. (L.) parvula. Still another specific name was introduced when Vaughan (1927, p. 4) gave the name L. (L.) miraflorensis to certain specimens from the Panama Canal Zone which Cushman (1918, p. 93) had misidentified as L. (Ezle- pidina) vaughani. Cole (1953a, p. 333) studied topotype specimens of L. (L.) muraflorensis and published several new illustrations. Woodring (1960, p. 29) has remarked that “The still younger La Boca marine member of Panama formation, also assigned to the early part of the early Miocene, contains the last species in the Canal Zone: two lepidocycline species L. miraflorensis and L. parvula (Cole, 19534). L. parvula later was synonymized with L. giraudi (Cole, 1957a, p. 41). The Culebra and La Boca species of Lepidocyclina also occur in late Oligocene formations in the Canal Zone, with the exception of L. miraflorensis.” Nuttall (1932, p. 34) described a stellate species from the Alazan formation (Oligocene) of the Tampico Embayment area of Mexico as L. (L.) asterodisca, Gravell and Hanna (1937, p. 528) found stellate spect- mens in cores from the Anahuac formation (Oligocene) from a well in Texas which they named L. (L.) texana. Cole (19534, p. 18) combined these two species, and later discussed and illustrated (19584, p. 201) additional specimens from Cuba. Thus, the specific names L. (L.) asterodisca, L. (L.) canellei, L. (L.) giraudi, L. (L.) miraflorensis, L. (L.) parvula and L. (L.) wayland- vaughani became established. However, in a study of the variation which may occur in species of Lepidocyclina Cole (19574, p. 41) demonstrated 386 BULLETIN 197 that L. (L.) parvula was a synonym of L. giraudi, a conclusion which was accepted by Grimsdale (1959, p. 28). At the present time six species, as L. (L.) mantelli must be included, of Lepidocyclina (Lepidocyclina) are recognized as occurring in the Americas above the top of the Eocene. The thesis developed in the next section of this discourse is that there are only two species of the subgenus, L. (L.) canelles and L. (L.) mantelli, in the Americas. L. (L.) asterodisca, L. (L.) givaudi, L. (L.) mira- florensis and L. (L.) waylandvaughani are synonyms of L. (L.) canellei as they were based upon selected “forms’’ within a variable species. VARIATION It has long been known that L. (L.) asterodisca, except for a stellate pattern, is similar in equatorial section to specimens referred to such species as L. (L.) giraudi and L. (L.) waylandvaughani. As a stellate pattern has been assumed to be a specific charater in the genus Lepidocyclina, it was possible to prepare a key for the recognition of the species in which this feature was used (Cole, 19574, p. 33). In the use of this character the internal structures were ignored. In addition, the other Oligocene species assigned to the subgenus Lepidocyclina were placed in the key on the characteristics of the vertical sections as it was admitted that all of these species had similar, if not identical, equatorial sections. Since that time certain problems have arisen which cast doubt on the validity of this key, and, thereby, on the species which the key was assumed to differentiate. As additional thin sections were prepared and studied, it became apparent that L. (L.) asterodisca, L. (L.) canellei, L. (L.) giraudi, L. (L.) miraflorensis and L, (L.) waylandvaughani were one species. The various specific names were based upon the superficial “form” of certain specimens rather than upon an analysis of the basic structures of the test. Moreover, environmental factors influence the development of the test. Therefore, one kind of test normally predominates at a given locality. At locality 4 many of the specimens (figs. 1, 4, Pl. 30; fig. 2, Pl. 34) are similar to the types of L. (L.) parvula Cushman (1919, figs. 3-7, pl. 3) (=L. (L.) giraudi), whereas at locality 5 the specimens (fig. 9, Pl. 30; figs. 2, 6, 7, Pl. 38; figs. 1, 3, 9, Pl. 39) which are topotypes of L. (L.) waylandvaughani have an appearance which is distinctive and at first glance different from those at locality 4. Moreover, the small to medium size specimens at locality 5 are so similar to L. (L.) canellei that Vaughan (1933, p. 15) considered them to be a dwarf variety of that species. LARGER FORAMINIFERAL TAXONOMY: COLE 387 At locality 1 specimens (fig. 2, Pl. 30) occur which are the same as the types of L. (L.) waylandvaughani and other specimens (figs. 5, 6, 13, Pl. 30) are identical with L. (L.) parvula (= L. (L.) giraudi). The mi- crospheric specimens (fig. 3, Pl. 36) at locality 5 had been referred to L. (L.) parvula (=L. (L.) giraudi) although the associated megalospheric specimens had been named L. (L.) waylandvaughani, Thus, in one population (loc. 4) the megalospheric and microspheric specimens had been assigned to the species L. (L.) parvula (=L. (L.) giraudi). At a second locality (loc. 5) the megalospheric specimens had been named L. (L.) waylandvaughani, whereas the microspheric specimens had been referred to L. (L.) parvula (=L. (L.) giraudi). At the third locality (loc. 1) both species seemingly are present. Although there are inconsistencies in this terminology in referring megalospheric and microspheric specimens to different species, it might still be possible that there are several distinct species. Therefore, numerous thin sections were made and other localities were studied. Specimens (figs. 1, 3-7, Pl. 34) from locality 3 were first identified as L. (L.) miraflorensis because of their size, shape, and the open, regularly aligned lateral chambers (fig. 7, Pl. 34). But, other specimens (fig. 3-5, 7, Pl. 34) from this sample which seemingly contained only one species of Lepidocyclina were similar to topotype specimens of L. (L.) wayland- vaughant. Additional thin sections (figs. 4-8, Pl. 39) of L. (L.) canellez from locality 9 were prepared to supplement those already published (Cole, HOSS petites. i3) 41216, pl. 16). The vertical sections which are illustrated can be grouped into species by superficial form as follows: 1. L, (L.) canellez Lemoine and R. Douvillé Plate 30, figures 8, 9; Plate 38, figures 2, 7; Plate 39, figures 3-6 8, 9. 2. L. (L.) giraudi R. Douvillé Plate 30, figures 1, 4, 5, 6, 10, 12, 13; Plate 34, figures 2, 8; Plate 36, figure 3; Plate 37, figure 3; Plate 38, figure 1. 3. L. (L.) miraflorensis Vaughan Plate 34, figure 7. 4. L. (L.) waylandvaughani Cole Plate 30, figures 2, 3, 7, 11; Plate 34, figures 1, 3-6; Plate 38, figures 3, 6; Plate 39, figures 1, 2. 388 BULLETIN 197 Admittedly, this is a subjectively determined listing as such features as the strength of the pillars became the critical feature upon which the specimen was assigned to a given species. The specimen illustrated as figure 1, Plate 38 (L. giraudi kind) has the same internal structure as does figure 4 of this same plate except it is more inflated and the pillars on one side are stronger. Figure 3, Plate 38 is almost identical with figure 1, Plate 39 (a topotype of L. wayland- vaughani) except the roofs and floors of the lateral chambers are slightly more curved in figure 1, Plate 39 than they are in figure 3, Plate 38. Other topotype specimens (Cole, 1952, figure 10, plate 18) of L. (L.) wayland- vaughani have lateral chambers with straight roofs and floors. Thus, it seems logical to group these specimens under one specific name rather than two as the specimen illustrated as figure 4, Plate 38 is intermediate between the other two specimens. If illustrations of L. (L.) miraflorensis (Cole, 1953, pl. 43) are compared with those given of L. (L.) canellei on Plate 39, it will be observed that the internal structure of those two species is the same. Like- wise, specimens such as those illustrated by figures 3, 9, Plate 39, have the same internal structure as L. (L.) canellei does. But, specimens such as those illustrated by figures 8, 9, Plate 30 are intermediate between L. (L.) canellei and L. (L.) waylandvaughani. Cole (19584, p. 201) has given a number of illustrations of equa- torial and vertical sections of L. (L.) asterodisca. If these are compared with the illustrations given in this article, it will be observed that the internal structure of this species which was named because of its stellate pattern is the same as specimens assigned to L. (L.) canellez, The first com- parison should be between the specimen illustrated as figure 3, Plate 38, and the one shown as figure 10, plate 23 (Cole, 19582). In the study (Cole, 19582) of L. (L.) asterodisca it was found that the associated microspheric specimens where not stellate, only the megalo- spheric specimens developed the stellate pattern. Another pair of species should be mentioned in this connection. They are L. (Eulepidina) tournoueri Lemoine and R. Douvillé (figure 5, Plate 32) and L. (Eulepidina) dartoni Vaughan (Cole, 19534, figures 1-8, plate 19). Except for the stellate pattern, it is impossible to separate these two species. They should be combined under the name L. (E.) tournoueri. It should be recognized that in Lepidocyclina the stellate pattern is produced LARGER FORAMINIFERAL TAXONOMY: COLE 389 only by certain individuals, probably