UPPERMOST ORDOVICIAN AND LOI^IERMOST SILURIAN

STRATIGRAPHY AND SOLITARY RUGOSE CORALS

OF THE EAST-CENTRAL UNITED STATES

Robert J. McAuleY

A thesis

presented to the Uníversity of Manítoba ín Partial fulfillment of the requírements for the degree of Master of Science

I^linnipeg, Manítoba 1985 UPPERMOST ORDOVICIAN AND LOWERMOST SILURIAN

STRATIGRAPHY AND SOLITARY RUGOSE CORALS

OF THE EAST-CENTRAL UNITED STATES

BY

ROBERT J. MCAULEY

A tlresis st¡bmitted to the Faculty of Graduate Studies of the University of Ma¡litoba in partial fulfìll¡ne¡rt of the requiretttettts of the degree of

MASTER OF SCIENCE

o 1985

Permission has been grartted to the LIBRARY OF THE UNIVER- SITY OF MANITOBA to lend or sell copies of this thesis. to the NATIONAL LIBRARY OF CANADA to microfilnr this thesis and to lend or sell copies of the film, and UNIVERSITY MICROFILMS to publish an abstract of this thesis.

The author reserves other publicatiolt rights, altd neitlter tlte thesis nor extensive ext¡acts from it may be printed or other- wise reproduced without the author's written perntissiott. l_

CONTENTS

1 Abs trac t

Introduc tíon 4 Abbrevíations and RePositories 8

9 Acknowledgments Stratígraphic Sections and Collectíons 10 Eastern I.^Jísconsin 11 l1 Northeastern Illinoís . Eastern lowa 13 i3 Nor thr¿estern I11inoís

T4 Northeastern Missourí . Southeastern Míssouri 15 16 Eastern Oklahoma I6 South-central Oklahoma StratígraPhY and SolitarY Rugose Corals 18

South-central Oklahoma 18

1B Lí thos tra tigraPhY Biota 23 24 Age of units Depositional envíronments 25 26 Northeastern Oklahoma LithostratígraPhY .. 26 26 Bio ta 26 Age of uníts 29 Depo sitional environments

Southern Illínois and Southeastern 1l-

Missouri 30 30 Lí thos tra tigraPhY 30 Bío ta

Age of uníts 36 Depositíonal envíronments' 3l Northeastern Míssourí and 38 üles t-central Illinois

3B Li tho s tra tigraPhY Biota ... 44 Intraregional correlations 47

51 Age of units Deposítional environments . "' 53 Northeastern lllinois and Eastern Wisconsín 55

Líthos tratigraPhY 55 Intraregíona1 correlatíons 60 62 Bío Èa

Age of units 66 67 Depo sitional environments

NorthwesËern lllínoís and Eastern Iowa 68

Líthos tra tigraPhY 6B Biota 13

Age of units 75 Depositional environmenÈs 75 '71 Solitary Rugose Coral Assemblages 83 Age of Units and Interregional Correlatíon al_1

88 PaleobiogeograPhY Evolutíon .... 91 93 Sys tematic PaleontologY Suborder Streptelasmatina l^ledekind , 1927 93 Family Streptelasmatidae Nícholson in Nícholson and LYdekker, 1889 93 Subfamily Streptelasmatínae Nícholson ín Nícholson and LYdekker, 1889 93

Genus StrePtelasma Hal1, LB47 93

96 S subr re (Savage, 1913b)

S. amsdení n. sP 1 2.?.

S. leemonense Elias, 1982 133 L4l S. sp. cf. S. leemonense Elías, 1982 L43 S. sp. A S. sp. of Elias, 1982 r46 r47 Genus Grewíngkía DYbowskí, 1873 r47 c. sp. A Subfamíly Dalmanophyllínae Lecompte, 1952 150 150 Genus Bodophvllum Neuman, 1969 B. shorÈi Elias, 1982 i50 151 Suborder Monacanthína Neuman, 1984 151 Famí1y Lambelasmatídae I'leyer, I973 Subfamily Coelostylinae Inleyer, L973 151 151 Genus KeeloPhyllun n. gen. 153 K oklahomense n. sP. rsB References Cíted 179 Pla tes l_v

200 Appendix 1: Growth Form and Curvature 209 Appendíx 2: Bíometric Data 233 Appendix 3: Cardlnal Fossula I'Jídth and Shape 242 Appendix 4: Tabulae Per Unít Length v

LIST OF ILLUSTRATIONS

TexË-figure Page

1. Map of the east-central Uníted States 5 2. SÈratigraphíc nomenclature and age assignments for units ín south- T9 central Oklahoma 3. Stratigraphic sections and locality

maps in south-cenËral and northeastern Oklahoma 2T 4. StraËígraphic nomenclature and age assignments for uníts in northeastern 2l 0klahoma

5 Stratígraphic nomenclature and age assignments for uníts in southern I11ínois and southeastern Missouri 31

6 Stratígraphic secËíons and localíty

map in southern Illinois and southeastern Míssouri JJ

7 SÈratigraphíc nomenclature and age

assignments for units in nort'heastern Míssouri and r¿est-central lllínois 39 I Stratigraphíc sections and locality 4t map in northeastern Missouri '

9 Stratigraphic nomenclature and age assignments for units ín northeastern fl1inoís 56 10. Stratigraphic sections and localíty

maps in northeastern Illínois and v1

eastern l.lisconsín 58 11. Stratígraphic nomenclature and age assignments for unÍts in northwestern Illinois and eastern Iowa 69 \2. StraÈigraphic secti-ons and l-ocality

map ín northwestern lllinoís and

easEern Ior¿a 7T

13. Composíte stTaÈigraphÍ-c sections

showíng age and correlation of uníts

and distributíon of solíÈary rugÕse c.orals in the east-central Uníted States 78 14. Paleobiogeography of Late Ordovícian and earlíesÈ Sílurian solitary Rugosa

in North Ameríca 89 15. Relationship between number of major septa and coral diameter ín SËreptelasma

subre ulare r02

L6. Relatíonship beÈween length of major septa and coral díame ter in StrePtelasma 105 SU aTe 17. Relationshíp between thÍckness of najor

sepÈa and co ra1 díameter in SÈrePtelasma

subr are 108 18. Relationship between width of cardínal fossula and coral diameter ín Streptelasma

subr re 111

19. Number of tabulae per centimeter of coral vl_ ]-

length in Streptelasma subregulare

and S. amsdeni 1i5

20. RelaÈíonship beÈween number of major septa and coral diameter in Streptelasma

amsdeni . L24 21. Relationship between lengÈh of najor septa and coral diameter in Strep telasma amsdení r26 22. Relationship between thickness of major

sep ta and coral diameter in Streptelasma

amsdeni t28

23. Relationship between width of cardinal

fossula and coral diameter ín Stre Èelasma

amsdeni 131 24, Relatíonshíp between number of major septa

and coral diameÈer in Streptelasma leemonense

and S. sp. cf. S . leemonense r36 25. Relationship between number of major septa and coral díameter Ín KeeloPhyllum oklahomense 155 val-l-

LIST OF TABLES

Table Page 1. Latest OrdovÍcian and earliesÈ Silurian solitary rugose corals Ín the easË-central UniÈed States 80 2. Gror¡th form and curvature for Streptelasma

subr ulare, S. amsdgní, S . leemonense

(including S. sP. cf. S. leemonense and

Keelophvllum oklahomense 100

J Proportions of data poínËs above, or on and below, arbitrary 1ínes drawn jn Te.xt-figures 15-18, 20-23, for characteristics of major septa and cardinal fossula in Streptelasma subreeulare and S. amsdeni 104 4. Length and thickness of cardinal septum in Streptelasma subr e and S. amsdeni 110

5 Proportions of each type of cardínal fossula

shape in Streptelasma subregulare and

r. 13 S amsdení 6. Morphologíc characteristícs of Streptelasma

subregulare and S. amsdeni... 118 I

UPPERMOST ORDOVICIAN AND LOI'IERMOST SILURIAN

STRATIGRAPHY AND SOLITARY RUGOSE CORALS

OF THE EAST-CENTRAL UNITED STATES

By

ROBERT J. MCAULEY

DepartmenË of EarÈh Scíences' UniversítY of Manítoba' Inlinnípeg, Manítoba, Canada R3T 2N2

ABSTRACT

succession of three so'lítary Ïugosan assemblages ís recognized ^ \^7ithín the uppermost ordovícian-1o\^Iermost silurian sequence in the east-cenÈral United States. The lowest is a Late Ordovicían assemblage (Elías' ín the upper Maquoketa Group (Richrnondian) ' Salvadorea randi

19B1) occurs in southern Illínois, north\,IesÈern Illinois and eastern Iowa. Grerdínskia canadensis (8i11íngs, 1862) ís presenË in easËern l{isconsín. These speci-es represent the Red River-Stony

Mountain and Richmond solitary coral provínces' respectively' They became extinct when Ehe epicontínental sea withdre\.I at the end of

Ríchmondian time, possíbly due to a glacíoeusËatic sea-level drop' This study is focused on Ëhe middle (Edgewood) assemblage. The strata containíng these corals are thin, dominantly carbonate uníts' due They were deposíted duríng a traûsgressíon from the south, possibly to a glacioeustatic sea-1evel rise. Normal, open marine envíronments vrere introduced to the region. The Edgewood corals \47ere derived from taxa prevíous1y restricted to the continental margin' The Keel Formation of south-central Oklahoma contains Streptelasma subre ate 2

(Savage, 1913b), S. amsdení n. sP.' S . leemonense Elias, t982, s. sp. cf. S. leemonense Grewingkia sP. A' and Keelophy l1um oklahomense n. Ben., n. sp. In southern Illinois-southeastern Missouri, specíes wíthin Êhe Leemon Formation are S. subregulare, S. leemonense,

Streptelasma s p. of Elias, 1982, and Bodophyllum shorti E1ias, I9B2 Streptelasma sp. A. is present in the Noix Limestone of northeastern

Missouri. The overlying Bryant Knob Formation yields S. sub regulare

from the unnamed member and S. subre ulare S . leemonense, plus Grewingkia sp. A from the Kissenger Límestone Member. The Cyrene Formatíon, whích ís laterally equívalent to the Noíx and Bryant Knob,

contains S. subregulare. I¡r uortheastern Illínois' S subregulare is

present ín the Schr¡eízer and Bírds members of the lJílhelrní Formatíon. This specíes has been reported from the base of the Mosalem Formation in northwestern I1línois. These ïugosans comprise the Edgewood

Solitary Coral Provínce. S . subregulare, the dominant speciest exhibits a wíde range of íntrasoecific varíabi1íty.

The Keel Formation, Leemon Formatíon, Noix Límestoner and lower

Cyrene Formation aïe considered to be Late Ordovician (Gamachian) in age. The lower part of the Schweizer Member, Wilhelmi Formation, and

lower part of the Mosalem Formation may also be Gamachian. The upper

part of the Schweizer Member plus the Birds Member of the l,lilhelmí Formation, the míddle portion of the Mosalem Formatíon, the Bryant

Knob Formation, and upper Cyrene Formation are Early Silurían (early

early Llandovery) . Thus, the Edgewood assernblage spans the time

interval from Gamachían to early early Llandovery, and solitary Rugosa cannot be used to delineate the posítion of the Ordovician-Silurian boundary in the east-central United States. 3

the The upper assemblage is characterízed by genera typical of EarlythroughMiddleSilurian.Dalmanopþyllumand,Phaulacrisare (late found wíEhin the upper part of the Mosalem Formatíon early Llandovery) in northwes tern lllínoís. In the upper Elwood Formatíon (1ate early to middle Llandovery) of northeastern Illinois' Dinophyllum and Dalmanophyllum occur' Ithegmap hv1lun Díno 1lum, (1ate and Dalmanophyllum are present in the Bowling Green Dolomíte early Llandovery) of northeastern Missouri. The sexton creek Limestone (rniddle Llandovery) of southeastern Míssouri yields Dalmanophyllum'

The cochrane Formatíon (1ate Llandovery) of south-central oklahoma contains PhaulacÈis. These SÍlurian corals \,üere noË derived from

Edgewood taxa or any known North American Ordovícian solitary

rugosans. 4

TNTRODUCTION

The uppermost Ordovician-lowermost sílurian sequence in the east-central United States ís exposed in eight seParate areas (Text-fig. 1). It comprises Late ordovician (Ríchmondían) strata that are prímarily shales (sylvan Shale and Maquoketa Group), succeeded by domínantly carbonate uníts which are Ëypícally thín and of límíted areal exËent. The 1aËter uníts were íncluded in the Sílurian and assigned to the Alexandrian Seríes by Savage (tgOAa, 1908b, 1909, 1910, tglz,1913a, 1913b, 1gL4,1916, IgL7,1926) and Reeds (19i1). More recenrly, Satterfíeld ( lgTI) studied conodonts in the Gírardeau Límestone of southeastern Missouri and southern lllinois, and considered them to be very lare ordovician ín age. Amsden (197lb, L974, 1980) has worked on the brachíopod faunas, and suggested that the Keel Formalion of south-central Oklahoma, the PetËi¡ Formatíon of noÏtheastern Oklahoma' an oölíte bed in the Cason Shale of north-cenEral Arkansas, the Leemon Formation of southern Illinois-souËheastern Hlssourí, and the Noix Líme- stone of northeastern Míssouri--r,rest-central lllínoís are Late ordovician (Ashgí1l; Hírnantian) ín age. overlyíng uníts, Íncludíng the Cochrane Formation of south-central Oklahoma, the Triplesía alata beds in the Cason Shale of north-central Arkansas, the Sexton Creek Límestone of southern I1linoís-souËheastern IÍissourí, and the Bryant

Knob Formation and Bowling Green Dolomite of northeastern l{íssouri were assigned Ëo the Early Silurian (t landovery) . Thompson and SaËterfield (Ig75) investígated the conodont faunas within the strata contíguous to the systemic boundary in eastern Míssourí and southwestern I1línoís'

The Leemon Formation of southern lllínoís-scrutheastern lfÍssouri' and the Noix Limestone and Cyrene Formatíon of northeastern Míssourí were 5

Text-figure 1.---Map of the east-central United sËates showíng outcrop areas of uppermost OrdoviCian and lowermost Silurian strata (A-H), several structural features of the region, and localítíes mentioned in the text. DeÈails of areas A, B, D-H are shown in Text-fígs. 3, 6,8, 10, and 12. 6

-ù 2 o wtscoNslN i tv I

u v

Co J ri towA F

z 4 lLLlNols 6 NOBIB z XANSAS EAAIN

KANSAS MISSOURI ozAFÍ UPLIÍf

c r, B nn1î*oôoKLAHOMA ARKANSAS

A "{""Ñ oÉooLtsÉ

+' ù' o

GULF OF MEXICO 7

considered to be Late Ordovícían. The overlying Sexton Creek Limestone of southern lllinois-southeastern Míssouri plus Èhe Bryant Knob Formatíon and Bowling Green Dolomite of northeastern Míssouri were included within the Early Sílurían. Elias (1982) suggested that the trtrílhelrní Formatíon of norÈheastern Illinois could be latest Ordovícian (?Garnachían), after examíning solitary rugose corals from that unít plus the Leemon Formation of southeastern Míssouri and the Cyrene

FormaËíon of northeastern Missouri Although there has been a renewal of ínterest in these units and faunas duríng the past 15 years, precise correlations and ages, plus facíes relationships, remain unccrtain to varying degrees within individual areas and on a regíona1 sca1e. This stratígraphic sequence ís of partícular significance because it was deposited at a time

when transgressions and regressíons related to glacial activíty have

been reported from other regions, including Anticostí Island, Qu6bec (petryk, 198la, 1981b; Johnson, Cocks, and copper, 1981), and Scandinavía

(Brenchley and Newall, 1980; Stridsberg, 1980; Brenchley and Cocks,

1982) .

Solitary rugose corals are a common faunal constituent in many

uppermost Ordovician and lowermost Sílurian uníts ín Èhe east-central United States. The purpose of this study ís to precisely document theír straËígraphíc and geogruphic distríbutions ín order to permit

more precise correlaÈions and age determínatÍons, as well as the ínterpretatíon of facies relatíonshíps (prelímínary work was done by Mattison, 1983, and McAuley, 1983). The global changeover from Ordovician to Sílurian coral faunas is poorly understood because those of earlíest silurian age are inadequately known (Hí11, 1981: PP.51' 8

53). The present study will contríbute to a better knowledge of geologíc history ín Ëhe easË-central UniÈed States, plus the paleobiogeographic and evolutíonary history of solitary Rugosa duríng latest Ordovícian and earlíest Silurian time.

ABBREVIATIONS AND REPOSITORIES

A co1l. : T.I{. Amsden collection. E coll.: R.J. Elias collection.

EM coll.: R.J. Elias and R.J. McAuley collection.

EMM co1l. : R. J. Elias , 8.tr^|. Mattíson, and R.J. McAuley collection. S coll.: T.E. Savage collection.

OGS: Oklahoma Geologícal Survey, Norman, Oklahoma' U.S.A.

UCGM: University of Cincinnati Geological Museum, Cincínnatí'

Ohio, U. S .A. UI: Uníversity of lllinoís at Urbana-Charnpaign, Urbana,

Illinois ' U.S.A. USNM: National Museum of Natural Hístory, Smithsonían Institutíon, Inlashington, D.C. U.S.A. ' 9

ACKNOI^ILEDGIÍENTS

This project Íras funded by grants to R.J. Elías from the Natural Sciences and Engineeríng Research Councí1 of Canada, plus a University of Mani.toba Graduate Fellowshíp and Canadian Society of Petroleum Geologists Graduate Student Scholarship to R.J.

McAuley. Field \^7ork r¡Ias conducÈed by R.J. Elias, R.J. McAuley, and

B.ü1. Mattison. Dr. T.l{. Amsden (Oklahoma Geologícal Survay, Norman,

Oklahoma) assisted in south-central Oklahoma, as did Mr. lI. Kuntz in northeastern Míssouri. Dr. D.B. Blake (Universíty of Illinois,

Champaígn, Illinois) arranged the loan of specimens. B.I^1. Mattíson and R.G. ZeLLstra (University of Manitoba, Winnipeg, Manitoba) prepared many thín section. R.G. Zeilstra and C.J. Knapp (University of Manítoba, I^línnípeg, Manitoba) assÍsted wíth photography of specímens. Dr. R.J. Elias (advísor), Dr. I^I.M. Last (Uníversíty of

Manitoba, trIinnipeg, Manitoba), and Dr. R.A. Mclean (Amoco Canada

Petroleum Company Ltd., CaLgary, Alberta) (examiners), and Dr. T.I^I.

Amsden read and criËiclzed the thesís. Marilyn Gray (University of Manitoba, ülínnipeg, Manitoba) typed the manuscrípt. I thank Dr. Elias for his excellent supervísion from the ínítial field work to the finished product. I thank my parents for theír contribuÊions during my extended universíÈy career. 10

STRATIGRAPHIC SECTIONS AND COLLECTIONS Outcrops of uppermost Ordovician and lowermost Silurian strata

ürere examíned in seven areas duríng this study (Text-fíg. 1, areas A, B, D-H). To ensure stratigraphic and paleontologíc control, all sections that r¡rere selected had been described in previous literature' and fossils had been lísted from most (see references cited below).

The 27 localities provide representatíve geographíc coverage within each area. Every sectíon was thoroughly examined for solitary rugose corals, whích were found at 18 of them. All specímens seen l¡/ere collected, except from a few íntervals in which they were so numerous that this was lmpractical (R.J. E1ias, B.W. Mattíson, and R.J. McAuley collection, L982; Elias and McAuley collection, 1983). The relative

abundance of corals was estimated qualitatívely. Additíonal specimens from these sections vüere íncorporated into thís study from collections made by T.I^I . Amsden ín south-central Oklahoma and R.J. Elías in southeastern and northeastern Míssouri. Data were obtained from oËher localitíes in souLhern I1linoís, northeastern Missouri, and

northeasËern Illinois using the collection of T.E. Savage. A total of. 638 solitary rugose corals from the combined collectíons are identifíed herej-n. Locations and stratigraphic-paleontologíc data

are shown in Text-fígs. 3, 6, B, 10' and 12. 11

The locations of straËigraphíc sections examíned in this study are listed below. They are designated using U.S. Geological Survey topographíc quadrangle maps (7224,000 scale). Precise coordinates are measured first east and Ëhen north from the south!üest corner of the map.

Eastern I,Iisconsín

1(Kate1l Falls) .-Bellevue , I,Iis., Quadrangle: 100 mm E' 224 mm

N; SE!4 SErá NE% sec. 32, T23N, R21E. l'Iaterfall and stream va11ey' just norËh of StaËe Route G, 0.5 krn west of junction with State Route V,

pp 189 190 f ig' 2; Brown County, I^lisconsin (Savage and Ross , 1916, . , ' I^Ii11man, I973, p. 13; Mikulíc and Kluessendorf, 1983, pp.26' 28-30'

figs. 1B-20) . 2 (Hieh CliEf).---Sherwood, L{is., Quadrangle: 269 mm E, 153 mn N;

SI^I% SnlZ sec. 36, T20N, RIBE. Abandoned quarry at top of High C1íff, along rrest síde of road through High C1íff State Park, Calrrnet County'

I^lisconsin (Wi11rnan 1973, p. 13; MÍku1ic and Kluessendorf, 1983, Pp. 23, 25, fig. 16).

Northeastern Illínois

3 (Garden Prairíe).- Riley, I11., Quadrangle: 179 mm E, 566 mm N;

nE% SI,rl% sec. 31, T44N, R5E. Abandoned quarry, 0.5 km south of U.S.

Route 20, McHenry County, Illínoís (Savage, 1926, p. 518; Willman'

1973, p. 12).

4( Schwei zer Inles t) .-Channahon , I11., Quadrangle: 302 mm E' T2

418 mm N; SI^l% SEk sec. 35, T35N, R9E. Cuts on both sides of lower (western) railroad, southeast side of Des Plaínes River valley, I^lí11 County, Illínois. Collectíng intervals 4-1, 4-Ia, 4-lc on west síde of tracks. Type section of üJíIhelmí Formation, and íts Schr¿eizet and Birds (lower part) members (Ross, 1962, fig. 1; !ii11man, 1962, p.84, stop 4; Willman, I973r pp. 50, 51, sec. 17; Líebe and Rexroad, 1977' p 854, loc. 8, f ig. 1; Elias, 1982, f ig. 2L, I^1i11 Co. sec.).

5 (Schweizer Norrh) .--{hannahon, I11., Quadrangle: 354 rnrn E, 449 mm N; SI,It4 SW% NE% sec. 36, T35N, R9E. Cut on southeast side of lower (¡,¡estern) railroad, and ravíne from there to southeast síde of upper

(eastern) railroad, at new concrete culvert, southeast sicle of Des

Plaines Ríver val1ey, I^Ii11 County, fllinois. Type section of Bírds

Member (upper part) of !trílhelmí Formation, and Ehvood Formation (Ross, 1962, fíg.1; I{íllman, 1973, p. 50, sec. 16; Liebe and Rexroad, 1977, p. 854,loc. 7, fig. 1; Elias, Ig82, fig. 21, trJil1 Co' sec.).

6 Plaínes l^lest .--{hannahon I11., Quadrangle: 405 mm E, 491 mm

N; NI^i% SE% SI^/k sec. 30, T35N, R108. Cut on southeast side of lower (western) raí1road, southeast síde of Des P1aínes Ríver va1ley, I^Ii11 County, Illínoís. Type section of Drummond, Offerman, and Troutman (lower part) members, Kankakee Formatíon (Ross, L962, f ig. 1; I^lillman' 1973, pp. 49,50, sec. 14; Líebe and Rexroad, 1977, p.854, loc. 6, fig. 1; E1ias, 1982, fig. 2I, h7í11 Co. sec.).

7 (Kankakee RÍver).-Bonf ield, I11., Quadrangle: 340 mm E, 401 mm

N; NEt NI^]t Sl'lk sec. 36, T32N, R108. Exposure on north bank of Kankakee Ríver, just southr^rest of loop road in Kankakee Ríver State Park campground, 0.3 km south of State Route 102 (I^lillman, 1962, pp.82, 83, stop 2; I{i11man, 1973, p. 48, sec. 8). 13

Eastern lowa

B (Kíng) .-Menomínee, I11. -Iowa, Quadrangle: 120 ¡nn E, 105 mm N' to 113 mm E, 133 mm N; E% SE% sec. 27' T88N' R3E. Cut on east síde of U.S. Route 52, just south of Kíng, Dubuque County' Iowa. Type section of Mosalem and TeËe des Morts formatíons (I^Iíllman' 1973, p. 52, sec.

22) .

26 Bellevue .--Spríngbrook, Iowa-Ill ., Quadrangle: 288 mm E'

559 mm N, to 262 mm E, 572 mm N; NE% sec. 19' T86N' R5E' Exposure along west side of U.S. RouÈe 52 and south side of road in Bellevue State Park, Jackson County, Iowa (hrhitlow and Brown, 1963' p' 13; Ross, 1964, p. LIO7, fíg.1; Rose,1967r PP. 44,45, fígs. 2Q,zla Anderson, 1983, fig. 5.6).

Northwestern Illínois ' g (l^línston).----llanover, I11., Quadrangle: 41 rnm E, 461 nm N;

SE¡r SI,i% NE% sec. 11, T27N, RlE. Quarry on east side of road, 1'8 km north of eastern end of l,Iínston raílroad tunnel , Jo Daviess County'

Illínoís (I^Iillman, 1973, p. 55, sec. 34) . 10(Lost Mound).-Green Island, Iowa-I11., Quadranglez 288 mm E,

412 rnm N; SI,tt Nl,I% 5çl-u sec. 28, T26N' R2E. East síde of quarry ín east' bluff of Míssíssíppi Ríver valley, 1.3 km northwest of Lost Mound, Jo Daviess County, Illínois (I^Ií11man, 1973, pp. 52, 53, sec. 24).

mm N; 1i S cha 11e .-Llízabeth, I11., Quadrangle: 92 rnm E, 558

¡¡gl.o ¡El sec. 1, T27N, R2E. Cut on east side of road, 3.2 km southwest of schapvíl]e, Jo Daviess county, I11ínois (tr^líllman, Ig73, p.54' sec.

30)

I2 S tockton .---l(ent, I11., Quadrangle: 148 rnm E, 359 mrn N; SEÞ+ T4

sI,I]¿ SI^1% sec. L7,I27N, R5E. Abandoned quarry aË north edge of ridge' just souËh of road, 4 km southeast of Stockton' Jo Daviess County' Illinois (Willman, 1973, p. 54, sec. 32).

Northeastern Míssourí

13 Bowli Gre .-Bowling Green' Mo., Quadrangle: 197 mm E'

497 mm t{; NI,t% NI^I| sec. 24, T53N, R3W. Cut on north side of u.s. Route

54, 1.5 km northeast of junction with u.S. Boute 61, Pike County, Missouri. Reference section of Cyrene Formation and Bowling Green Dolomite (Koeníg, Martin, and Collinson, L96I, fíg. 15; Amsden' 1974, p. 84,1oc. D, figs. 4, 7; Thompson and Satterfíeld, 1975, pp. 96,99, fÍg. 11, sec. B; Elias, L982, fig. 2I).

14 (Hísei nbotharn Farm) . Mo., Quadrangle: 39 1 urm E, 4I8 -Cyrene, mm N, anð, 392 mm E, .424 mm N; I,I% UI^I% NE% sec. 28, T53N, RII^I. Exposures souÈh (collecting intervaL 14-2) and north (collectíng ínterval 14-1) of abandoned house, just east of State Route D, Pike County, Míssourí (Laswell,7957, p.20, sec.5; Amsden, 1974, p- 83,loc. A, fig' 4;

Thompson and Satterfield, 1975, p. 93, fig. 16). 15 (Calumet).-{yrene, Mo., Quadranglez 415 mm E, 432 rnm N' Ëo 404 mm E, 434 mm N; Sr¿ Str< sec. 2I, T53N, RII^I. Abandoned quarry east of Stark Cemetery, 0.5 km east of State RouÈe D, Píke County, Missouri (Thompson and SaËterfield, 1975, p.93, sec. 5, figs. 15, 16). Collecting ínterval i5-0 ín loose blocks, 15-1 in in sítu strata.

I6 Clinton S ra .-Louisiana, Mo.-I11. , Quadrangle: 312 mm E'

312 mrn N; Sl^Ik ¡¡l'o ¡l^ILo sec. 20, T54N, RII^I. Exposure just west of

Clínton Spríng on \Àrest side of State Route 79, southern edge of Lou{siana, Pike County, Míssouri. Type sectíon of Noix Límestone 15

(Laswell, Ig57, PP. 18, 19, sec.4; Koenig, Martin, and Collinson' i961, p. 34, stop B, ftgs. 2I,22; Birkhead, 1967,loc. I, fig' 4;

Amsden, 1974, p.83, loc. B, tj-g.4; Thompson and Satterfíeld, L975' p. 89, sec. 7, fig. 12; Elias, 1982, p. 40, fíe. 21, loc' 21b)'

L7 (Clarksví I 1e) .---{ larksvi 11e , Mo.-I11 ., and Pleasant Hill tr'Iest'

I11.-Mo., quadrangles: 333 rnm E, 564 rrn N (Clarksville) to 313 mm E'

I mm N (Pleasant Hill l^Iest); SW% sec. 9, T53N, RlE. Cut on r¡est side of State Route 79, northern edge of Clarksvi11e, Pike County, Missouri (Arnsden,1974, p. 84,loc. E, fígs. 4-6; Thompson and Satterfield, 1975, pp. 99,100, sec. 6, fíg. 13; Elias' 1982, p.40,loc' 2la; McCracken and Barnes, 1982, fig. 2). Collectíng ínterval :17-0 at souËhern end of exposure, I7-2a from southern end to central portion, I7-I, la, 2 from central portion, I7-2b, 3 from north end.

1B Kiss er .-Annada, Mo.-I11. , Quadrangle: 15 mm E, 312 mn N; g6t-u sec. 35 (projected) , T53N, RlE. Cut on r¡rest side of State Route 79, Just vlest of Kíssenger Hill and south of spríng. Type section of Bryant Knob Formation and its Kissenger Limestone Member (Amsden, 1974, pp. 84,85, loc. F, fíg.4; Thompson and satËerfield'

1975, pp. 97-100' sec. 11, fíg. 14).

Southeastern Missourí

19 (N ew We11s) .----l,Iee 1ys Landing' Mo.-I11., Quadrangle: 24 mrn E'

254 nn N; Nlf% SI^Ik SI^It4 sec. 9, T33N, R13E. Exposure along channel and east bank of Blue Shawnee creek, 0.5 kn east of New ltlells, Cape Girardeau County, Míssouri (Amsden, lg74r PP. 2Ir 22, 87r 1oc' U, fig'

17; Thompson and Satterfíeld, 1975, p.79, sec. 4, fíg.9; Elias, 1982, p. 39, fig. 2I,loc. 20b) (noÈe: coordínates of this sectíon T6

are incorrect in previous publicatíons) . Collecting ínterval 19- 1 ín northern part of exposure, I9-2 ín southern part' 19-3 ín loose blocks. 20( Short Farm).---tape Girardeau NE, Mo., Quadrangle: 44 mm E'

276 mm N; SEk ¡¡Lo sI,If sec. 21, T32N, R13E. Exposure along creek channel just east of barn, 0.25 km east of State Route hI' Cape Girardeau County, Missouri. Collecting íntervalL 2O-1 in in sítu strata, 2O-2 to 5 in loose blocks. Type section of Leemon Formatíon (Amsden, 1974, pp. 19, 85, 86, 1oc. K, fíg' 16; Thompson and Satterfield, L975, sec. 3, fig. 7; Elias, L982, p.39, fíg'2L,loc'

2Oa).