under the influence of ecological conditions, and that this pattern is not genetically produced. Therefore, it does not have value as a specific character. Specimens assigned previously to the species L. (L.) asterodisca, L. (L.) canellei, L. (L.) giraudi, L. (L.) miraflorensis and L. (L.) waylandvaughani have identical equatorial sections. The species, therefore, have been recognized by differences in the shape of the test and by the structure observed in the vertical sections. Although L. (L.) mantelli (Morton) (Cole, 19574, p. 38) has a similar equatorial section to that of L. (L.) canellei, the vertical section 1s markedly different. In L, (L.) mantelli the lateral chambers have notice- ably thick roofs and floors, the chamber openings are slitlike, and they are never in alignment. Therefore, L. (L.) mantelli is retained as a valid species. The supposed differences used in the recognition of these species are summarized in Table 2. Such differences as do appear can be more readily interpreted as the result of individual variation in most cases produced by ecological rather than genetically produced structures, Moreover, it has been well established that all of these supposed species have the same stratigraphic ranges. The only useful purpose in retaining different specific names would be to define populations developed under different ecological conditions. However, any advantage so gained would be offset in concealing the fact that only one species was present at the different locilities. Moreover, the usual concept of a species would be violated. THE SPECIES ILLUSTRATED Many of the specimens illustrated have been mentioned already in the text. However, other specimens which may not have been mentioned are included in the illustrations for completeness and may be useful in making additional comparisons. With the exception of localities 4 and 9 all the species of larger Foraminifera found at the other localities are illustrated. Cancninceo jimarcns7 tn (ON KeyPalmen yy wee) aot see eae nok Plate 28 dia Cole sandePontom) te i: aces ne ea erates eee Plate 29 BULLETIN 197 390 AyrrepnZaq1 aWOS yoryy AjayeIspoyy 13]J2UvI "TT YIM [eoTUAPT Aylie[NFaIIT IUIOS ypry} Ajoyerapoyy Iypnsoy Uy (ubqsnvapurjidem "TJ YyAs [eoTWUap] jUNWUSITy s1OOH pur sjooy STIQUIVYD [PIO}eT ]]Jews ‘May Je[NIUs] passaidwoy | supgsuvapuvjrn ]Jews ‘Maz qepNoyUs] passardwoD | S1suasoyfPatul asiey ‘Aur JypNINUST payepyuy ipnrus [Jews ‘Ma7 | TepNdjUe] pajepuUr 0} passardwioy | 121{auvI [Jews “MoT 37] [93S vosiposajsy ("J) “7 “send ae ez ‘ sapeds aa saidads ay} UdaMjoq saduatayIp Jolepy—Z IqVL LARGER FORAMINIFERAL TAXONOMY: COLE 391 Lepidocyclina (Lepidocyclina) canellei Lemoine and R. Douvillé . . . Plate 30; Plate 31; Plate 32, figures 1-4; Plate 33; Plate 34, figures 1-8; Plate 35, figures 1, 2, 4, 5; Plate 36; Plate 37; Plate 38 (Eulepidina) tournoueri Lemoine and R. Douvillé . . . Plate 32, figure 5; Plate 34, figure 9; Plate 35, figure 3. PALEOECOLOGICAL IMPLICATIONS At locality 1 there were abundant specimens of Camerina dia in association with a modest number of specimens of Lepidocyclina (Lepido- cyclina) canellei. At locality 3 there were abundant, large size specimens of L. (L.) canellei and a modest number of specimens of C. dia, or just the reverse of the situation at locality 1. At locality 4 Heterostegina antillea in modest numbers occurred with rare specimens of C. dia and numerous specimens representing two species of Lepidocyclina, L. (L.) canellei and L. (E.) undosa. At localities, such as locality 5, L. (L.) canellei in abundance was associated with numerous specimens of Streblus mexicanus mecatepecensis (Nuttall) and Elphidium. At locality 9 L. (L.) canellei in abundance occurred with Msogypsina antillea (Cashman) and other species of Lepidocyclina. However, camer- inids were not found at this locality. These associations suggest that ecological controls were operative to some extent. Cole (1957, p. 751) had written “‘, . .Heterostegina te- quire(s) warm, shallow protected situations. Operculina (—Camerina) favors partly protected conditions, but is more tolerant of greater depth and lower temperatures.” Elsewhere he (Cole, 1959, p. 354) stated “The average depth at which Heferostegina occurred in the vicinity of Bikini and the Philippine Islands was 25 to 32 fathoms.” Bandy (1960, p. 11) wrote, ‘Most rotaloids with pillars are inner shelf inhabitants, as represented by the cosmopolitan Srreblus. . . Streblus is euryhaline and eurythermal whereas the others mentioned are steno- haline and stenothermal.” The abundance of Streblus and Elphidium at locality 5 as well as the character of the sediments, massive cross-bedded sandstones between which occur thin, fossiliferous beds of sandy clay, suggest that these sediments accumulated in shallow water in a somewhat protected situation such as a large bay. This is the environment suggested for such localities as 1, 3 392 BULLETIN 197 and 5 of which locality 5 represents the shallowest environment with the most variable conditions and locality 3 represents the deepest environment of these three localities. In contrast to these localities the sediments at locality 9 in which Miogypsina occurred with Lepidocyclina, but without camerinids seemingly were deposited in waters which were too deep or too cold for the camer- inids. The faunal association at locality 4 is suggestive of conditions which represent intermediate conditions, probably those which occur near the lower limit of the ecological controls favorable to the camerinids. Specimens of L. (L.) canellez with weak pillars and thin floors and roofs of the lateral chambers would be those of the deeper environments, whereas specimens with larger pillars and thicker floors and roofs of the lateral chambers would represent kinds which inhabited shallower and probably warmer water. Stellate specimens of L. (L.) canellez are associat- ed commonly with abundant specimens of Heferostegina, and seemingly are developed in the situations which are optimum for the development of Heteroste gina. LITERATURE CITED Barker, R. W. 1939. Species of the foraminiferal family Camerinidae in the Tertiary and Cretaceous of Mexico. U. S. Nat. Mus., Proc., v. 86, No. 3052, p. 305- 330, pls. 11-22. Bandy, O. L. 1960. General correlation of foraminiferal structure with environment. Internat. Geol. Congress, Session 21, Pt. 22, p. 7-19. Cole, W.S. 1928. A foraminiferal fauna from the Chapapote formation in Mexico. Bull. Amer. Paleont., v. 14, No. 53, p. 203-231, pls. 32-35. 1945. Stratigraphic and paleontologic studies of wells in Florida—No. 4. Florida Geol. Surv., Bull. 28, p. 1-160, 22 pls., 8 text figs. 1953a. Some late Oligocene larger Foraminifera from Panama. Jour. Paleont., v. 27, No. 3, p. 332-337, pls. 43, 44. 19534. Eocene and Oligocene larger Foraminifera from the Panama Canal Zone and vicinity. U.S. Geol. Surv., Prof. Paper 244, p. 1-41, 28 pls., 2 text figs. (1952). 1953c. Criteria for the recognition of certain assumed camerinid genera. Bull. Amer. Paleont., v. 35, No. 147, p. 28-46, 3 pls. 1956. Jamaican larger Foraminifera. Bull Amer. Paleont., v. 36, No. 158, p. 205-233, pls. 24-31. 1957a. Variation in American Oligocene species of Lepidocyclina. Bull Amer. Paleont., v. 38, No. 166, p. 31-51, pls. 1-6. 1957b, Larger Foraminifera from Eniwetok Atoll drill holes. U.S. Geol. Surv. Prof. Paper 260-V, p. 743-781, pls. 230-249, 1 text fig. LARGER FORAMINIFERAL TAXONOMY: COLE 393 19584. Names of and variation in certain American larger Foraminifera— No. 1. Bull. Amer. Paleont., v. 38, No. 170, p. 179-213, pls. 18-25. 19586. Names of and variation in certain American larger Foraminifera, particularly the camerinids—No. 2. Bull. Amer. Paleont., v. 38, No. 173, p. 261-284, pls. 32-34. 1959. Names of and variation in certain Indo-Pacific camerinids. Bull. Amet. Paleont., v. 39, No. 181, p. 349-371, pls. 28-31. 1960. The genus Camerina. Bull. Amer. Paleont., v. 41, No. 190, p. 189- 204, pls. 23-26. 1961. Names of and variation in certain Indo-Pacific camerinids—No. 2. A reply. Bull. Amer. Paleont., v. 43, No. 195, p. 111-128, pls. 14-16. , and Gillespie, R. 1930. Some small Foraminifera from the Meson formation of Mexico. Bull. Amer. Paleont., v. 15, No. 574, p. 125-137, pls. 18-21. , and Herrick, S. M. 1953. Two species of larger Foraminifera from Paleocene beds in Georgia. Bull. Amer. Paleont., v. 35, No. 148, p. 49-62, pls. 4, 5. Cushman, J. A. 1918. The larger fossil Foraminifera of the Panama Canal Zone. U.S. Nat. Mus., Bull. 103, p. 89-102, pls. 34-45. 1919. Fossil Foraminifera from the West Indies. Carnegie Inst. Washing- ton, Publ. 291, p. 21-71, pls. 1-15, 8 text figs. Doornink, H. W. 1932. Tertiary Nummulitidae from Java. Geol.