Northeastern Oklahoma

mm N; 28 (Q ualls) . ---Qualls, Ok1a., Quadrangle: 283 rnm E, 441

¡¡çf sEk N¡¡% sec. 2, T14N, R21E. Exposure on west bank' I4fhite oak Branch of Greenleaf Creek, 1.5 km west of Qualls, Cherokee County'

Oklahorna (Amsden and Rowland,1965, PP. 24,95,96, sec' C1n4, fíg'7, pl. B) .

South-cen tral Oklahoma 2r( Rock Crossine) .-Overbrook , Okl-a., Quadrangle: 310 mm E'

348 mm N; SE% NE% SI^I% sec. 35, T5S, RlE. Exposure on west bank of Híckory creek, east side of road, 0.15 km south of brídge, carter County, Oklahoma (Amsden, 1960, PP. 208-210, sec' Call, panel 1)' Collecting intervals 21-1, la to lc ín different lenses of bíoclastic

limes tone. 22( Cedar Víllaee) .-{urner Fa1ls , Ok1a., Quadrangle: 437 mm E' I7

326 mm N; SEIø NEI'¿ NI,I| sec. 30, TlS, R2E. Cut on \¡/est síde of U.S. Route 77, 0.5 lrn south of junction v¡ith Interstate Route 35, just north of Cedar Village, Murray County, Oklahorna (sectíon enlarged and ímproved since descríbed by Amsden, 1960, PP. 256-258' sec. l"ll7 , panel 1) . 23 (Lawrence Quarry).-Ahloso, Okla., Quadrangle: 93 mm E, 302 mm N to 98 mm E, 296 mm N; Nl^ll-u SEt4 NE% sec. 36 (northern síte), and 92 mm E, 282 mm N; NI^I% NEl-a SE% sec. 36 (southern site), T3N, R5E. East side of rdeal cement company quarry at LaT¡/rence' Pontotoc county'

Oklahoma. Collecting intervals 23-I, 2, 2a, 3, 4 at northern síte, 23a-I at southern síte. Type sectíon of Keel Formatíon and íËs ldeal

Quarry Member (Amsden, 1960, pl. 1, figs. 1, 2, panel 2' pI. A'; 1974, p. 87, Loe. P22).

24 Coal Creek .-Harden Cíty, Okla. , Quadrangle: 253 mm E'

208 mm N; NI^ik SEl¿ NI^i'ø sec. 22, TlN, R7E. Exposure on north bank of Coal Creek, 0.4 lcn east of Gobbler Knob, Pontotoc County, Oklahoma (Amsden, 1957, fig. 5; 1960, pp. 279-282' sec. P9, panel 1; 196I, fig. 2s). 25 (ttunton) .---l^iapanucka North, Okla. , Quadrangle: l4 mm E,

519 mm N; NEl-u Snk NE% sec. 7, T1S, RBE. Exposure 0.5 km south of northeast corner of section, Coal County, Oklahoma. Base of type sectíon of Hunton Group (Amsden, 1960, pp. I82,184-lB8' sec. Cl, panel 2, pI. B). 1B

STRATIGRAPHY AND SOLITARY RUGOSE CORALS

South- central Oklahona

LiËhos trati .--{he history of stratigraphic nomenclature of uppermost ordovícian and lowermost sílurían uniÈs ín the Arbuckle Mountaíns - Criner Hills region of Oklahoma is summarízed in Text- fig. 2, The líthosrraËigraphic termínology of Amsden (1967, L974) is followed hereín (Text-fig. 3) . The areal distribution of the Keel

Formarion was shown by Arnsden (1960, fig. L2; 1974, fíg. 19). Thís unít ís also present ín the subsurface Ltíthín the Anadarko Basin to the west (Amsden, 1975, p. 19) and Arkoma Basin to the east (Amsden' 1980, p. 30). An equivalent dolornític oölite zone occurs in the North

Kansas Basín (Lee, l-956, pp. 48-50; Goebel, 1968r PP' 15, 16)' The type secËion of Ëhe Keel Formation and ldeal Quarry Member is at

Sectíon 23 (Lawrence Quarry) (Maxwell, L936, p' 50; Amsden, 1957' pp' g,11). The formation ís commonly about 1.5 rn thíck, but can be as much as 4.5 m thick (Amsden, 1960, p' 44, fíg' 1'2)'

The Keel comprises tTrree maín lithologies. Most of the formation is 1íght gray oölite, and ís commonly sílicífied (Amsden, 1960, P1. 10, figs. 4-6, pI. 11, figs. 1-6). Some pisolític beds are pTesent at section 23 (Lawrence Quarry). The second lithologY is the yellowish

brown bioclastic calcarenite of the Ideal Quarry Member (Amsden, 1960, p1. 10, figs. 1-3). ItS stratigraphíc position ranges from the base to near the rniddle of the Keel, and this member is present at most outcrops (Arnsden, 1960: pP. 33, 35). The thírd Keel lithology is a ye1low-brown, laminated calcilutíte unit sítuated between oöliËes of the Keel at a few outcrops ín the easteÏTl Arbuckle region, íncludíng Sectíon 24 (Coal Creek) (Amsden, 1960, p' 40)' L9

Text-fígure 2.--11ístory of stratigraphic nomenclature and age assignmenËs for uppermost Ordovicían and lor¿ermost Silurian units ín south-central Oklahoma. E. = early, L. = 1atêr LLAND. = Llandovery SILURIA¡¡ { MEDINA cLtf,Tot¡ øÍ r_co I< 3ãÉ 2 AL AÈORIAN HUNTON OP. CHIMNEYHILL LST. _[-¡ ¿o a too - PI@E r:? o OBDOVICIAN 9tLURlAll ALEXANDRIAT = CHIMT{EYHILL L3T ñ{ o E o J- 2 i!{ ¡ât JI

oRDOVICI^fl SILUFIAN AHAOErl. A9HSILL L. LLANO 1et 1 ELI^9. 19E2i RICHMONDIAtr g^M^cHlax LLATO PRE9EXl 9lUOY

t.) O N) H

Text-f igure 3.-stratigraphic sections (to scale) and locality maps in south-central (A) and northeastern (B) Oklahoma. For legend, see Text-fíg. 10. I.Q. = Ideal Quarry. For precise locations of ttSouth- sections plus references, see ttNortheastern Oklahomatt and central Oklahoma" under STRATIGRAPIIIC SECTIONS AND COLLECTIONS. 23 m 20 a I PONTOTOC co. COAL o CHEROKEE co. lâ co. MURRAY 24. c È co. o25 o o ! E 22. la o 2S (!(! E al o OO Qualls tÐ v, OOOtâ OKLAHOMA ol \!r-È CARTER CO. an=Èo) GC.0¡ ËE Gcc :o(âÈ OKLAHOMA -__l Ito Èr:.o 21 o{ (¡) > o::€ B o km 20 ) à! Q. (ú rÈ"G A l{ ^ o: øo i ! *: È GÈ o a4Ø-o o râì G\ ËËçiS" E o !¡, z u= c I tsts. ùt ìã

f! 23

The Keel overlíes the green Sylvan Shal-e with apparent conformíty (Amsden, 1980, p. 10), and is unconformably overlaín by glauconitíc bioclastic calcareníte Èo light-colored calcilutíËe of the Cochrane Formation or by younger Silurian sËrata. Biota.-Reeds (1911, pp. 259, 261, 267; 1926, p. 470) reporËed crinoída1 fragments, and IísËed níne species of brachiopods, three gastropods, two trílobites, one tabulate coral, md two solitary rugose corals identified as Streptelasma cf. bilateralis and

EnÈerolasma \¡/aynense from the Keel Formation (hís oö1ític member of the Chimneyhíll Limestone). Maxwell (1936, table 1) recorded two specÍ-es of brachíopods, one gastropodr t\,,ro bivalves' one bryozoan' t\,/o Èabulate corals, and one so1íËary coral identified as Zaphrentís subregularís from Ëhe Ideal Quarry Member of the Keel Formatíon (hís

Hawkins Limestone). He also 1ísted two brachíopods, tI^7o gastropods, four tabulaÈe corals, and Ëhe solitary coral Streptelasma sp. from the oölitic porËion of the Keel (Maxwell, 1936, Ëab1e 2) . Amsden (1957, p. 10, 11; 1960, p. 35) noted pelmatozoan p1-ates and snails, and identified two specíes of brachíopods and one bivalve in the Ideal

Quarry Member. He also mentioned pelmatozoan fragments, five species of brachíopods, one gastropod, tl,/o bívalves, and one tabulate coral from Èhe Keel oölite (Amsden, 1957, pp. 12, 15; 1960' p. 44). Amsden (1971b, p. 22) Later listed ten specÍes of brachiopods from the Keel Formation. He subsequently reported alga1-coated graíns, crinoids, gastropods, bivalves, and tabulate plus rugose corals, and described the ten brachíopod specíes in the Keel, íncluding íts Ideal Quarry

Member (Amsden, 1974, pp. 25,26). One of Èhese brachíopods has been 24

identífied from a core through the Keel Formation ín the Anadarko

Basín of western Oklahoma (Amsden, 1975, p. 19). The same species ís known from a core of thís unít ín the Arkoma Basín, easËern Oklahoma (Amsden, 1980, p. 30).

In additíon Ëo prevíously reported fossí1s, ostracodes, stromatoporoids, and colonial rugose corals were observed ín the Keel during thís sÈudy. Cornulitíds are present in the laminaÈed calcílutite unit. The solitary rugose corals Streptelasma sub regulaEe

(Savage, 1913b), S. amsdeni n. sP., S . leemonense Elías, 1982, S. sp. cf. S. leemonense, Grewinskia s P. A' and Keelo llurn oklahomense n. gen., n. sp. are descríbed herein from the Keel Formation. Phaulactís sp. occurs at the base of the overl-ying Cochrane FormaËion (P1. B, fig. 19). Theír stratigraphic and geographic distributions are shown ín Text-fÍg. 3. Solítary corals \,¡ere noÈ observed in the Keel Formation at Section 22 (Cedar Víllage). Age of uníts.-{he history of age assignmenËs for líthostratigraphic units in this area ís summarized in Text-fig. 2.

Amsden (1971b, p. 22; 1974, p.26;1980, pp. 10, i6) considered brachiopods of the Keel FormaËion to be Late Ordovician (late Ashgill; Hirnantían). The underlyÍng Sylvan Shale contains late Late 0rdovician grap tolites of Èhe DicellogËap!lls complanerqgq Zone (Decker, 1935, p. 698)' and Late Ordovician chitinozoans (Jenkins, 1970, pp. 284, 285). Sweet (1983) reporËed Late Ordovician (1ate Edenían to early Maysvillían) conodonËs beneath the Sylvan ín Ëhe I^Ielling

Formatíon. The Cochrane Formation, which overlies the Keel, contaíns the brachiopod Triplesía alata, which Amsden (1971a, p. L45;1980' p. 25

17) has consid.ered to be Early Sílurían (early late Llandovery).

Conodonts considered to be late 1aÈe Llandovery in age were identified in the uppermost Cochrane by Barrick and Klapper (Lg76, p. 66) .

s .-Ams den ( 19 60 pp. 42, 160) Depo itional environments ' 4I, considered the Keel oölite Ëo have formed in \¡Iarm' sha11ow, agitated but not strongly turbulenË \^7ater wíthin the zone of effective light penetration. The gradational contact between the Ideal Quarry calcarenite and Keel oölite probably índícaÈes shoaling (Amsden, 1960' p. 43). The lirhology and beddíng of the laminated calcilutite unit suggest that it may have been deposited ín lor¿er energy condiÈions than other facies of the Keel Formatiorr. 26

Northeastern Oklahoma Lithostratísraphy.--{he history of sËratigraphic nomenclature of uppermost Ordovícían and lornrermost Silurían units ín the Marble Cíty region of Oklahoma is summarízed in Text-fig. 4. The lithostratígraphic termínology of Amsden (1980) is followed hereín (Text-fíg. 3). The PettitFormation is locally present wíthin a 1300

sq. km area in the vícinity of Lake Tenkiller (Amsden and Rowland,

1965, p. 22, fig. 8). The type sectíon is located about 100 n south of Section 28 (Qualls) (Amsden and Rowland, 1965, p' 22, pL' 3, fig. 2). The Pertir ís less than 0.6 m thick. IÈ is an oö1íte that

ís commonly partía1ly or cornpletely silícified (Amsden and Rowland,

1965, pl. 6, fígs. 1-6).

The Pettít Formatíon overlies the Sylvan Shale wíth apparent conformíty (Amsden, 1980, p. 10), and is unconforrnably overlain by the

tan dolomíte member of the Blackgum Formatíon. At Section 28 (Qua11s), the Sylvan is generally ín contact r¿ith the Blackgum, and the Pettit oölite occurs as brecciated blocks at the base of the latter unít (Amsden and Rowland, 1965, p. 24). Bíota.-Fossil debrís including pelmatozoan plates is present in the formatíon, but megafossils have not been found (Amsden and Rowland, 1965, pp. 26, 27). This unít was carefully examined for solitary corals at Section 28 (Qua11s), but none were found (Text-fíg. 3).

Aee of units.-{he histo ry of age assÍgnnents for lithostratigraphíc units ín thís area is summarízed in Text-fig. 4. Amsden (1980' p. 24) tenËatÍvely consídered the Pettít Formatj.on to be Late Ordovícían (Ashgi1l; Hirnantian) on the basís of íts lithology, plus straËígraphÍc relatj-ons and positíon. From the underlyíng Sylvan 27

Text-fígure 4.---ittistory of stratigraphíc nomenclaËure and age assignments for uppermost Ordovician and lowermost Sílurian units in northeastern Oklahona. L. = late. 28

HUFFMAN, AMSDEN AND 1953, 1958 ROWLAND, 1965 AMSDEN,1980

UPPER UPPER LIMESTONE ÍE =lr LIMESTONE MBR. z l¡¡ MBR, =E o f É, l!= f a z ut o Y s z o E sT. o 5= TAN !) IAN 3 CLAIR o (9 DOLOMITE J J DOLOMITE j FM. Y MBR. J o MBR. z o J út J J J o PETTIT OOLITE PETTIT FM MBR. z J o j z = o ; I o (t) 9= o É SYLVAN SH SYLVAN SH SYLVAN SH o o o tr o 29 shale, Huffman (1953, p. 450) and Decker and Huffman (1953) reported the late Late Ordovician graptolite DicellograplEqq cogplanaÈus. The

Blackgum Formation, which overlies the Pettit' contains the brachiopods Tríplesia alata and MicrocarqinafÉe protríplesíana, indicatíng an Early Sílurian (ear1y late Llandovery) age (Amsden, I97Ia, p. I45; 1980, p. 24). Depositíona1 environments.-The Pettít I'ormation was deposíted ín high energy conditions, as índícated by the numerous broken oöids

(Amsden and Rowland, 1965, pp. 22-24). 30

Southern IllinoÍs and SouËheasÈern Missourí Lithos tratisraphv.--{he hís to ry of stratigraphic nomenclature of uppermost OrdovicÍan and lowermost Silurian uníts in Alexander County'

Illinois, and Cape Gírardeau County, Missouri, is summarized in Text-fig. 5. The líthostraÈígraphic terminology of Thompson and Satterfield (i975) is followed hereín (Text-fig. 6).

The Èype section of the Leemon Formation is at Section 20 (shorr Farm) (Thompson and SaËterfield, 1975, p. 77). The formatíon has a maximun exposed thickness of 3.8 rn (Thebes North Sectíon), but is locally absent. Inlillman and Atherton (1975' p. 99) reported that this unit (their Edgewood) thickens eastward ín the srrbsr.trfac.e to as much as 18.3 m. Lithologies wíthin the Leemon include oölite, oö1ític bíoclastic calcarenite, and calcareous shale. Srnall biohermal mounds up to 0.5 m high occur at the base at Section 19 (New I'Ie11s). They

\{ere described by Arnsden (1974, pp. 21, 22). Quartz sand grains are most common in the Illinoís sections (Arnsden, 1974, p. 24), and clasts of the Gírardeau Limestone are generally present near the base. The

Leemon Formation unconformably overlíes the Orchard Creek Shale or' where present, the Girardeau. The latter unit consísts of irregularly bedded limestone with shale partíngs. The Leemon ís unconformably overlaín by the Sexton Creek Límestone, whích contains bands of chert nodules. Bíota.--{^Iorthen (1866, p. 127) reported one trilobíte species' two brachíopods, and a tabulate coral from the Leemon Formatíon ín Alexander County, Illlnoís (basal part of his Clear Creek Limestone). He later identified a solitary rugose coral as Zaphrentis (Worthen, 3i

Text-figure 5.---lÌistory of stratígraphic nomenclature and age

assignments for uppermost Ordovicían and lowermost Sílurian uníts in southern Illinoís and southeastern Míssouri. E. = Early, L' = later

L1and. = Llandovery' GAMACH. = Gamachian' 32

8W^ LLOW. ; WORTHEN, s^vAGE, 9AV^OE, 1926i gAITERFIELD THO HP SOT U ELtAS, r9t2; t865; t868, t868 sAv^GE. s^v^oE, lel3s. l8fgb, WELLER A¡ID PRYOR AND AND o PRESEHT 9HUMARD, t87r 1900â, tsoab 1900, t0to 1g 17 FO9A, r 062 t97i SATTEPFIELO f456. r873 EKBLAw. 10,10 ôTUDY f976 = - z ê 0 E SEXTON 9EX10N gEX E z (ilr^GAFA E sExl0N 8E X ION TON 8E X10il SEXION F FM. K t oP.) 0 CLINTON CREE CRËEX CREEK CREEK CRE EK CRE ÈK CREE X o FM. LSl, LSl L8t. z LSt. J LS1. c s LA1. U qÈU 2 f u z z E U É íJø. o o tJ z : 2 ¿ c a I E e EDOEWOOD I LIMESTO NE ¿ o o U I E (MSRS.3b. EDOEWOOD z EDOEWOOD 2 EDOEWOOD EDOÊWOOD LEEMON LEETOX o Þ (CYRENE FM. - FM. U Fl,l, FIT. Ft. o 3c) MSR,} 2 ! = CAPE ; U U 0 GIRAR DEAU f LSl, c z ; o f CAPE 2 CAPE qIR OIRARDEAU GIRAROEAU OIRARDEAU GIFAFDEAU O IRA RD EAU OIRARDEAU 9 ARDE AU OIRARD E A U OIRARDEAU LST. LST, LSl. LSl. L S1. z LST. L8T. LST. (MaR.36) U o LST. j À : o I 2 0 c T : 2 o ô z 2 z z 2 2 U z z = o F o : : T : =F ts F o õ F I HUDSON = 9 AR D ORCHARD OFCHARD SHALE ORCH oRcftARD ORCHARD 2 U = ORCHARD o OR CHARO R IVER THEBES SH. z CREEK 2 CREEX CRËEX CREEX CREE K o (MBÊ.2b) gH. ; CPÊEK CRE EK GP. = o sH. sH, o o sH. 8H. 8H. ; 8H. ô = =o ô =q E c f o o o =o =o =o t

Should be zíg-zag ttne for Savage, 1926 (, (r)

Text-figure 6.-stratigraphic sections (to scale) and locality map in southern I11ínois and southeastern Missouri. For legend, see Text-figure 10. M.-U. = middle to upper. For precise locations of sections plus references, see "southeastern Missouri" under STRATIGRAPHIC SECTIONS

AND COLLECTIONS.

Thebes North Section.-Thebes, I11.-Mo., Quadrangle (1:24,000): SE% sec. 5, T15S, R3W.

Exposure on east bank of Mississippi River, 1.5 lcn southwest of Gale and 1.8 lrn north of Thebes, Alexander County, Illínois (Savage, 1910, pp. 331, 332, pL. 36, fig. a; 1913br PP. 20, 2I; LgI7, pp. 77-79) (see also Wel.ler and Ekblaw, 1940, pp. 8-10; Pryor and Ross, 1962, PP. 7-10, fig. 3; Satterfield, I97I, p. 266, f.ig. 1; Amsden, 1974, pp. 23,24,86, 1oc. M; Thompson and Satterfield, 1975, pp. 77,78, sec. 1, fíg. B; Kolata and Guensburg, 1979, p. II2l,loc. 1, fíg. 1).

Gale Section.-Thebes, I11.-Mo., Quadrangle (1:24,OOO): NEL sec. 4, T15S, R3Il. Abandoned quarry 0.4 kn southeast of Gale, Alexander County, Illínois (Savage, 1910: PP. 332, 333' p1. 37, fíg. a; 1913b, pp. 21, 22; L9L7, p. 79> (for cut along State Route 3 ín same vicinity, see I,treller and Ekblaw, Ig4O, pp. 8-10; Pryor and Ross, Lg62r pp. 7-10, fig. 3; Cote, Reinertsen, and

Killey, 1968, pp. 7-LO) stop 1, f igs. 6, 7; Amsden, 1974, pp- 23, ?-4, 86, loc' L) " UPPER ORDOVICIAN LOWER SILURIAN RICHMONDIAN G AMACHI A N M. - U. LLANOOVERY

ORCHARD GIRAB_ CREEK DEAU LEEMON FM SEXTON CREEK FM SH- LST.

-l Þ I o m q, o m U) Þ z o o o o 1t n Stteptelasña subÌeguldtø m -{ I O¡ tandl o o (o = Salvadoted A) Qi o (n o E (J> o o o '¡ Ø o ç o o m c Þ ft L c) z1 A) J o eg c F Þ Þ o z_ r o ös o o z o z o Þ Þ Þ I o I o ct ALE XANDER r Þ Þ m Þ Þ co. o Þ

Strepterasm d I e e monen se

20-2 1,

20- | Q, ó3l0¡ -{ o Strepterestt a sub¡egutate ;z o f, ru Strepterasrna leêmonense c Strepterasttta sp. Bodophyllum shottl Delña nophytlurn

jùo

zu) o mm Þ ãc-{ €õ o mZ Þ t- l-J u)@ Strepterasma subtøgutere Ð 3

l-rC 35

1868a,p . 25; basal part of hís Lower Helderberg Límestone) ' Meek and l,trorthen (1868, pl. 6, f igs. 1-6) descríbed and illustrated Ëhe same trílobite and one of the brachiopods lísted previously, plus two additional brachiopods, a gastropod, and a bivalve (their Níagara Group). In the synthesís of his work, Savage (1913b, PP'24,25; I9I7, pp. 82, 83) described tv/enty brachiopods, six gastropods' one bivalve, four trilobiËes, one stromatoporoid, four tabulate corals' plus the solítary corals Zaphren-lE:þ cf . ambigua' Z. subre ula , and

Z. cf. stokesi from the Leemon Formation (his Cyrene Member of the

Edgewood Formation).

- Ams

Leemon Formatíon (included ín his basal Edgewood zone). He reported the presence of pelmatozoan pla:Lesr g,astropods, bryozoans, and coloníal plus solitary corals within the Leemon Formatíon ín Cape Gírardeau County, MissourÍ (Amsden, Ig74, PP. 19, 2L, 22, 85)' From those localities and others in Alexander County, I1linoís, 17 brachiopod specíes were also descríbed (Amsden, L974, fig. 20). Thompson and Satterfíeld (1975, fígs.7-9) identífied a total of 12 conodont taxa within the Leemon ín this region. Elías (1982, fíg. 2I) reported the solitary corals Streptelasma

leemonense Elías, \982, Streptelasma s p., and Bodophyllurn shorti Elias , IgB2 frorn the Leemon Formatíon at Section 20 (Short Farm), and s. subregulare (Savage, 1913b) at Section 19 (New l^lells). During the present study, the latter species was also found at Section 20 (Short Farm), and was identified ín Savagers collection from the

Thebes North Section. S. treemonense ís represented Ín Savager s 36

collection from the Gale Section. DalmanoPhYllun sp. occurs at the base of the Sexton Creek Formation, which overlies the Leemon (P1. B' fj_e. 12). Salvadorea randi (Elias, 1981) was described from the orchard creek shale at the Thebes North sectíon by Elias (1982' pp. 61, 62, p7.6, fig. p; Elias, 1985, p. 45). The stratigraphic and geographic dístributions of these corals are shov¡n in Text-fíg. 6.

Aee of units.-{he histo ry of age assígnments for lithostratigraphic units in thís area is summarízed ín Text-fig. 5.

Amsden (1971b, p. 2l; 1974, pp. 19,22,24) considered Ëhe Leemon

Formatíon to be Late Ordovician (Ashgill) ín age on the basis of braclriopr.rrls. Thompson and Satterfield (1975, p. 79) also considered the unit to be Late OrdovícÍan, based on the abundance of the conodont

Amorpþog4alhCq ordovícicus. SatËerfield (1971) and Thompson and Satterfíeld (1974, pp. 73, 74, fig. 6) assigned the underlyíng Gírardeau Límestone to the very late Qrdovicían on the basís of stratigraphíc relatíons and conodonts representing theír Prioníodus ferrarius fauna. Crinoids in the Girardeau suggested a Richmondian or younger Ordovician (Gamachian) age to Brower (1973, p. 265). Kolata and Guensburg (1979, p. IL22) considered crínoíds in the underlying Orchard Creek Shale to be Richmondían.

From the Sexton Creek Limestone, whích overlíes the Leemon,

Amsden (I974, p. 24) identified the Early Sílurian (early late

Llandovery) brachíop od Microcardinalia sP. cf M. proÈríp1esíana at a section in Alexander CounËy, Illinoís. I^líthin the lower Sexton Creek in Cape Gírardeau County, Míssourí, Thompson and Satterfield (1975' figs. 6, 7, 9) reported conodonts of their Early Silurian Paltodus dyscrítus fauna, which corresponds to the Isriodina irregularíq 37

Assemblage Zone of Nicoll and Rexroad (1968)

( p 19 13b, 20 , Dep ositional envíronments .-savage 1910 ' . 331; PP' 27; I9I7, pp.77,79> interpreted the Leemon Formatíon of Illinois as havíng been deposíted in a channel that \À7as cut ínto the Gírardeau Limestone during an earlíer period of exposure. Ansden (1974, p. 24) noted that Ëhe presence of quartz sand and sílt ín the Leemon of Tllinois and Missouri indicates depositíon near a source area. He observed that brachiopods show 1ítEle fragmentatíon and are commonly articulated, and ínferred moderate energy envíronments. The development of sma11 bíoherms at Section 19 (New Wells) suggests open, normal marine condítíons. 38

Northeastern Missourí and üIest-central l11ínoís Líthostratigraphy.--{he hístory of stratigraphic nomenclature and., age assignments of uppermost Ordovícían and lowermost Silurian sËrata ín Píke County, Missourí, is surunarízed ín Text-fig. 7. The lithostratigraphic termínology of Thornpson and Satterfield (1975) ís followed herein (Text-fig. B). The Maquoketa Shale, Noíx LimesËone'

Bowling Green DolomiËe, and Sexton Creek Limestone also occur across the Míssissippi River in Calhoun and other counties, Illínois. There' however, the Bryant Knob Formatíon is apparently absent (Savage, 1914, p. 29; Trapp, 1950, p. 32; Rubey, 1952, PP. 25, 27; Arnsden, L974, p. 18).

The Noíx Limestone of the Edgewood Group occurs ín a norËhriüest-trending outcrop belE Ëhat ís about 75 km long and at least

11 km wíde (Thornpson and Satberfield, 1975, p.89)' and extends a short distance to the east ín the subsurface of west-central Illinois

(Trapp, 1950, p. 32). The type section of the Noíx ís Section 16 (Clínton Spring). This unit is up to about 2 rn thick, and is thickest along the west bank of the Míssissippí Ríver. It is tyoícally a 1íght gray oölíte (Amsden, 1974, pl. 28, figs. 5,6), and is cross-bedded ín places. At a few 1ocalíties, it is in part argillaceous' phosphatíc' and conglomeraËíc (Thompson and Satterfield, 1975, fLg. 10). The Noix unconformably overlies the Maquoketa Shale, and ís overlaín by the

Bryant Knob Formation or Bowlíng Green Dolomite. It is a lateral equivalent of part of the Cyrene Formation, which ís located to the r¡rest (Thompson and Satterfield , 1975, PP. 85, 103). Geographically, Ehe dístribution of the Bryant Knob Formation approximaÈely coincides wíth thaÈ of the Noix (Thompson and 39

Text-fígure 7.--17ísÈory of stratígraphic nomenclature and age assígnments for uppermost Ordovícian and lowermost Silurían uníts in northeastern Missouri and west-central Il1inois. E. = Ear1y, L. Late, B. K. = Bryant Knob, LL. = Llandovery, GAl"f. = Gamachian, M.-L. = mídd1e to late. 40

WORTHEN, SAVAGE, SWALLOW K E YES, ROWLEY ROWLEY KREY THOMPSON AND AMSDEN 1 866, 1 868b, '1913a. 1913b, PRESENT STUDY 't 855 f 898 1 908 1916 1924 SATTERFIELD, 1 975 1 974 1 870 '19 17 J J J z SEXTON SEXTON CREEK LST J SEXTON SEXTON CREEK LST CREEK LST z CREEK LSI J E 5 tr BOWLING o z BOWLING BOWLING BOWLING l BOWLING GBEEN BOWLING tr BOWLING z z 2 GREEN s BROWN GBEEN GREEN GREEN J DOL, tr GREEN u GREEN LST, f õ u DOL. ooL. f s tr LSI z E ts MAR. MBR. j MBR, a UNNAMED UNIT À À E ô Ø ã L o z NIAGARA J L o o o ) z o J o ô o LST LST. o o o WATSON tr o j KISSENGER z o z o KISSENGER o t2 r o o o LST. MBR. j L LST, MBR. U 6 z o ó)ts o LST. MBR. o CYRENE o o J o u o ¿ u >a U J È J È Y j J 3 = I CYRENL 3 MAR. B v U U F u U u u UNNAMED MBR. Bi u UNNAMED MBR, NOIX ooLllrc 8E LST. MBR. o o Ei a ui o z Ei OOLITE z LST, o o ô o U ô e< o U o ù U tr l U ua 4 U NOIX U NOIX o z CYRENE e OOLITE LST, o NOIX LST MBR. f MBR. Ëì o MBR. o z z z ; z z z f f J f s F ts â o È. E ; E I z HUDSON HUDSON MAOUOKETA MAOUOKETA MAOUOKETA f, CINCINNAII z BUFFALO z RIVER z MAQUOKETA MAOUOKETA SH. Ø MAOUOKETA SH. RIVER sH. sH. sH. SH. SH, GP. ¿ GP, z z SH. U Ø o ts T õ z z= o ui úi z J õ õ õ E 4T

Texr-f igure B.-Stratígraphic secËions (to scale) and locality map in northeastcrn Missourí. For lcgend, aee Text-figure 10. GAI'Í. Gamachían, B. K. = Bryant Knob, KIS. = Kissenger. For precise locations of of sections plus references, see rrNortheastern llissourítt under

STRATIGRAPHIC SECTIONS AND COLLECTIONS. UPPER ORDOVICIAN LOWER SILURIAN UPPER ORDOVICIAN LOWER SILURIAN LLANDOVERY RICHMONDIAN GAMACHIAN LOWER LLANDOVERY = RICHMONDIAN LOWER MAQUOKETA t-Z BRYANT KNOB FM. BOWLING GREEN MAQUOKEÏA NOIX LST B. K. FM. BOWLING U'O SH. GREEN SH. DOL. Kts. DOL. ;{i UNNAMED KISSENGER LST. MBR. LST. MBR.

MBR. @ @J t 1 o c) ylô m 18- r 8-3, 4 -=ø 't T o = o îø a. Ífl t @ c o o o $ o ø 6' I o a)= õ $ õe o o ô I @ si o o Þ -:, o o g¡ J - o o c o o @ Ð 2õi o $ q9 o o o tr { az z o sìä tr¿ o o o c) o o- o I ä; Streptelasma Za Strepf erasma z Þ o A) o subregulare -Þ o o subregulate ! 9 ! ^m f- i o @ m 1- o T 17-2a 1 5-0 15- 1 2 o (I) t- I o rJ g¡ a c) I om [= g) z\m o oI ØO o >o L.o på <+ o trJ o c o l.t z , Hamburg tro mo m¿. o - (rl ";- Streptefasma sp. A gi ; Strepterasma subtegulate Streptelast?a subtegulete c : Dalmanophyllum c { St ¡epte I a sma I e e mon ense I

- 17 -2 14-1 17-2a o I | I ,o-, 4, o o o ãA Þ ncm o oï-{= zÐ- o iã-i o o *z Þ >

Satterfield, 1975, p. 85). The type section of thís formation and its

Kissenger Lj-mestone Men:ber is Section 18 (Kissenger) (Thornpson and

Satterfíeld, 1975, p. 98). An unnamed member that occurs at the base of the Bryant Knob aË the latter section' and locally elsewhere, overlíes the Noíx rÀrith apparent conformity (Thornpson and Satterfíeld'

1975, p. 103). This mernber consists of up to 2 m of dolornitic limestone and/or shale. The Kíssenger Limestone Member is Ëhe upper portíon of the Bryant Knob Formation r,rhere the unnamed member is present, and the only portion of the formatíon that occurs elsewhere.

Thís unit ís up to perhaps 5 m thíck. It ís a líght BraY, medium- Ëo coarse*graíned, massívely bedded bíoclastíc calcareniËe (Ameden, I974, p1. 28, fígs. 3, 4) that overlies the unnamed member wíth apparent conformity, or unconformably overlies the Noix. The Bryant Knob

Formation is overlain unconformably by Èhe Bowling Green Dolomíte.

The Cyrene Formatíon occurs ínurediately wesE of the Noix-Bryant

Knob. The type section, abouË 4 km northeast of Edgewood, Missouri, was located by Thompson and Satterfield (1975, PP. 82, 96). They described Section 13 (Bowling Green) as an excellent reference section.

This unit ís about 2 rn thick. It ís a brown to bluish Etay, fíne- to medium-graíned, dolomítÍc limestone (Amsden, 7974, pL. 27, figs. Ia, b, 2a, b). The Cyrene overlíes the Maquoketa Shale' and ís overlain by the Bowling Green Dolomite. The latter contact is ínconspicuous in the vícinity of Sectíon 13 (Savage' 1913b' p. 23t L9I4, p.29; 1917, p. 80; Rowley, 1916, p. 317; Amsden, 7974, p.11).

The Bowling Green Dol-omite ís the upper unit of the Edgewood Group. The type section is located about 1 km east-northeast of 44

Sectíon 13 (Bowling Green), which Thompson and Satterfield (1975, p.99) designated as a príncípal reference section. Thís unít has an average thíckness of 6 to 9 m ín Pike County (Krey, 1924, p. 27). It consists of buff, earthy, massive dolomite (Arnsden, 1974, Pl. 27, figs. 3a, b, p1. 28, fígs. Ir2),locally with beds of chert nodules ín the upper tr¿o thirds. In the eastern part of thís area, the

Bowling Green unconformably overlíes the Noix Limestone or Bryant Knob

Formatíon. To the west, it overlies the Cyrene Formation. The

Bowlíng Green Dolomite is overlaín unconformably by the Sexton Creek Limestone or younger strata. Biota.--Swallow (1855, p. 107) reported the solitary rugose coral

Zaphrentis cornicula and a tabulate coral from his Onondaga oölite beds (lloix and Bryant Knob) at Louisíana, Míssouri. Other fossíls listed from his Onondaga Límestone (Swal1ow, 1855, p. 219) are not from Ëhe

Edgewood Group of present usage.

From the Noix Limestone plus Bryant Knob Formation (his oölitíc limestone), Rowley (1908, p. 23) recognized one specÍes of stromatoporoíd, seven brachiopods, one tentaculiÈid, tr¡Io gastropods, one cephalopod, two bivalves, one trilobite, two Ëabulate corals, and s o1í tary corals identified as Zaphrentis s p . and Cyathophyllum sp

From the Bowlíng Green DolomíËe (hís brown, earthy límestone), he 1ísted two specíes of stromatoporoíds, three crÍnoids, eleven brachíppods, one conularÍd, ten gastropods, one cephalopod' one bivalve, È\nro cornulitids, four trilobites, six Labulate corals, and the solitary corals Cyathophyllun s p. and Cystí 1lun s p. Rowley found L2 ouE of his 50 species in both st.ratigraphic uníts. 45

From the Noix Limestone plus Bryant Knob Formation (his Noix oölite) ín rhe vicínity of section 16 (clinton Spríng), savage (1913b' pp. 24, 25;1917, pp. 82,83) identified one species of stromatoporoid, 24 brachíopods, eight gastropods, three bívalves, Èhree or four trílobites, four tabulate corals, plus the solitary corals Zaphrentis cf. ambígua, Z. subregularís, and Z. cf' stokesi' From the Edgewood

Group near Edgewood, he recorded one Stromatoporoidr tl^Ienty brachiopods, nine gastropods, three bivalves' one cephalopod, five Èrilobites, three tabulate corals: plus the same solitary corals listed above. A totaT of 32 or 33 of the 59 species described by Savage were recognized ín both collectíons.

Rubey (Ig52, p. 170) ÊabulaËed five specíes of brachiopods and Zaphrentís sp. from the Noíx Límestone in Calhoun County, Illinois'

One cornulitid, 16 brachiopods, unídentífíed bryozoans' one bívalve'

t\47o gastropods, one tentaculítid, four trilobítes' one tabulate coral' plus Zaphrentis sP. anð Z. sp. I'small'r were lísted f rom the Bowlíng

Green Dolomíte. Birkhead (Ig67, table 3) described two species of stromatoporoids associated wíth solitary corals ín the basal bed of the Kíssenger

Límestone Member, Bryant Knob Formation (hís cyrene Member), at Section 16 (Clinton SPring).

Amsden (1971br pp. 2I,22) listed the brachíopod fauna of the

Edgewood Group in Pike County, Missouríoand Calhoun County, Illinois'

Amsden (Ig74, figs. 10, 11, 20) described a total of 23 brachiopod species from these strata. of these , 17 are known from the Noíx Limestone, 14 frorn the Bryant Knob Formation (including cyrene 46

Formatíon at Section 13), and five from the basal Bowling Green

Dolomite at a locality 1.5 krn north-northwest of Section 13 (strata equivalent to the Cyrene FormatÍon). Amsden (1974, p. 12, fíg. 9) demonstrated that, except for pelrnatozoan plates, brachiopods overwhelmingly domínate the fauna ín the above uníts. Bryozoans, trilobites, gastropods, bívalves, tabulate corals, and tentaculítids are rulnor constítuents.

Thompson and Satterfield (7975, figs. 10-15) lisred 49 conodonr species within the Edgewood Group in Pike county, Missouri. of these, they found 16 ín the Noix Limestone, three in an unnamed unít beneath Èhe Bryant Knob For-natiort buL above the Noix at Sectlon 15 (Calumet), eight in the unnamed member and 12 ín the Kissenger Limestone Member of the Bryant Knob, 18 Ín Èhe cyrene Formation, 11 ín their unnamed unít at the base of the Bowlíng Green Dolomite, and 26 in the Bowling

Green. Thompson and SaËterfield (1975, pp. 87, 96, 97, fig. 14) concluded that some conodonts in the Noíx, Bryant Knob, and Bowling

Green are reworked. At Sectíon 17 (Clarksvi1le), McCracken and Barnes

(1982, table 1) identified 16 conodont specíes, of which eight occur

ín the Noix and nÍne in the Bowling Green. They described some of these taxa. Thompson and Satterfield (1975, pp. 97, 9B) reported two graptolite taxa from the unnamed member of the Bryant Knob.

Elias (1982) described the holotyp e of Streptelasma subregulare

(Savage, 1913b) from the Cyrene Formation near Edgewood, Missouri. In thís study, s. subregulare r^¡as found in the cyrener plus the unnamed member and Kissenger Limestone Member of the Bryant Knob Formation.

Streptelasma s p. A occurs in the Noix Limestone, and S . leemonense 47

Elias, 1982 and Grer¿inskía s r¡. A are present ín the Kissenger Limestone.

Rep resentatives of Dinophyllun (Pl. 8, fig. 6), Dalmanophyllum (P1. 8, figs. 13, 14), and Phaulactis (Pl. Srfigs. 20-22) are ídentífied frorn the Bowling Green Dolomite, and Rhegmaphyllum (Pl. 8 figs. 1-5)' Dinophyllurn (P1. I , figs. 7-10), and Dalganophyllurn (Pl. 8, figs. 15' 16) are recognized in límestone patches withín the Bowlíng Green. The stratigraphic and geographic distríbutions of these solitary corals ¿¡s shown in Text-fig. 8.

Int.raregional co rrelatíons .-Earl y workers reported that the upper part of their "oölíte" (= Bryant Knob Formatíon of current terminology)

¿t eastern exposures in Píke Cour-rty, Missourí, contaíns abundant solitary and coloníal corals, as does the upper portíon of the Cyrene at western sections in the vicinity of Edgewood (Rowley, 1908, p. 20;

1916, pp. 319, 320:' Savage, 1913b, p. 22;1917, p. 80). Savage (1913b' p. 25: I9I7, p.83) consj-dered the "oölíte" to correspond to the upper half or two thirds of the Cyrene, and Rowley (1916, p. 319) noted that the coral horízon in the Cyrene is equívalent to his llatson

Limestone. However, Thompson and Satterfield (1975, pp. 83, 85, 87, 96,99, I03) inËerpreted the Noix Limestone of current usage (which underlies the Bryant Knob) as a facies of the upper part of the Cyrene

Formatíon. The conodont faunas that they Ídentífíed from the Cyrene at Section 13 (Bowling Green) also occur in the Bryant Knob (Thompson and Satterfield, 1975, figs. 10, 11). On the basis of brachiopods and lithologic símilarity, Amsden (1974, pp.9,11, 14r 15) considered the upper half of Thompson and Satterfield's Cyrene at Section 13, plus Rowleyrs l¡Iatson Límestone, to be Bryant Knob. The interpretatíon that the Cyrene FormatÍon is a facies equivalent of the Noix Limestone plus 48

Bryant Knob Formatíon is followed herein (Text-fig. 7) . S treptelasma subregulare occurs in the Cyrene and Bryant Knob.

Strata overlying Ëhe Maquoketa Shale in a quarry located 1.5 km north-north\trest of Sectíon 13 (Bowling Green) were assígned to the

Bowling Green Dolomíte by Amsden (L974, p. B). He identified five brachíopod species from Ëhe lower 3 m'of that unít, whích was tentatively correlated wíth the Noíx Limestone (Amsden, I974, pp. 15,

18). Three of the brachiopods occur ín both the Noix and Bryant Knob Formatíon, one ís known from the Bryant Knob, and one ís unique. It ís suggested herein that these beds, no\,/ covered by water, correspond to the Cyrene Formatíon.

Amsden (L974, pp. 16-18, figs . 12, 13) considered two hypotheses for the relationship between the Bryant Knob Formation and overlying

Bowling Green DolomiËe. 0n the basís of lithostratigraphic data, he favored the ínterpretation that these uníts are laterally and verÈícally intergrading facíes, rather than discrete units having separate depositíona1 hístories. Amsden ínferred that basal strata of the Bowling Green at Sectíon 17 (Clarksvílle) are equivalenË to the unnamed dolomiËic mernber comprísing the lower portíon of the Bryant Knob at Section 18 (Kíssenger) (see Text -Ííg. 8). At the latter 1oca1iÈy, a thin bed containíng abundant solitary corals ís present at the base of the Kissenger lrimestone Member, whích comprises the upper portíon of the Bryant Knob. This bed is also sítuated at the base of the Kissenger at Section 16 (Clinton Spríng), where the unnamed member is absent (ElÍas, 1982, p. 40, fíg. 21; Birkhead, 1967, fig. 7), and has been reported in the same stratigraphic position at a 49

loeality about 2 km southeast (Rowley, 1908, p. 20). During the present

study, this solítary coral bed was also found at the extreme sout.hern

end of SectÍon 17, where it is bounded by shale ínterbeds, overlies the Noix Limestone along an írregular contact, is overlain by the Bowlíng

Green along an undulatory surface, and pinches out norËhlrard along the exposure. The coral bed, containíng abraded and a1gal- andfor

stromatoporoid-coated solitary rugosans, is ínterpreted as a 1ag deposit and ís considered to be a synchronous marker. streptelasma

subr are , the only solíËary rugosan speci.es in the coral bed,

occurs in the unnamed member plus other strata included ín the Kíssenger Límestone Member of the Bryant l(nob Formatíon. The solÍtary coral

assemblage ín the basal Bowlíng Green Dolomíte at Sectíon 17, both above and lateral Èo the coral bed, ís entirely different. rt ís inferred

that the unnamed member of the Bryant Knob is older than the Kissenger

Límestone Member, which ín turn is older than the Bowling Green Dolomite. The above interpretation, based on the distríbutÍon of solitary Rugosa, ís consístent wíth the nature of contacts between the various units ín this sequence. I^lhere the unnamed member of the Bryant Knob

Formation is present (e.g., section 18), it overlies the Noíx Límestone wíth apparent conformity (Thompson and Satterfield, !975, p. 103).

I^Ihere the solitary coral marker bed at the base of the Kissenger Limestone lfember of the Bryant Knob overlies the Noix, the contact is unconformable (e.g., sections 17, 16: see prevíous paragraph and E1ías, 1982, p. 40). The contact between the Bryant Knob and Bowllng Green is unconformable at some sections (e.g., Sections LTr lB; see previous paragraph and Thompson and Satterfíe1d, L975, pp.98, 103). It l_s 50 concluded that the unnamed member and Kissenger Limestone l'fember of the Bryant Knob Formation, and the Bowlíng Green Dolomite' are díscrete units, as recognízed by Thornpson and Satterfield, (1975, p. 103).

Thompson and Satterfield (1975, PP' 89, lO0, figs' 13, 14) reported an unnamed unit composed of soft, whÍte limestone locally present at the base of the Bowlíng Green Dolomite. It was described as thin "lenses" on the Bryant Knob Formation at Section 18 (Kissenger), and as two 1owttmoundstton the Noix Limestone at Section 17

(Cl¿rksvílle). Thompson and SatterfÍeld noËed Ëhat the "mound" aË

the north end of Ëhe latter section ís associated with an írregularity along the upper surface of the Noíx, aud is enclosed by a thin sh¿]le seam. During the present study, this unít was not exposed at Section 18, but twottmoundstt were observed on r¡/eathered faces of the exposure at Sectíon 17. One was at the norËh end, and the other was located toward the south. It is uncertain r,rhether these are the same "moundstt

reported by Thompson and Satterfíeld. In 1983, slumping along parts of Section 17 exposed fresh surfaces. Two irregular patches composed of soft, whíte 1ímestone that is índístínguíshable from the "mounds" Ì.{ere observed wíthín the Bowling Green Dolomite about 3 m above the ttmound.tt Noíx. one r¿as sítuated above, and separated fromrthe southern The other was found farther north, along part of an inclined joint or fracture. It contained chert nodules at Èhe same stratigraphic positions as the surrounding dolomíte. These observations suggest that areas of lirnestone at the base of, and within, the Bowling Green represent undolomiËízed remnants of Èhis unit' rather than a discrete

stratigraphíc interval. Dalmano 1lum and Dínophyllum have been found in both lithologies. Although Rheginaphyll.um is recognízed 51 only ín the limestoneand PhaulacÈís is knor,¡n only from the dolomite' these apparent differences may be related to Èhe overall rarity of solitary corals ín the Bowling Green, and the relatively poor preservation of fossíls Ín the dolomiËe'

Age of uníts.-{he history of age assígnments for lithostratigraphíc uníts in this area is summarized in Text-fig' 7 ' Brachiopods of the Noix Límestone r¡7ere consídered to be Late Ordovician by Arnsden (1971b, p. 22; 1974, pp. 13, 14)' Arnorphognathus ordovicicus and other conodonts in the Noíx índícate a Late Ordovicían age (Thornpson and Satterfield, 1975, p. 87). McCracken and Barnes

(1982, p, 1477) noted that the Noj-x conodont fauna has characterístícs of a slíghtly rnodífied Fauna 12 (late Ríchrnondian) rather than Fauna 13

(Gamachian). Thompson and Satterfield (1975' p. 93) reported the

Late Ordovícían Príoníodus ferraríus conodont fauna from coquina (their bioherm) situaËed beneath Ehe Bryant Knob Formatíon at Section 14 (Higginbotham Farm).

Amsden (Lg7Ib, pp. 2L, ?2;1974, p.14) tentatively assigned the

Bryant Knob Formatíon Èo the Early Silurian (early Llandovery), priruarily on the basis of stratigraphic position and the absence of certain characËeristíc Noíx brachiopods. Conodonts ín the unnamed

member at the base of the Bryant Knob Formation ínclude representatives of A. ordovícicus' Icriodella? s p. r and the Paltodus dyscrítus fauna

(Thompson and Satterfíeld, 7975, P. 97, figs' 10' 14) . The conodonts ' plus graptolites (Berry ín Thompson and Satterfie ld, L975, pp. 97, 98)

r^rere considered to indícate an Early Silurían age (Thornpson and Satterfield, 1975, p. 101). The overlying Kíssen ger Límestone Mernber of the Bryant Knob contaíns A. ordovicicus plus the Prioniodus 52 ferrarius and Paltodus dyscritus faunas, and vras also referred to the

Early Silurían (Thornpson and SatterfÍeld, 1975, p.101, fígs. 10, 12, 14,15). Nowlan (in Bolton and Nowlan, 1979, pp. 5,2I) suggested that this mixed fauna íncluding A ordovicicus plus Paltodus dys critus night be Late Ordovician, based on an occurrence elsewhere in undoubtedly Ordovicían strata.

Brachiopods in the Cyrene Formation as recognized herein were tentatively assigned Late Ordovician and early Llandovery ages by

Amsden (1974, pp. 14, 15). Thompson and Satterfield (1975, p. 96, fíe. 11) reported A . ordovícicus plus the Príoníodus ferrarius and PalËodus dyscríËus faunas ín the Cyrene. They consídered Èhis unít to be Late OrdovicÍan, but it ís hereín equated wÍth the Noix plus Bryant Knob, as discussed previously.

Thompson and Satterfield (Ig75, pp. 96, 97, 101, 102) identífied the Paltodus dyscritus fauna in the Bowling Green Dolomíte (includíng

Ëheir unnamed unit), and concluded that this formation is Early Sílurían. They considered conodonts ín eastern exposures to be younger than Ëhose ín western sectíons on the basis of three specimens identifíed as Neospathognathodus cel1oni. McCracken and Barnes (1982, p. 1475) suggested that the laÈter conodonts represent Oulodus? cf.0.? nathani, of which they found one specimen in the Bowling Green. On the basís of the latter índividual, they ínferred that this unit may be earliest Llandovery in age (McCracken and Barnesr l9B2, p. 1477).

The Bryant Knob Formation, Bowling Green Dolomíte, and Sexton

Creek Formation were assígned to the Icriodina irregularis Assemblage

Zone of. Nícol1 and Rexroad (1968) based on the presence of the P. dyscritus fauna (Thompson and Satterfield, 1975, p. 70). 53

Savage (1913b, p. 30; 1.917, p. 88), I.Iillman (7973, p. 16), and

I,Jíllman and Atherton ( I975, p, 97) reporËed the brachiopod Platymerella manniensis at the base of the Sexton Creek Límestone (Kankakee) ín northeastern Míssouri and adjacent lllínois. This zone v/as placed ín the rníddle Llandovery by Berry and Boucot (1970, pl.2). Specimens of

MLcrocardínalia s p., also f rom the Sexton Creek, r^rere considered to be late Llandovery by Amsden (1974, pp. 18, 24).

Depos itional environments .-S avage (1914, p. 30) concluded from the 1íthostratÍgraphic record that the sea ín which the lorser Edgewood

Group was deposited was deepest in the r¡rest, where the Cyrene Formation accumrrlated, and hecame plîogressively shallower to\.,rard the east, where the Noíx Limestone was formed. The shorelíne gradually receded

\¡/estward during Bryant Knob time. Deposítion of the Bowlíng Green

Dolomite was ínitiated by a slight up1íft (but not emergence) to the \"/est and subsídence to the east, resultíng in an eastward onlap.

Thompson and Satterfíeld (Ig75, pp. 93, 103, fig. 16) ínterpreted a coarse, bioclastíc 1írnestone situated beneath the Bryant Knob Formation at Section 14 (Higginbotham Farm) as a bioherm. This unit is hereÍn considered to be a coquína within the Bryant Kncb Formatícrr.

They suggested that ít v/as a sourorÌ of nuclei for oöíds thaL formed to the east, and acted as a barrier that separated Noíx and Cyrene deposítion. McCracken and Barnes (1982, p. I477) consi-dered conodont assemblages to indicate that the Noix Li-mestone formed in relatively shallow vrater, and the Bowlíng Green Dolomíte was deposited during a transgression. On the basís of conodont data, Thompson and Satterfield

(1975, p.97) concluded that deposítion of the Bowling Green began earlíer at Section 13 (Bowling Green) in the west than at Section 17 54

(Clarksville) in the east. However, McCracken and Barnes (1982, PP.

1475, I477) ínterpreÈed conodonts from the latter section as representing an earlier zone than that indicated by Thompson and Satterfíe1d. The latter authors suggested that 1oca1 structural movements contributed to the complex facíes relations and unconformities in the Edgewood sequence (Thornpson and Satterfield' 7975, p. 103). 5s

Northeastern Tllinois and Eastern l^Iisconsin

Lithos tratigraphy.-The hís to ry of stratígraphíc nomenclature of uppermost Ordovician and lowermost Sílurian strata ín Will County and vícinity, I11inoís, ís summarized in Text-fig. 9. The lithostratigraphic termínology of l,tríl1man (1973) is followed herein

(Text-fíg. 10).

The areal distribution and thíckness of the Alexandrian Series was shown by Llillrnan and Atherton (1975, fig. S-14). The ltlílhelmi Formatíon ís exposed at only a few localities. The type sectíon of thís formaËion plus íts Schweizer Member is at Section 4 (Schweizer

I.iest), and the type section of the BÍrds Member ís at Section 4 plus

Section 5 (Schweizer North) (t^li1lman, 1973, pp. 12-L4). The Wí1he1mi

ís up to 30 rn thick where it fil1s or nearly fills channels eroded into the underlyíng Maquoketa Group, but ís thín or absent elsewhere in the area. The Schweizer Member, whích is up to 24 m thíck, is generally present only where the formation is relatively thick. The lower portíon consists primaríly of gray, dolomitic shale, whereas the upper part is very argillaceous, si1ty, thín1y bedded dolomite.

This unít is overlain conformably by the Birds Member, which ís up to 6 rn thick. The Birds is a gray, slightly argillaceous, flaggy dolomite.

The tr^Iílhelmí Formation unconformably overlies strata of the Maquoketa

Group, ranging from the uppermost unit, Ëhe Neda Formation, down to the top of the Fort Atkinson Limestone, whích underlies the Braínard Shale. The ItIilhelrni is overlain conformably by slightly argillaceous to pure dolomíte of the Elwood Formation, whích contains numerous layers of chert (Wíllrnan,7973, p.14). The type section of the 56

Text-figure 9. --tlistory of stratÍgraphíc nomenclature and age assignments for uppermost Ordovician and lowermost Silurian units in northeastern Illinois. E. = Early, L. = Late, SIL. = Sílurlan, ALEX. = Alexandrian, NIAG. = Niagaran, GAM. = Gamachian. 57

F WORTHEN, BANNISTER, SAVAGE, sAvAGE. 1926: WILLMAN,1973; z> SAVAGE WIL L MAN, UO PERCIVAL 1866, 1871 1470; SAVAGE SAVAGE 1913a,1913b SAVAGE g62i LIEBE AND Ø) 1 856 BRADLEY. SHAW. r910 1912 1917 1914 r9 t6 I REXROAD. r977 UF 1870 1873b BOSS.1962 Eq À

o J LST SEXTON SEXTON KANKAKEE KANKAKEE : CREEK CREEK LST. FM. NIAGARA 2 (BRASS- (BRASS- KANKAKEE GP. 2 L ST. FIELD) LST FIÊLD) LSI E U E z ELWOOD FM. z z LST I o E BOWLING o f z ESSEX GFÊE N o c MOUND tr NIAGARA f L ST. o BIRDS MBR. z Þ z I z ESSEX LSI. MBR. L ST. L ST, j (, È LST. J o EDGEWOOD r J : z U ESSEX LST. EOGÊWOOD ( z J LST. MBR. CH AN_ J : NAHON) U= u LSÌ. I ¿ scr'twEtzER CHAN- CHAN- ru CHAN- CHAN- MBR. U NAHON U NAHON NAHON OQ LST. NAHON = j ) LST LST. ôo LST. MAR. CINCINNATI ùo MBR. o GP. = z z NÊDA FM. z z U À f ; ¡ o ; ts z BLUE SH. ) CINCINNATI MAOUOKETA z MAOUOKETA z MAOUOKEIA MAQUOKETA MAOUOKETA MAOUOKEIA u o I GP, sH. sH. SH, sH. sH. sH. o ø l BRAINÀRD FM f o =o o t; 9 o =o G 5g

Tex.t*fígure 10.-=-stratigraphíc sectíons (to scale) and locality maps Ín northeastern Illinois (tr') and eastern l,Iísconsfn (G). L. S. B = Líttle SLurgeon Bay, U. = Upper. For precÍse locations of sectíons plus references, see ttEastern IüisconsÍntt and ttNortheastern Illinoistt under STRATIGRAPHIC SECTIONS AND COLLECTIONS. 59

U U z F U o o Y o o vvyv É YT 6 MCHENRY CO. z z a I 3 I o Y 9 z j È ô I

; :G

tLLlNols cÈi.s DU PAGE a.! co. oÈ o :6 cooK co, 1m ôô ç 6 È sÊ E 5 6 6 SECTION Ê (PLAINES o channahon o wrLL co E Custe¡ WEST) GRUNDY a Park q. o km 20 co. K ANK AK EE ¡ Essex co. LEGEND LITHOLOGIES LIME STONE

DOLOMITE WISCONSIN G -----7- DOLOMÛtC _/- . LI MESTONE ooF co. -._7- SHALE a o ""/ ¿ CALCAREOUS SHALE oØ c L DOLOMITIC SHALE @ o ^^t^ a I BROWN /_- õ a CHERT OR co. 0 slLlclF lcA I loN o SECTION 5 F I (SCHWEIZER o ^u 9o ARGILLACEOUS o È - - 'ìó ¿ 3.3 NORTH) JO o EO z I CONGL OMERA T IC I o ¡ È a _/- o :ô o o o ooLtTlc J =j r u, õg ¡J SOLITARY CORAL = _¿_ -¿ "3 j> - MARKER BED o E ;s FACIES CONfACT ù¡ ! o IU _ _r- DEFINITE a f J-L z I z o Ø _J FACTES CONTACT E 4 :o õz // fr o -/-' È6 _-/_ _ APPROXIMATE f o or;3 J o EE ôo 2 o> --L O U) J Qd CORRELATION = T X u o: *ã u) E AMI NED É. E o- DEFINITE d POSITION IN fE E u UNCOMMON o Éä SECTION 3 SECTION 4 d8 INÏERVAL UNCERT A IN RARE j (GARDEN PRAIRIE) (SCHWEIZER WEST) 60

Elwood Ís Section 5 (Schweizer North). To the north, in eastern !üisconsin, the lower portíon of the

Mayville Dolomíte ís equivalent to the l,Jílhelmi-Elwood sequence

(Savage, 1916, pp. 310, 31I; I^Iil1man, 1973, p. 13; Mikulic and

Kluessendorf, 1983, fíg. 2). The Schweizer Member ís traceable eastward in the subsurface into northv¡estern Indíana, where it is included rnrithin Ëhe Sexton Creek Límestone (Rexroad and Droste, 1982, pp. 4r 5, fig. 3). The Birds Member and Elwood Formation may also be present ín this region, but are not differentiated (Rexroad and Droste,

1982, p. L2) .

Intraregional correla ti.ons .-Sav age ( 19 10, pp. 334, 335) proposecl the name Channahon Limestone for Alexandrían strata in the vicinity of Channahon in I^Ii11 CounËy, Illinois, On the basís of an exposure near Essex ín Kankakee County, Savage (1912, pp. 100, I02) established the term Essex Límestone for Alexandrian strata above the posítíon of the Channahon, up to and including a zone containíng the brachiopod

Platymerella manniensís . He subsequently lowered the upper contact to the top of a fossilíferous limestone unit (Savage, 1913b, p. 28;

1917, p.86). Using data from addítional exposures, Savage (1914, pp

31-33) considered the Channahon and Essex to represent the 1ower,

"more fossiliferous portíon of the Edgewood Formationril and assigned

Ëhe ttalmost barren magnesían límestonerr between the Essex and P. mannl_ens1s zone to the Bowling Green LímesËone. He later included the

D manníensis zone at the top of the Edgewood (Savage, 1916, p. 315), but finally íncluded that zone at the base of the Kankakee Limestone

(Savage , 1926, p. 518) . It is suggested hereín that the Schweízer Member of the l^lilhelrni 6I

Formation in hlillmants (1973) stratigraphic revision corresponds to the I'more fossíliferous portion of the Edgewoodr" or Channahon and Essex, of Savage (19.13b, I9I4, l9I7). The Bírds Member of the I'trilhelmi is considered equívalent to hís ttalmost barren magnesian limestoner" or Bowling Green. The Edgewood (Channahon) stratigraphíc sequence descríbed by Savage (1926, p.518) neal Belvídere ín Boone County is very simílar Èo that at Section 3 (Garden Praírie). At the latter locality, the basal bed above the Maquoketa Shale, plus the almost barren flaggy dolomite above it, was identifíed as the I^lilhelmi Formation by l,Iillrnan (1973, p. L2) and is herein assigned to the Birds Member. The overlying dolomite containíng chert layers represents

the Elwood Formation (I^li11man, 1973, p. 14).