-Mijnbouwk. genoot. v. Nederland en Kolonién, Verh., v. 9, p. 267-315, pls. 1-10, 2 tables, text figs. a-l. Douville, R. 1907. Sur des lépidocyclines nouvelles. Soc. Géol. France, Bull., ser. 4, v. 7, p. 307-313, pl. 10, 3 text figs. Drooger, C. W. 1960. Some early rotaliid Foraminifera. Koninkl. Nederl. Akad. Wetensch., Amsterdam, Proc., ser. B, v. 63, No. 3, p. 287-334, Spls., 3 text figs. Eames, F. E. 1953. The Miocene/Oligocene boundary and the use of the term Aquitanian. Geol. Mag., v. 90, No. 6, p. 388-392. , Banner, F. T., Blow, W. H., and Clarke, W. J. 1960. Mid-Tertiary stratigraphical palaeontology. Nature, v. 85, No. 4711, p. 447, 448. Gravell, D. W. 1933. Tertiary larger Foraminfera of Venezuela. Smithsonian Miscell. Coll., v. 89, No. 11, p. 1-44, 6 pls. , and Hanna, M. A. 1937. The Lepidocyclina texana horizon in the Heterostegina zone, upper Oligocene, of Texas and Loursiana. Jour. Paleont., v. 11, No. 6, p. 517- 529, pls. 60-65. 1938. Subsurface Tertiary zones of correlation through Mississippi, Alabama. and Florida. Amer. Assoc. Petrol. Geol., Bull., v. 22, No. 8, p. 984-1013, apis: 394 BULLETIN 197 Grimsdale, T. F. 1959. Evolution in the American Lepidocyclinidae (Cainozoic) Foramini- fera: an interim review. Koninkl. Nederl. Akad. Wetensch., Amsterdam, Proc., ser. B, v. 62, No. 1, 8-33, 1 text fig. Lemoine, P., and Douvillé, R. 1904. Sur le genre Lepidocyclina Giimbel. Soc. Géol. France, Mem. No. 32, p. 5-42, 3 pls., 3 text figs. Nuttall, W. L. F. 1932. Lower Oligocene Foraminifera from Mexico. Jour. Paleont., v. 6, No. 1, p. 3-35, pls. 1-9. Palmer, Dorothy K. 1934. Some large fossil Foraminifera from Cuba. Soc. Cubana Hist. Nat., Mem., v. 8, No. 4, p. 235-264, 5 pls., 19 text figs. Palmer, R. H. 1948. List of Palmer Cuban fossil localities. Bull. Amer. Paleont., v. 31, No. 128, p. 277-452. Smout, A. H., and Eames, F. E. 1960. The distinction between Operculina and Operculinella. Contrib. Cushman Found. Foram. Res., v. 11, Pt. 4, p. 109-114. Tan, S. H. 1932. On the genus Cycloclypeus Carpenter. Nederland Akad. Wetensch. Meded., No 19, p. 1-194, pls. 1-24, 7 tables. Vaughan, T. W. 1927. Larger Foraminifera of the genus Lepidocyclina related to Lepidocy- clina mantellt. U.S. Nat. Mus., Proc., v. 71, Art. 8, p. 1-5, 4 pls. 1928. Species of large arenaceous and orbitoidal Foraminifera from the Tertiary deposits of Jamaica. Jour. Paleont., v. 1, No. 4, p. 277-298, pls 43-50. 1933. Studies of American species of Foraminifera of the genus Lepidocy- clina. Smithsonian Miscell. Coll., v. 89, No. 10, p. 1-53, 32 pls. Se an Cole Wis: 1932. A new species of Lepidocyclina from the Panama Canal Zone. Jout. Washington Acad. Sci., v. 22, Nos. 18, 19, p. 510-514, 1 pl. 1941. Preliminary report on the Cretaceous and Tertiary larger Foraminifera of Trinidad, British West Indies. Geol. Soc. Amer., Sp. Paper 30, p. 1- 136, 46 pls., 2 text figs. Woodring, W. P. 1957. Geology and paleontology of Canal Zone and adjoining parts of Panama. U.S Geol. Sur. Prof. Paper 360-A, p. 1-145, 23 pls. 1958. Geology of Barro Colorado Island, Canal Zone. Smithsonian Miscell. Goll., v. 135, No. 3, p. 1-39, 3 pls. 1960. Oligocene and Miocene in the Caribbean Region. Second Carib. Geol. Gonf., Trans., p. 27-32, 1 table. Yabe, H. 1918. Notes on Operculina-rocks from Japan with remarks on “Nummulites cumingit Carpenter. Tohoku Imp. Univ., Sci. Rep., ser. 2 (Geol.), v. 4 No; 3) p: 107-126; pl. 17. PLATES This study was made subsequent to the ones by Cole and Applin and Cole which had been accepted for publication (Contrib. Cushman Found. Foram. Res., v. 12, pt. 4, 1961). Therefore, some of the specific names of Lepidocyclina used in those articles have been changed —Editor’s note. 396 BULLETIN 197 Explanation of Plate 28 Figure Page 1-7. Camerina cojimarensis (1). IK. Palmer) .......::c0:.eeeeeeees 378, 379 1. Central part, X 40, of a median section of a megalospheric specimen. i) Transverse sections; 2, X 20; 3, X 12.5; of megalospheric specimens. 4. Transverse section, X 12.5, of a microspheric specimen. 5,6. Median sections; 5, X 20; 6, X 12.5, of megalospheric specimens, 7. Part of a median section, X 12.5, which is not ground to the median plane in the central area of a microspheric specimen. 1-7. Loc. 2—see text for locality descriptions. PLATE 28 BULL. AMER. PALEONT., VOL. 43 wall Abr TR ws is Banh ort PLATE 29 VOL. 43 > PALEONT. BULL. AMER. LARGER FORAMINIFERAL TAXONOMY: COLE 397 Explanation of Plate 29 Figure Page 1-13. Camerina dia (Cole and Pontomn)......cccceeeteeeeeee B83 All figures, X 20. 1, 3, 6, 9, 11, 13. Median sections. 2, 4, 5, 7, 8, 10, 12. Transverse sections. 1-5, 12. Loc. 1—see text for locality descrip- tions. 6G, ©, 10). Ilex, {3}. 7H & wil, We, koe, 2 ,OH BULLUTIN 197 Ixplination of Plate 40 ligure Pape 118. Lepidocyelinn Chepidoeyelina) canetlei Faonolne jd 2 Dauyille oo BSG, 887, BSB, BOL Pigures 1-7, 10, 11, X 20; 8, 9, 12, 13, X 40, 1-14 Vertical sections of me nilospherne specimens to illustrate K Vabiation 1, 4, 10, Loe, d--see text for locality deseriptions, Zor Opes uOCweL, vie, v1 Loc, 6 BULL, AME, PALHONT,, Vou, 4% VPLATH HO BuLL. AMER. PALEONT., VOL. 43 PLATE 31 LARGER FORAMINIFERAL TAXONOMY: COLE 499 Explanation of Plate 31 Figure Page 1-5. Lepidocyelina (Lepidocyelina) canellei ILS TIE DiaGlJ82, “TDYons hab OsaesconrasoscesaucosooscococecocusacsucnncsAa-anoceaeracccestoce et aiTl 1. Part of an equatorial section, X 40, of a megalospheric specimen the peripheral equatorial chambers of which are illustrated as figure 1, Plate 36. 2. Equatorial section, X 40; the vertical section of a similar specimen is illustrated as figure 8, Plate 30. 3. Part of an equatorial section, X 40, of a specimen illustrated previously as figure 11, plate 7 (Cole, 1945). 4, Part of an equatorial section, X 40, the peripheral equatorial chambers of which are illustrated as figure 5, Plate 35. 5. Part of an equatorial section, X 40; the vertical section of a similar specimen is illustrated as figure 7, Plate 30. 1. Loc. 4—see text for locality descriptions. D; More, 6; Yo & sel [o) lo) 4 wade 7 400 BULLETIN 197 Explanation of Plate 32 Figure Page 1-4. Lepidocyelina (Lepidocyelina) canellei Lemoine and! 2D ouvilllescccocccen eco eevee 391 1. Equatorial section, X 40; the vertical section of a similar specimen is illustrated as figure 8, Plate 30. ho Equatorial section, X 40; the vertical section of a similar specimen is illustrated as figure 13, Plate 30. 3. Equatorial section, X 40; the vertical section of similar specimens are illustrated as figures 1, 4, Plate 30. 4. Equatorial section, X 40; the vertical section of a similar specimen is illustrated as figure 9, Plate 30. 5. Lepidocyelina (EKulepidina) tourncueri Bemoine and! Res WOuivillli@hescce-costscccecseecnceesacesteseeeseeeesenreener Sper) otek Equatorial section, X 40. 1, 5. Loc. 6—see text for locality descriptions. As \broye,. il, 2, Ibeye, at AP LOGwDr ULL. AMER. PALEONT., VOL. 43 PLATE 3 @ Qs =| 6-8 @; Se KD BULL. AMER. PALEONT., VOL. 43 PLATE 33 LARGER FORAMINIFERAL TAXONOMY: COLE 401 Explanation of Plate 33 Figure Page 1-4. Lepidocyelina (Lepidocyeclina) canellei WEEMOUTEST ATCA ID OVA @secev-sccceccces-seseeees ceeccecessescesce ccscecossiennesssseees| OIL 1. Equatorial section, X 40. 2. Equatorial section, X 20; the vertical section of a similar specimen is illustrated as figure 2, Plate 30. 3. Part of an equatorial section, X 40, of the same specimen illustrated as figure 4, Plate 35. 4, Equatorial section, X 40; the vertical section of a similar specimen is illustrated as figure 6, Plate 30. 1. Loc. 6—see text for locality descriptions. 2, a. IUee. Ao 3 LOGS: 402 BULLETIN 197 Explanation of Plate 34 Figure Page 1-8. Lepidoeyelina (Lepidocyelina) canellei JO(eravonbavevszbovel 18%, ID Yoh ralll (eheeerepscccccecoso-cocoousocoo sceococo sec nC 386, 387, 391 1. Part of a vertical section, X 40, of the same specimen illustrated as figure 3 of this plate. 2-5, 8. Vertical sections, X 20. 6, 7. Parts of vertical sections, X 40. 9. Lepidocyelina (Eulepidina) tournoueri WEMOINE ANG BE. DO UVilleiecccccocecswoceovceotetersesscenscoete cote oeeeeeeneeatoneeene 391 Vertical section, X 40, of a small specimen. 1, 3-7. Loc. 3—see text for locality descriptions. Dei Moyes 4, OF Loc. 6: BULL. AMER. PALEONT., VOL. 43 PLATE 34 ie egrien: ~ pwengel an 404 BULLETIN 197 Explanation of Plate 36 Figure Page 1-5. Lepidocyelina (Lepidocyelina) canellei MLENOINE eA OV WO OUIVA Es ceceeectcters -cteseeacesecesee- teense ees 387, 391 1. Peripheral equatorial chambers, X 40, of the specimen illus- trated as figure 1, Plate 31. to Part of an equatorial section, X 40, of a specimen similar to the one illustrated as figure 12, Plate 30. 3. Vertical section, X 20, of a microspheric specimen. 4. Part of an equatorial section, X 20, of a microspheric spec- imen. 5. Part of an equatorial section, X 40, of a specimen similar to the one illustrated as figure 5, Plate 30. Loc. 5—see text for locality descriptions. Loci S: IKoXes. Te Mn &R NH Ww Loc. 1 BULL. AMER. PALEONT., VOL. 43 PLATE 34 eagvien’

Sess « + 29% o's? 0n0,0,¥, eeebece See 50: 809%, 0 &) ao? ,o& POLS (4 TeTeee + Bes, és ‘Se LARGER FORAMINIFERAL TAXONOMY: COLE 405 Explanation of Plate 37 Figure Page 1-5. Lepidoecyelina (Lepidocyclina) canellei BEINOLMEN ANIC cael) Ollvallll@eeeeeteecee a nceaceeeeesescaeanes sentra cseresceceseseceees see 391 1, 2. Parts of the same vertical section, X 20, of a micro- spheric specimen. 3. Vertical section, X 20, of a microspheric specimen with large pillars. 4, 5. Parts of the same equatorial section, 4, X 40; 5, X 230, of a microspheric specimen to illustrate the initial equatorial chambers. EN 2 A Loc. 3—see text for locality descriptions. De 35 Woe, Fo 406 BULLETIN 197 Explanation of Plate 38 Figure Page 1-7. Lepidocyclina (Lepidocyelina) canellei Tuemoime Bird! TR. WO uivilll@s. cr sccrvererecececn-+eeerneesesnssoses sas 386, 387, 388 1. Part of a vertical section, X 40, of the specimen illustrated as figure 4, Plate 30. 2. Vertical section, X 40. 3. Part of a vertical section, X 40, of the specimen illustrated as figure 3, Plate 30. 4. Part of a vertical section, X 40, of the specimen illustrated as figure 2, Plate 30. 5. Part of an equatorial section, X 40. 6. Vertical section, X 20. 7. Part of a vertical section, X 40, of the specimen illustrated as figure 3, Plate 39. 1. Loc. 4—see text for locality descriptions. 2. Soy, Lee, SD: Loc. 6. Ais 1beoyes, it BULL. AMER. PALEONT., VOL. 43 PLATE 36 = a @ .4°e ie te 4 o ‘ © , © BULL. AMER. PALEONT., VOL. 43 PLATE 387 LARGER FORAMINIFERAL TAXONOMY: COLE 407 Explanation of Plate 39 Figure Page 1-9. Lepidocyelina (Lepidocyclina) canellei IbereaKonhare ave 18%, ID Yo AyAllExsscooconoccoeouecoocnscsccebecoucoosaeconES MtSKOy Btellig Bret 1. Part of a vertical section, X 40, of the specimen illus- trated as figure 6, Plate 38. iw) Vertical section, X 40, of a small specimen. 3. Vertical section, X 20. 4, 5. Vertical sections, X 20. 6 Part of a vertical section, X 40, of the specimen illus- trated as figure 4 of this plate. 7. Part of an equatorial section, X 40. 8. Part of a vertical section, X 40, of the specimen illus- trated as figure 5 of this plate. 9. Vertical section, X 40. 1, 3, 9. Loc. 5—see text for locality descriptions. DiWA-Se wu LOCHO: * pe . XXXII. XXXIV. XXXV. XXXVI. XXXVII. XXXVIII. XXXIX. XL. XLI. XLII. XLII. Volume I. II. It. (Nos. 115-116). 738 pp., 52 pls. 20... Haier eG, CaM Bowden forams and Ordovician cephalopods. ROCIO EET) 4 Gar He GD) PISS a een NI fo Ol ute Jackson Eocene mollusks. (Nosy (118-123). 458'ppi, 27 'pIS./ yet ae ol eS Venezuelan and California mollusks, Chemung and Pennsyl- vanian crinoids, Cypraeidae, Cretaceous, Miocene and Recent corals, Cuban and Floridian forams, and Cuban fossil local- ities, (Nos; 029-133). 294 pp.3-39) pls.) Sogn ele Silurian cephalopods, crinold studies, Tertiary forams, and Mytilarca. GNos.: 1342139). , 448 pp. Si 4pls. 0 ee Devonian annelids, Tertiary mollusks, Ecuadoran stratigraphy paleontology. (Nos; 140-145). 400° pp., 19 pls.0i... a eee Trinidad Globigerinidae, Ordovician Enopleura, Tasmanian Ordovican cephalopods and Tennessee Ordovician ostra- cods and conularid bibliography. (Nos,/ 146-154). 386 pp., (31 pls. ison G. D. Harris memorial, camerinid and Georgia Paleocene Foraminifera, South America Paleozoics, Australian Ordo- vician cephalopods, California Pleistocene Eulimide, Vol- utidae, and Devonian ostracods from Iowa. (Nos.. '155-160)% |’ 412) pp. 53 piss: isla ly eo Globotruncana in Colombia, Eocene fish, Canadian Chazyan fossils, foraminiferal studies. (Nos. 1697168): /'486, ppii37 pis) fii id cece hed ts ck Antillean Cretaceous Rudists, Canal Zone Foraminifera, Stromatoporoidea. (Nos. 165-178)3) 447 pp., 53 pisi joo VM Venezuela geology, Oligocene Lepidocyclina, Miocene ostra- cods, and Mississippian of Kentucky, turritellid from Vene- zuela, larger forams, new mollusks, geology of Carriacou, Pennsylvanian plants. (Noa.\ 177-183). /448 pp 36 pls. ik rh We ee Panama Caribbean mollusks, Venezuelan Tertiary formations and forams, Trinidad Cretaceous forams, American-Eur- opean species, Puerto Rico forams. (Ne /984). \.7996. ppb pliss ok Sl ie ee a Type and Figured Specimens P.R.I. (Nos. 185-192). 381\ pps) 3a pls:| yao le ON Or A Australian Carpoid Echinoderms, Yap forams, Shell Bluff, Ga. forams. Newcomb mollusks, Wisconsin mollusk faunas, Camerina, Va. forams, Corry Sandstone. ; (No. 193). In press. (Nos. 194-197). Ordovician stromatoporoids, Indo-Pacific camerinids, Missis- sippian forams. PALAEONTOGRAPHICA AMERICANA (Nos. 1-5). 519 pp., 75 pls. Monographs of Arcas, Lutetia, rudistids and venerids. { Nos. 6-12) -! 53d pps 37 ple et ile esi Oy Nl fe Heliophyllum halli, Tertiary turrids, Neocene Spondyli, Pale- ozic cephalopods, Tertiary Fasciolarias and Paleozoic and Recent Hexactinellida. (Nasi) 15-20). 515 ppci6l plas illic a ha Ul dirk Paleozoic cephalopod structure and phylogeny, Paleozoic siphonophores, Busycon, Devonian fish studies, gastropod studies, Carboniferous crinoids, Cretaceous jellyfish, Platy- strophia, and Venericardia. (Nos. 26-28). | 128 pp., 18 pls. 0.0... WAH Neh a ag CEE Rudist studies, Busycon 18.00 15.00 12.00 10.00 12.00 12.00 12.00 13.50 15.00 16.00 16.00 20.00 16.00 21.00 25.00 CONDENSED TABLE OF CONTENTS OF BULLETINS OF AMERICAN PALEONTOLOGY AND PALAEONTOGRAPHICA AMERICANA Vols. I-VI. Vil. VITI-XV. XVI. XXVI. XXVII. XXVIII. BULLETINS OF AMERICAN PALONTOLOGY See Kraus Reprint (NO. S25) 730 Pp sy9O ple wipe ae ee Rae i EA Ue dy 15. 00 Claibornian Eocene scraphopods, gastropods, and cephalopods. See Kraus Reprint 16 East 46th Street, New York 17, N. Y. . 140 pp’) 48 pls) Sk eee eG (Nos. 59-61). 6.00 Venezuela and Trinidad Tertiary Mollaker (Nos, \62-63).. 283) pp.433. plse 3 8 ky eee 11.00 Peruvian Tertiary Mollusca. (Nos:-64-62) 286 pps-29l plsi ik Ae ee 11.00 Mainly Tertiary Mollusca and Cretaceous corals. (No. 68), 2726ep.. 24 ply ee el a Zetec 10.00 Tertiary Paleontology, Peru. (Nos. 69-700). 266 pox26/plsi sui Ba ee 10.00 Cretaceous and Tertiary Paleontology of Peru and Cuba. (Nos: 71-32); 322 ppi, 22’ psa Bae ne Ey Pe at 11.00 Paleozoic Paleontology and Stratigraphy. (Nos. 33-76) © 356) pps) SU pls.) oF ela RN 12.00 Paleozoic Paleontology and Tertiary Foraminifera. (Nos, 22-69) 250) ppg '3 5) pls ions cess dees hoes ree nene 10.00 Corals, Cretaceous microfauna and biography of Conrad. (Nos. 80-87). SSA DD ADA nc Van Mul adh conn uenentan 10.50 Mainly Paleozoic faunas and Tertiary Mollusca. (Nos, 88-94B). °306 pp., 30/ pls. bx. - uu. an aes ae 10.00 Paleozoic fossils of Ontario, Oklahoma and Colombia, Meso- zoic echinoids, California Pleistocene and Maryland Mio- cene mollusks. (Nos. (95-100), 420° ppy 58) pls... Aa ee 11.00 Florida Recent marine shells, Texas Cretaceous fossils, Cuban and Peruvian Cretaceous, Peruvian Eogene corals, and eology and paleontology of Ecuador. (Nos. 102-108).:°°376 pp../ 36 pls: sts ced i Was eae 12.00 Tertiary Molusca, Paleozoic cephalopods, Devonian fish and Paleozoic geology and fossils of Venezuela. (Nos;109-114)..,; 412. pp, “S4uplsee a Tayi een con 12.00 Paleozoic cephalopods, Devonian of Idaho, Cretaceous and Eocene mollusks, Cuban and Venezuelan forams. : . s) : ee =] DWLLETINS. ; OF AMERICAN PALEONTOLOGY VOL? ALT NUMBER 198 1961 Paleontological Research Institution Ithaca, New York Un SA; PALEONTOLOGICAL RESEARCH INSTITUTION 1961-62 i, PRESIDENT cz Syzuch sb osc opts Sates pg aged peseh tetpapa hee het Pak ca aes MUN E Sa JoHN W. WELLS . VICE-PRESIDENT Jo ey) a oA EAS De Ech AXEL A. OLSSON SEGRETARY? TREASURER UU PU GQ ah ade Oi a a un ehh TO oe ad REBECCA S. HARRIS DRRCTOR $s Vic eat dl ad NN ak SEG Ok KATHERINE V, W. PALMER COUNSEL Eo ) Bie HL Te ROAR IB TIRE RL RIANA AL NT ast Bee A ARMAND L. ADAMS REPRESENTATIVE ‘AAAS ‘COUNGIB 3): ftp ae a KENNETH E, CASTER Trustees KENNETH E. CASTER (1960-1966) KATHERINE V. W. PALMER (Life) DoNALD W. FISHER (1961-1967) RALPH A. LIDDLE (1956-1962) REBECCA S. Harris (Life) AxEL A. OLssoN (Life) SOLOMON C. HOLLISTER (1959-1965) NORMAN E. WEIsBoRD (1957-1963) JoHN W. WELLS (1958-64) / BULLETINS OF AMERICAN PALEONTOLOGY and PALAEONTOGRAPHICA AMERICANA KATHERINE V. W. PALMER, Editor Mrs, Fay Brices, Secretary Advisory Board KENNETH E. CASTER HANS KUGLER A. MyrA KEEN Jay GLENN MArRKs Complete titles and price list of separate available numbers may be had on application. All volumes available except vol. I of Paleontographica Americana. Subscription may be entered at any time by volume or year, with average price of $16.00 per volume for Bulletins. Numbers of Paleontographica Americana in- voiced per issue. Purchases in U.S.A. for professional purposes are deductible from income tax. For sale by Paleontological Research Institution 109 Dearborn Place Ithaca, New York U.S.A. BULLETINS OF AMERICAN PALEONTOLOGY Vol. 43 No. 198 RUDIST ASSEMBLAGES IN CUBA By L. J. CHUBB Geological Survey, Jamaica November 21, 1961 Paleontological Research Institution Ithaca, New York, U.S.A. Library of Congress Catalog Card Number: GS 61-305 MUS. COMP. Z00L LIBRARY DEC - 7 1961 HARVARD UNIVERSITY Printed in the United States of America CONTENTS Page PREYS SUG Cert amen eet en Phat Siac aeh ln ah Mitty banal dame me eee iaww Rare ca desedigee ase ee 413 BTCV NEG TOY TP ssakesnodecece ee cea doce cee REN AEOE Beat neiscooat UMBC RNGe Get SE ET RAT a ene ae ORAS ae 413 Barcham leraposarcoittes tartyas, tn Guba \.s....s02ee ofc s05-consce-sesss das shoesivse woes 414 NES TONS JBC ree TAS lOO are, na a eae ARR OR Be ap eR ee eI a RED. an 417 CLES AVG) RS) VOY en Go Re Reo eg oN seg PH ARUP