Along the Du Page River about 7 to 9 km north of channahon' D.J. Fisher (Ig25r pp. 26,27) described a unit of gray, flaggy dolomite and an overlying ínterval of dolomite contaíníng chert layers,

siEuated beneath the P . manníensís zone at the base of the Kankakee. Those strata probably represent the Bírds Member of the I'trilhelmí Formation and the Elwood Formation, respectively. I^Iillnan (1973' P. 14) noted that the conËact between the Elwood and Kankakee formatíons is situated within the P. manniensís zQne, which is 2.6 m thíck ín the víciniÈy of the type Elwood (Ross , 1962, fíg. 1). He also stated Èhat beds containing P. manníensis at Ëhe top of the !trílhelmi

Formation near Essex may be equívalent Lo the Elwood. Along the Kankakee River near custer Park ín l,trill County,

savage (1913b, p. 26; 1917, p. 84) reported "a bed of iron-stained

oolite ... which ís thought to be the equivalenË of the Noíx oolite ín Missouri and western Illinoisr'r sítuated above the Maquoketa 5¡¿1s 62

and beneath a unit resembling his Bowling Green Limestone. He considered the oölíte to be the youngest member of Ehe Maquoketa (Savage, 1916, p. 306). Arhy (1928, pp. 33-35) identified this unit as the Noix Oölite Member of the Edgewood Formatíon. It ís the Neda Formatíon of the Maquoketa Group in current nomenclature (l'trillrnan and Buschbach, 1975, p. 86). At Section 2 (Hígh Cliff) in eastern Wísconsin, I^líllrnan (1973' p. 13) noted that the lower 3 m of the Mayville Dolomíte, which overlies the Maquoketa Shale, resembles the l^Iílhelmi Formation, and

the overlying 6 m of Mayville is like the El¡¡ood Formatíon. Wíllnan (1973, p. 13) stated that the Mayvìlle at Section I (Kate11 Falls) consists largely of Kankakee 1íthology, but Ehat approxímately the lower meter overlyíng the Neda Formatíon is sírnílar to the l{ílhelmi.

Biot-a.-savage ( 1913b, p. 27 ; I9l7 , p. 85) described eleven species of brachíopods, Ëhree gastropods, one bivalve' one cephalopod' three trílobítes, one osËracoder plus solitary rugose corals identified as Zaphrentis ambigua, Z. subregularis, and Z. stokesí from the lower

part of the Schweizer Member, I,Iílhelmí Formatíon (his Channahon), along the Des Plaines River about 1.6 km southeast of Channahon. He noted that corals were restrícted to hís bed 2 (Savage, 1913b, p. 26;

I9I7, p. 84). Along Èhe Des Plaines Ríver, 3.2 k¡n south of Channahon,

Savage (1914, p. 31) reported that strata correspondíng to his bed 2

overlíe Ëhe MaquokeËa Group. From a zone 1.5 to 2.1 m above those strata, and from an equívalent zone exposed 2.4 kn farther along the

river from Channahon, he identífied seven species of brachíopods' one gastropod, one trílobite, and one tabulaËe coral. Savage (1914' p. 33) 63

considered the beds containing these fossils to correspond to his

Essex. They probably represent the upper part of the Schweizer Member. At the latter localíty, overlying strata up to a posítíon

that would be 5.8 to 6.4 m above bed 2 contain two brachíopod species

(Savage, 1914, p. 31). Savage (1974, pp. 32,33) indícated that rhose st.rata are equivalent to his Bowlíng Green. They probably belong to the Bírds Member of the WilhelmÍ Formation. From the l{ilhelrní

(his Essex) along Horse Creek about 2.4 km east of Essex in Kankakee County, Savage (1913b, p. 291' I9I7, p.87) lísted 17 species of brachíopods, five gastropods, one cornulitid, two bívalves, two tabulate coraJ-s, p Ius Zaphrentis sp. Savage (1926, p. 5I8) reported

Z subregularís from the Birds Member of Èhe l^Iílhe1rni (his Edgewood), and three species of brachíopods from the Elwood Formation (also his

Edgewood), about 5.5 km south of Belvidere. D.J. Fisher (L925, pp. 26,27) lísted four species of brachiopods and a trílobíte from his Edgewood along the Du page Ríver about 7 km north of Channahon. Those strata possíbly represent the Birds

Member of the l.Iilhelmí Formation.

From the l^lilhelm:i (his Essex) at Savagef s localiËy near Essex,

AËhy (1928, pp. 40r 4L) reporÈed two specíes of cornulítids, one tentaculítid, 29 brachiopods, seven gastropods, 11 bivalves, one conularíd, algae?, two tabulate corals, and solitary corals ídentífÍed as Z. stokesi and Z . subregulare. He also lísted one s pecies of tentaculitid, seven brachiopods, one trilobite, and algae? from the same unít exposed along Horse Creek 0.4 km west of Custer Park in l,rlill County. 64

Ross (1962) descríbed three species of graptolites from the argillaceous dolonr-ite ín the upper part of the Schweizer Member, tr^Iilhelrni Formatíon (his Edgewood), at Section 4 (Schweízer trIest). His co11ecËíon \^Ias subsequently reexamíned, and four species were recognized (Berry and Boucot, 1970, p. 145). Buschbach (1964, p. 59) reporËed scolecodont fragments in the l^Iilhelmi-Elwood sequence (his

Edgewood) ín northeastern Illínois. Liebe and Rexroad (L977, fÍgs.

2, 4) reported 12 specÍes of conodonts from the Schweizer Member of the l,rlílhelmí Formation in üIill County, 29 specíes from the Birds

Member, and 29 f.rom the Elwood Formation. Collectíons l¡¡ere made at Sections 4,5 and 6. MíkulicreL al. (1985, p. i0) reporÈed lingulid brachiopods, trilobites, and trace fossíls ín the basal shaly straËa' and gastropods, trilobites, brachíopods, bryozoans, pelmatozoan debris, plus orthoconíc cephalopods ín the upper dolomític part of the l.lí1he1mi. ElÍas (7982, pp. 40,57, fig. 2I) studied two of Savage's

collections of solitary corals from the Channahon Límestone. These

ínclude specímens that Savage had identified and illustraËed as

Z. ambigua ¿nd Z . subregularís. Elias concluded that they represent

one sPe cíes, Streptelasma subre re (Savage, 1913b). He assumed

they came from the upper part of the tr^Iilhelmi Formation, based on statements in Ross (1962, p. 1385) and l{illrnan (1973, pp. 12' 13). However, from informatíon presented by Savage (1914, p. 31; 1916, p.

306), and collections made duríng this study at Section 4 (Schweizer hlest), it is apparent Ëhat the species also occurs in Èhe lower portíon of the Schweizer Member. Brachiopods, bryozoans' trilobites,

gastropods, cor:nulítids, and colonía1 corals r^rere observed at the 65 latter locality. During the present study, additíonal so1ít.ary corals obtained by Savage ín the vicinity of Channahon were examíned. S . subregulare is the only taxon that is represented. The same specíes occurs in his collection from near Belv:idere, and has been found in the Bírds

Member of the l,lílhelrni Formation at Sectíon 3 (Garden Prairie).

Solítary corals r¡/ere not observed ín the Birds Member at Section 5

(Schweizer North). The gene ra Dinophy11um (P1. 8, fig. 11) and

Dalmanophyllum (P1. 8 , fí9. 17) appear in the upper portion of the Elwood Formation at Section 6 (Plaines l^lest). The dístributíon of these corals ís shown in Text-fig. 10. At Sectíon 7 (Kankakee Ríver), solitary corals \n¡ere noË found ín the 0.3-rn-thick l,{í1he1mi Formatíon, or in the underlying Neda Formation of the Maquoketa Group. The Kankakee Formation overlies the Wílhelmi at thís locatÍon.

In eastern I^Iisconsin, solitary corals \,rere not observed in the basal 3-rn-thíck unit, or ín íurnediately overlyíng strata, of the

Mayville Dolomite at Section 2 (Hígh Cliff). Solítary Rugosa \^/ere not found in the lorver meter of the Mayví11e, or in the underlyíng Neda Formation, at Section 1 (Katell Falls). This Ís the only locality at whích the Neda is knovm to contain fossíls. Savage and Ross (1916, p. 191) ídentified one species of asteroid, one bryozoan, three brachiopods, three bivalves, and one gastropod. In addition to the above groups, J. Emerick has found conularids and trilobites (l,tlkulic and Kluessendorf, 1983, p. 29). In the vicinity of Little Sturgeon

Bay, E.O. Ulrich observed a coral-rich dolorníte up to 2 m thick, and in places overlaín by a thin Ínterval of the Neda, 1ocal1y preserved 66

between the Maquoketa Shale and Mayville Dolomite (Mikulíc and Kluessendorf, 1983, p. 36, fígs. 27,28). Elias (1982 pp. 29,67, fig. 18, p1. 10, fig. B) identífíed the solitary rugosan Grewíngkia canadensis (Bi1lings, 1862) ín Ulrich's collection from the coral-rich unit. Age of units.-The hístory of age assígnments for líthostraÈígraohic units ín this area is summarized ín Text-fig. 9. Ross (L962) considered graptolites from a bed in the upper part of the

Schweizer Member, Wilhelmi Formatíon, to be Early Silurian (early Llandovery) in age. This was confirmed by Berry (in Berry and Boucot, 1970, p. 145). Liebe and Rcxroad (1977r PP. 848, 849, fig. 5) and Rexroad and Droste (1982, fig. 6) assígned conodonts of the Schweizer to the Panderodus simplex Zone, inferred to be early Llandovery.

However, correlation and age assigrurents on the basis of these conodonts are unrelíab1e because diagnostic, biostratigraphically important taxa are not present (Liebe and Rexroad, 1977, p.848; Mikulic, et al., 1985, p. 16). Conodonts ín the Birds Member of the Wílhelmi and the overlying Elwood Formatíon were assigned to the

Ozarkodina (or Spat thodus ) hassí subzone of the Distomodus (or

Icriodina) írregularis Zone (= Paltodus dyscrítus fauna of Thompson and Satterfield, 1975). Mikulíc,et al. (1985, n. i0) noted that 0. hassi suggests a middle to early late Llandovery age.

Savage and Ross (1916, p. 191) and Savage (1916, p. 309) assígned a Late Ordovicían (nichmondian) age to the Neda Formation, which is

the uppermosÈ unit of the Maquoketa Group. Thís seems reasonable on the basís of lithostratígraphic data (Míku1ic and Kluessendorf, 1983, p.3; Kolata and Graese, 1983, p. 3l). The underlying Brainard 67

Formation is Ríchmondían also (¡likulic'et a1., 1985, p. 8).

Savage (1913b, p. 30; L9L7, p. 88), I^Iillman (1973, pp. !4, 15), plus ltIillman and Atherton (1975, p. 97) reported the brachiopod Plat¡rmerella manníensis from the upper Elwood Formatíon and basal

Kankakee Formation. This zone LTas placed in the míddle Llandovery by Berry and Boucot (1970, pl. 2).

Depositíonal environments.-savage ( 1913b r pp . 34 , 35; 1916, p. 3I4; I9I7, p. 92) consídered the l^lilhelrni Formation (his Edgewood) to have been deposited during a transgression that followed a period of erosion. hlillman (1973, p. 12) noted that this unít occupíes channcls that had bccn cut into the lfaquoketa Group. The basal bed of the Inlilhelmí is conglomeratic at Section 4 (Schweízer l^Iest), and contaíns clasts of Maquoketa shale at SectÍon 3 (Garden Prairíe).

The Schweizer Member, which ís very argillaceous and si1ty, occurs only in the deeper parts of major channels (I{íl1man, 1973, p. 13). As the surface of the Maquoketa became covered, the amount of argíllaceous materíal in the overlying deposits decreased. Líebe and Rexroad (1977, p. 844) reported that reworked Ordovician conodonts decreased ín abundance upward in the Schweízer Member, and occur sporadically above

ít. Thís ís the same dístributíon as argillaceous material deríved from the Maquoketa. The Bírds Member of the ülilhelmi is slightly argí11aceous and the overlying Elwood Formation contaíns 1ittle or no clastic material. The lithologíes and beddíng in this sequence suggest deposition ín relatively low energy conditions. 68

Northwestern Illinois and Eastern Iowa

Li thos tratísraphy.--{he his to ry of stratigraphíc nomenclature and age assignments of uppermost Ordovician and lowermost Silurian sÈrata ín the vícinity of Jo Davíess County, Illínoís, and Jackson County'

Towa, is summarized in Text-fÍg. 11. The 1íthostratigraphíc

Èerminology of Lrilhnan (Ig73) ís followed hereín (Text-fig . 12).

The type section of the Mosalem Form,¡ltíon is Sectíon B (Kíng)

(I^fillrnan, 1973, p. 32). The Mosalem is up to 30 m thick where ít fills channels eroded ínto the underlying Maquoketa Group, but thíns almost to absence above paleotopographíc highs (Brovm and trlhít1ow, L960, pp. 34, 36-39, figs. 9, 10; I{hit1o\47 and Brown, 1963, PP. 11, 13' fig. 62.2; Wil1man, 1973, pp. 31-33). Where the Mosalem is relatívely thick, Ëhe lower part is composed of gray, dolomitic shale and very argillaceous dolomite. The clastic content decreases upward. The upper portíon of the unit consisËs of slightly argillaceous dolomite wíth a few bands of chert. I^Ihere the Mosalem is comparatívely thin' only the upper dolornitic portion is present. This formatíon unconformably overlies strata of the Maquoketa Group ranging from the

Neda Formation, preserved on paleotopographic highs, down inÈo the

underlying Brainard Shale. tr^I1 thln channels, the base oi Lhe Ì"íosaiem ís characterized by a thín, persístent conglomerate containing clasts

derived from Ëhe Maquoketa. The Mosalem Formation is overlain wiËh

apparent conformity by the massiver vuggY, pure dolomite of the TeËe des Morts Formation ín the northern part of this area' and by relatively pure, cherty dolomíte of the Blandíng Formatíon in the south. 69

Text-f ígure 11.-History of stratígraphÍc nomcnclaturc and age assJ.gnments for uppermost Ordovician and lowermost Silurian units ín northwestern lllinois and eastern lor¡a. E. = Early, L. = Late, GAM. =

Gamachian. 70

HALL AND BROWN AND F SAVAGE, z> WHITNEY, 1858 wHtTLOW. Uô CALVIH AND SAVAGE SAVAGE fS26i WILLMAN owEN. t844 PÊRCIVAL WHITNEY, 1A66 wlLsoN, 1895 1935; r 960; ø- BAtN, l SOO 1 SO6 f9t4 suTToN, 1973 UF 1856 WORTHEN, WELLER, 935; WHITLOW ÉØ 1 466. 1 a7 r; scosEY, ' 1938 AND BROWN o SHAW, 1873a f 963

CHERT KANKAKEE KANKAKEE BEDS (SRASS- KANKAKEE z z 2 WAUCOMA FM. Ft,. E o z LST. z FIELD) 2 f E ts u LOWER E L ST. f z BASAL f É CORALLINE LOWEB = ; E o o ô o o o É E BEDS OUARRY f o z z z 2 MOUND NIAGARA BEDS z r LST, GP, (LST.) TETE J s u u DÊS u fÊIE DES z MORTS MORIS FH. BASAL BEDS MBB. CORALLINE WINSTON EDGEWOOD AND L S1. LST. PEHTAHERUS BEDS OF TRANSITION TBANSIfION MOSALEM MOSALEM BEDS PASSAGE BEDS BEDS MBR. = j OF UPPER o MAGNESIAN z i (CLIFF) LST. 1 2 NEDÂ MAR. z NEOA FM. z ts z 9 U f : ts ê o o z ; HUDSON J UPPER il z SLUE SH, ¡ RIVER MAOUOKETA ô MAOUOKETA MAOUOKETA MAOUOKEIÂ yl (ctNctNNAlt) SH tr MAQUOKETA sH. sH. sH. ot o I sH. t GP, ARAINARD =o SRAINARD ¡ = 3l MBR 9 fl =o É 7I

Text-figure I2,--stratigraphic sections (to scale) and localíty map ín northwestern lllínois and eastern lowa. For legend, see Text-

f íg. 10. GAI'Í . = Gamachian, M. = mídd1e. For precíse locatíons of sections plus references, see trEastern lowa" and "Northwestern lllinoisrt under

STRATIGRÁPHIC SECTIONS AND COLLECTIONS. UPPER ORDOVICIAN I LOWER SILUR]AN 2 I RICHMONDIAN ?GAM LOWER LLANDOVERY ? M. LLANDOVERY

MAQUOKETA GP MOSALEM FM BLANDING FM.

o o o

Øo6n >r Þr Þ Þ l{ Þ N { -] oz o I 3 I Þ "< c lo 3Ë Dalmanophyllum solitary Rugosa t. I TETE DES MORTS I FM. U) (Dm o mo o i IJ a Þ l t- a I ì I I Þ mo t t \ I Þ gorS ¡\) ¡ solitary Rugosa .r graptolite bed

C @ c @ g oP o c o o Ð x o eb c U, ç l) o € o c c z N o o) L Þ Þ o a o ef; )¡ (o tr o o I o (n=o X N ì Þ a s r U)- m r {o \ o (D o )t U) Ø z o Oz :Þ I Þ ! Ð o Ð "-.- NJ fl o I z 3.o þr Ð o o N Ø f a o a f r z - A' r Phaulactis 73

Bíora.---Calvin and Baín (1900, p. 445) identified a species of brachiopod from the lor,rer part of Ëhe }fosalem Formation (their t'transiÈion beds") at Rockví11e, Iowa. Savage (1906¡ PP. 601, 602) reporÈed three specíes of brachiopods and one trílobite from the Mosalem (hís transition beds) near Bellevue, and one of the brachiopod species from those beds ín Prairie Spring Townshíp. From a section ín Jo Daviess County, Illinois, Savage (I9I4, p. 34) listed three species of ínartículate brachiopods, five articulate brachiopods, and three rrilobites ¡¿íthin the Mosalem (his l^Iinston). Savage (1926r PP. 527,

528) also reported fossils from the Mosalem (his Edgewood) at t\"/o sec.Liurls i¡ Carroll Coupty, T11ínois. At one of these, where the formatíon is 18 m thick, he mentioned two species of brachiopods, one trÍlobite¡ plus s01ítary rugose corals Ídentífied as Zaphrentis subregularis from near the base, and a different species of brachíopod from the upper part. At the other locality, he ídentified five species of brachiopods, one bivalve, one trílobi¡e, and Zaphrentis sp.

From the Mosalem and Tete des Morts formations (his Edgewood) in Iowa, Scobey (1938, table 2) listed one specíes of stromatoporoid, two bryozoans, one inartículate brachiopod, 16 articulate brachiopods' four gastropods, three cephalopods, one ostracode, seven trilobites, six tabulate corals, plus Z . subregularís and Zaphrentis sp. Many of these are probably from the Tete des Morts. Broum and hrhítlow (1960' pp. 37-39) stated that brachiopods, bryozoans, md trílobítes are the domínant fossils ín the Mosalem of Dubuque County, Iowa. They noted the presence of probable conodonts, especíally ín the basal 1.5 rn where burrow rnottling is common. At localities where the Mosalem is Èhin, 74

possible algal stromatolÍtes were reported at the base. In the lowermost bed of the formatíon aË one section, smal1 phosphatic

fossils resembling the "depauperate fauna" at the base of the Maquoketa

Group were observed. Cornrninuted fossil fragments from the Cornulites

zone in the upper Brainard Shale \^rere noted within the basal

conglomerate of the Mosalem.

Ross (1964) described one species of graptolite and reported a

specimen representing a dífferent genus from a horízon siËuated about

3.4 rn above the base of the Mosalem Formation as currently recognized at Section 26 (Bellevue) (see Rose, 1967, fig. 21). He reported

Ëypíca1 Maquoketa fossils frou the basal 0.6 irr t-híck cuuglomeratf-c, si1ty, dolomitic calcarenite of the Mosalem at thís locality (Ross,

1964, p.1107), but it ís not known íf they are reworked. trühitlow and Brown (1963, p. 13) found phosphatic fossil fragments in this bed. During the present study, three solitary corals were collected from an interval 1.8 to 2.4 m above the base of the Mosalem Formation at Section 26 (Be11evue). They are too poorly preserved for identífícation. However, the specimens from Carroll County, I11inois,

that were ídentified as Z . subregularis by Savage (1926) are

tentatíve1y considered to be Streptelasma subregulare (Savage, 1913b). All of his other reports of this specíes, ín norËheastern r11inoís, northeastern Missouri, and southern 11linois, have been confirmed in thís study. Dalmanophvllum (P1. B fig. 1B) and Phaulactis (P1. 8, fig. 23) occur near the Èop of the Mosalem at Section 9 (Wínston North) and SecËion 10 (Lost Mound), respectively. The stratigraphíc distribution of these corals ís shown in Text-fíg. 12, One 75

unidentifíable specimen was also found in the upper 2 m of the Mosalem at Sectíon 11 (Schapville). Solitary Rugosa r¡rere not observed ín this formaÈíon at Sectíons 8 (Kíng) and 12 (Srockron) . Salvadorea randi (Elias, 1981) \^7as described frorn the Brainard Shale of the

Maquoketa Group at Sterlíng, Illínois, and Clayton County, Iowa, by Elías (1982, pp. 61,62, pL.6, figs. I-71' see also Elias, 1985, p. 45). Age of units.--{he histo ry of age assign¡nents for lithosËratigraphic units in thís area Ís summarízed Ín Text-fíg. 11.

Ross (1964) noted thaË graptolítes from a bed about 3.4 rn above the base of the Mosalem Formation represent an Early Sj-lurían (ear1y

Llandovery) zone.

Faunal and lithostratigraphic correlatíon of the upper Brainard

Shale and íts uppermost Cornulítes zone (Maquoketa Group) in Iowa and Illinois wíth the Late Ordovician (latest Ríchrnondían) t'Elkhorn" strata in the Cíncinnatí Arch region was considered híghly probable by

Ladd (1929, pp. 369, 370) and Templeton and l^Iillman (1963, pp. 132,

133). The upper portion of the Maquoketa ín northern l11ínoís was considered to be late Maysvillian and Ríchmondian on Ëhe basis of prelíminary work índícatíng conodonts of Fauna 12 (votaw and Kolata,

1981). Glenister (1957, pp. 720, 721) plus KolaËa and Graese (1983, pp. 5' 6) assigned the Maquoketa Group of eastern lor¿a and north\^/estern

I11Ínoís to the Maysvillian through Richmondian.

The age of units overlyíng the Mosalem is imprecisely knov,rn, because ímportant bÍostratigraphíc marker zones are absent.

Deposítional envíronments .-{avage (1914, p. 34; 1926, p. 528) recognízed that the Mosalem Formation was deposited duríng a 76

transgression. Brovrn and l,rrhítlow (1960, p. 36) interpreted the

Mosalem as havíng been deposíted in a shallow marine envíronment as a sea advanced over the eroded Maquoketa surface. As sedíments accumulated ín low areas, Ëopographic híghs continued to be eroded, either above or below sea level. The detrital content of the

Mosalem decreased as the summits became covered wíth marine deposits.

Erosional re1íef on the Maquoketa ís 41 m ín Dubuque County, south of Dubuque, Towa (Bro\,rn and trrfhítlow, 1960, p. 23; I^Ihitlow and Brown, 1963, p. 11). 77

SOLITARY RUCÐSE CORAL ASSEMBLAGES

A succession of three solitary rugosan assemblages is recognized within the uppermost Ordovicían-lor^/ermost Silurian sequence in the east-central Uníted States (Text-fig. 13, Table 1). The lowest is a Late Ordovícian assemblage in the Maquoketa Group. Salvadorea randÍ, a Maysvillian-Richmondian species (flias, 1985, p. 45), is presenÈ ín the Orchard Creek and. Braínard shales (81ías, LgB2r pp. 35, 36).

Grewingkia canadensís occurs immedíaËe ly below the Neda Formation in eastern l^Iísconsín (Elias, L982, p. 29). It ís a Richmondian specíes

(Elias, 1982, p. 67) .

The upper assemblage is Silurían ín age, and íncludes repr esentatives of Rhegmaphyllum Dínophy11um, Dalmanophyllum, and

Phaulactís. These genera are typícal of Èhe Early through Middle Silurian (Hill, 1981r pp. 159, 160, 163,252), and occur in the laLe early to late(?) Llandovery Brassfíeld Formatíon of the Cincínnati

Arch regíon ín Kentucky-Indíana-Ohio (Laub , 1979). Collections made from the strata containing this assemblage are not extensive, and most of the specimens \47ere not identifíed because of poor preservatíon.

No attempt r^ras made to dífferentiate species within these genera.

This study ís focused on the middle assemblage, here termed the Edgewood. Streptelasma subregulare ís the most wídely distríbuËed specíes, followed by S. leemonense. Seven other species are also recognized (Tab1e 1). Theír stratígraphic posÍtíon between L¿te

0rdovici¿n (Richmondian) and Early to Middle Silurian assemblages suggests a latest Ordovician to earliest Sílurían age range. Solitary

Rugosa of the Edgewood assemblage are comparable primarily to species in the following units (refer to díscussíons of taxa 1n SYSTEI'IATIC 7B

Text-f igure 13.-{omposíÈe stratigraphic sections showíng age and correlation of rrpper:most Ordovícían and Lowermost Síl-urian unÍts and distributíon of solitary rugose corals ín the east-central Uníted states. strata contaíning Èhe Edgewood solitary coral assemblage

(Gamachian to early early Llandover¡z ín age) are stippled. Hachures

índíca te Platl¡merella manniensis zone. GAM. = Gamachian E. = early, LLAND. = Llandovery. LAIE ORDOVI CIAN I EARLY SILURIAN RICHMONDIAT{ nou. LATE LLAiIDOVERI I I

-n o oc

-¡ ..'...'...... _ Sfrcptarosma sub¡agulr¡e lô oI ...... _ Stropartrsmê laoñonansc >t S- rp. cl. S. taaûo¡ansa c¡.*tngklt a9. A Kaetophttlum oklafuñOnsa - Phaulôclts - I- t==\ iz 6_ - .3a. ;:o: n= '; ^i à¿

¿l SalradoteD tãDdl _z St¡apaorrsñà aubragutarc !o Strcptcrrsñâ l.amÚønsa øã sarepterrsña.p. o> - Bodophylt!ñ cz - shotat ¡o - Dâ,ñ8îoPhrttum I- f- ) t TBRYANT xrãFin-I------lZ ñ .ã z o I l,,u@'97ç ¡ I Streptcrrsñr !p- A - Strapterasrr suh tatutar ø Streplcr¿sDa Iøøñonansa Gtevlngklê BÞ- - I ^ zÐ Dlnophtt,um Dalñanophylluñ = o - I ! !o n{ 9Á

Straplolarmâ

z o _¡ { ol rõ -I 9ø Sarcpaataaña t 2 aubtagulara Dlãophrttuñ Dalmtnophtttum ¿ >¡o i 21 EF Þ¡ a ;nr -t ¡È d.; iE ! ds ;- Salradoraa ¡addl :F (7) Stfapaatasma s!àtagutaìa D.tñ.noÞhtttum ï=tz phautacllt ! - - \o õ .. ..^noo"r*, :1"11"]:'l- l'"^*l i I,i.IT'ol LATE oRDovtctANl EARLy stLuFitAN 80

Table 1.-Latest Ordovician and earliest Silurían solítary rugose corals in the east-central UnÍted States.

Sílurían Assemblage

Suborder S trepËelasmatina

Farnily S treptelasmatidae

Sub f amily SÈreptelasmatinae

Rhegmaphyllum

Sub f anily DÍnophyllínae Dinophyllun

Sub f amíly Dalmanophyllinae

Dalmanophyllum

Suborder Lycophyllina Farnily Lykophyllídae Phaulactis

Edgewood Asserrblage [ndg.rood Province] Suborder Streptelasmatina

Farníly S treptelasmatídae

Sub f amily S Èrep telasmatinae

S trep tel asma subregulare (Savage, 19 13b)

SËreptelasma amsdení n. sp

Streptelasma leemonense E1ías, T982

S . sp. cf. S. leemonense Elias, 7982

Streptelasma sp. A

Streptelasma s p. of Elías , 1982 81

Grewingkj-a sp. A

Sub fauríly Dalrnanophyllinae

Bodophylluro shortjl E1ías, L982

Suborder Monacanthína

Family Lambelasmatídae Subfamily Coelostylínae

Keelo llun oklahomense n. gen., n. sp

Late Ordovicían Assernblage

Suborder S treptelasmatina

Family S treptelasmatídae

S ubfarníly Streptelasmatinae

Salvadorea randí (E1ías, 1981) fned niver-Stony Mountain Province]

Grewingkía canadensis (Billings , 1862)

[nichrnond Province] 82

PALEONTOLOGY): Vauréal and Ellís Bay formations (Richmondían,

Gamachian), AntícosËí Island, Québec, Canada; unnamed uníts (Ashgill) in the eastern Klamath Mountains, Ca1ífornía, and Penobscot County, Maine, U.S.A.; Stages 5a plus 5b (Asheill) and Stage 6a (early

Llandovery), Norway; Boda Límestone p lus Dalmanitina Beds (Ashei1l) and possi-bly younger strata (earliest Llandovery), Sweden; and Pírgu

Stage (Ashgill), Estonian S.S.R. Neuman (1982, p. 34) noted that several species ín Norway range from the Ashgill ínto the early

Llandovery. On Antícosti Island, one species ranges from the

Richmondían through Gamachian and ínto the early Llandovery (E1Ías, unpublíshed data).

The three solitary rugosan assemblages in the east-central UniEed

States have no specíes in common, and the overall generic compositíons are also dístínct. Diversity at all taxonomic levels íncreases from the Late Ordovícian to Edgewood assemblages and, at least at the subfamily level, from the Edgewood to Sílurían assemblages (Tab1e 1). 83

AGE OF I]NITS AND INTERREGIONAI CORRELATION

Amsden (I97Ib, pp. 2!,22; 1974, p. 26) consídered the Keel-Edgewood brachiopod assemblage in souÈh-central Oklahoma, southern I1linoís and southeastern Míssourí, and northeastern Missourí and west-central I11ínois to be fairly characÈeristíc of the latest Ordovicían (1ate AshgÍ11) to earliest Silurian (ear1y Llandovery). Brachiopods ín the

Keel Formation, Leemon FormaÈion, and Noíx Limestone most closely resemble the latest Ordovicían Hírnantia fauna, but the species are different. This may be due, at least ín part, to ecologic facËors.

Amsden concluded that the Ordovicían aspecÈ of brachíopods ín the Kee1,

Leemon, and Noix índícated a latest Ordovícian age. The brachíopod assemblage ín the Bryant Knob Formatíon, which overlies the Noíx ín northeastern Missouri, is different in some respecËs, and was tentatively assÍgned to the early Llandovery (Arnsden, I97Ib, p. 22;

1974, p, 26).

Brachiopods of the lower Edgewood assemblage vrere provisionally considered to be post-Hírnantían by Lespérance (1,974, p. 22).

Lespérance and Sheehan (L976, pp. 7I9, 720) noted that these brachiopods could represent a latest Ordovícian endemic North American fauna, with specíes derived from Ëhe Hírnantía communíty and other

North European Province species. However, they suggested that ít was most likely a Silurian fauna with a few holdovers from the Late

Ordovícian North Amerícan Provínce. A Hirnantian age r^ras accepted by

Jaanusson (1979, p.154), based on a trílobíte and other indications from beds ín I11inois.

In víew of the presence of Ordovícian conodonts ín the Leemon 84

Formation and Noix Límestone, the Ordovician aspect of the brachiopods

in the Keel Formation, Leemon, and Noix, plus the posíti.on of these uníËs above Late Ordovícian (Richmondian) strata, a latedt Ordovician

(Gamachian) age is accepted herein, as suggested and discussed by E1ías (I982¡ pp. 38, 39) (Text-fig. 13). Streptelasma subregulare,

S. leemonense , Grewingkia sp. A , and other solítary corals in the Keel, Leemon, and Noix, are consídered to have first appeared in the

east-central United States during Gamachian time.