AP Si TTS ep 419 REfEReTI CES reenter ee ae cee rnc r ea, anh A ORS i ORE ARCs setie. ALCL Nye ete cu Een 422 eT My ee Bae RUDIST ASSEMBLAGES IN CUBA L. J. CHUBB Geological Survey, Jamaica ABSTRACT The existence of separate Barrettia and Titanosarcolites assemblages in Cuba having been questioned, this paper explains how these faunas may be distinguished, and the localities where they may be found; makes a necessary correction; gives a more definite age (Campanian) than was pre- viously possible for the Barrettia fauna; and recapitulates the corrected faunal lists, including the larger Foraminifera found with Barrettia and Titanosarcolites. INTRODUCTION In 1905 the writer read a paper before the First Caribbean Geological Conference, in Antigua, entitled Rudist Assemblages of the Antillean Upper Cretaceous, which was subsequently published (Chubb, 1956). The prin- cipal purpose of this paper was to prove that the oft repeated statement that Barrettia and Titanosarcolites occur together in the Caribbean area 1s erroneous, and an attempt was made to show that in Jamaica, Cuba, and the other Antillean islands, there are two distinct rudist faunas, with hardly a species in common—an older associated with Barrettia and a newer associated with T7tanosarcolites. Another still older rudist fauna, character- ized by Tepeyacia, was recognised in Cuba. In a separate section of the paper the age of the different rudist faunas was briefly discussed. This problem was treated on a regional basis, in the light of evidence from different parts of the Antillean and Central American area. Recently Torre (1960, pp. 53-64) criticized the opinions expressed in this paper, in so far as they concern Cuba. With regard to the Tepeyacia fauna we are in agreement both as to its existence and its age, which we believe to be Cenomanian-Turonian. Our differences are mainly concerned with two questions: (a) the existence within the Habana formation of a Barrettia fauna, distinct and separate from the Titanosarcolites fauna, and (b) the age of the Barrettia fauna. These two problems were considered separately in the original publica- tion (Chubb, 1956), but throughout his paper Torre confused them, never discussed the first problem apart from the second, and attributed to the writer views that he does not hold. In this paper, for the sake of clarity, the two problems will be discussed independently. 414 BULLETIN 198 BARRETTIA AND TITANOSARCOLITES FAUNAS IN CUBA Torre made no attempt to examine the foundations of the writer’s belief that two distinct faunas exist in the Habana formation. He seemed to treat it as merely a personal opinion, based perhaps on guesswork. Actually the separation of the two faunas was achieved by a meticulous and detailed analysis of all published fossil lists available to the writer, especially those of the Utrecht geologists who investigated considerable areas of Cuba in the years 1933 and 1938-9. The work of these geologists is of exceptional value because they were diligent collectors, and they recorded the exact site of every find, gave it a distinguishing letter and number, and pinpointed it on their maps. Thus it became possible to as- certain which rudist species were associated together in Cuba. The lists referred to will be found in the publications of Rutten (1936, p- 37), MacGillavry (1937, p. 24), Thiadens (1937, pp. 43-4), Vermunt (1937a, pp. 36-7), Van Wessen (1943 pp. 57-8) and Hermes (1945, pp. 20-1). Much information may be extracted from these lists. A study of Vermunt’s list will show that at locality H870, in Pinar del Rio, the following rudists were collected: Barrettia monilifera, B. multilir- ata, Torreites sanchezt, Biradiolites cf, aguitanicus, B. tschoppi, Tampsta ruttent, Chiapasella cubensis, and Plagioptychus sp. Obviously, as all these species were found together they must be regarded as members of one fauna. Rutten’s list shows that at locality H550, in northern Santa Clara (Las Villas), the following species were found: Barrettia monilifera, Torreites sanchezi, Parastroma sp., Biradiolites cubensis, Parabournonta bispida, and Chiapasella cubensis. It will be noted that three species are common to both lists. All the species at both these localities are associates of Barrettia and must be regarded as members of the Barrettia fauna. Locality H698 in MacGillavry’s list of Camaguey rudists may be con- sidered next. Here were found Titanosarcolites giganteus, Bournonia thiadensi, B. cf. bournont, Biradiolites lumbricoides and Parastroma guitarti, Nermunt’s list shows that locality H774, in Pifar del Rio, yielded Titanosarcolites giganteus, Orbignya sp. (determined as O. mullerriedi by MacGillavry, 1937, p. 111), Praebarrettia sparcilirata, Bournonia thiadensi, Chiapasella pauciplicata, and Caprinula cf. annulata. Two species are com- mon to the lists. Being associated with Titanosarcolites the fossils from both these localities belong to the T7tanosarcolites fauna. CUBAN RUDIST ASSEMBLAGES: CHUBB 415 It will be noticed that not one of the species found at the Barrettia localities, H550 and H870, was found at the Titanosarcolites localities, H698 and H774. If Thiaden’s list of rudists in southern Santa Clara (Las Villas) be compared with Rutten’s list of those in northern Santa Clara, it will be found that there is not one species common to the two. The former list includes T7tanosarcolites in several localities, the latter in- cludes Barrettia. If all the abovementioned fossil lists of the Utrecht geologists be analysed and compared, it will be found that none of them recorded Barrettia from the same locality as Titanosarcolites, and the rudist species associated with the former genus were always different from those associat- ed with the latter, with one possible exception, Biradolites aquitanicus. If they are plotted on a map it will be found that the Barrefta localities are always many kilometers away from the T7tanosarcolites localities. These statements are not guesses, they are not opinions, they are not theories, they are facts. The main purpose of Torre’s article seems to be to demonstrate that there is only one rudist assemblage in the Habana formation, including both Barrettia and Titanosarcolites. Vf this is true it should be easy to prove, for it is only necessary to cite a few localities where the two genera may be found together, but there is no mention of even one such locality throughout his article. Torre laid great stress on, and repeatedly referred to, a brief mention in the writer's paper (Chubb, 1956, p. 11, lines 8-13) of the limestones of Loma Yucatan. The fauna of these limestones was referred to only incidentally, not as a representative, but as a doubtful example of the Barrettia fauna; it was expressly stated that Barrettia had not been found there. These limestones were provisionally included in the Barrettia beds mainly because Vaccinites occurs in them, and elsewhere in the Antillean area this genus is generally associated with Barrettia, for example at 3 km. W. S. W. of San Diego de Los Bafios, Pinfiar del Rio. Vaccinites is also found with Barreftia in Puerto Rico, and the same genus has recently been found in Jamaica, 5 km. southeast of Lucea, Hanover, where it again occurs with Barrettia. It was, therefore, thought that a further search of the Loma Yucatan limestones would probably reveal the presence of Barrettia. But if Dr. Mario Sanchez Roig denies the existence of this genus in these limestones (Torre, 1960, p. 57) his word must be accepted. Evidently the Loma Yucatan limestones contain an intermediate rudist fauna, newer than 416 BULLETIN 198 that of Tepeyacia and older than that of Barrettza. It is preferable to call this the Durania fauna, rather than to use Torre’s term, Dwrania and Vaccimites fauna, as the latter genus occurs in other horizons. Torre observed that the only way to clarify the problem of the exist- ence of distinct Barrettia and Titanosarcolites faunas in Cuba would be by an exhaustive investigation, including field-work, collection, and_strati- graphic study. To assist in this programme some localities will be suggest- ed where the investigation might be carried out profitably: (a) The Barrettza fauna (without T7tanosarcolites) may be found in Pinar del Rio west of Verracos and southwest of San Diego de los Bafios ; in Las Villas about six to seven km. east and southeast of Esperanza, one km. west of Bernia, and three km. northwest of Pastora; in Camaguey at about 17 km. and 27 km. west of Camaguey city on the La Florida road, at Arroyo Hondo, and at 8 km. west and 14 km. east of Sibanicu. It is poss- ible, but not certain, that Barrettia might also be found in Las Villas at seven to eight km. east of Fomento, at five to six km. northwest of Cab- aiguan, and at four km. south of Camajuani. (b) The Titanosarcolites fauna (without Barrettia) may be found in Pinar del Rio west of San Juan y Martinez and thence in a northeasterly direction to the neighbourhood of Guayabo; in Las Villas, west of Jutia and immediately north and east of Fomento; in Camaguey, east of Ciego de Avila, west and north of Piedrecitas, around Ingenio Grande and in an area five km. southeast thereof, at five km. and 17 km. north-north-east of San Francisco on the road to Veinte y Uno, and at four to six km. south of Berrocal. Special attention should be paid to an exposure about 11/4 km. south- west of San Diego, Pifar del Rio (H802). Although in his stratigraphic paper Vermunt (1937a, pp. 36-37) recorded only Barrettza and species belonging to the Barrettia fauna at this locality, in another paper (1937b, p. 263) Titanosarcolites giganteus was added to the list. This record is thought to be erroneous, perhaps a slip of the pen, perhaps a printer’s error. However that may be, this is the only definite locality known to the writer where it has been claimed, by any geologist who has worked in Cuba, that Barrettza and Titanosarcolites occur together. It is also suggested that the Loma Yucatan fauna should be sought, not only in the hill of that name north of Camaguey, but also in northern Pinar del Rio, around and between the harbours of Bahia Honda and Cabafas. CUBAN RUDIST ASSEMBLAGES: CHUBB 417 When this work has been accomplished and the existence of the two faunas in the Habana formation recognised, it may be possible to find the solution of other problems, such as why, in Pinar del Rio, Las Villas, and Camaguey, the outcrops of Barrettza limestone always lie some 10 to 30 km. north of those of T7tanosarcolites limestone. AGE OF THE BARRETTIA FAUNA There is no need to discuss here the age of the T7tanosarcolites fauna as there is general agreement that it is Maestrichtian. The question of the age of the Barrettia fauna was dealt with only briefly in the earlier paper (Chubb, 1956, pp. 16-17). It was considered on a regional basis in the light of evidence drawn from Jamaica, Cuba, and south Mexico. The following facts were mentioned: (a) that in the St. Ann’s Great River section, Jamaica, the shales below a Barrettia limestone yield Turon- ian-Coniacian fossils; (b) that in northern Las Villas, Cuba, Rutten (1936, pp. 7, 36) found Turonian-Coniacian ammonites apparently below a Barrettia limestone; (c) that in Chiapas, south Mexico, Mullerried (1936, p. 160) reported Turonian-Coniacian ammonites, not below, but above Barrettia; (d) that the apparent inconsistency would be resolved if it were assumed that Barrettia ranged from Upper Turonian to Lower Senonian; (e) that recent evidence suggested that Barrettia ranged into the Campanian in Puerto Rico and Cuba; and finally (f) that Campanian Foraminifera had been found in the shales below Barrettia in St. James, Jamaica. No attempt was made to draw any final conclusion from these varied pieces of evidence. Torre, however, persists in treating the mention of the Turonian-Lower Senonian as the writer's considered opinion of the range of Barrettia, and devotes much space to attempts to discredit it. He is tilting at windmills. He is evidently unaware that in the last few years a considerable amount of research on the problems of the Caribbean Cretaceous has been carried out (Chubb, 1958a; 1958b; 1959; 1960a; 1960b) and that new evidence has led to the possibility of a more exact evaluation of the age of the Barrettia beds. As Mullerried’s reported discovery of Turonian-Coniacian ammonites above Barrettia in south Mexico conflicted with evidence from other areas, it was decided to visit Chiapas, in order to study the Cretaceous sequence 418 BULLETIN 198 personally. Accordingly, after the Twentieth Session of the International Geological Congress in Mexico City (September 4-11, 1956) the writer spent a full month in the state (Chubb, 1959). Most of Mullerried’s faunal horizons were discovered, but unfortunately not the Barrettza and ammonite zones. It was found, however, that Campanian rocks rested directly upon Turonian, both Coniacian and Santonian were absent, and the opinion was formed that the Chiapas Barrettia horizon was probably Cam- panian., The Barrettza bed in St. Ann’s Great River, Jamaica, which is under- lain by beds with a Turonian-Coniacian fauna, is now known to be over- lain by beds with a Campanian one. The possibility, therefore, arises that this Barrettia bed might be Santonian, as was suggested in a paper read to the Mexico Congress in 1956 (in press), but it is now regarded as more probably basal Campanian (Chubb, 1960a, p. 91), the Santonian being absent. As previously mentioned the St. James Barrettia bed is underlain by a thick shale formation yielding Upper Campanian Foraminifera and ts succeeded by 800 meters of beds without diagnostic fossils, above which lies the basal bed of the Maestrichtian with the first Titanosarcolites. This Barrettia bed is, therefore, believed to be Upper Campanian (Chubb, 1960a, p. 88). In another recent publication (Chubb, 1960b, p. 17) it was stated that “the genus Barrettia could perhaps be regarded as an index fossil of the Campanian in Jamaica as well as in the other Greater Antilles,” and it might be added, in south Mexico. Torre (1960, p. 57) quoted the occurrence of orbitoidal Foraminifera, such as Pseudorbitoides, with Barrettia, as evidence of a Maestrichtian age. Evidently he does not know of the work of Bronnimann (1957, p. 591) who, after an exhaustive study of Pseudorbitoides israelskyi Vaughan and Cole, including topotype material from Louisiana, and specimens from Mississippi, Texas, Chiapas, Cuba, Haiti, and Puerto Pico, concluded that this species is restricted to the Campanian. The Utrecht geologists included the larger Foraminifera in their fossil locality lists. By an analysis of these lists it is possible to ascertain which Foraminifera were associated with Barrettia and which with Titanosar- colites; the former may be regarded as Campanian, the latter as Maestricht- ian. Pseudorbitoides israelskyi and P. trechmanni were found with Bar- rettia but not with Tztanosarcolites. CUBAN RUDIST ASSEMBLAGES: CHUBB 419 Three species were reported to be common to both groups, Vawghan- ina cubensis, Orbitoides browni, and Lepidorbitoides minima. According to Bronnimann (1957, p. 591) V. cubensis, Orbitoides palmeri, and Sulc- operculina dickersoni form an assemblage which is diagnostic of late Maestrichtian beds, and as would be expected, all three were found in the Titanosarcolites limestones of Cuba. Vaughanina cubensis, however, would not be expected in the Barrettia beds, and Rutten alone, among the Utrecht geologists, reported it there, not in his palaeontological paper (1935, p. 528) but only in his stratigraphical paper (1936, p. 36). Possibly the report may have been due to a mistaken identification, as there has been considerable confusion between this species and Pseudorbitoides israelskyi (Bronnimann, 1954, pp. 91-93). CONCLUSION In the Upper Cretaceous rocks of Cuba four successive rudist faunas may be recognised. The fossil lists previously published (Chubb, 1956, pp. 10-13) require revision owing to the separation of the Loma Yucatan fauna from the Barrettia fauna. The larger Foraminifera of the Campanian and Maestrichtian are included in the lists. (a) Tepeyacia fauna of the Provincial limestones; the age is prob- ably Cenomanian-Turonian. Caprinuloidea perfecta Palmer Coalcomana ramosa (Boehm) Sabinia sp. Ichthyosarcolites sp. Tepeyacia corrugata Palmer (b) Durania fauna of the Loma Yucatan limestones. The age is believed by Torre, following Albear and MacGillavry, to be Upper Cam- panian; but in view of the absence of orbitoidal Foraminifera a somewhat earlier age, perhaps Santonian or Coniacian, may be suggested. Duranta curasavica (Martin) D, lopeztrigoi (Palmer) Vaccinites macgillavry: Palmer Torrettes tschoppi MacGillavry Praebarrettia coralli (Palmer) (c) Barrettia fauna of the lower Habana formation. The age is Campanian. 420 BULLETIN 198 RUDISTS Plagioptychus antillarum (Douvillé) Antillocaprina crassitella MacGillavry Biradiolites cubensis Douvillé B. macgillavryi Vermunt B, tschoppi Vermunt B. cf. acuticostatus A’ Orbigny B. cf. lameracensis Toucas B. cf. aquitanicus Toucas Parabournonia hispida Douvillé Radiolites macroplicatus Thiadens non Whitfield Chiapasella cubensis Rutten Tampsia ruttent Vermunt Vaccinites vermunti MacGillavry Torreites sanchezt Douvillé Parastroma sanchezi Douvillé Barrettia monilifera Woodward B. multilirata Whitfield FORAMINIFERA (d) Vaughanina cubensis Palmer (according to Rutten) Orbitoides browni (Ellis) Torreina torrez Palmer Lepidorbitoides minima Douvillé L. planasi Rutten L, cubensis (Palmer) L. rooki Vaughan & Cole L. aguayoi Palmer Pseudorbitoides trechmanni Douvillé P. israelskyi Vaughan & Cole Titanosarcolites fauna of the upper Habana formation. age is Maestrichtian. RUDISTS Mitrocaprina tschoppi (Palmer) Antillocaprina annulata (Palmer) A. pugniformis (Palmer) The CUBAN RUDIST ASSEMBLAGES: CHUBB 421 Titanosarcolites giganteus (Whitfield) Biradiolites galofrei (Palmer) B. aquitanicus Toucas B. lumbricoides Douvillé Bournonia planasi Thiadens B. thiadensi Vermunt B. cancellata (Whitfield) B. cf. bournoni Des Moulins Thyrastylon adhaerens (Whitfield) Chiapasella bermudezi Palmer C. pauciplicata Mullerried Orbignya mullerriedi Vermunt Parastroma guitarti (Palmer) Praebarrettia cf. peruviana (Gerth) P. sparcilirata (Whitfield) P. porosa Palmer FORAMINIFERA Sulcoperculina dickersoni (Palmer) Vaughanina cubensis Palmer Orbitoides apiculata Schlumberger O. browni (Ellis) O. palmeri Gravell Lepidorbitoides estrellae van Wessem L. macgillavryi Thiadens . minima Douvillé . minor (Schlumberger) . nortont (Vaughan) . palmeri Thiadens . ruttent Thiadens . rutteni var. armata Thiadens . tschoppi van Wessem SS ish lest eh ist Ie 422 BULLETIN 198 REFERENCES Bronnimann, Paul 1954. Upper Cretaceous orbitoidal Foraminifera from Cuba, Part I, Vaughanina. Contr. Cush. Found. Foram. Research, vol. 5, pp. 91-105. 