In northeastern I11ínois, Streptelasma subre re l_s present ín the schweizer and Birds members of the lJilhelmí Formation. rt occurs both below and above a bed in the upper Schweizer that contains early Llandovery graptolÍtes (Ross , 1962, p. l3B3; Berry ín Berry and Boucot, 1970, p. 145) and conodonts (Líebe and Rexroad, 1977, fig.5;

Rexroad and Droste, 7982, fígs. 5, 6). Therefore, the range of S. subr ulare extends ínto the Silurían. Lower Schweizer strata infí1ling

the deepest channels ín the eroded Maquoketa, below the posítíon of the graptolíte bedr mây be Gamachían in age, as suggested by Elias (1982, p. 40, fig. 2l) (Text-fíg. 13).

Ross (1964, p. 1107) and tr{íllman (1973, pp. 13, 31, fig. 2) correlated the lower part of the l^lilhelmi Formation with the lower portion of the Mosalem FormatÍon in norÈhwestern IIlínois and eastern Iowa on the basis of graptolites and lithology, respectívely.

Graptolítes near the base of the Mosalem are sj"milar to those in the I,Iílhelmi, and are early Llandovery in age (Ross, 1964). Solítary corals tentatively considered to be Streptelasma subregulare occur in the basal Mosalem. It ís suggesËed herein that lower Mosalem strata infÍllíng the deepest channels eroded ínto the Maquoketa, below the posítion of the graptolíte bed, mây be Gamachian in age (Text-fíg. 13). B5

In northeastern lllínois, corals of the Silurían assemblage occur r.¡ith the brachiopod Platyrnerella manniensís in the upper Elwood

Formation. These strata are considered to be middle Llandovery in age by Berry and Boucot (1970, pl. 2). In northwestern lllinoís, this coral assemblage appears in the upper part of the Mosalem Formatíon.

The upper Mosalem is considered younger than the upper part of the

Wílhelrni Formation because Streptelasma subregulare occurs in the

Birds Member of the tr^Iilhelmi, whereas the Sí1urían assemblage ís presenË in the upper Mosalem. The Edgewood and Sílurian assemblages are not known to co-occur. Although l,Iíllman (L97 3 r pp. 15- 17, 35 , 36) tentatively correlated the Elwood with the Blandíng Formation of northwestern lllinoís on the basis of 1íthology, he noted that the

Tete des Morts Formatíon plus the Blanding could correlate with the lower Kankakee Formation, whÍch overlies the Elwood. From the coral evidence, ít is inferred that the upper Mosalem must be equivalent to aÈ least the lower part of the Eh,¡ood (Text-f ig. 13).

In northeastern Missouri, the Silurian coral assemblage occurs in the Bowling Green Dolomite at'an eastern exposure. The middle

Llandovery Platymerel-la manniensis zone is present at the base of the

Sexton Creek Limestone, whích overlíes the Bor¿ling Green. Therefore, the Bowling Green is correlated with the lower El¡'sood and upper Mosalem and ís considered late early Llandovery ín age (Text-fig. 13). Corals of the Edgewood assemblage Ín the Bryant Knob Formation, which overlíes Èhe Noix Límestone and underlies the Bowling Green

Dolomite ín northeastern Missouri, could be Gamachian or early early

Llandovery in age. Streptelasma su-bregulare, S . leemonense , and

Grewíngkia sp. A are also known from the Keel Formatíon (Gamachian) , B6

and S. subregulare plus S. leemonense occur ín the Leemon Formation

(Gamachian) . However, S subr ulare ís known to extend into ear Iy

early Llandovery strata of the l^Iílhelrní Formation, in whÍch the other species are not represented. rnterpretations of brachiopods

(Amsden, lg7Ib, Ig74; Lespérance, 1974; Lespérance and Sheehan, 1976), conodonts (Thornpson and satterfíe1d, I975>, and graptolítes (Berry ín

Thompson and satterfíeld, r975) ín the Bryant Knob Formatíon suggest a silurian age, and the unit ís herein consídered to be early early

Llandovery on the basis of íts position beneath the Bowlíng Green. (Text-fig. 13).

The lower and upper portíons of the Cyrene Formation are equated r^Iith the Noix Límestone (Gamachían) and Bryant Knob Formatíon (early early Llandovery), respectívely, which occur Ímmediately to the east. The evidence for Ëhese correlaËíons, based on conodonts, brachiopods, and lithologic sínílarity, \,üas díscussed in a previous section.

S treptel¿sma subregulare occurs in the mídd1e of the Cyrene and in the Bryant Knob. A hiatus has never been recognized between the cyrene Formatíon and the overlyíng Bowling Green Dolomj-te (late early

Llandovery). Therefore, the Cyrene is herein considered to be G¿machian through early early Llandovery in age (Text-fíg. 13).

The lower part of the Sexton Creek Límestone in southeastern

Míssouri and southern rllinois could be as old as the Bowlíng Green

Dolomite (1ate early Llandovery). BoËh uníts contain conodonts representing the Paltodus dyscrítus fauna (Thompson and Satterfield, 1975, fígs. 6,7r 9,11-15)r plus solitary corals of the Silurian assemblage. Early late Llandovery brachiopods are also present ín 87

the Sexton Creek (Amsden, 1974, p. 24). The Sílurian solitary coral assemblage ís represented in basal beds of the Cochrane Formation ún south-central Oklahoma. The

Cochrane contains early late Llandovery brachiopods (Amsden, L97la, p. L45; 1980, p. 17).

The Edgewood solítary coral assemblage is latest Ordovicían

(Gamachian) to earliesÈ Sílurian (early early Llandovery) in age, and therefore these rugosans cannot be used to delineate the position of the Ordovícían-Silurían boundary ín the east-central United States. In Il-linois and Missouri, they occur in strata Èhat ¡¿ere included within the.Alexandrian SerÍes by Savage (see Text-figs. 5, 7, 9). Reeds

(1911) extended the use of that term for correlative strata ín Oklahoma.

Thís series r^ras proposed by Savage (1908ar pp. 434, 442, 443; 1908b, pp. 110, i11) to include strata, thought to be earlíest Silurían in age, sítuated between the Richmondían Stage of the Cincínnatian Series

(Ordovician) and the Níagaran Seríes (Silurian). It has been recommended that the term Alexandrian be díscontinued as a seríes because of a prolíferatíon of synonymous names (D.w. Fisher, 1954, p. 1984), and because outcrops in the type area are meager, the uniÈs are noÈ especiall-y fossílíferous, and unconformities are present withín the sequence (Amsden, I974, p. 5). 88

PALEOBIOGEOGRAPHY

Two paleobiogeographic provinces are represented by solitary rugose corals of the Late Ordovicían assemblage ín the Maquoketa Group. Salvadorea rand.L in lowa and Illinois ís also known from middle Maysvillían strata in the Selkirk Member (Elías' 1981r PP.

20, 2l) and the Richmondían Fort Garry Member of the Red River Formation in southern Manitoba (Stias, unpublíshed data). It belongs to the Red River-Stony Mountain Solitary Coral Provínce (Text-fig. 14). The distributíon of thís species índicates díspersion across the Transcontínental Arch between the Williston Basin and the area of Maquoketa deposítion. Grew 't nqkia canarlensis , whích ís present in Ëhe Maquoketa Group of eastern trIisconsin, is a characteristic specíes of the Richmond Solítary Coral Province (Text-fig. 14). Elías (1982, p. 29) suggested that this occurrence may represent a \^/est\4rard shift in the geographíc range of the species associated viith a regression during the late Ríchmondían. S. randi and G. canadensis, plus other solitary rugosan taxa' disapneared from the east-central Uníted States during the fína1 regressíon of the epicontinental sea at the end of Richmondían tíme, possibly due Èo a glacioeusËatic sea-level drop (E1ías, 1982, pp. 48, 51).

The so1ítary Rugosa of the Edgewood assemblage represent the

Edgewood Solitary Coral Province (Text-fig. 14). The inclusion of south-central Oklahoma in this province ís confirmed hereín, and the boundary ís tentatively extended to include north\{estern Illínoís and eastern Iowa. The Edgewood Provínce corresponds to a predomínantly carbonate sequence deposíted during a transgression that probably B9

Text-figure Iî.-Paleobiogeography of Late Ordovician and earliest SilurÍan solitary Rugosa in North America. A, Edgewood

Province of Gamachían to early early Llandovery age coincided wíth transgressíon thaË introduced open, high energy environments to continental ínÈerior (E1ías, 1982, pp. 51, 52). B, Red River-Stony Mountain Province of EdenÍan to Gamachían and possibly early early Llandovery age íncluded vast ínterior regíon characterízed by carbonate sedímêntation in somewhat restrícted seas, plus contínental margin with open, normal maríne enviïonments (Elias, 1981, pp. 2, B, 10; 1982, pp. 48, 49;1983, pp. 927-93I; 1985, PP. L6-20; Elías and Potter, L984, pp. 1205, 1206); i.solated areas to west are Cordilleran terranes with possíble Red Ríver-stony Mountaín assemblages. c,

Richrnond Province of Richmondían age corresponded to carbonate

!i-^-!^1 åL^å oolimanl-a plaErorm Doroerrng gPIcollLIlIeIILa-L scd-^^ LlldL -^^^'í"^JrsLEIvEu uIeÞ^1 ^^¡.i^ Lru

from delÈaÍc eomplex to east (Elías' 1982, pp. 49-5I). 90

¿l

P 9T

proceeded from the souËh (Savage, 1913a, pp. 373,374:1913br PP' 34,35; 1916, pp. 314-316; 1917, pp. 91, 92), possíbly due to a rise in sea-level relaËed to deglacíatíon (E1ías, 1982, p. 39). Thís event introduced open, normal maríne environments to the east-cenËral United

States. The Edgewood species were not derived from corals of the Late Ordovician assemblage ín this region. Theír resemblance to taxa previously resËricted lo the contínental margin of North Ameríca suggests that they origínated from such forms. I^lithin the Edgewood Province, diversiEy at all taxonomic levels decreases from south to north (Text-fíg. 13, Table 1). This apparently corresponds to an envíronmcntal gradíent from contÍnental margí-n to epi e'ontínental conditíons. Solitary corals of the Edgewood Province became extínct during early Llandovery Ëíme. Genera recognized ín the succeeding Silurían assemblage vrere not deríved from Edgewood taxa or other known North Amerícan Ordovician solitary Rugosa. They must have origl-nated elsewhere and been introduced to this region. Laub (L975' p. 280; lg7g, p. 45) noted that rugosan specíes in the late early to late(?) Llandovery Brassfield FormaËíon of Ëhe Cíncinnatí Arch region are not known ín pre-Brassfield strata of North America, but some occur in the Baltic area, the siberían platform, and possibly venezuela.

EVOLUTION

The only recognízable evolutionary event, wÍthín the Edgewood Province involves Èhe derívation of StrePtelasma amsdemí f rom S. subregulare, apparently by geographic speciatíon. The rnorphologícal símilarities and dífferences betr^reen these two specÍes are díscussed

ín SYSTEI4ATIC PALEONTOLOGY, under S. amsdení (see also Table 6). The 92 hÍgh degree of íntraspecífíc variabilíty in S. subregul.are aoparently allowed small populations of atypícal índíviduals to survive in atypical environments. S. amsdení 1ike1y arose as a result of the founder effect. The high degree of varíabilíty is probably what enabled S. subregulare to domínate the Edgewood so1íta ry rugosan assemblage. Over

80 percent of all specimens are S. subregulare. 93

SYSTEMATIC PALEONTOLOGY

Subclass RUGOSA Milne-Edwards and Haime' 1850

Order STAURIIDA Verríll, 1865

Suborder STREPTELASMATINA lledekind, 1927

Farnity STREPTELASMATIDAE Nícholson in

Nícholson and tydekker, 1889

Subfamily STREPTELASMATINAE Nicholson ín

Nicholson and Lydekker, 1889

Genus Streptelasma Ha1l, IB47

Streptelasma Ha1l, 1847, p. 17 (as Streptoplasma), and page facing

p. 338 (see Laub, 1979' p . 60); Neuman, 1969, pp. 8-10; Mclean, 1974, pp. 38-41; Laub, 1979, pp. 59-6I; Elias, 1982,

p. 52.

Type species.-Designated by Roemer ( 1861' p. 19) : Streptelasma corniculum Ha11 , 1847, lower Trenton Límestone (upper Míddle

Ordovícían), Middleví11e, New York. Diagnosis.---Solita ry or with fer¿ offsets. Septa nondílated to

¡+^1tr Åi1-+^.1 i- õ+áoô li'l qr-i^- ,rorr¡1 1v rlpnrprqpq drrr'íno ^^*^'luv¡uP¡çLsIJ urf oLçu ¡rr ^-r11'ser¿J ù Lq6et seugr¿J ontogeny. Major septa straight or \¡7avy, generally extend to axis in early stage and become shorter during intermediate to late stages. Septal lobes and rarely lame11ae can form a typícally símple axial structure in intermedíaÈe andfot late sÈages. CardÍnal septum and fossula inconspicuous Èo prominent. Díscussion.--Neumanfs (1969, PP. B-11) study of the lectotype of 94

S treptelasma corniculum has formed a basis for the generally accepted concept of StrepËelasma. This genus ís considered to ínclude streptelasmaËids with major septa that are 1ong, thin to moderately thick, and usually joined to form a símp1e axial structure during early

to íntermediate stages. These septa become shorter and Ëhinner in late stages, when an axial structure is seldom present. However, because intraspecifÍc variabílity of the type specíes is unknown,

Streptelasma remaíns poorly understood. Furthermore, most species presently included ín the genus are based on small collections. Mclean (I974r pp. 3B-41) srarsd rhar SËreprelasma , Dínophyllum

Lindström, 1882, and Porfiríevíulþ lvanovslciy,Ig63 mûy provc to be synonymous. He also noted that many species resembling S t rep te1 asma

ín late stages are not well enough known ín earlíer stages to be included in the genus wiËh certaínty. Elias (1982, p. 52) indícated that further study may demonstrate that Streptelasma , Helicelasma Neuman, 1969, Borelasma Neuman, 1969, and Grewingkia Dybowski,1873 are synonyms. He showed that in S. divaricans (Nícho1son, 1875) there is complete gradatíon from corals wiËh open axial regions to those with axial structures simÍ1ar to Grewingkía (Elias r9B2 , ' PP. 52, 55, 56, p1. 1, figs. 1-19)

S. subregulare (Savage, 1913b), described in this study on the basis of a large collection, ís ímportant in establishing the range of variability ín Stleptelasma. In thís highly variable species there ís continuous gradation from coralla that closely resemble s. corniculum , to those Èhat are símí1ar to Helíce1_asma,

Borelasma, and ullelnglasrna Neuman, 1975. hlithin some individuals, 95 different ontogenetic stages would be assigned Èo dífferent genera íf they Írere considered independently. The diagnosís of StrepÈelasma is hereín broadened Êo ínclude all representatíves of S. subregulare. 96

Streptelasma subregulare (Savage' 1913b) Plate 1, fígures I-28; Pl-ate 2, figures l-22; Plate 3, figures 1-10

Zaphrentis subregularis Savage, 1913b' P 62, pJ.. 3, fíg. 5' Pl. 7, fíg. 1; I9I7, p. 113, p1. 5, fig. 5, pl. 9, fie. 1. Zaphrentis ambigua Savage, 1913b, PP. 109' 110, pl. 7, fig. 2; I9I7, p. 149, pI.9, fíg. 2.

S trep telasma subre lare (Savage, 1913b). Elías, L982r PP. 57' 58, p1. 4, figs. 7-22.

Holotype.-By original designatiou: UI X-851 (Savage, 1913b' p1. 3, fig. 5; IgI7, p1. 5, fíg. 5; Elias, L982, Pl. 4, figs. 7, B)' S co11., Cyrene Formatíon' near Edgewood, Píke Cot¡nty, Míssouri. Additional material.-UI C1619 (6 specíurens 1abel1ed Zaphrentis subre ularís ) S co1l., Birds Member, I^lilhelmiFormatíon (1abelled Channahon), near Belvídere, Boone County, Illinois; USNM 3-2-2, 8, 11'

12, interval 3-2, EMM coll., USNM 3-3-13, 1ã, 16, 24,27,29,30,

interval 3-3, EM coll., Birds Member, Irrí1he1mí Formation, Section 3

(Garden Praírie), McHenry County, Illinoís; UI C1560 (7 specimens labelled Zaphrentis channahonensis), UI C1563 (2 slabs and I specimen labelled Zaphrentis ambigua), S co11.., Schweizer Member, Wílhelmi

Formation (1abe1led Edgewood and Channahon Límestone' respectívely),

Channahon, I^1i11 County, Illínois; UI Cl58l (5 specimens labelled Z. subregularís), S co11., Schr¿eízer Member, Inlílhelmí Formatíon (Iabelled

Channahon Limestone), southeast of Channahon, I{í11 County, Illinois;

tJI CL547 (slab ¡¿ith 2 specímens 1abelled Z. channahonensís), UI C1561

(10 specimens labelLed Z. subregularis), uI x-947 (type specímens of 97

Z. ambjgua, 1 specimen plus slab with 5 specimens, one figured by

Savage, 1913b, pl. 7, fig. 2; L917, pL.9, fig.2), S col1., Schweízer

Member, I^Iilhelmi FormatÍon (labe11ed Edgewood), near Channahon, Inlill

County, Illínois; UI X-926 (2 specímens labelled Z. subregularís, one figured by Savage, 1913b, pl. 7, fig. 1; L917, p1- .9, fig. 1), S co11., Schweizer Member, ItlÍlhelmi Formation (labelled Edgewood,

Channahon Limestone), Wíl1 County, 11linoís; USNM 4-I-L-4-I-6, Ínterval 4-1, frlM co11. , Schr¿eizer Member, Wilhelmi Formation, Sectíon 4 (Schweizer Inlest), I^Til] CounÈy, Illinoís; UI CB64 (labelled

Zaphrentis), S col1. , Cyrene Formatíon (tabelte¿ Edgewood Límestone),

Edgewood, Píke County, Míssouri; USNM 13*1-1-i3-1-5 , ínterval 13-1, RfM coll., Cyrene Formation, Section 13 (Bowl-ing Green), pike County,

Missourí; USNM I4-I-2-4,9-20,22-21,30, 32, 33, interval I4-I, H"f coll., Kissenger Limestone Member, Bryant Knob Formatíon, Sectíon 14

(Higgínbotham Farm), Píke County, Missouri; USNM 15-1-1-15-L-7 , interval 15-1, EMM coll., USNM 15-1-9, 11, 13-20,40, interval 15-1,

Rf co11., Kissenger Limestone Member, Bryant Knob FormaËion, Sectíon

15 (Calumet), Pike County, MÍssourí; UCGM 45643-45645, USNM 2Ib-2-3, 4,8, interval 16-1, E coll., USNM l6-1-1-Ba, 9Þ-1tr, ]9-!l_, ínrerval 16-1, EI&l col1., Kíssenger Límestone Member, Bryant Knob Formation,

SectÍon 16 (Clinton Spring), Pike Counry, Míssourí; USNM 17-O-L-34,

36, 37, 39, ínterval I7-0, EM coll., Kíssenger Límestone }{ember, Bryant

Knob Formation, Section 17 (Clarksví11e), Pike County, Míssouri; USNM

18-1-1-18-1-20, interval- 1B-1, EMM co1l., usNM i8-1-25-IB-L-29 ínterval

1B-1, frf coll.r, unnamed member, Bryant Knob Formation, USNM 18-2-1-16,

18, 19, interval LB-z, USNM 18-9-1-f8-3-11, interval 18-3, EMM col1., 98

USNM 18-3-I5-IB-3-22, interval 18-3, USNM 18-4-1, ínterval 18-4' EM coll., Kissenger Límestone Member, BryanÈ Knob FormatÍon, secÈíon 18 (Kissenger), Pike County, Míssourí; UCGM 45618-45634, E co11.' USNM 365918, 19-l-1-5, L-J2, ínterval 19-1, USNM 19-2-1-19.-2-23, ínterval Lg-z, USNM 19-3-1-12, L2a-2I, 21-!2, ínÈerval 19-3, EMM coll., Leemon Formatíon, Section 19 (Ner¡ lJells), Cape Girardeau County, Missouri;

USNM 365919, 20-1-1-5, J-9, 11-14, interval 2O-L, EMM coll.' USNM

20-1-16-20-1-18, ínterval 2O-1, EM co11., USNM 2O-2-I, 20-2-2, interval

20-2, EMM coll., USNM 2O-3-2-20-3-lO, ínterval 20'3, USNM 2O-4-I,

20-4-3, interval 2O-4, USNM 20-5-1-3, 10, 11, ínterval 20-5, EM col1"

Leemon Formation, Section 2O (Short Farm), Cape Girardeau County, Missouri; UI ENT-1, ENT-2, S col1., Leemon Formation (1abel1ed

Edgewood), Thebes North Section (1abel1ed near Thebes) , Alexander County, Illínoís; USNM 2I-I-I, 21-I-3, ínterval 2I-I, EMM col1. ' USNM 2I-Ia-7-2I-Ia=4, íntervaL 2I-1a, USNM 2I-lb-I-!, B, 9, interval zl-Ib,

USNM 21-1c-1-4, !-8, 10, 13, 17, ínterval 2I-Ic, EM co1l', Ideal Quarry Member, Keel Formation, Sectíon 21 (Rock Crossíng), CarËer

County, Oklahoma; USNM 23-l-!, interval 23-1, USNM 23-2-1-31, Jg, 34,37- |Lu,4Ib,Q-45, 47, 49-Þþ,Ínterval 23-2, EMM co1l., Ideal Quarry

Member, Keel Formation, USNM 23-2a-L, 3, 5, interval 23-2a, EM co1l',

USNM 23-3-6, 23-3-9, ínterval 23-3, EMM col1., USNM 23-3-I4-I8,

24, 25, 2l-22., 3I, 32, 12-!9, ínterval 23-3' USNM 23a-I-4 Þ; I' interval 23a-I, EM co11., Keel Formation, Section 23 (Lawrence Quarry),

Pontotoc County, Oklahoma; USNM 25-I-I, 3-å, intetvaL 25-1, EMM coll., Keel Formation, Sectíon 25 (Hunton), Coal CounÈy, Oklahoma. 0ccurrences. Ordovicían (Gamachían) : Leemon Formation' -Uppermost southeastern Missourí and southern lllínois; Keel Formation including 99

Ideal Quarry Member, south-central Oklahoma. Uppermost Ordovícian (Gamachian) to lowermost Silurian (lower lower Llandovery): Schweizer

Member, !üílhelrní Formation, northeastern l11inoís ; Cyrene FormaËion' northeastern Míssouri. Lowermost Silurian (lower lower Llandovery) :

Birds Member, I,Iilhelmi Formation' northeastern Illinois; Bryant Knob

Formation including unnamed member and Kissenger Límestone Member, northeastern Missouri. DÍagnosis.---So1itary, generally ceratoid. In early stages' major sepËa generally moderately to greatly dí1ated and exËend to axis, where distal ends join. During ínÈermediate to late stages, septal length and dilatíon decrease, axíal regíon opens. Cardinal septum commonly conspicuous ín late stages. Cardinal fossula usually

ínconspicuous, but can be very broad or distinctívely shaped. Minor septa typíca1ly extend a short distance beyond relatively narro\¡/ stereozone. Tabulae generally moderately Ëo wídely spacedr. comrnonly depressed in cardínal fossula.

Description of corals.--{he largest specimen ís 102 mm long and

44 mn ín diameter at the calíce rím (USNM 1B-4-i). Gror¿th form is trochoid (Pl.1, fíg.5) to ceratoíd (Pl.1, fig. 1) to rarely subcylindrical, and coralla vary from straight to modera¡ely curved (Pl. 1, fíg. 13) to gradually curved through 90 degrees (ta¡le Z). Several corals have slight to moderate bends Ín two different dírections. A few individuals have single right angle bends (Pl. 2' fig. 13), but none have more than one such bend. Corallun shape in cross sectíon ís generally circular, but a few are elliptícal.

I^Iell-preserved specimens show prominent septal grooves and ínterseptal

rídges, plus growth línes. Coarse rugae are present on some 100

Table 2.-Gror,rth forn and curvature for spec imens of Streptelasma subregulare, S. amsdeni, S leemonense (including S. sp. cf. S leemonense), and Keelophyllum oklahomense. Data frorn Appendix l.

Growth form Curva

.Non- ì{odera telv Greatly -2 S ecÈion Trochoíd Ceratoid Cylindrical crlTvecF "rrt.r"d! "rr',r.d1 Streptelasma subregulare

3 * BelvÍdere 8 (looz) o ( oz) o (o%) 3 (38%) s (637") o ( o"/")

4 * Channahon 15 (s6z) 12 (44"t) o(o%) 6 (222) 20 (74"/") | ( 41i)

13 * Cyrene

* Edgewood 4 (r007.) 0 ( o7") o(o%) 3 (7s7") 1 (2s%) o(oz)

I4 4 (rrt) 1B (827!) o(oz) 3 (r7"t) 14 (782) r (62)

-15 e (75%) 3 (25%) 0(02) 7 (58%) 5 (42"/") o(02)

L6 I (207") (8oz) o(02) 20 (s]z) 17 (432) 3 ( B"Á) t7 6 (rgzt) 26 (7e"/") r(3%) 13 (437.) 14 (477") 3 (toi¿)

Lg-r,2 4 (367.) 7 (64%) o(o%) 3 (27"t) 7 (64"t) | ( e7.)

1B-3, 4 6 (5o%) 6 (507") o (o%) 5 (422) 7 (582) o ( 07")

19 26 (292) 60 (67%) 3(3%) 42 (48%) 4r (477.) s (62)

20 te (767.) 6 (24i¿) o ( o7.) 6 (267") rs (6s1¿) 2 (e%)

2I 4 (807") i (20%) o(o%) 2 (40%) 3 (60"/.) o (oz) aa 44 (8oZ) 11 (20%) 0 ( o"Á) 26 (477.) 26 (472) 3 ( 57.) z) 3 (r0o%) 0 ( o7") o ( o"/.) 2 (67"/.) r (33"/") o ( o"/")

S trep telasma arnsdení

¿c 0 ( 07") 2s (53%) 22 (472) 22 (48t) 23 (507.) t ( 2Z)

StrepÈelasma leemonense 14+15+20

* 23 * Gale s (43%) Lo (48't) 2 (ro?) I (38%) 13 (627.) 0 ( 0z)

Keelophyllun oklahomense 23+25 r(207") 4(B0Z) 0(07.) 3(60it) r(202) r(20%)

1Nor,-",rt.r"d = 0o to 10o curvature of growth axís'

å"tod"r"t"1y curved = 11o to 7Oo curvature of growth axis. %ru.t1y curved = )70o curvature of growth axls. 101

índíviduals. Rejuvenatfons, if present on a coral' are few in number and not pronounced. On the convex cardínal side at the apex'

two specímens have small grooves (Usut't 23a-L-8, 23-2a-T . These are ínterpreted as atÈachnent sLructures. Depth of the ca1íce is

commonly about 50 percent of the coral length, but varies from 30 percent to perhaps as much as 90 percent ín several individuals that have unusually short major septa throughout onËogeny (USNM I9-I-2,

19- 1-5 , L9-2-7 , r9-2-t6 , 19- 3- 34) . Ontogeny and int.ernal structures.-The relaËíonshíp between number of septa and coral díameÈer ís shown ín Text-fig. 15 and Table 3. During early ontogenetíc stages (P1. I, fLgs.21 9, 14, 20,23, PI.2, figs. 3, 10, 19, P1. 3, fíg. 1) major septa generally extend to or near the axis, where their dístal ends meet in smal1 groups. Septa are shorter in some specimens, but only rarely extend less than half the coral radius. During íntermediate (Pl. 1, fígs. 3, 4, 6, 7, 10, 11, 15, 2I, 24, PI. 2, figs. 4, 5, 11, 14, 16, 20, 27, PL. 3, fígs. 2,4-9) and late stages (P1. 1, figs. 8, 12,16' 17,22,25, PL.2, fígs. 6, 12,15, 17, 18,22, Pl. 3, figs. 3, 10), the septa usually decrease ín length gradually (Text-fig. L6,

Table 3). However, they remain long in some corals, and rapidly

decrease in length in others. Septa are relatívely straight to vravy

in cross sections. A few septal lobes are present in some índividuals (PL.2, figs. 12,21), but paliform septal lamellae are rare (P1. 3, fíe. B).

Major septa can be nondilated Ëo completely dílated in any ontogenetíc stage. Typíca11y, the degree of dilatÍon ís moderate to ro2

Text-f igure 15.---*.elationship betr¿een number of major septa and coral díameter ín Streptelasma subregulare. Numbers besíde data points indicate frequencíes greater than one. Arbitrary líne was used to derive proportions shown in part of Table 3. Data from

Appendix 2. 103

Cl 2

50

o 2. tr o o o O o D o o 40 El o o o2 o Q2 . o o o E 2)z.4 . no t) o o t- a. 3 . 2¡/2.1 2.1 O2 fL o LlJ trE 2/: "" v) D 2.) .)I o O l' 3.) O . z) 02.o É 3. 2. 3 I ooo O2 E . z. o 21 .) OoO. o 30 . . 40 26. z. I . 02 2.) 3 .)3 . 02 0 . 2.1 ay'z. O2 o 2. 6. 2. 2 .) 3.)2 3. . Eza)lz. z .) o l! ' @23' 02 o 2t 1.1 6.) . o o o g.)/t. g.>s2.) o o ¿./ oo o o É Dt ) 3€ l¡J 20 3.1 2 E o o dl 3. o2 o o o o f o o1 O3 z o

o o Sections 19 and 21: 112 cross sect¡ons from 57 corals 10 o Section 2O: 39 cross sections from 25 corals . Alf other sect¡ons: 251 cross sect¡ons from 161 corals

0 5 10 15 20 25 30 DIAMETER (mm) 104

Táble 3.-Proportions of data points above (A)ror on and below (B),arbíÈrary lines drar¡n in Text-figures 15-18, 20-23, for characËerístics of major septa and cardínal fossula in Streptelasma subregulare and S. amsdeni.

Number of septa Length of 6epta Thickness of septa I'Itdth of fossula

B S ec tion A B A B A A

s treptelasma subregulare (too%) 3 3 (432) 4 (s7"t) | (Lrií) I (8eZ) 4 (447") 5 (56%) o ( 07") 5

(67%) (8e7.) 4 5 (As"t) 6 (s57.) | (r\"t) 6 (867") 3 (337") 6 r (rfl) 8

13 3 (43"/.) 4 (s7%) o ( 0i¿) 7 (ro0%) 2 (2ei() s (7 r"/") o(oz) 6 (1002) (92%) T4 7 (297") 17 (7rz) s (27%) 2s (83"Á) 2r (72i() I (28%) 2 ( 87") 23 t5 3 (237!) t0 (777.) 3 (232) ro (772) 6 (46%) 7 (s4%) 0(02) r3 (1002) t6 L2 (33%) 24 (67%) 9 (20i() 36 (8C7.) 27 (6rZ) 17 (3e7.) 2 ( 57.) 38 (es%)

I7 29 (s9%) 20 (4r%) 6 (tti/.) 47 (89"/.) 27 (5r%) 26 (497") 2 ( 4"/") 52 (e67")

18- I 5 (367") e (64%) | ( 77") 13 (93"/.) r0 (7rz) 4 (2e7.) e (69i() 4 (3r7") t8-2 6 (38"¿) Lo (63%) r(6%) rs (94"/.) r0 (63%) 6 (38%) 5 (362) e (64"t) 18-3,4 e (32"/.) t9 (68Z) 20 (6ez) 9 (3r7.) 20 (697") 9 (3r%) 7 (267.) 20 (74i!)

(62%) t9 I ( e7") 7e (9 r"t) s ( s"t) 8e (es%) rr (L2Z) 81 (882) 31 (382) 5t

20 30 (777") e (23%) B (207") 33 (8oZ) 9 (22%) 32 (787.) t(32) 34 (97'/.)

2t 3 (t2"t) 22 (88%) L(4%) 24 (e67.) 12 (487") 13 (527") o ( }iL) 2s (r}o't) ta. 8 (2e%) 3s (B1Z) 13 (257") 40 (7sz) 23 (4514) 28 (ss%) r ( 27") t o (987")

( 25 o(oz) 3 ( 1002) 0 (0%) 2 (100"1) r (s0%) r (50"/.) o ( o"t) i 1002)

Streptelasma amsdeni

(82%) ¿4 2 ( 4Ð st (s6%) 4 ( 8"/.) 48 (s2"1) 0 ( 0z) 51 (1002) I (I8Z) 37 10s

Text-fígure 16,--Relatíonshíp bctwccn lcngth of major septa and coral díameter in streptelasma subregulare, for specimens yielding more than one transverse thin section. The length of a typícal septum

!üas measured and dívíded by the coral radíus, yíelding a ratíon between

0.0 and 1.0. Arbítrary líne (dotted) was used to derive proportions shor¿n in part of Table 3. Data from Appendíx 2. 106

1.0

0.9

0.8 ct) f õ fE äo.t fr o o .t. [ 0'6 [rJ U) fr oì É o.u !L o oÞ zO.4 UJ

0.3

Section 18-3, 4 35 cross sections from 14 corals

o.2 All other sections 247 cross sections from 103 corals

o 5 10 15 20 25 30 DIAMETER (mm) 107 greaÈ in early stages and decreases during ontogeny. The actual thickness of septa generally increases ín early to intermedíate stages, and then decreases (Text-fig. 17, Table 3). However, in some corals the septa decrease in thickness throughout ontogeny, and ín others their thickness remaíns about the same.

The cardinal sepËum is most commonly inconspícuous, beíng the same length and thíckness as other major septa (Table 4). However, ít can be distinct if ít is relatively short or 1ong, and thin or

thick. Prominence of thís sepÈum varíes among corals, and can vary ín dífferent stages within indíviduals. In many specimens, the

cardinal sepËum becomes relatively short and thín ín late stages near the base of the calice. In early to ínterrnediate stages of a few individuals, the cardínal and counter septa are longer than other major septa (P1. 1, fig. 7). The cardínal fossula is usually

ínconspicuous, havíng the same width and shape as oËher paírs of interseptal spaces. However, it becomes very broad in some corals (Text-fig. 18, Table 3). Fíve basic intergradatíonal shapes are

recognized in cross sections, as follows: ( 1) wídttr decreases from periphery toward coral axís, (2) width constant, (3) wídth increases

to\^rard axis, (4) biconvex wiÈh maxímum wídth midway between periphery

and axía1 end, (5) hourglass-shaped wíth constricËion mídway between periphery and axial end (Table 5). Shapes (3) to (5) can be

especially distínctive . In ontogenetic stages where major septa are nondilated to slightly dÍlat,ed, rninor septa extend a short dístance beyond the stereozone. In a few individuals, the mínor septa írnmediately adjacent to the counter septum are anomalous in being longer than the 108

Text-f ígure 77.-RelationshÍp between thickness of major septa and coral diameter ín Streptelasma subregulare, for specimens yieldíng more than one Èransverse thin sectíon. Septal thickness was measured in transverse thín secÈions halfway between the axíal and peripheral ends of a typical septum on the counter síde (usual1y the counter septum). Arbítrary line (dottea) was used to derive proportions shown

ín part of Tabl-e 3. Data from Appendix 2. 109

o.8 Sections 14 and 18: \ 50 cross sections from 20 corals o.7 \ Sections 19 and 20: 0.6 109 cross sections from 45 corals cE 5 o.s U) CD zIIJ All other sections: ð o.¿ I \ 139 cross sections from 5g corals t- I o.3 uJ U) \

o.2 \-__-__

o.1

0 5 10 15 20 25 30 DIAMETER (mm) . 110 Table 4.-LengÈh and thickness of cardinal septum, compared with oÈher typical major septa, for transverse thin sections of

Streptelasma subr egulare and S. amsdení (Sectíon 24). Data from

Appendix 2.

Length of cardinal septum Thickness of cardinal septum

Section Shorter Same Longer Thinner S ame Thicker

Streptelasma sub ulare

3 0 (0%) 6 (1007!) o ( o"/") t (r7"Á) 3 (s0%) 2 (33%)

4 I (Lfl) 3 (337") 5 (s6%) 3 (337") s (s6%) I (112)

13 2 (40"A) 2 (40"Å) | (2oz) 2 (407") 2 (40%) r (20%)

T4 3 (r2%) le (73%) 4 (rs%) 6 (237.) t7 (6s7") 3 (r27")

15 1 (ni¿) B (80%) 1 ( 10Z) 2 (20'/") 7 (707") I ( 1o%)

16 s ( lsz) 27 (7e7!) 2 ( 67") 7 (2L"/.) 24 (7 r"/.) 3 (e%)

T7 B (16%) 31 (63%) 10 (207!) 18 (377.) 2s (sr%) 6 (t2"/")

18- 1, 2 s (207!) 11 (447") e (367") to (37%) 1s (s6%) 2(7%)

1B- 3, 4 s (r7%) le (66%) 5 (17%) 6 (21%) 20 (6e7") 3 (t07")

I9 le (22%) 34 (40"/") 32 (3Bi() 23 (27%) s7 (687") 4 ( s7")

20 4 (r07.) L6 (4t%) 1e (4e%) e (23%) 28 (72%) 2 ( 57.)

2T r ( 4"/") I (3si() 14 (6r%) 7 (2e"/") 10 (42"/") 7 (297")

23 s (r2%) 20 (48%) t7 (407.) 16 (337.) 26 (s47.) 6 (r37")

Streptelasma amsdení

24 0 ( 0"/") 26 (53%) 23 (47%) 0 ( O"/") 48 (e8%) t ( 27.) 111

Text-f ígure 18.-RelaÈíonship beËween width of cardínal fossula and coral dlameÈer ln SËtepÈelasma subretsulare. Ididth of cardfnal fossula \"ras measured between median línes of septa immediately adjacent to Èhe fossula, midway between axíal and perípheral ends of septa bounding the fossula. Numbers beside data poínts índícate frequencies greater Èhan one. Arbitrary line was used Èo derive proportions shown in part of Table 3. Data from Appendíx 3. LT2

o o 5 o o Sections 18 and 19:

136 cross sections from 70 corals o E o E 4 o o

f o o U) o U) o o o o o o I't- o o o 3 o o O2 oo o o o z o o o2 o ooo o o o o o o É, o o 2.) ooo 02O s) o o 2.)2 o oo 3 o2 I O2 ' o o o o lL 02O 2.) -o02 . z. . 2O o o O 02 o 2. oo 3. oo o o-,2 . 2 o2 . 03 z.) ooo O,/ O2 2.) o . 4) o r .) .3 .) s. .) t- o .'/"/O .) )e .) 2.) o .) O2 )3 )3 a ) o o 1 ) .g o Ð B s s.)3 2 .)2 oo ={ o 6)22. .) o 2. 2 3. All other sect¡ons: o 252 cross sect¡ons from 6O corals

0 5 10 15 20 25 30 DIAMETER (mm) 113

Table 5.-Proportions of each type of cardinal fossula shape for transverse thin sections of SËreptelasma subregulare and S. amsdeni. In cases v/here the shape on eíther síde of a fossula is different'

each side vras counted as one half. Fossula types are descríbed ín

SYSTH.,IATIC PALEONTOLOGY under S. subregulare. Data from Appendix 3.

Fossula shape

Sectíon 1 2 3 4 5

S treptelasma sub regulare

3 r (207") i (207() 3 (607.) 0 ( o%) 0 ( 07.)

4 o (0%) I (1r%) 2.5 (28%) 2 (227.) 3.5 (39"a)

13 o (o%) 0.5 ( B%) 3 (50"/,) I (17%) 1.5 ( e.Á)

I4 6 (247i) 4 (16"/") 6.5 (26%) 3 (r2%) 5.5 (227.)

15 o ( 07") 4 (3r%) 4 (3L"/.) 1 ( 8i() 4 (3r%)

T6 24 (s6"/") 7.5 (177i) 8.5 (20"/") 1 ( 2"/") 2 ( s%)

L7 16 (317.) 20.5 (39"/") 7.5 (r4"/,) 5 (r0"/.) 3 ( 6%)

1B- 1, 2 2.5 ( 9"/") 7.5 (287") 6 (22"/") 3.5 (13iá) 7.5 (28%)

18- 3, 4 r.5 ( 6"/") I2 (44%) 7 (26%) I ( 4%) 5.5 (207")

19 t7 (zr"a) 17 .5 (2t%) 15.5 (r97.) 18. 5 (23%) 13. 5 (t67")

20 0.s ( r%) 10 (287") 6 (t7%) 12. 5 (35"/") 7 (lg'/.)

2T | (4%) 11.5 (46%) 3.5 (t4%) 7 (28%) 2 ( 8%)

23 6 (rsz) 15 (377.) 8.5 (2r%) 8.5 (2r%) 3 ( 7%)

Streptelasma amsdení

24 19 (42"/.) 4.s (r07.) r ( 2iÐ 7.s (177.) 13 (297!) TT4

other minor septa, and can be almost as long as the major septa (P1. 2, figs. 12,17,18; E1ias,1982, pl. 4, fig. 13). Thickness of the stereozone ranges from 5 to 15 percenÈ of the coral radius. Specimens t¿íth thick septa tend to have thíck stereozones.

Tabulae are conmonly complete and thin (P1. I, fígs. 18, 19,

26-28, PI.2, fígs. 1, 2,7-9). They are usually convex upward ín the septal region, but can be flat or rarely concave upward. In the axial region, they are concave or flat. They are generally moderately to widely spaced, but can be very closely spaced (Text-fig. i9). Tabulae are usually depressed in the cardinal fossula (P1. 2, figs. 8,9; Elias;7982, p1. 4, fig. 7).

Microstructure.-In transverse thin sections the najor septa are fíbrous in all ontogenetic sÈages. However, fibers are dífficult to discern if septa are thín. The fibers originate at the median line within the septum, and curve outrnrard in the direction of the coral axis so that their convex sides face axíally. I,lhere the major septa are greatly Ëo completely dilaÈed, minor septa appear as tríangular wedges beËween them (e.g., Elias, 1985, fig. 17). tr{here major septa are nondílated to s1íght1y dilated, U-shaped lamellae with concave sides facing the coral axis form the stereozone between adjacent major and minor septa (e.g., Elias, 1982, p1. 2, fig. i0). A contorted suture extends through the 1ame11ae ín a medial posítÍon between adj acent septa. The epítheca ís composed of shorË fíbers oríented approximately perpendicular to the outer surface of the coral. In longitudinal thÍn sections, septal fibres are inclined from the periphery of the coral toward the axís at an angle of about 40 degrees.

Dís cuss ion.-S avage (1913a) mentíoned Zaphrentis subregularis 115

Text-figure 19.-ì.Iumber of tabulae (counted along coral axis) per cenÈímeter of coral length in longitudinal thin sections of Streptelasma subregulare (Sections 13 to 21) and S. amsdení (Section

24). Numbers besíde data points índícate frequencies greater than one.

DaLa from Appendíx 4. NUMBER OF TAAULAE PER CENTIMETER OF CORAL LENGTH ]Þ lÞ o o| ô ot o (,l

o) a

à a a a a

(¡ a

o) aaa a CD m ai{ aa a a a a a õ- z@ aai a a

ao aa a a

N o O

lÞ a a a

Þ N à¡\) -

ol LT7

n. sp. and Z. ambigua n. sp. in his text and tables, but descriptÍons and i1lusËrations of these species were publíshed later (Savage, 1913b,

1977). Elías (1982, p. 57) established that Z. ambigua is a synonym otZ . subregularis, and assigne d the species to Streptelasma.

Zaphrentis channahonensís n. sp. ri/as listed ín a table by Savage (I9I2, pp. 98, 99), but he dld not provide a descríption or illustrations, and the species r^ras not menËíoned in subsequent literature. Therefore, this ís a nomen nudum. Specímens labelled Z. channahonensis by Savage hrere examined ín this study. They are from the same unit and locatíon as others whích he identified as Z. subregularis and Z. arnbigua. Thín sections of one prove that it is

Streptelasma subregulare (P1. 1, figs. 2-4) .

The continuous spectrum of values for the numerous features measured and compared in this study demonstrates thaË there are no morphologic discontinuítíes among specimens in the large collection described above. Those characteristics exhibiting anomalous trends at some localities or in particular stratígraphíc íntervals always fal1 wíthín or overlap the range of values for corals from elsewhere. There are no apparent geographic or stratigraphíc patterns, or inLerrelatíonshíps among these anomalíes (Tab1e 6). It is concluded that S. subregulare is a híghly varíable species. An important confírmation of thís intraspecific varíabílity ís the great range of characteristics seen within some individuals. Solitary corals from the Keel Formation at Section 24 (CoaI Creek) generally líe within the range of variability for thís taxon, but most of the individual characteristícs are atypícal (Table 6). 118

Table 6.-l'forphologic characterístics of Streptelasma

subregulare (Sections 14-21 , 23) and the closely relaÈed species S.

amsdenÍ (sectíon 24) for sectíons ¡"rith relatively large sample

sÍzes, based on inspection of coral lengths and data in Tables 2-4 plus Text-fígure 19. H = unusually high frequency; T = typical frequency; L = unusually low frequency; - = insufficient data (fewer than 10 data poínts for comparison, except for "closely

spaced tabulaerr r¿here all points r^rere used) .

Sections

IB-1, 1B-3,

Charac teris tics 14 15 76 17 and 2 and 4 19 20 21 23 24

Long corals T T T T T H H H T TH

Trochoid L H L L T T T H HL

Cylindrical T T T T T T T T TH

S traigh t L H T T L T T L TT

Greatly curved T L H H H L T H TL

Numerous septa T T T T T T L H L TL

Long major sepÈa T T T T T H T T T TT

Thin rnajor septa L T T T L L H H T TH

Long cardinal sepËum T T T T T T T H H TH

Thick cardinal septum T T T T T T T T H TT

Irride cardinal fossula T T T T H H H T T TT

Closely spaeed tabulae T T T H T T T T T -L 119

They cornprise a populatíon that is considered to represent a different species, S. amsdenj- n. sp.

Some specimens of S. subregulare r¿íth moderately dilated septa closely resernble the lectoÈype of S . corniculum Ha11 1847, from the

Trenton Límestone (upper Middle Ordovícian) of New York (Neuman,

1969, pp.10, 11, figs. 51 6). The number of septa, wídth of the cardínal fossula, and spacing of tabulae in the laËter specimen are about average for S . subregulare. However, the major septa are slightly longer than usua1, and the degree of septal dilatíon is greater on the cardínal síde Ëhan on the counter side. Further com¡arÍ.son is not possible at this time because the range of varíability in S. corniculum ís unknown.

Some representatives of S. subregulare wiÈh thin: wâVy septa are símilar to S. affine (Bí11íngs, 1865) from the Vauráal Formatíon

(Richmondian) and El1ís Bay Formation (Gamachían) on Anticostí Island,

Québec (Bolton,1981, p1.3, fígs.3-8; E1ías,1982, pp.59,60, p1.5, figs. 4-18), S. prímum (l.riedekind, 1927), an Ashgill species found ín

Stage 5a of Norway, the Boda Limestone of Sweden, and the Pirgu Stage of the Estonian S.S.R. (Neuman, 1969, pp. 11-I7, figs. Ta-c, e-h, 8-I0; see also Neuman, 1975, pp. 357, 358), and S. unicum Neuman, 1975 frorn the Dalmanitina Beds ( uppermost Ashgí11; Hírnantían) or lowermost

Llandovery of Sweden (Neuman, 1975, pp. 353, 356-358, figs. 15, 16).

However, in S. affíne and S. primqm the cardinal septum is always indistínct, and a cardinal fossula ís never developed. In S. unicum, the cardínal septum becomes short and the fossula ís conspicuous in late stages, but early ontogenetíc stages and intraspecific varíability are unknor^rn. Mínor septa are longer in S. affíne than I20

ín the other three specíes. A few individuals of S. subregulare resemble Helicelasma simplex Neuman, 1969, from the Dalmanitína Beds (uppermost Ordovícian;

Hirnantían) of Sweden (Neuman, 1969, pp. 29-33, fígs. 23-26). In the latter species, major septa are greatly to completely dilated in early stages, and gradually become thinner duríng ontogeny. A simple axial structure of fused septal Ëíps is formed during the intermed.iate and late stages. The cardinal septum and fossula are inconspicuous in H. símplex, but are most commonly conspicuous in comparable corals belongÍng to S . subregulare.

Like some specímens of S. subregulare, tsorelasma crassitangens

Neuman, 1969 from the Dalmanitina Beds (uppermost Ashgill ; Hirnantian) of Sv¡eden has thíck major septa that are greatly Ëo completely dilated

ín early stages and decrease in length duríng ontogeny (Neuman, 1969, pp. 66-69, figs. 57-59). A diagnostic characteristíc of this taxon is Lh. long card.inal and counEer septa in early stages, a feature that is rare in S. subregulare. The cardínal septum and fossula are inconspicuous in late stages Borelasma spp" a and b were reporled from Stages 6b and 6c (lower Llandovery; Rhuddanian-Idwian) and SËage 6c (Idwian), respectively, of Norway (Neuman, Ig82, p1. 1, fígs. l4-lg).

They are similar to B . crassitangens, but the cardinal s eptum becomes short and a fossula is developed ín late stages.

Specímens of S. subregulare wÍLhthick septa that are greatly to completely dílated ín early stages, and a few distantly spaced tabulae, resemble Ullernelasma svartoeyensis Neuman, 1975 from Stage 5b (uppermost Ashgí11; Hirnantían) and Stage 6a (lowermost Llandovery; T2I

Rhuddanian) of Norway (Neuman, 1975r pp. 348, 350-353, figs. 10-13).

In the latter species, the cardinal septum is dístínct and becomes

short in late stages, and the cardínal fossula ís conspicuous. Those

features are less conmon in similar indivíduals of S. subregulare.

Neuman noted that a few íncomplete tabulae seem to be presenÈ ín U. svartoeyensis. Tabulae in S. subregulare are complete, but their

presence ís not always revealed ín cross sections because they can be widely spaced and approximaËe1y horizonËal. r22

S trep telasma amsdeni n. sp.

Plate 3, fÍgures 1I-28; Plate 4' figure 1

Derívation of name.-The s pecífíc name honors Thomas l,tr. Amsden of the Oklahoma Geological Survey, who collected some of the specímens described hereín.

HoloLvpe.-USNM 24-2-36, ínÈerval 24-2, EMM co11.

P ara typ e s .--lJSNl't 24-I-1, íntervaL 24-I, EMM coll., USNM 365920'

OGS-5, 10, 13, interval 24-2, A coll.' USNl"l 24-2-11, 17, 24,27,29, interval 24-2, EMM co11.

AdditÍonal ma ter ial .--USNM OGS-I (slab with 3 speclmens) , 2, 4, 6-9, 11, 12, 14, interval 24-2, A coll-., USMÍ 24-2-I-I0, I2-J9, 18-21, 26, 28, lg-fl, ]-/-Þ2, ínterval 24-2, EMM co1l. Occurrence.---{Jppermost Ordovician (Gamachían) : lower oä1íti" and middle laminated calcilutite units (intervals 24-1 and 24-2, (Coal respectively) of the Keel Formation, Sectíon 24 Creek) ' Pontotoc County, south-central Oklahoma. Diagnosis.---So1ítary, slender ceratoid to cylindríca1. Major septa thín, nondilated to slíghtly dil-a"ted an.ci exl-end to axis in early stages, gradually withdraw from axis duríng ontogeny. Cardinal septum indistinct to relatively long and conspícuous. Cardínal fossula usually ínconspicuous, buÈ can be dístinctÍvely shaped. Mínor septa typícally extend a short dístance beyond very narrow stereozone. Tabulae widely spaced.

Des crip tion of corals .--{he greatest observed length and díameter are 155 nm (USNM qGJ:Þ, incomplete at both endsi

P1. 4, f ig. lb) and 23 mm (Ustl¡l 24-2-55, íncomplete calice), respectively. In early ontogenetic stages, the majoríty of corals are r23 slender ceratoid ín forrn, with moderate or s1íght curvature (Pl. 3, fíg. 16). The typical adult form ís long and cylíndrieal, but some remain slender ceratoid (Table 2). Specímens are generally relatívely straight, but have slight to moderate bends plus several constríctions and rejuvenaÈions (P1.4, fig. 1). A few have ríght angle bends' Periodicíty of growth has been observed only ín the straíght portion of one indívídual, where six successíve constríctions are spaced 6 to 7 mm apart (average 6.8 nrn; Pl. 3, fig. 28). Septal grooves and ínterseptal ridges, plus growth 1ínes, are preserved on all specímens.

Attachment structures are not present. DepÈh of the calice is esËimated to be about 20 percent of the coral length in smal1 índivíduals, and is probably less Èhan 10 percent in adults.

Ontosenv and internal structures.-{he relaËíons hip between number of septa and coral diameter ís shown ín Text-fig. 20. In early ontogenetic stages (Pl. 3,figs. L2-I5r 20), the major septa extend to or almosË to the axís, where they meet. During íntermedíate sËages (P1. 3, figs. 2I, 22,24,26, 27)' the septa withdravr from the axis, leaving an open axial regíon. They shorten to half the coral radius or less ín late sËages (Pl. 3, figs. 23,25; Text-fig. 2I). Major septa are generally straight to s1íghË1y curved ín early stages, and become wary by late sËages in many individuals. They are thin throughout ontogeny (Text-fig.22; Pl. 3, fig. 11)' but can be slightly dílated in early stages.

Compared with other major septa, the cardinal sept1rrn ís the same length or longer, and vírtua11y always the same thickness, during all stages (Table 4). The cardinal fossula ís about the same width as other pairs of inËersepËal chambers in most specímens, but ís somewhat r24

Text-f lgure 20.-Relationship between number of major septa and coral tlianeter ín StrePtelasma amsdeni. Numbere beside data poínts índicate frequencíes greater Ëhan one. Arbítrary line (in same position as that for S. subr re in Text-fígure 15) was used to deríve proportions shown in part of Table 3. Data from Appendix 2. I25

a ao a a o a a 2a ata Þ30 a t À o 2a a LrJ o 2a a a 2a Ø a a o a a fr a o o a o ?2o a O 3a a 2a ll o oa 10 a a fi o m 53 cross sections from 26 corals zl o 5 10 15 20 D¡AMETER (mm) L26

Text-figurc 2l.--fl.elatíonohip between length of major septa and coral diameter in Streptelasma amsdeni. The length of a tyoícal septum was measured and dívided by Èhe coral radíus, yieldíng a ratio between 0.0 and 1.0. Arbitrary line (dotted, ín same posítion as that for S. subregulare ín Text-figure 16) vras used to derive proportions shown in Table 3. Data from Appendíx 2. 127

1.0 3

o'n 3 2 o E J 0.8 fr o o .t' o.7 a o- t¡J Ø 0.6 fE o 'l E o.s IL o I 2 (, l..¡+ z t¡J J a 0.3 52 cross sections from 26 corals

o 5 10 15 20 DIAMETER (mm) r28

Text-figure 22.-Relationship bet\,reen thickness of major septa and coral díameter ín Streptelasma amsdení. Septal thickness was measured ín transverse thin sections halfway bet\,reen the axíal and peripheral ends of a typical septum on the counter side (usually the counter septum). Línes join data poínts from índividual specimens.

Numbers beside data points indícate frequencíes greater Èhan one.

Arbitrary lÍne (dotted, in same posítion as that for S . subregulare in Text-figure 17) was used to derive proportions shown in part of Table 3. Data from Appendix 2. r29

? .9 o.e Ø ct) lIJ o.z a a oQ. a a a 3a a =F -¡ O.1 2a a5a 4a a a 4 2a a a2a a 2a 2a À LrJ 51 cross sections from 26 corals U) 0 5 10 15 20 DIAMETER (mm) 130

wider in intermediate and 1aÈe stages of a few (Text-fig. 23) .

Shapes of the fossula are as described for S. subregulare (Table 5). Minor septa generally project a short distance beyond the very narro\,I

s Ëereozone. Throughout ontogeny, the tabulae are usually compleËe' very thín, and relatívely widely spaced (Pl. 3,figs. 17-19; Text-fig. 19). They

are most commonly convex upward in the septal region, but can be flat. In the axial region, they are flat to concave upward.

MícrostrucËure.--{he microsLructure in transverse and

longítudínal thin sections ís the same as described for specímens of S. sgbrggulare having nondílated to slightlv dilated septa.

Discussíon.--{here is relative ly 1íttle varíatíon among corals ín the collectíon described above. The morphologic characterístÍcs

generally lie r¿ithin the range of variabilíty ín S . subregulare

(Savage, 1913b), but are not typical of that specíes (Table 6). The most striking features are the long, cylíndrical growth form and thín septa. The corals are consídered to compríse a populatíon

representing a dístinct taxon, SjIsglgþgng amsdeni n. sp., because

of these consístent differences. Thís specíes was referred to as

S trep telasma sp. in previous paleobíologic sÈudies (Elias, L9B4a, tables 1, 3-5; 1984b, pp. 535, 536).

S. amsdení resembles S. primr-rn (wedekind, 1927) and S. unicum

Neuman, 7975, which were discussed under S. subrsgulare. However,

the new species ís dístínct ín having more widely spaced tabulae. The

cardínal septum does not become short, as ín S. unicum 131

Text-figure 23.-Relationship between wídth of cardinal fossula and coral diameter in Streptelasma amsdení. I^ridth of cardinal fossula r,ìras measured between median lines of septa Ímmediately adjacent

Ëo the fossula, mídway between axial and peripheral ends of septa bounding the fossula. Numbers besíde data poinÈs índicate frequencies greater than one. Arbitrary line (in same position as that for S. subregulare ín Text-f igure 18) was used to deríve proportions shov¡n in part of Table 3. DaËa from Appendíx 3. 132

o E 3 o E o o -< J a f a o Ø a U) a 2 a 2a olr a 2a 2a a o o J a 2a O a o z a o 2a o a õ 1 3a a fr o o 2a () a 45 cross sections from 25 corals otL I F o o 5 10 15 20 DIAMETER (mm) = 133

Streptelasma leemonense Elias' 1982 Plate 4, fígures 2-I2; Plate 5, fígures I-4

S tre telasma leemonense Elias, L982, p. 56, p1-. 4, fígs. 1-3.

Holotvpe.-UCGM 45614 (Elías, 1982, pl. 4, figs. 1, 2), same interval as 2O-3, 2O-4, 20-5, E coll., Leemon Formation, Section 20

(Short Fa,rm), Cape Girardeau County, Missouri. Paratype.-UCGM 45615 (81ías , 1982, pl. 4, fig. 3), same interval as 20-3,20-4,20-5, E col1., Leemon Formation, Sectíon 20 (Short

Farm), Cape Girardeau County, Missouri.

j-nterval EM col1. Addi tional material .-USNM I4-I-5, 3I, 34, 14-I, ' Kíssenger Limestone Member' Bryant Knob Formation, Sectíon 14

(Higginbotham Farm), Pike County, Missouri; USNM 15-1-B' 15- 1- 12

interval 15-1, EM col1., Kissenger Límestone Member, Bryant Knob

Formation, Section 15 (Calumet), Píke County, Míssouri; USNM 20-1-10'

2O-I-I5, ínterval 2O-1, EMM co1l., USNM 20-l-19, 20-l-20, interval 20-I,

USNM 20-3-1, íntervaL 2O-3, USNM 20-4-2, intervaL 2O-4, EM coll',

Leemon Formation, Sectíon 20 (Short Ibrrn), Cape Gírardeau County' Missourí; UI C1448, S coll., Leemon Formatíon (labelled Edgervood),

Gale Section, Alexander County, Illinois; USNM 23-2-32, 23-2-36'

interval 23-2, EMM coJ-1., Icieai Quarry iuiember, Keei Formation' USIìÌ'í

23-2a-2, interval 23-2a, EM coll., USNM 23-3*I,3, 4,5, B,.lg-13'

interval 23-3, EMM co11., USNM 23-3-20, 23' interval 23-3' USNM 23a-I-2, 3, interval 23a-I, EM coll., Keel Formatíon, Section 23 (Lawrence Quarry)' PonÈotoc County, 0k1ahoma. Occurrences. Ordovícian (Gamachian) : Leemon Formatíon, -Uppermost southeastern Míssouri and southern lllinoís; Keel Formation íncluding r34

Ideal Quarry Member, south-central Oklahoma. Lowermost Silurian (lower lower Llandovery): Kíssenger Limestone Member' Bryant

Knob Formation, northeastern Míssourí. Diagnosís.---Solítary or with peripheral offsets, generally ceratoíd. Major septa typícally thin, extend to or almost to axís throughout ontogeny. Cardinal septum indístinct to relatively long' cardínal fossula usually inconspícuous. Mínor septa at least half the

length of major septa, commonly contraclined to contratingent' extend beyond narro\Ár to very broad stereozone. Tabulae moderately to closely

spaced.

Descríption of corals.--{he greatest observed length and

díameter are 55 mn (USt¡t"t 23-3-Il, incomplete at both ends) and 20 mm (usn¡l 20-3-7 at base of calj-ce), respectively. Of 12 índivÍduals' six are ceratoíd, three are trochoid, and three are cylindrical (Pl. 4,

fig. 10). Ten are slightly Èo moderately curved, and two are straight.

Corallum shape ín cross section is generally circular, but can be irregular (P1. 5, fig. Ð . The presence of septal grooves and ínterseptal ridges has beerr verífied ín transverse thín sections of specimens enclosed in matrix. The measured depth of the calíce is

approximately 10 percent of the coral length, but ca1íce ríms in those individuals are poorly preserved and may be incomplete. Clusters of up to about 20 índíviduals were collected at Sections

15, 20, and 23 (UStlU Þl:9, 20- 3- I 23-3-23 . Smaller clusters \,'Iere also found, consísting of at least six coralla at Sectíon 14 and fíve at SecÈion 20 (USNM 14-1-5, 20-r-20 Enclosure ín matrix or

poor preservation makes ít diffícult to establish whether they represent true coloníes or pseudocoloníes. Evidence from one large cluster and 135

several otheï coralla índícates that buddíng did occur (USNM 20-3-I, 23-2-32, 23-3-3; P1. 5, figs. 1-4). Definite perípheral offsets are located between the older and younger wa1ls at constrictions, and are initially orÍented approximately para1lel to the protocorallíte. Some

diverge ouËward in later stages. Offsets are found on a1ar, counter,

and cardinal quadrants of Ëhe parents with about equal frequency. One

specimen has at leasË seven at the same heíght, and Èhey are distributed over about 75 percenL of the circumference (USNM 23-3-3). The offsets

can become quite large. In one cluster, several of the bíg indivíduals with numerous offsets began as buds themselves (P1. 5, figs. 1-4). Other specímens could represent budding or a gregarious, epizoic habít. In two clusters, several relatively srnall corals located on only one side of a larger indívídual are oriented approxímately

perpendícu1ar to iE (USNM 15-1-B' 20-r-20 . They may have used an

exposed side as a substrate for attachment. In other cases, small corals occur on the exteríor of a large indívidual that lacks

constrictíons at those sítes (e.g ., usNM 23-3-5 They are usually oriented at hígh angles to the grol^/th axis of the host or protocorallite. Peripheral offseÈs and/ot epizoíc índíviduals are present in approxímately 25 percent of the specimens studied herein.