1957. Morphology and stratigraphic significance of Pseudorbitoides israel- skyi Vaughan & Cole. Eclog. Geol. helvet., vol. 56, pp. 582-604. Chubb, L. J. 1956. Rudist assemblages of the Antillean Upper Cretaceous. Bull. Amer. Paleont., vol. 37, No. 161, pp. 1-23. 1958a. The Cretaceous rocks of Central St. James. Geonotes, vol. 1, pp. 3-11. 1958b. The Cretaceous inlier of St, Ann’s Great River. Ibid, pp. 148-152. 1959. Upper Cretaceous of central Chiapas, Mexico. Bull. Amer. Assoc. Petrol. Geol., vol. 143, pp. 725-756. 1960a. Correlation of the Jamaican Cretaceous. Geonotes, vol. 3, pp. 85-97. 1960b. The Antillean Cretaceous geosyncline. Second Carib. Geol. Con- ference, Puerto Rico, Trans. pp. 17-26. Hermes, J. J. 1945. Geology and palaeontology of east Camaguey and west Oriente. Cuba Geog. en Geol. Med. Utrecht. Ser. 2, No. 7. MacGillavry, H. J. 1937. Geology of the Province of Camaguey, Cuba, with revisional studies of rudist palaeontology. Ibid, No. 14. Mullerried, F. K. G. 1936, La edad estratigrafica de la Barrettia y formas cercanos. An. Inst. Biol. Mexico, vol. 7, pp. 155-164. Rutten, M. G. 1935. Larger Foraminifera of northern Santa Clara Province, Cuba. Jour. Paleont., vol. 9, pp. 527-545. 1936. Geology of the northern part of the Province of Santa Clara, Cuba. Geog. en Geol. Med. Utrecht. No. 11. Thiadens, A. A. 1937. Geology of the southern part of the Province of Santa Clara, Cuba. Ibid, No. 12. Torre, Alfredo de la 1960. Notas sobre rudistas. Soc. Cubana de Hist. Nat., Mem., vol. 25, pp. 51-64. Vermunt, L. W. J. 1937a. Geology of the Province of Pittar del Rio, Cuba. Geog. en Geol. Med. Utrecht, No. 13. 1937b. Cretaceous rudistids of Pinar del Rio, Cuba. Jour. Paleont., vol. 11, pp. 261-275. Wessem, A. van 1943. Geology and palaeontology of central Camaguey, Cuba. Geog. en Med. Utrecht, ser. 2, No. 5. re elena rnyo INDEX VOLUME XLIII Light face figures refer to page numbers. to plate numbers. For index to Bulletins 194 and 196 see those B A ef. acuticostatus, Biradiolites .... 420, 421 adhaerens, Thyrastylon Albatross station 113 aguayol, Lepidorbitoides 420 Aguila Petroleum Company . Slat ammonoides, Camerina UG) Wey ls, IG, Is} 120, 123 “Operculina”’ 119 Operculina 114, 117 Operculinella 116 Amphistegina 115 Andonegui station, Mexico 377 annulata, Antillocaprina 420 Cf. annulata, Caprinula 414 annulatus, Cycloclypeus 382 Katacycloclypeus 382 Antigua... 384 antillarum, Plagioptychus 420 antillea, Heterostegina 384, 391 Miogypsina 391 Antillocaprina 420 Apia Harbor, Uporu, Samoa Islands 120 apiculata, Orbitoides 421 Applin, Esther R. 113 aquitanicus, Biradiolites 421 cf. quitanicus, Biradiolites 414, 415, 420 Arbol Grande station, near Tampico 377, 384 Assilina Ody, BT asterodisca, Lepidocyclina 3G), aay ox oy 386, 388, 389 B Bahia, Honda, Cuba 416 Bajada de Chichimeca, Vera Cruz, Mexico Butt Bandy, Orville 391 HARVARD sgvesiry Bold face figur Barker, R. Wright 381 iBarrevvlames ee: 413-420 Barro Colorado Island, Panama Canal Zone Syii7/ bartschi, Camerina 120 Operculina IPA. iA? “Operculina”’ 120 bermudezi, Chiapasella 421 Berrocal ee romceacs 416 Bikini Island 391 Biradiolites 414, 420, 421 Bournonia 414, 421 ef. bournonl, Bournonia 414, 421 Bronnimann, Paul 419, 422 browni, Orbitoides 419-421 bullbrooki, Spiroclypeus 384 Byram marl 374 (e Cabanas, Cuba 416 Caimito formation 383 Camaguey, Cuba 414, 416, 417 Camajuani, Cuba 416 Camerina 111-118, 120, 123, 31, 3111, o16, 000, 382, 383, 389, 391 Campanian 413, 417 cancellata, Bournonia 421 canellei, Lepidocyclina 30-39 375, 376, 383, 384, 386, 388, 389, 391, aaa Caprinula Caprinuloides As Caribbean 381 Carpenter, W. P. Has}. Sts} catenula, Camerina 382, 383 Chapman, F. and Parr, W. J. . 115 Chiapas, Mexico 417, 418 Chiapasella 414, 420, 421 Chubby lar 413, 417, 422 Chubb; i. J., Rudist Assemblages in Cuba 413 Cienfuegos, Cuba 376 Coalcomana . 419 cojimarensis, Camerina 28 378, 379, 389 “Operculinella’”’ 376, 380 Cole, W. S. 116, 120-122, 377, 380, 383-385 7HOL INDEX Cole, W. Storrs, An Analysis of Certain Taxonomic Problems in the Larger Foraminifera 373 Cole, W. S. and Herrick, S. . 383 Cole, W. Storrs, Names of and Variation in certain Indo-Pacific Camerinids—No. 2. A Reply 1401 complanata, Camerina 15, 16 120-123 Operculina iPAil., 1p Coniacian 418 coralli, Praebarrettia 419 Cornell University 113, 376 corona, Difflugia 113 corrugata, Tepeyacia 419 crassicosta, Lepidocyclina 384 crassitella, Antillocaprina 420 Cuba 376, 378 cubensis, Biradiolites 420 Chiapasella 414, 420 Lepidorbitoides 420 Vaughanina 419-421 cumingii, Amphistegina eae “Nummulites”’ 378 Operculinella 114 “cumingii”’, Camerina 115 curasavica, Durania 419 Cushman, J. A. 112, 120, 384, 385 Cycloclypeus 381, 382 D dertoni, Lepidocyclina 388 Eulepidina 388 dia, Camerina 29 383, 389, 391 dickersoni, Sulcoperculina 419, 421 Difflugia 113 dius, Operculinoides 374 Douvillé, R. 384 Drooger, C. W. 380, 381 Durania 416, 419 lopeztrigoi 419 E Eames, F. E. 116, 378 elegans, Operculina 120 Elphidium 391 Eocene: 224 ee eee 112, 114, 117, 374, 375, 378, 381, 386 Esperanza te eee 416 Espiritu Santo 118, 119, 120 estrellae, Lepidorbitoides 421 Eulepidina 374, 384, 385, 388, 391 F Fiji PAL, WA First Caribbean Geological Conference 413 Florida 374 Fomento 416 Foraminifera JHGL, its, 1740), 122, 373-375, 389 G gaimairdi, Operculina 120 galofrei, Biradiolites 421 Gatun Lake 383 gaymard1, Operculina 112, 114, 117, 120, 121 “Operculina” . 118 giganteus, Titanosarcolites 414, 416, 421 giraudi, Lepidocyclina 373, prs Graham, J. J. and Militante, P. J. . 120 granulosa, Operculina 120 Gravell, D. W. and Hanna, M. A. .. 374 Grimsdale, T. F. 386 Guam : 382 guitarti, Parastroma 414, 421 Gurley, William F. E., Foundation for Paleon- tology of Cornell University 373 H Habana formation 413, 414, 416, 417 hanzawai, Operculina 114, 119, 120 IBIAS, de ds. scensreommencee 414, 422 Heron-Allen, E. ............ 114 Heterostegina 384, 391, 392 hispida, Parabournonia 420 Hausteca Petroleum Company 377, 384 INDEX Ichthyosarcolites sp. 419 Indo-Pacific region 111, 378 indo-pacificus, Cycloclypeus 382 International Geological Congress, Mexico City 418 Ishigaki-shima Yaeyamagunto Ryukyu-retto israelskyi, Pseudorbitoides 418-420 J Jamaica, B.W.I. 384, 413, 415, 417 Jones, S. M. 377 K Katacycloclypeus 382 L La Boca marine member 375 Ladd, H. S. and Hoffmeister, J. E. 113 La Laja, Mexico 377 cf. lameracensis, Biradiolites 420 La Titance, Cuba arta Las Villas, Cuba 416, 417 Lavoutte, Cuba Sy7U Lepidocyclina 111, 113, 114, 123, 373-376, 383-389, 391, 392 Lepidocyclina aff. morgani? 385 Lepidorbitoides 419-421 Loma Yucatan 415, 416 Loma Yucatan limestones 419 lumbricoides, Biradiolites 414, 421 M Miogypsina 391, 392 miraflorensis, Lepidocyclina 373, 375, 385- 389 Miramar, Mexico Sir Miscellanea Ia, S377, BES Mitrocaprina i 420 monilifera, Barrettia 414, 420 Mullerried, F.K.G. 417, 422 mullerriedi, Orbignya 414, 421 multilirata, Barrettia 414, 420 MacGillavry, lal, dj. 414, 419, 422 macgillavryi, Biradiolites 420 Lepidorbitoides 421 Vaccinites 419 macroplicatus, Radiolites 420 mantelli, Lepidocyclina 373, 374, 386, 389 Marianna limestone 374 Martin-Kaye, P. H. 377 Massilina 114 matleyi, Lepidocyclina 384 mecatepecensis, Streblus 391 mexicanus mecatepecensis, Streblus ........ 391 Mexico ........ ae Sui 384, 417 Mindoro, Philippine Islands 120 minima, Lepidorbitoides 419-421 minor, Lepidorbitoides 421 Miocene 375, 378 N Nagappa, Y. ... il we Nagura-gawa 113 Nakoshi, Haneji-mura, Okinawa-jima 113, 118-122 SAINTE UMN TIS) asoceesc cetccoeoes 115 New Hebrides 113 nortoni, Lepidorbitoides 421 Nummulina - ; 116 Nummulites ie Shree: “Nummulites” 381 nuttalli, “Nummulites”’ 381 oO Oligocene 117, 374, 383, 384, 386 Oneata, Lau Islands, GIR tates ae TLS y, TAAL 119-92 Operculina . 112, 114, 117, 121, 11222, Bi), BIT, Stell. 383, 391 Operculinella 112, 114, 116, 374, 377, 378, 380, 383 INDEX Orbignya .... 421 Orbignya-sp.9 = 232 414 Orbitoides . 