Ontogeny and internal structures.-The relationship between

number of septa and coral díameter is shovm in Text-fíg. 24. In early (P1. 4, fígs. 2,3, P1. 5, fígs. 1, 2), intermediate (Pl.4, figs.4, 7, 12, Pl. 5, fíg. 3), and 1aÈe ontogenetíc stages (P1. 4, figs. 5, B, g, P1. 5, fíg. 4), the major septa extend to or almost to the

axís, where they commonly mee¡ ín srnall groups. A counterclockwíse 136

Text-figure 2î.---lìelationship between number of major sepÈa and coral diameter ín Streptelasma leemonense and S. sp. cf. S. leemonense. Numbers beside data poínts indicate frequencíes greater than one. Data from Appendix 2 r37

a 40 2a o .o. o a2a a Oo o o O. l- o oo À a a t t 2t trJ o Ø a a 20 a 30 oa (r O. . o o o 3a 2a a o 2a I 2a a 2a o Oo 20 oTL O. fr . Strepte/asma leemonense I,JJ d) 52 cross sections from 26 corals Ð 1 0 z O S, sp. cf. S, ,eetnonense 7 cross sections from 2 corals

rì 5 10 15 20 DIAMETER (mm ) 138 axial whorl is present in some specimens. The septa are usuelly slightly curved to wary. They are generally thin, but can be slíghtly to rarely greatly dílated ín early stages. The cardinal septum ís as long as or longer' and ín some cases slíghtly thícker, than the other major septa. The cardínal fossul¿ is usually inconspicuous, havíng the same wídth and shape as other paírs of ínterseptal chambers, but it can be slightly wider or biconvex ín cross section. The length of minor sepËa is generally about 50 percent of the coral radius, but varies frorn 30 to 70 percent. Minor septa are conmonly contraclined to contratingent. They extend beyond thc stereozone. The thíckness åf ,f,u stereozone is typíca11y 10 to 20 percent of the coral radius, but can be as great as 40 percent. The stereozone is very thick at sites of rej uvenescence. Tabulae are generally complete (P1. 4, figs. 6, il)' fn the septal region, they can be relatively flaË and approximately horizontal to steeply ínclined upward tov/ard the axís' or convex up\^lard. They

are ilat Ëo concave upward ín the axía1 region. Spacíng of tabulae varies frorn 9.3 (USNM 20-!-10) to 20 per centímeter of coral length

( usNM 23-3-1 1 Mícrostructure.-In transverse thin secËions, the major septa are fíbrous. The fíbers are visible ín or near the stereozone within thin septa, and along the entíre length of relatívely thick septa. Fibers originate at the median line within the septum' and extend outward in the dírection of. the coral axis. They are generally slightly curved, with convex sides facíng the axís. In the stereozone' major and minor septa are expanded into lateral contact along a 139

conËort.ed suture. The epítheca consists of fíbers oriented approximately perpendicular to the ouËer surface of the coral. In longitudinal thin secÈíons, septal fibers are ínclined from the periphery of the coral Ëoward the axis at an angle of about 45 degrees

Dis cus s íon. t reptelasma leemonense Elías, 1982 was previously -S knorvn only from the holotype and paratype, which are small, íncomplete, and lack offsets. The ne\^/ material documented above provides data on all ontogenetic stages, mícrostructure, and blastogeny. This species Ís easíly ídentified by íts long, contraclined to contratíngent mínor sepËa. The presence of offsets and occurrence ín clusters is uníque among the taxa descríbed hereín. Specímens from Oklahoma that were referred to as S. sp. cf. S. leemonense in a previous paleobíologic sÈudy (U1ías, 1984b, p. 536) are S. leemonense. Three indivíduals from the Keel Formatíon at Section 23 (Lawrence Quarry) resemble S. leemonense, but are anomalous in havin g very long counter as well as cardínal septa. They are described as S. sp. cf. S . leemonense in this paper.

S. leemonense resernbles S. etnaense Elias iq Elias and Potter,

1984 from an Upper Ordovician (Ashgíl1) limestone ín the Horseshoe

Gulch unit, eastern Klamath Mountains, California (fl:-as and Potter,

1984, pp. 1207, 1209, fíg. 2a-g), S. eccentricum Neuman, 1969 from

Stage 5a (Ashgill) of Norr,ray (Neuman, 1969, pp. 25-28, figs. 20, 2I), and S. ostrogothícum Neuman, 1969 from the Dalmanitína Beds ( uppe rmos t

Ashgí11; Hirnantian) of Sweden (Neuman, 1969r pp. 2l-23, fígs. 13, 14).

All have relatively l-'ong minor speta, thin major septa that commonly meet in groups axially and can form an axial whorl, a cardínal septum that ís índistinct to long, and a typically inconspicuous cardínal 740

fossula. However, tabulae are convex upward in S. etnaense and S eccentrícum, offsets are intracalícular ín S. etnaense and S. ostrogothicum and lacking in S. eccentricum, septal lobes form a very

small axía1 structure in S. erqnaqq?' and in S . eccentricum the axís \ is displaced toward the counter side during late stages and the stereozone is very thin. The mínor septa can be longer in S.

leemonense Èhan in the other three species. I4T

Streptelasma sp. cf . S leemonense Elias, L982

Plate 4, fígures 13-17

tcf. ] strep telasma leemonense Elias, 1982, p. 56, p1. 4, fígs. 1-3.

Magerial.-USNM 23-2a-4, interval 23-2a, USNM 23-3-22, inËerval 23-3, USNM 23a-1-7, interval 23a-I' EM co1l.

Occurrence. Ordovícían (Gamachían) : Keel Formation, -Uppermost Sectíon 23 (Lawrence Quarry), Pontotoc County, south-central Oklahoma Description of corals.-The greatest length and diameter are estímated Èo be 30 nn and 22 mrn, respectively (USl¡i't 23a-I-7, incomplete apex and ca1íce rirn). The growth form ís slender ceratoíd and slightly curved (USX¡I 23-3-22 to questionably trochoid (US¡IU

23a-l-7 . SepÈa1 grooves and ínterseptal ridges are present (USNM 23-2a-4).

Ontogeny and internal structures.-{he relationship between number of septa and coral diameter is shown in Text-fig. 24. The major septa extend to or near the axis in early (P1. 4, fig. 13) to

ínÈermediate stages (Pl. 4, fig. 15), where some of them meet in pairs or smal1 groups. All except the cardinal and counter septa withdraw from the axís during late stages (P1. 4, fígs. 16, 17). The major septa are straíght to usually slightly curved. They are nondílated to slightly dilated duríng early to íntermediate stages, and thin in late stages. The cardinal and counter septa are longer than rhe oËher major septa Èhroughout ontogeny. They are joined to form a median lamella

during early to intermedíate srages, and become disconnected and

gradually wíthdra¡¿ from the axis in late stages. Their axial ends r42. are dilated. The cardínal fossula is inconspicuous. Minor septa are

1ong, buË theír length is less than half the coral radius. They are seldom contraclíned or contratingent. The minor septa extend beyond the sÈereozone, which has a thíckness that is abouË 10 to 30 percent of the coral radius. Tabulae are convex upward ín the septal region' and flat to concave upward ín the axíal region (P1. 4, fig. 14). Microstructure.--{he mícrostructure in transverse and longitudína1 thín secËíons is the same as described for S. leemonense.

Discussion.--{he specimens descríbed above are dístinguished by theír cardinal and counter septa, which form a medían lamella during early to intermediate sÈages and remain longer than other major septa in late stages. Other characterj-stics lie rrlíthin the range of variability in Streptelasma leemonense E1ías, 1982, although the number of septa is comparatívely high (Text-fíg. 24) and Èhe minor septa are relatively short. These three incomplete specimens l¡¡ere found together with S. leemonense, but ít ís uncertaín whether they are atypical corals of that species, or represent a closely related new specíes that ís rare in the Keel Formation at Section 23 (Lawrence

Quarry). They are Èherefore identífied as S. sp. cf. S . leemonense. r43

Streptelasma sp. A Plate 5, fígures 5, 6; Plate 6, figures 1-5

Materia!.-UsNM 15-0-1, 14, lC, ínterval 15-0' EM col1. Occurrence.-Uppermost Ordovician (Gamachian) : Noíx Limestone' Section 15 (Calumet), Píke County, northeastern Missouri. Descriptíon of corals.-Al1 three indivíduals are epízoic, less than 3 mm in díameter, and probably less than 5 mm in length. They are located on ¡¿hat is probably Ëhe upper síde of a síngle, horizontally oríented bryozoan (P1. 5, figs. 5, 6, Pl. 6, figs. 1-5).

Two are spaced about 11 rnm apart, and the third is situated approxímately 20 mm from the others on what ís likely the same colony. The corals grew subparallel and then perpendicular to the surface of the bryozoan. They are probably attached by their cardinal sides. The apíca1 part of the aËtached síde is flattened and conforms to the shape of the host, whereas unattached portions are rouncl, with septal grooves and interseptal ridges. The bryozoan colony eventually gre\¡t around Ëhe sides of the epizoíc corals.

Ontogeny and internal structures.-From 72 to 17 major septa are present at diameters of 2 to 3 mm. In early stages they can be as liËtle as 50 percent of the coral radius in length (PL. 6, fig. 3), or can extend to the axis (P1. 6, fig. 1). During intermediate to late stages, they meet at the axís ín one indívídual (P1. 6, fígs. 4r 5).

In another, a few fine septal lobes at the axis occupy less than 10 percent of the coral diameËer (P1. 5, figs. 5, 6). The third has several coarse septal lobes occupying almost 20 percent of the coral diameter (P1. 6, fig. 2). The major septa vary from relatívely r44 straÍght to wavy, and are thin throughout ontogeny.

In one specimen, what may be the cardínal septum is longer than other major septa (USNM 15-0-14). The cardinal fossula is índistinct.

Minor septa, where present, are very short. The thickness of the stereozone varies from less than 5 percent to about B percent of the coral radius. Tabulae are possibly present ín the late stage of one indivídual (P1. 6, fig. 5), but longitudinal sections could not be prepared for confírmation. MicrosËructure.--{he mícrostructure could not be dÍstínguíshed ín transverse thin sections of these sma1l corals having very thin septa and stereozones.

Discussion.-The epizoic habit and morphology of the specimens described above are simílar to Streptelasma dívaricans (Nicholson,

1875). The latter, highly varíable species is knov¡n from the Uphan

Dolomite Member of the Second Value Dolomite (middle Edenian to lowermost

Maysvillían), Montoya Group, New Mexico and Texas (Elias, 1985: PP. 37, 38, 40, figs. 14.L-14.14, and the follor.ring Richmondían uníts: Dillsboro Formatíon, I{hiÈewater Formation, and Rowland, Bardstor^7nr Saluda

DolomiÈe, and Preachersville members of the Drakes Formation,

Cíncinnati Arch region, Kentucky-Indíana-Ohío; Bay de Noc Member,

StoningËon Formation, Michígan; Meaford and Kagawong beds, upper member, Georgían Bay Formation, Ontario (E1ias, I9B2¡ pP. 53-56, P1. 1, figs. 1-41, pl. 2, fígs. 1-16, pl.3, figs. I-23;1983, pp.9,10' p1. 2, figs. 16-33). Although corals of S . divaricans are sma1l (81ías , 1982, fig . 14), Ëhe individuals from the Noix Limestone are even r4s

Smaller. However, it is uncertain whether they are mature because only three are known, and all are probably attached to the same host. s. (?) parasiticum Ulrich in l,trínchell and Schuchert' 1895, f rom the upper Míddle Ordovicían rrTrenÈon limestone'r (= Platt.eville Limestone; Blackriveran) and rrTrenton shalesrr (= Decorah Shale; Rocklandian) of Minnesota, forms pseudocolonies or colonies attached to bryozoans (l[inchell and schuchert, 1895, pp. 89, 90, fig. 6; see Bassler, 1950' pp. 14, 15). The coralla are only several míllimeters 1ong, but ínternal structures are unknown. The specímens described herein are identÍfied as Streptelasma sp. A because of these uncerÈainties. L46

Streptelasmâ sp. of E1ías, I9B2

Streptelasma sp. Elias, 1982, PP. 56, 57, pI. 4, figs. 4-6

Material.-UCGM 45616' same interval as 2O-3, 2O-4, 20-5, E coll' Occurrence.-Uppermost Ordovician (Gamachian) : Leemon Formatíon,

SecÈíon 20 (Short Farm), Cape Gírardeau County, southeasÈern Míssouri.

Díscussion.-Additional materíal \^7as not found duríng Èhe present study. This specímen may be Streptelasma subregulare (Savage, 1913b), but cannot be positívely identifíed as thaË specíes because it Ís smal1 and incomplete. r47

Genus Grewinekia Dybowski, 1873

Grewingki4 sp. A Plate 6, fígures 6-10

Material.-USNM 14-2-7, interval I4-2, EM co11., Kíssenger

Límestone Member, Bryant Knob Formation, Sectíon 14 (Hígginbotham

USNl"t inËerval 23-3, EM coll. Farm), Pike County, Missourí; 23-3-]!' ' Keel Forrnation, Sectíon 23 (Lawrence Quarry), Pontotoc County'

Oklahoma.

Occurrences. Ordovícian (Gamachían): Keel Formation, -Uppermost south-cenËral Oklahoma. Lowermost Sílurian (lower lower Llandovery) ; Kissenger Límestone Member, Bryant Knob Formation, northeasËern Missouri.

Descriptíon of corals.-The 1a rgest specímen ís 25 mm long and 14 mm in diameter (USNM 74-2-7, apex and calice incornplete). Its growth for¡n ís trochoíd and curved. An attachment structure ís located on what is almost certainly a cardínal-alar quadrant (P1. 6, fig. 7).

Ontogeny and internal sËructures.-{he numbers of rnajor septa

at diameters of 5 rmn, 7 mm, and 11 urn are 20, 22, and 32' respectively

(USNM 14-2-7). In early ontogenetíc stages, a few septal lobes

are preseni ai Ëhe axis (Pi. 6, fig. 6). An axiai si-r.-uciure of sepial lobes and lamellae develops during íntermediate stages (Pl. 6, fígs. 7, B). In late stages, the major septa become relatively short, and

the moderately complex axíal structure comprisíng long, curved to

contorted septal lobes and 1ame1lae has a radíus that is 40 to 50 percent of the coral radíus (P1. 6, figs. 9,10). The septa are straíght to slightly curved and thin to moderately thick in all known r48

stages. Thecardinalseptumandfossulaareinconspícuous.InlaËe stages, the length of mínor septa is 40 percent of the coral radius' Minor septa extend beyond the stereozone' which has a thickness of 10 to 20 percenË of the coral radius. Several Ëabulae are apparent ín one transverse sectíon (P1.

6, fig. 10) . MícrostrucLure.-Mícrostructure ís preserved in portions of these silicified specímens. In transverse thin sections, fibers appear to

originate aË medial positions wiÈhin major septa' and curve s1íghtly

outr¿ard in the dlrection of l-lte crrral axis. In the stereozone, major

and minor septa are expanded into lateral contact' Díscussíon.-AlËhough the specimens documented above are poorly preserved, they clearly díffer from the other streptelasmatids described herein in havíng axial structures of septal lobes and lamellae. In that respect, and in the nature plus arrangement of major septa and length of minor septa, they resernble Èhe single representative of Bodophyllum shorti Elias . IgB2, describe,i previously from the

Leemon Formation (uppermost Ordovician; Gamachían) at Section 20 p1' (Short Farrn) in southeastern Míssourí (Elias , L982, PP' 77 ' 78' 13, figs. 10-14). However, ín the latter taxon the axial structure is solid in early stages, includes a medían 1ame1la ín íntermediate stages and is comparatively small ín late stages, and more tabulae are present ín transverse sections. In view of fhese differences and the 1ímited amount of data, the two specímens descríbed herein are

ídentified as Gr ewínekia sp. A.

The nature plus arrangement of major septa and length of minor I49 septa in Grewíngkþ sp.A are símí1ar to the following species: G. penobscotensis Elias, lg82 from Upper Ordovícían (Ashgill) strata within an unnamed formation ín Penobscot County, Maine (Elias, 1982, pp. 72, 73, pl. 12, fígs. 1-6), and within the Horseshoe Gulch unít in the easËern Klamath Mountains of California (¡lias and Potter' 1984, pp. 7209, I21O, fig. 2h-L); G. anguínea (Scheffen' 1933) from Stage 5a

(Ashgi11) in Nonvay (Neuman, 1969, PP. 48-50, fígs . 39-41); G . contexta

Neuman, 1969 from the Boda Lírnestone (Ashgill) of Sweden (Neuman, 1969, pp. 43, 45-48, figs. 34-38); and G. cuneata Mclean, L977 from the Cape Schuchert Formatíon (upper Llandovery) of nor¡hwestern Greenland (Mclean, I977, pp.11, 12, pl. 1, figs. 8, 10, 12)- However, in late stages Ëhe axíal structure ís símpler with fewer lamellae ín G. penobs co tens is , septal lamellae are typícally shorter ín G. anguinea' lamellae are more numerous and the axial structure ís more complex ín G. contexËa, and ín G. cuneata many fine 1amel1ae are concentrated at the períphery of the axial strdcture' and only a few coarse lamellae are present at the axis. 150

Subfamily DALMANOPHYLLINAE Lecompte, 1952

Genus Bodophyllum Neuman, 1969

Bodop hyllurn shortí Elias , r9B2

Bodophyllum shorti Elias, 1982: pp. 77,78, p1. 13' figs. 10-14.

Holotype.-UCGM 45613' same interval as 20-3, 2O-4, 2O-5, E coll. Occurrence.-U ppermost Ordovician (Gamachían) : Leemon Formatíon,

Sectíon 20 (Short Farm), Cape Gírardeau County, southeastern Míssouri. Díscussion.-Additíona1 materÍal v/as not found during the present study. Thís specimen was oríginally assígne d to Bodophyllum because ít has a so1íd axial structure in early stages, and a prominent dÍlated median septal l-amella in intermedíate stages (Elias, 1982, p. 78). However, it was noted that, unlike B. shorti, other species of the genus have a dense to so1íd axial structure ín late stages as wel1. It is possíble that this coral represents â genus ín the

Subfamily Strep telasmatinae. The sírnilaríty to Grewingkia sp. A v/as discussed under the latter taxon. 151

Suborder MONACANTHINA Neuman, 1984

Farníly LAMBELASMATIDAI l,Ieyer, I97 3

Subf arnily COELOSTYLINAE l{eyer, I973

Genus Keelogþ¿llgm n. gen.

Derivation of name.-The generíc name refers to the landowner after whom the Keel Format ion was named by Maxwell (1936, p. 50).

Type and onl¿ specåes .---l(eelophy llum oklahomense n. sp., Keel Formation (uppermost Ordovician; Gamachian), south-central Oklahoma. Díagnosis.--Solitary, ceratoid to Ërochoid, cardinal side convex. Septa monacanthine, imperforate, radially arranged. Minor septa very 1ong. Axial structure of moderate size and complexíty. Tabulae numerous. Discussion.-Kee lophyl1uq n. gen. is included in the Suborder

Monacanthina Neuman, 1984 because of its monacanthine mícrostructure.

Placement within the Famify LambelasmatÍdae l^Ieyer, I973 ís justified by the ceratoíd to trochoid growth form, and lack of díssepiments (refer to Neuman, 1984, p. 125; Elias, ín press). Thís famíly was orígínally intended to include corals with porous sepÈa (I^ieyer, L973, p. 33). However, the presence of perforations requires verifícatíon rll lllvo L vr Lltg Irru¿uuuu óLr¡L!q \uçe rr¡¿r t L¿ vL, rr'

Keelophylluqr rnay be related to the Neotryplasmatidae Elias, in press. ItS septal arrangement, axial structure., and long minor septa are símilar to Neotrypl4sma Ka1jo, 1957, but it differs in having imperforate septa and lackíng dissep íments. Neot lasma is knov¡n from the upper Middle and Upper Ordovician of the U.S.S.R.' and the Upper Ordovícian of the Estonian S.S.R. and Texas. 152

The subfarnilies of Laurbelasmatidae were revíewed by Neuman (1984, p. I25) . Keelophv1lum is placed wíthin the Coelostylínae trIeyer, 1973 because of íts long, radially arranged septa, convex cardinal síde, and tabulae. The very long mínor sep ta ín Keelophv11um distinguísh it from all other members of the subfarnily. The only other coelosty lins wíth axía1 structures are Coelos 1is Lindström 1n

Angelín and Lindström, 1880 from the Middle Ordovician of Scandínavia, and Rectígrewingkia Ka1 jo, 1961 from the Upper Ordovician of the Estonian S.S.R. Keelophyllum díffers from them ín having well developed tabulae. 153

Keelophyllum oklahomense n. sP. Plate 7, fígures 1-16

Derivatíon of name.-The specifíc name refers to the state ín whích the specimens \¡Iere found

Holotype.-USNM 23-3-33, interval 23-3, EM co1l., Section 23 (Lawrence Quarry), PonËotoc Cotrnty, Oklahoma.

EMI'I 23-3-19, ParatYpes .-USNM 23-3-2 interval 23-3, co11. ' usNM 23-3-30, inÈerval 23-3, USNM ?3a-1-1, EM co11., Sectíon 23 (Lawrence Quarry), Pontotoc County, Oklahoma; USNM 25-l-2, interval 25-1' El'ß'f col1., Section 25 (Hunton), Coal County' Oklahona.

Occurrence. Ordovícian (GamachÍan) : Keel Formation, -Uppermost south- central 0k1ahoma. Díagnosíq.-Septa nondilated, taper axíal1y' some with smal1' Írregular carínae; ín lateral contact at períphery to form moderately thick stereozone. Cardinal septum and fossula inconspicuous. Minor septa more than two-thirds the length of major septa. Axial structure in late stages consists of septal lobes plus numerous palíform to long and contor¡ed septal lamellae thaE can be thickened by sclerenchyme; occupies about one third of coral radius. Tabulae convex upward ín septal regíon, generally with upturned peripheral edges; slightly concave Èo greatly convex upward in axial regíon.

Descriptíon of corals.-{he greatesE observed length and díameter are 50 mm and 21 rnm, respectively (USNI'I 23-3-2, apex and calice incomplete). The corals are generally trochoid (USNM 23-3-33, 33-3-30,2 índividuals in 23a-1-1; P1. 7, fig. 7) and curved (USNM 23-3-2, 23a-1-l , but can be ceratoid (USNM 23-3-2, 23-3-19, 25-I-2; rs4

P1. 7, fig. +) and possibly straiChÈ (USNM 25-1-2 . Septal grooves, interseptal rídges, and rugae äre preserved on mosË specimens. One corallum that is epízoíc on a halysitid colonial coral has two smal1 índividuals attached to ítself (Pl. 7, fígs. 1-3). They are probably also epizoans, because there ís no evidence to suggest an origin as offsets. Attachment by the cardinal sÍde can be confírmed in the large coral and ín the uppermost epízoan. Another specímen has a sharp bend and possibly an attachment sÈrucËure at Ëhe apex (P1. 7, fig. 7). Depth of the calíce could not. be established accurately, but is 1ike1y less than 30 percent of the coral length. A low calícular boss ís formed by elements comprisíng the axial strLrctlrre.

Ontoseny and internal structures.--{he relatíonshi p between number of septa and coral diameter is shov¡n in Text-fig. 25. In early (P1. 7, figs. 1, 11) to early intermedíate ontogenetic stages (Pl. 7, figs. 2, 12), the major septa extend Èo or almost to the axis, where they meet in groups that are commonly enclosed ín sclerenchyme. During late ínterrnedíate (Pl. 7, fígs. 5, 14) Ëo late stages (Pl.

7, fígs. 3, 6, 13, 15), che major sepEa r.¡íthdrarv frorn the axis, and an axial structure develops. It compríses septal lobes plus numerous paliform to long and contorted septal lamellae that can be thíckened by sclerenchyme, and occupies about 30 percenÈ of the coral radius in late stages. The major septa are curved and somewhat írregularly oriented in early stages, buË become straight and radíally arranged in later sÈages. They are nondilated throughout ontogeny, but are thick

ín the stereozone and taper axially. Srnall, irregular carinae can be p res en t. The cardinal septum ís índistínct, but ís slightly thícker than 155

Text-figure Z1.---Relationship between number of major septa and coral diameter in Keelophyllum oklahomense. Numbers beside data points indícate frequencies greater than one. Data from Appendix 2 t56

oo a a 3a a a 30 a o fL lIJ U) îÍ. .?o 20 o I

o olJ. tÍ. 1 0 [rJ fn 14 cross sections from 6 corals zD o 5 10 15 20 DIAMETER (mm) r57 the other major septa ín one indívidual (USNM 25-I-2). The cardínal fossula is ínconspicuous. Minor septa are about two-Ëhírds as long as the major sepËa in early stages, and can be contraclíned to contratingenÈ. By late stages, Èhey can exËend to 95 percent of the length of rnajor septa; very few are contraclined' and none are contratíngent. The rninor septa extend beyond Ëhe stereozone. Thickness of the stereozone decreases duríng ontogeny, from 25 percent of the coral radius in early stages to 15 percent ín late stages.

The compleËe and íncompleÈe tabulae are convex upward in the septal region, and commonly have upturned peripheral edges (P1' 7, figs' 4' 8-10). In the axial region, they are slíghtly concave upward to greatly convex upward. The close spacÍng of Labulae within the cardinal fossula in one transverse section suggesËs that they are depressed wíthin that structure (Pl. 7, fíg. 14)' Mícrostructure.-It is established from t.ransverse and longitudinal thin sectíons that the septa are monacanthíne and imperforate. Monacanths are inclíned from the periphery of the coral towarci the axis at an angie of abo¡-¡i 40,jeg::ees, and Ëhe edges cf septa can be acanthine (P1. 7, fig. 4). In the stereozone, adjacent septa are expanded into lateral conËact along a contorted suture (Pl. 7, fig. 16). Discussion.--{he monacanthine, radially arranged sepËa of

Keelophyllum oklahomense n. sp. are uníque among the species described helein. The relatíonship to other Laxa \.Ias díscussed under the genus' 158

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Rubey, I^I .l^I . 1952, Geology and mineral resources of the Hardin and Brussels quadrangles. United States Geologícal Survey, Professional Paper 218, 179 pp. Satterfíe1d, I.R.

I97I Conodonts and stratígraphy of the Girardeau Límestone (r\*Åattini.r-\ \vruvv¡urerr/ nf cnrrrþsasÈ Missourí and south\desf IilÍnois. Journal of Paleontology, vo1. 45' pp. 265-273. Savage, T.E. i906 Geology of Jackson County, pp. 563-648 in Annual Report,

Iowa Geological Survey, vo1. 16,

1908a On the lower Paleozoíc stratigraphy of southwestern I11ínoís. American Journal of Science, vol. 25, pp. 43L-443.

f90Bb Lor¿er Paleozoic stratígraphy of southwestern lllínois'

pp. 103-116 ín T11ínois SÈaÈe Geological Survey, Bul1etÍn

No. B 173

1909 Ordovícian and Sil-urían formatíons ín Alexander County, I1linois. American Journal of Science, vo1. 28' pp.

509-5 i9 .

19 10 Faunal successíon and correlatíon of the pre-Devonian formations of southern lllinois. Illinoís State

Geological Survey, Bulletin 16, pp. 302-341.

7912 Ihe Channahon and Essex límesËones ín Il1ínois. Illinois

Academy of Scíence, Trans¿ctíons (1911), vo1. 4, pp. 97-103.

19 13a Al-exandrian Series in Missourí and Illínois. Geological Society of America, Bu11etin, vol. 24, PP. 351-376-

19 13b StraLígraphy aLrcl paleotrtology of the Alexandrian Seríes ín Illínoís and Missouri, Part one. Extract from Bulletín 23, Illinois State Geologíeal Survey, 124 pp.

L914 Relatíons of the Alexandrían Seríes ín Illinoís and Missouri to the Silurían section of lowa. American Journal of Science, vo1. 38, pp. 28-37.

t916 Alexandrian rocks of northeastern Illínois and eastern

tr^Iísconsin. Geological Socíety oi ^A,urericq Bu11eiín, vo1. 27, pp. 305-324.

19 T7 Stratigraphy and paleontology of the Alexandrían Series in Illinoís and Missourí, Part one. Illinois State Geological Survey, Bulletin 23, pp. 67-160.

t926 Silurían rocks of Illinoís. Geological Society of Ameríca, Bu11etin, vo1. 37, pp. 513-533.

Savage, T.E ., and Ross, C.S

T9T6 Age of the Íron ore ín eastern trrlísconsín. American Journal of Scíence, vo1. 4I, pp. 187-193. 174

Scheffen, Irtr. 1933 Die Zoantharía rugosa des silurs auf Ríngerike ím OslogebeiÈ. Norske Videnskaps-Akademí, Oslo, utgítt 1, MathemaEisk-naturvídenskabelig Klasse,

Schrífter, vol. 2, No. 5, 63 PP.

Scobey, E.H

1938 The Alexandrían Series in lowa. Journal of Geology' vol. 46, pp. 207-217.

Shaw, J.

LB73a Geology of northwestern Illinois, PP. I-24, Geology of Jo Daveiss County, pp. 25"56, Ceology of Stephenson County, Pp. 57-74, Geology of Carroll County' pp. 75-81' Geology of I'rlhitesíde County, pp. L4O-166 in Geologícal Survey of Illinois, vo1. 5, Geology and Palaeontology.

1873b Geology of Boone County, pp. 95-103 in Geologícal Survey of Illínois, vo1. 5, Geology and Palaeontology.

Shumard, B.F.

L! !L^ rt.: D'i*'^- f Q+ I()lJ\tgul-UBI(jaJ-SC(-LIUIIUITLIIEiI!ÞÞrÞÞryPtr\rve!!rv¡rrv!'-r --1 -^' ^^:^^4 ^^-í -^-

Louis to Commercer PP. 139-208 ín Míssouri Geologícal Survey, lst and 2nd Annual Reports, part 2.

1873 Cape Gírardeau County, PP. 258-27 6 in Reports on the Geological Survey of the State of Míssouri, 1855-1871.

Strídsberg, S. 1980 Sedímentology of Upper Ordovícían regressíve strata in Västergötland' Geologíska Föreníngens í Stockholn Förhandlingar, vo1. lO2, pp. 213-22L.

SutËon, A.H. 175

1935 Stratígraphy of the Sílurian System of the upper Míssissippí valley, pp. 268-280 ín Kansas Geologícal Society Guídebook, 9th Annual Field Conference.

Swallow, G. C. 1855 Chapter 1, Geology of Missouri, pp. 59-L7O ín Missouri Geological Survey, lst and 2nd Annual Report'

Sweet, W.C.