419-421 Ozulama, Mexico 377 Pp Palacio Penal, Mexico 377 Palaeonummulites 116, 378, 380 Paleocene 375, 381 Palmer, Mrs. D. K. 377 palmeri, Lepidorbitoides 421 Orbitoides 419, 421 Palmira road, Pueblo Grifo, Santa Clara Province 376 Panama Canal Zone 377, 383, 385 Panama formatiin 375 pancanalis, Lepidocyclina 384 Panuco River SIU Parabournonia 420 Paraspiroclypeus 377 Parastroma 414, 420, 421 parvula, Lepidocyclina 373, 384-387 parvula crassicosta, Lepidocyclina 384 Pastora 416 pauciplicata, Chiapasella 414, 421 Pellatispirella 383 Pena Blanca, Panama Canal Zone 383 pencanalis, Lepidocyclina 384 pengaronensis, Camerina 378, 380 perfecta, Caprinuloidea 419 cf. peruviana, Praebarrettia 421 Philippine area IPA, iis) APA 122 Phillippine Islands 120, 391 Pinar del Rio 414, 415, 417 Plagioptychus 420 Plagioptychus sp. 414 planasi, Bournonia 421 Lepidorbitoides 420 Planocamerinoides Srl planulata, Camerina 381 porosa, Praebarrettia 421 Potrero, Vera Cruz, Mexico 377 Praebarrettia 414, 419, 421 pristina, Nummulina 116, 378 Provincial limestones 419 Pseudorbitoides 418, 420 Puerto Galera area 120 Puerto Rico 415 pungiformis, Antillocaprina 420 Q Quaternary aly R Radiocycloclypeus 382 Radiolites . 420 ramosa, Coalcomana... 419 Ranikothalia _...377, 380, 381 Recent 111, 112, 120, 35) Rio’ ‘Chagres 4... 383 Roig, Dr. Mario Sanchez 415 rooki, Lepidorbitoides . 420 Rutten, M. G. 414, 417, 419, 422 rutteni, Lepidorbitoides 421 Tampsia ee 414, 420 rutteni var. armata, I .epidorbitoides 421 S Sabinia sp. 419 Samoa Islands 120 sanchezi, Parastroma 420 Torreites 414, 420 San Diego de Los Banos, Cuba 415, 416 San Francisco, Cuba 416 Santa Clara (Las Villas), Cuba 414, 415 Santa Clara Province 376 Santonian 418 secans, Massilina 114 Selsey 114 Senonian 417 Smout, A. H. and Eames, F. E. allah ales ila 115) ATS 23 sparcilirata, Praebarrettia 414, 421 Spiroclypeus 384 St. Ann’s Great River, Jamaica 418 St. James, Jamaica . 417 St. Lucia, West Indies 377 Streblus ales. 391 striatoreticulata, Operculinella el, INDEX Sulcoperculina 419, 421 supera, Lepidocyclina 373, 374 aT Tacloban Anchorage, Philippine Islands... 113 Tamaulipas, Mexico .... 377, 384 Tampico, Mexico 376, 377, 384 Tampico penbesaer ALC Alen nce: = 377 Tampsia .... 414, 420 Tanhuijo, Vera Cruz, Mexico 5. ave U tempanii, Lepidocyclina 384 Eulepidina 384 Tepeyacia 413, 419 Tertiary ... 117, 381 Thiadens, A. A. 414, 422 thiadensi, Bournonia 414, 421 Thyrastylon 421 Titanosarcolites 413-416, 418- 421 Togoland . ® 381 Torre, Alfredo de la. 413-415, me torrei, Torreina 420 TMQTAREWORY 22 joenessoonssenasessos 420 Torreites 414, 419, 420 tournoueri, Lepidocyclina 32, 34,35 384, 388, 391 Eulepidina 32, 34, 35 384, 388, 391 trechmanni, Pseudorbitoides 418, 420 rina diee 384 tschoppi, Biradiolites ...... 414, 420 Lepidorbitoides 421 Mitrocaprina 420 MROGLeWES ae ee 419 Turonian 417, 418 U undosa, Lepidocyclina 384, 391 Eulepidina aoe 384, 391 U. S. National Museum 112, 113, 376 Vv Waccinites =. 415, 419, 420 variolaria, Camerina 381 Vaughan, T. Wayland 111, 113, 114, 384-386 Vaughan, T. W. and ColesiWeesseee = 111, 384 Nia hanna: 419-421 Venezuela 384 venosa, Camerina 14 115, 116, 123, 378 Operculina 119 Operculinella 112-114, 116 “Operculinella” 118, 380 venosus, “Nautilus” 115 Vera Cruz, Mexico 377 Vermunt, L.W.J. vermunti, Vaccinites Verracos 414, 416, 422 420 416 WwW waylandvaughani, Lepidocyllina 373, 376, 385- 389 Wessem, A. van 414, 422 West Indies 377 willcoxi, “Nummulites” 378 “Operculinoides” 380 Windward Islands, West Indies 377 Woodring, W. P. 377, 383 XY Zz Yabe, H. and Hanzawa, S. 113, 120-122 yurnagunensis, Lepidocyclina 384 Eulepidina 384 er ‘ s ei i se, ee ie a Ph £ : ‘ ye ea ; ; 1 : * iM 4 y ! i ‘ « + - ae hs YP iho We Kit if AF, 1S Fuel ; al aby UN Pes , Thar ' j ‘ ‘ s ‘ aes CURR aS ¥ rte Wie ef > 7 ; ‘oo ; A ie avs Vk a med Uy ay i ; , A Pies et Oa 7 a ie "hie i/ de. ‘ ‘ - Cd (eres U care pier SOT ARCS ta : >% pe 4 My ’ + } DE vil ula ih i. rod ' fe a ‘ Ti wt : TL een Ray a a eS Cy A i ; Ve 7) th Wd a | Pas Ty 7 big PPS. high Share. ii v if ¥, : @ a\'eaeaile : ty on ire sah We ; 7 a tab re) ad rp Wed tlhe “et Ms ; Os Pe ens). LA~ at hits ide SN Dt Se hers at Pane Lad hae 1 al ie at , Pee, es ah Cinkae ; n * vie PTS) iia & DY ' | ; Vitale tar . = pA a 7 Pps (fata ; f le : PR: haat tf i rr La 5 ‘a a ry i 7 J 4 " . “i i } il — « . : * i 7 i} A a py 4 Pa vine a 2 i ‘ ‘t j , ly ° = is , ‘ = of < i ’ ad . ) a 4 * p I a 14 ; pd ; A he) ee % i « : Pitind f 7 rf : aL lh XXXV. XXXVI. XXXVI. XXXVIII. XXXIX. XL. XLI. XLII. XLII. Volume I. tl. I. CNos;) LIS-MG) 738 pps) 52 plist oc ub eh wh Bowden forams and Ordovician cephalopods. CNG SURE) An BOs Dp G9) pase Wile So we ta ackson Eocene mollusks. (Nos. 118-128) ..) 458 opis '27 ‘pls. ooo wea ue ad Venezuelan and California mollusks, Chemung and Pennsyl- vanian crinoids, Cypraeidae, Cretaceous, Miocene and Recent corals, Cuban and Floridian forams, and Cuban fossil local- ities. (Nog. 1292133) .,.:294 pp.) 39 pls.- i. on eb Sie eo geal lle Silurian cephalopods, crinold studies, Tertiary forams, and Mytilarca. Nos.) 194-139).1; 448 pp. °51 pls i ROR ae Devonian annelids, Tertiary mollusks, Ecuadoran stratigraphy paleontology. (Nos, 140-145). 400 pp., 19 pls. ooo. ceeceeseeeeeeeee Trinidad Globigerinidae, Ordovician Enopleura, Tasmanian Ordovican cephalopods and Tennessee Ordovician ostra- cods and conularid bibliography. (Nos, 146-154)... '386.\pp., 131) plsi 200) ot ee G. D. Harris memorial, camerinid and Georgia Paleocene Foraminifera, South America Paleozoics, Australian Ordo- vician cephalopods, California Pleistocene Eulimide, Vol- utidae, and Devonian ostracods from Iowa. (Nos. 155-160) ..//,412, pp, 53) pls. y3 03 ie dey del Globotruncana in Colombia, Eocene fish, Canadian Chazyan fossils, foraminiferal studies. (Nos: T6L-164)>) (486 ‘pp: 37) plsp 2. huc ho fh A RRA Antillean Cretaceous Rudists, Canal Zone Foraminifera, Stromatoporoidea. (Noa.)168-176).'/ 447 ppi53 pis. be Venezuela geology, Oligocene Lepidocyclina, Miocene ostra- cods, and Mississippian of Kentucky, turritellid from Vene- zuela, larger forams, new mollusks, geology of Carriacou, Pennsylvanian plants. (Nos.'177-183):."| 448 ppiyi36 piss ci) ch hot eee Panama Caribbean mollusks, Venezuelan Tertiary formations and forams, Trinidad Cretaceous forams, American-Eur- Opean species, Puerto Rico forams. Ko T84).) 906 pp, pls a Reh ae he ae Type and Figured Specimens P.R.I. (Nos. 185-192). SS Uippe'S5) plsx he Nes hPa eae Australian Carpoid Echinoderms, Yap forams, Shell Bluff, Ga. forams. Newcomb mollusks, Wisconsin mollusk faunas, Camerina, Va. forams, Corry Sandstone. (No. 193). — In press. (Nos, 194-197). Ordovician stromatoporoids, Indo-Pacific camerinids, Missis- sippian forams. PALAEONTOGRAPHICA AMERICANA (Nos. 1-5). 519 pp., 75 pls. Monographs of Arcas, Lutetia, rudistids and venerids. (Nos. /6-E2)7) 1531 pp.) 7) pls. ial Mie et Heliophyllum halli, Tertiary turrids, Neocene Spondyli, Pale- ozic cephalopods, Tertiary Fasciolarias and Paleozoic and Recent Hexactinellida, CNes.))15-20) 4-513 pp, G1) pls. it Mt ee ain doa an tim Paleozoic cephalopod structure and phylogeny, Paleozoic siphonophores, Busycon, Devonian fish studies, gastropod studies, Carboniferous crinoids, Cretaceous jellyfish, Platy- strophia, and Venericardia. (Nas.4/26-28) 21), 228 pp. 18. pss. oul ERR RN A, Rudist studies, Busycon 18.00 15.00 12.00 10.00 12.00 12.00 12.00 13.50 15.00 16.00 16.00 20.00 16.00 21.00 25.00 6.50 CONDENSED TABLE OF CONTENTS OF BULLETINS OF AMERICAN PALEONTOLOGY AND PALAEONTOGRAPHICA AMERICANA BULLETINS OF AMERICAN PALONTOLOGY Vols. I-VI. See Kraus Reprint VIE. ONO. 32s. 730 pp, 90 pls. wth de tne eae 15.00 Claibornian Eocene scraphopods, gastropods, and cephalopods. VIH-XV. See Kraus Reprint 16 East 46th Street, New York 17, N. Y. XVI. (Nos. 59-61). 140 pp., 48 pls. oo... e. i ecsik pes Naas pre 6.00 ’ Venezuela and Trinidad Tertiary Mollusca. A\VIE,.- .CNos. 62-63)... ''283' pp. 33, 'pls.e)) eos lL i RON 11.00 Peruvian Tertiary Mollusca. AVIEIT. .. (Nos! 64-67) .\ | 286:pp! 29.pls. i.) pM 11.00 Mainly Tertiary Mollusca and Cretaceous corals. SER. <: (NOA6B).", (272 ppis24 pls. eA 2 a ea ae 10.00 Tertiary Paleontology, Peru. XK. . (Nos, 69-70C). 266 pp., (26, pls. \. 2) ag deg seco eesccieekesadueageal 10.00 Cretaceous and Tertiary Paleontology of Peru and Cuba. Ms (Nos. 91-72). - 1321-ppy\ 12spls. oe ee en 11.00 Paleozoic Paleontology and Stratigraphy. XXII. (Nos. 73-76). 356 pp., 31 pls. ......... sagaridaeehs got OO Paleozoic Paleontology and Tertiary Boraminifera RXTE. CNos. 33-7990" 251 ppst3d) pls.ja. esa ay ag eae ae aces 10.00 Corals, Cretaceous microfauna and biography of Conrad. XXIV. GNos; 80-87): (334 pps 27 plsS La a a 10.50 Mainly Paleozoic faunas and Tertiary Mollusca. XXV,'.(Nos.'88-94B).:".306' pp:,, 30, pls.25.6: nti alin 10.00 Paleozoic fossils of Ontario, Oklahoma and Colombia, Meso- zoic echinoids, California Pleistocene and Maryland Mio- cene mollusks. MXVE. CNos.--95-100). S420 -pp.,/58 (pls) niin feel ee ae 11.00 Florida Recent marine shells, Texas Cretaceous fossils, Cuban and Peruvian Cretaceous, Peruvian Eogene corals, and geology and paleontology of Ecuador. XXVEL.. (Nos, 401-108). 376 pp.,. 36! pls. 0 os AS ae 12.00 Tertiary Molusca, Paleozoic cephalopods, Devonian fish and Paleozoic geology and fossils of Venezuela. XX'VILE. (Nos. 109-134). 412 pp. S54) pls \) Su et Rin ohh oe eee 12.0073 Paleozoic cephalopods, Devonian of Idaho, Cretaceous and Eocene mollusks, Cuban and Venezuelan forams. i ur ; : H } at. .< , ) ib; Mi 3 2044 ln arose + Coe Piceceewnenwwnimtnme hocannuoend