1983 Upper Bromide Formatíon and Viola Group (Middle and Upper Ordovícían) in eastern Oklahoma, Part II - conodont

biosËratigraphy of Fíte Formatíon and Viola Group: PP'

23-35 in Oklahoma Geological Survey, Bullettn 132 ' Taff, J.A. Igo4 Prelímínary report on the geology of the Arbuckle and I^Iichíta mountains in Indian Terrítory and Oklahoma' Uníted States Geologíca1 Survey, Professional Paper

3I ' 111 PP. Templeton, J.S., and Willnan, H-8.

qÁ I ? chnmnlv^¡u¡uF +u+ ¡í ni¡¡ an Seri as (t'lid¿le Ordovician) in Illinois . I11ínoís State Geologícal Survey, Bulletin 89, 260 pp'

Thompson, T.L., and Satterfield' I.R. lg75 stratígraphy and conodont biostratigraphy of strata contíguous to the ordovícian-silurian boundary ín eastern Míssourír pp. 61-108 ín Ì{issouri Geologícal Survey, Report

of InvestÍgations No. 57, I72 PP,

Trapp, H., Jr Missourí' 19 50 The Noix oolite of Pike County, Missouri' l"1.Sc. thesís, Washíngton Uníversíty' St' Louís' 176

Verrill, A E.

1 865 Classification of polyps (Extract condensed from a synopsís of the polypí of the North Pacífíc Exploring Expedition, under captaíns Rínggold and Rodgers, U.S.N.)

Essex InstíËute, Proceedings, vo1. 4, pp. 145-149.

Votaw, R. B , and Kolata, D.R.

1981 Prelimínary lithostratigaphy and bíostraÈígraphy of the

Maquoketa Group (Upper Ordovician), northern Il1inois.

Geologícal Socíety of America, Abstracts with Programs,

vo1. 13, p. 320.

I,letlekír-rd, R.

L927 Die Zoantharia Rugosa von Gotland (besonders NordgoÈland):

Nebst Bemurkungen zur Biostrat,ígraphie des Gotlandium. Sveríges Geologíska Undersökníng, series Ca, No. 19, 94 pp. trrle11er, J l.l .

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Kansas Geoiogícai Socíety, Gui<Íebook, 9ih Annual Fiei

Conference. hle1ler, J M., and Ekblaw, G.E.

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InIhíÈney, J.D.

1866 Geology of Lhe lead regíon, pp. 153-207 ín Geological Survey of lllinois, vol. I, Geology.

I^lí11man, H. B.

1962 The Silurian strata of northeastern Illinois, PP. 6L-67, Description of stops, second day, pp. 8I-96 ín Sílurían rocks of the southern Lake Michigan area. Michigan Basin Geological Society, Annual Field Conference, Illinois

State Geological Survey, Reprínt L962-l'1, I973 Rock stratígraphy of the Silurian System ín northeastern and northwestern Il1ínois. I11ínois State Geological Survey, Círcular 479, 55 pp.

Tli 1 1--- lI D !L^-!^- n wIl-l-ltl¿ttt, ft.rj)., dtrLl^-J trLrrc!^ LLJLlr !. 1975 Silurian System, pp. 87-104 in Handbook of lllÍnois Stratigraphy. Illinois SLate Geologícal Survey, Bulletin

95.

I,trillman, H. B. , and Buschbach, T. C . L975 Ordovicían System, pp. 47-87 in Handbook of Illinois Stratigraphy. Ill-ínoís StaÈe Geological Survey, BulletÍn

95.

Wilson, A.C. 1895 The Upper Sílurían ín northeastern Iowa. Amerícan 178

Geologist, vol. 16, PP. 275-28I. Wínchell, N.H., and Schuchert, C. 1895 Sponges, graptolítes, and corals from the Lower Sí1urían of Mínnesota, Chapter 3, pp. 55-95 in The Geology of Mínnesota, vol. 3, No. 1, Paleontology. MÍnnesota Geological and Natural History Survey.

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1868a Geology of Alexander County, pp. 20-32, Geology of Union County, pp. 33^57 in Geologícal Survey of lllínoís' vol, 3, Geology and PalaeontologY.

1868b Geology of Jersey County, pp. 104-12L in Geologícal Survey of lllinois, vo1. 3, Geology and Palaeontology. 1870 Geology of Calhoun County, pp. L-23, Geology of Pike County, pp. 24-42 in Geological Survey of l11ínoís, vol' 4, Geology and PalaeontologY.

1 Òtr ñ--^-1-^ +L^ +-i-,^ +La NIi ocara ¡nrì tlro LO I L 1lÞ (/lr^- Lllc -^1t ç14 ^ Lav s oóL^^^ ^çvr ulle rr ¿s6q ^gllldl so-called Lower Helderberg groups. Amerícan Associat.ion

for the Advancement of Science, vol. 19, pp - I72-I75. 179

PLATES

Exteríor vier¡s are of specimens coated r,ríth ammoníum chlorlde.

Transverse and longitudínal sections (except photomicrograph) were prepared usíng thín sections as negatives ín a photographic enlarger. Transverse sections are oriented as they appear looking dovrn from the calice towards the apex of the coral, wíth the cardinal side facing

Ëhe bottom of the page, unless otherwíse noted. Longítudinal sections are oriented wíth the calícal end facing the top of the page. Dashes wíth figure numbers beside exterj.or views and longitudínal sections índícate posítion of transverse sections. 180

E)PLANATION OF PLATE 1

Figure Page

1-28. Streptelasma subregulare (Savage, 1913b) 96

(1-4, Schweizer Ìr{br. , I^Ií1he1mi Fm., Channahon, Wí11 Co., Illínois; 5-8, Schweizer Mbr., I,trílhelmí fTn., southeast of Channahon, I¡Iill Co., I1linoís; 9, 10, Birds Mbr., Wilhelmi

Fm., Sectíon 3 (Garden Prairie), McHenry Co., Illínoís; 11, 12, Cyrene Fm., Section 13.(Bowling Green), Pike Co., Mi-ssouri;

13-16, Kíssenger Limestone Mbr., Bryant Knob Fm., Section 14 (Híggínbotham Farm), Píke Co., Míssouri; 17, Kissenger Limestone Mbr., Bryant l(nob Fm., Section 15 (Calumet), Pike

Co., Míssourí; 1B-25, Kíssenger Límestone llfbr., Bryant Knob Fm., Section 16 (Clinton Spring), Pike Co., Missouri; 26-28,

Kíssenger Limestone ¡fbr., Bryant Knob Fm., Section 17

(Clarksví1le), Pike Co., Missouri) .

I-4, UI C1560a; 1, exterior cardinal víevr, x 1; 2-L, transverse sectíons, x 2.5.

E O rrr tr :' 1 . J-o¡ ur ^tto1-.rJl )()L.t; ), exLef.^--!' -- IUI'-- carcr]_nal--,-r. vl_gvJ, x I; 6-q, transverse sectíons, x 1.5.

9, I0. USNM 3-3-30; interval 3-3; transverse sectÍons, x2.

11, 12. USNM 13-1-2; ínterval i3-1; transverse sections, x2.

13-15. USNM I4-L-2; ínterval 14-1; 13, exteríor alar view, cardínal side to ríght, x I L4, 15,

transverse secËions, x 2.25 . lBt

16. USNM 14-1-13; ínterval 14-1; transverse section, x 2.25.

I7, USNM 15-1-15; interval 15-1; transverse section, x 1.5.

18-22. USNM 16-1-5; interval 16-1; 18, 19, longitudína1 sections, cardinal síde unkno\{n, x 3; ?0-4., Ëransverse sectíons, cardinal side unknown, x 3.

23-25. USNM 16-I-29; interval 16-I; transverse seclions, x 2.

26-28. usNM i7-0-10; interval 17-O; longitudinal sectíons, cardinal side to left, x 2.5 t82 PL. 1

-,j 6:

' .,'a!:,; 183

E)PLANATION OF PLATE 2

Figure Page I-22. Strep telasma subre are (Savage,1913b) 96 (1-5rKj.ssenger Límestone Mbr., Bryant Knob Fm., Sectíon 17 (Clarksvílle), Pike Co., Missourí; 6'12, Kissenger

Límestone Mbr., Bryant Knob Fm., Sectíon 18 (Kíssenger) ,

Pike Co., Míssouri; 13-18, Leemon Formation, Section 19

(New Wells), Cape Girardeau Co., Missouri; 19-22, Leemon

(Short Co. Formation, Section 20 Farm), Cape Girardeau '

Missouri) .

1-5. USNM 17-0-6; interval 17-0i I, 2' longitudinal sections, cardinal side to left'

x 2.5; _1-å' transverse sections, x 2.5. 6. USNU 18-2-15; interval I8-2; transverse section, x 1.5.

7-72. USNM 18-3-17; interval 18-3 Z-2, longitudinal sections, cardinal side to ríght'

ô ôE - 1^ 1â I ,)( X-- Z, L); Jyj Ll-dtlUvsIÞs ticL;LluIlÞ,^^+-l ^-^ -- L' L)' !_4.¡ ^

13. USNM 19-3-L2a; ínterval 19-3; exterior víew, cardinal side unknown, x 2'5'

14, 15. USNM 19-1-4; ínterval I9-I; transverse sections, x 1.5.

16-18. USNM 19-1-15; interval 19-1; transverse """.rorolr., . I9-2I. USNM 20-1-,3; interval 20-I; transverse secLions , x,2.5.

22. USNM 20-4-1; ínterval 2O-4; transverse section, x 1.5 184 PL. 2

1

1.9t

16 185

E)GLANATION OF PLATE 3

Figure Page

1-10. Streptelasma subregulare (Savage, 19i3b) 96

(1-3, Ideal Quarry Mbr., Keel Fm., Section 21 (Rock

Crossing), Carter Co., Oklahoma;4-7, Ideal Quarry Mbr., Keel Fm., Sectíon 23 (Lawrence Quarry), Pontotoc Co., Oklahoma; 8, Keel Fm., Sect|on 23 (Lawrence Quarry), Pontotoc Co. , Oklahoma; 9, 10, Keel Fm., Section 25 (Hunton), Coal Co., Oklahoma).

1. USNM 21-1-3; inËerval 2I-L; transverse section, x 2.5.

2, 3. USNM 21-Ia-l; ínËerval 2l-la; transverse sections, x 1.5.

4, 5. USNM 23-2-28; ínterval 23-2; transverse sectíons , x 1.5.

6, 7. USNM 23-2-45; interval 23-2; transverse sections , x 1.5.

B. USNM 23-3-25; interval 23-3; Ëransverse

v9vL¡vtI'êôôfi^ñ ¿:v 4.)

9, 10. USNM 25-1-4; intervaL 25-L; transverse sections, x 1.5 II-28. Streptelasma amsdeni n. sp. r22

(IL-25, 28, míddle lamínated ealcilutite unit, Keel Fm.,

Sectíon 24 (Coal Creek), Pontotoc Co., Oklahoma; 26, 27,

lower oölitic unit, Sectíon 24 (Coal Creek), Pontotoc Co.,

Oklahoma) .

11. USM{ 24-2-55; interval 24-2; transverse section,

Èop of bed faces top of page, x 1.5. 186

12, 13. USNM OGS-5; interval- 24-2; transverse sectíons, x 4.5 (paratype).

L4, 15. USñI 24-2-24; interval 24-2; trènsverse sections, x 6 (paratype).

16-23. USNM 24-2-36 ; interval 24-2i 16, exterior

counter víelü, x 1; _lZ--1-9_, longitudinal

secÈions, cardinal síde to right, x 2t 29-23_,

transverse sectíons, x 2.5, x 2.5, x 2, x 2 (holotype).

24, 25. USNM 24-2-17; íntervaL 24-2; transverse

sections, x 1.5 (paratype) .

26, 27. USNM 24-1-1; ínterval 24-I, transverse

sections, x 1.5 (paratype) .

28. USNM OGS_2 ínËerval 24-2; exteríor view,

cardinal side unkno\^7n, x 1 (paratype). tB7 PL" 3

14 ffi

24 188

E)PLANATION OF PLATE 4

Fígure Page

1. StrepÈelasma amsdení n. sP 122 (middle laminated calcilutíte unít, Keel Fm., Section 24 (Coa1 Creek), Pontotoc Co., Oklahoma)"

1. USNM OGS-la b c; ínterval- 24-2; exterior

víew, on bedding plane, x 1.

133 2-I2. Strep telasma leemonense Elias ' !982 (2, Kíssenger Limestone Mbr., Bryant Knob Fn., Sectíon

14 (Hígginbotham Farm), Píke Co., Míssourí; 3-8, Leemon Fm., Section 20 (Short Farm), Cape Girarrleau Co., Missouri; g-I2, Keel Fm., Sectíon 23 (Lawrence Quarry), Pontotoc

Co. , Oklahoma) .

2, USNM 14-1-5c; ínterval 14-1; transverse section, x 2.5.

3-5. USNM 20-1-19; intervaL 2O-1; transverse sections, x 2.5.

Á-8 - ITSNM ?O- !- 1O: i nterr-¡¡l 20- 1 : 6. I onsí tudinal section, cardinal síde to lef t, x 2.5i l-, 8, transverse sections, x 2.5.

9. USNM 23-3-3; inËervaL 23-3; transverse section, x 2.5.

I0-I2. USNM 23-3-ll; inËerval 23-3; 10, exteríor cardinal view, x 1; 11, longítudínal section, cardinal síde to ríght, x 2.5; 12, Ëransverse section, x 2.5. 189

L3-L7. Streptelasma sp. cf. S. leemonense Elias , rgg2 r4l

(Keel Fn. , Sectíon 23 (Lawrence Quarry), Pontotoc Co.,

Oklahoma).

13. USNM 23-3-22; interval 23-3; transverse

sectíon, x 5.

1,4-16. USNM 23-2a-4; interval 23-2a; 14, longitudínal

section, cardínal side unknown, x 2.5; 15, 16, transverse sections, x 2.5.

17. USNM 23a-1-7; interval 23a-L; transverse section, x 2.5. 190

P1" 4

' ..,ir1: :.' '12':-

11,

10

13 14 ffi -15 191

EXPLANATION OF PLATE 5

Figure Page

I-4. Strep telasma leemonense E1ías, 1982 133

(Leemon Fm., Section 20 (Short Farm), Cape Girardeau Co.,

Missouri) .

I-4. USNM 20-3-ta; inËerval 20-3i two offsets (a and b), transverse sections, x 2.5.

5, 6 Streptelasma s p. A 143

(Noix Limestone, Sectíon 15 (Calumet), Píke Co

Missourí) .

5, 6. USNM 15*0,-1; interval 15-0; transverse sections,

cardínal síde unknown, x 10. 192 PL. 5 r93

EPLANATION OF PLATE 6

Figure Page

1-5. Strep telasma SP. A t43 (Noíx LimesËone' Section 15 (Calurnet), Pike Co.' Missourí)

1, 2. USNM 15-0-14; interval 15-0; transverse sections, cardinal síde unknown, x 10.

3-5. USNM 1å-0-lC; interval 15-0; transverse sections, cardínal síde unknown, x 10.

6-10. Grewínekia s p.A r47 (6-9, Kíssenger Lfmestone Mbr., Brya[t Knob Im', Section 14 (Higginbotham Farm), Pike Co., Missouri; 10, Keel Fm.'

Section 23 (Lawrence Quarry), Pontotoc Co., Oklahoma) .

6-9. USNM 14-2-7; interval I4-2; transverse secËions, x 3.

10. USNM 23-3-34; interval 23-3; transverse

sectíon, x 3. t94 ?L. 6

II

i.i';f t, -..4' 195

EXSLANATION OF PLATE 7

Figure Page

1-16. Keelo llurn oklahomense n. gen., n. sp r53 (1-13, Keel Fm., Section 23 (Lawrence Quarry), PonËotoc Co., Oklahoma; 14-16, Keel Fm. , Section 25 (Hunton) , Coal Co., Oklahoma).

1-3. USNM 23a-1-1; interval 23a-I; transverse sectíons, x 5, x 3, x 2.5 (paratype).

4 USNM 23-3-2 inÈerval 23-3; longitudinal sectíon, cardinal side unknohrn, x 2 (paratype).

5, 6. USNM 23-3-19; Ínterval- 2i-1; transve.rse sectíons, x 2.5 (paratyoe).

7-13. USNM 23-3-33; intervaL 23-3; 7, exterior cardinal víew, x 1; g-_19; longítudinal secÈions, cardinal

side not shown, x 2,5; l1-_l_3., transverse sections,

x 5, x 3, x 2.5 (holotype).

74-16. USNM 25-1-2; ínterval 25-1; 14, 15, transverse

seetions - x 2 -\:-- 16^ nneirí-'o nhn¡nmi¡¡nav-^r, ' _==' v5LaPLt (for position see fig. 15), x 20 (paratype). FI ffi

L '1ð. 961 r97

EXPLANATION OF PLATE 8

Figure Page

1-5. Rhegmaphyllqm 47

(1-4, límestone facies at base of Bowling Green Dolomíte, Sectíon 17 (Clarksville), Pike Co., Míssourí; 5, límestone

facies r¡ithin Bowlíng Green Dolomite, Section 17 (Clarksville), Pike Co., Míssouri).

1, 2. USNM 17-1a:4; ínterval I7-l; transverse sections,

x 5.

3, 4. USNM 17-3-5; intervaL I7-3; transverse sectíons, x 5.

5. USNM 17-2b-5; ínterval I7-2b; transverse section,

x 5.

6-11. Dinophyllum 47, 65 (6, llmestone facies within Bowling Green Dolomíte,

Section 17 (Clarksvílle), Píke Co., Missourí; 7-10,

limesÈone facies at base of Bor,¿ling Green Dolomíte, Section

17 (Clarksville), Píke Co., Missourí; 11, Elwood Frn., Section 6 (Plaines tlest), tr{Íll Co., Illínoís).

6. USNM 17-2b-3; ínterval I7-2b; transverse secríon, x3.

7-10. USNM 17-3-1; interval 77-3t 7, B, longírudinal sections, cardinal side to right , x 2; 9r I0, transverse sections, x 2,

11. USNM 6-1-9; interval 6-1, transverse sectíon, x 2.

72-IB. Dalmanophyllum 36, 47, 65, 74

(12, Sexton Creek Limestone, Section 20 (Short Farm), 198

Cape Gírardeau Co., Míssourí; 13, 14, Bowling Green

Dolomite, Section 17 (Clarksvil-le), PÍke Co. , Missouri; 15, L6, límestone facíes at base of Bowlíng Green Dolomíte,

Section 17 (Clarksville), Píke Co. , Missouri; t7, Elwood Fm. , Sectíon 6 (Plaines I^Iest), Will Co. , Illinoisi lB, Mosalem Fm., Sectíon 10 (Lost Mound), Jo Daviess Co.,

I11ínoís ) .

12. UCGM 45639; transverse section, x 2.5.

13, 14. USNM 17-2a-2; inËerval I7-2ai 13, 1-ongitudinal section, cardinal side to right, x 3; 14,

transverse section, x 3.

15, L6. USNM 17-1-10 ínËerval 17-I; transverse sections, x 5.

17. USNM 6-1-5; interval 6-1; transverse sectíon,

x 4.

18. USNM 10-2-5; Ínterval IO-2; Ëransverse section,

x 4.

19-23. Phaulactis . 24, 47, 74

l1O r'^^L--*^ E* Q^^+ia- lf r^ì,,---,'\ D^ñr^r^^ \I/t VULrI!OlIs tl[. t JçLLrvII ¿J'ra \lowlçlluç YusrrJ ), L

Co., Oklahorna; 20-22, Bowling Green Dolornite, Sectíon 17

(Clarksvílle), Píke Co., Míssouri; 23, Mosalem Fm., Section

9 (I^línston) , Jo Davíess Co., Illínoís) .

19. USNM 23-4-1; interval 23-4; transverse

section, x 2.

20-22. USNM I7-2-L; interval I7-2; 20, longitudinal

section, cardinal síde to 1eft, x 2; 2I, 22,

transverse sections, x 2.

23, USNM 9-1-6; interval 9-1; transverse section, x 2.5. 1-Q9 PL. B 200

APPENDIX 1: GROWIH FORM AND CURVATURE tr (trochoid) = ratio of length to diameter <2:L, cer (ceratoíd) = ratio of length to diameter >2:I. cyl (cylíndríca1) = diameter approximately consËant for at least half the coral length. non (noncurved) = 0o to 10o curvature of growth axís" mod (rnoderately curved) = 11o to 70o curvature of growth axís. great (greatly curved) = >70o curvature of growt.h axís.

Note: sharp bends are not considered the same as smooth curvature of the growth axis, and are ignored.

Identical specimen numbers in Appendíx I represent different índividuals catalogued under Èhe same number. --:: GROI^ITH GROI^ITH

SPECIMEN FORM CURVATURE SPECIMEN FORM CURVATURE

S trep telasma sub regulare

UI X-851 tr non UI C1619 tr non

UI C16 19 tr non uI c1619 Ër mod

UI C16 19 tr mod UI C1619 tr mod a a 1a I J-J_.LJ LI -^ulu u 3:3-27 ncfl

3- 3- 30 tr mod UI C1560a cer mod

UI C1560 cer mod UI C1560 tr mod

UI C1560 cer mod UI C1560 tr mod

UI C1560 cer non UI C1563 cer mod ur c1563 tr mod UI Cl5Bla tr mod

UI C1581 tr mod UT CI547 cer mod 201

non UI C1547 cer mod UI C1561 fT non UI C1561 tr non UI C1561 tr

UI C1561 tr mod UI C1561 tr mod

UI C1561 tr non rJT X947 cer mod ur x947 cer great tJr x947 cer mod

UT X926a tr non UI X926b tr mod

4-t-r cer mod 4-r-2 tr mod 4-1-3 tr mod 4-r-4 tr mod 4-L-5 tr non 4-r-6 cer mod

mod UI CB64 tr non 13-r-2 tr

13-1-3 tr mod 14-l-2 cer mod

mod 14- 1- 3 cer mod 14-r-4 cer

14- r-7 cer mod 14- 1- I cer 14-r-9 tr great 14- 1- 10 cer mod

14-1-11 tr 14-L-12 cer

14- 1- 13 cer mod t4-r-14 cer mod

1¿-1-tq mod, 14-T-16 cer

t4-r-17 cer mod 14_I_T9 cer mod 14-r-20 tr non 14-l-22 cer non

t4- r-24 cer mod t4-I-26 cer mod

L4- L-27 cer mod I4-T-28 tr non non 14- 1- 30 cer mod 15-1-1 cer

15-r-2 cer mod 15-1-3 tr mod

L5- 7- 4 tr nort 15- 1-5 tr non

15- 1- I I tr non 1s-1-13 cer mod

15- 1- 14 tr mod 15- 1- 15 tr non 202

15-1-16 tr non 15-1-19 tr non i5-1-20 tr mod 2rb-2-3 cer non 27b-2-4 cer non ztb-2-B tr mod IG1-1 cer non

T6J T_2 tr mod 16-1-3 cer mod

16-r-4 cer non I6-1-5 cer non

16- 1-6 cer non 16-I-7 cer non

16- 1- 8a cer non 16- 1- 8b cer mod

16-t-9 cer mod 16- 1- 10 cer non

16-1-11 tr mod 16-r-1.2 cer

16-1-13 cer non 16-7-14 cer mod

16- r- 77 Ër non 16- 1- 19 cer non

16-r-20 cer non 16_T_27 cer fron

16-I-22 tr non 16-r-23 cer non

16- r-25 cer great 16-r-26 cer mod

16-r-27 cer mod T6_I_28 cer mod

16-7-29 tr mod 16- 1- 30 cer mod

16-1-31 ceI non 16- 1- 33 cer mod

16- 1- 35 cer mod 16- 1- 36 cer mod r6-1-37 cer non IO-I-Jö tr IIIU O

16- 1-40 cer non 16-1-4r cer mod

16-L-4s tr non 16-t-46 cer great

16-1-47 cer great

I 7-0- 1 cer mod 77-O-2 tr non

I 7-0- 3 cer non r7-0- 4 cer great

1 7-0-5 cer mod t7-0-6 cer mod

17-o-7 cer mod 1 7-O-8 tr great 203

t7-0-9 cer mod 1 7-0- 10 cer mod

17-0-11 cer non r7-o-12 cer great

17-0-13 cer 17-0-14 tr mod

17-0- 15 cer non 17-a-r6 cer mod t7-0-17 cer non 17-0-18 cer mod

L7-0-19 tr non 17-0-20 cer non t7-0-2r cer non 17-o-22 cer mod

T7-0-23 cer mod 17-o-2s cer norr

17-0-27 cer 17-o-29 TT mod

17-0-3r tr non 17-O-32 cer mod

I 7-0- 33 cer mod 17-o-34 cer

17-0-36 cer non 17-0-37 cer non

17-O-39 cyl non 18-1-14 cer great

1B- 1- 19 cer non 1B- 1-2 B cer mod

18-2-3 cer mod 1B-2-5 cer non

18-2-7 cer non 1B-2-10 cer mod

18-2-i1 tr mod i8-2-13 tr mod

LB_2_ T6 tr mod I8-2-19 Lr mod

18-3- 1 tr non 18-3-2 tr non

1 B- 3-4 cer mod l"B-3-9 cer mod

1B-3-10 tr non 18-3-15 cer non

18-3-16 fr mod 1B-3-17 cer mod

18-3-19 cer mod 18-3-21 tr mod

18-3-22 tr mod 1 B-4- 1 cer non

UCGM 45618 tr non UCGM 45619 fr non ucclf 45620 cer non ucc't"I 4562I cer mod 204

cer non tJcGþ1 45622 tr non UCGM 45623

UCCl"t 4562s tr mod UCGM 45624 tr mod tr mod uc?tl, 45626 cer non UCGM 4s627

UCG}I 4s629 tr mod UCGM 45628 tr non

UCGM 4s6 33 cer non UCGM 45630 cer mod

UCGM 45634 cyl non cer non USNM 365918 cer non 19-r-2 19-L-4 tr mod 19- 1- 3 cer non 19- 1-6 cer non 19- 1-5 cer mod cer flon 19--1-7 cer non 19- 1- B tr non L9- r-9 tr mod 19-1-10 tr mod r9-1-11 tr great 19-I_L2 cer non 19-1-13 tr mod t9-r-L4 cer mod 19- 1- 15 tr non I9-2-r cer non L9-2-2 fr great t9-2-3 cer mod 19-2-4 cer mod 19-2-5 mod t9-2-6 cer non L9-2-7 cer tr mod 19-2-9 cer mod 19-2-ro cer mod 19-2-17 cer non 19-2-12 cer non t9-2-13 tr non 19-2-r4 cer non 19-2-15 cer mod 19-2-16 non L9-2-17 cer non L9-2-18 tr cer mod 19-2-19 cer non L9-2-20 cer non 19-2-22 cer non 19-2-23 19-3-2 tr mod 19- 3- 1 tr great tr non 19- 3- 3 cer mod 19-3-4 cer mod L9-3-5 cy1 mod 19- 3-6 205

t9-3-7 cer non 19- 3- 8 cer non

19- 3-9 cer mod 19- 3- 10 cer great

19-3-11 cer mod 19-3-12 cer non

19-3-i3 cer 19-3- 14 cer mod

19- 3- 15 cer mod 19- 3- 16 cer mod

19-3- L7 cer non 19- 3- 18 cyl great

19- 3- 19 cer mod 19-3-20 cer mod

19-3-2r cer non 19-3-23 cer non t9-3-24 tr non 19-3-25 cer mod

19-3-26 cer non 19-3-27 cer mod

19-3-28 cer non 19-3-29 cer mod

19- 3- 30 cer mod 19-3-32 cer mod

19- 3- 33 cer non 19-3-34 cer non

19- 3- 35 cer mod 19- 3- 36 cer mod

19- 3- 39 L.]r mod 19- 3-40 tr mod

79-3-4r tr non 19-3-42 cer mod

20- 1- 1 cer mod

20-L-2 tr great 20-t-3 fr great

20-r-4 cer mod 20-r-5 tr non

20- I-7 tr non ¿u- L- ó cer mod 20-r-9 cer 20-1-11 cer non

20-r-12 tr mod 20-1-t4 tr mod

20- 1- 18 tr non 20-3-2 tr mod

20-3-3 tr mod 20-3-4 fr mod

20-3-6 tr mod 20-3-7 tr mod

mod 20- 3- B tr mod 20-4-l tr 206

20-5-2 tr mod 20-5-3 tr non

20-5-5 tr mod 20-5-B cer mod

UI ENT-.I tr non UI ENT-2 tr 2I-Ia-I tr non 2I-Ia-4 tr mod

21- lb- I tr non 21-lb-B cer mod

2I-Lc-3 tr mod 23-1-I cer mod 23-2-I cer non 23-2-2 tr non

23-2-3 tT non 23-2-4 tr mod

23-2-5 tr mod 23-2-6 tr mod

23-2-7 tr non 23-2-B tr great

23-2-9 cer mod 23-2-lo tr great

23-2-Lr tr mod 23-2-13 Ër non

23-2-14 tr non 23-2-15 cer mod

23-2-16 Ër non 23-2-17 tr mod

23-2-20 tr mod 23-2-2r tr non

23-2-22 tr mod 23-2-23 cer mod

23-2-24 tr non 23-2-26 cer non 23-2-3r cer non 23-2-33 tr non 23-2-38 tr non 23-2-39 tr mod

zJ- z- +vt^ tr 23-2-4Ia tr non

23-2-4rb tr mod 23-2-42 cer mod

23-2-43 cer mod 23-2-45 tr mod

23-2-47 tr non 23-2-48 cer non

23-2-49 ET non 23-2-55 tr non 23-2a-I tr non 23-2a-3 tr mod

23-2a-5 tr mod 23-3-9 tr mod 207

23-3-14 tr mod 23-3-15 tr non

23-3-16 cer mod 23-3-17 tr non

23-3-18 tr mod 23-3-21 tr non

23-3-24 tr mod 23-3-25 tr non

23-3-27 tr mod 23-3-28 tr non

23-3-3r Ër mod 23-3-35 tr non

23-3-37 tr great 23a-I-B tr mod

25-r-I tr mod 25-I-3 tr floll

25-L-4 tr non

StrepLelasuta amsdení

OGS- la cy1 non ocs- lb cy1 non non OGS- 1 c cyl mod OGS- 2 cy1

OGS- 3 cer non OGS-6 cy1 non

mod OGS_ 7 cyl OGS- B cer

OGS-9 ceI ocs- 10 cer mod

mod ocs- I 3 cy1 non 24-L-r cy1

24-2-i cer moo ¿.+- ¿- J u-y f ttvll

24-2-4 cyl mod 24-2-5 cer rron

24-2-6 cer non 24-2-7 cer non

., 24-2-B cy1 non l,_.r-o cy1 mod

24-2-70 cer non 24-2-lr cy1 mod

24-2-12 cer non 24-2-13 cer mod

24-2-r4 cer mod 24-2-15 cer mod

24-2-16 cy1 non 24-2-17 cyl non

24-2-78 cer mod 24-2-19 cer mod

24-2-22 cer mod 24-2-23 cy1 non 208

24-2-24 cer mod 24-2-26 cy1 mod

24-2-27 cer mod 24-2-28 cy1 mod

24-2-29 cer mod 24-2-30 cyl non

24-2-31 cer non 24-2-33 cyl non

24-2-34 cer mod 24-2-35 cyl nofl

24-2-36 cer great 24-2-38 cer mod

24-2-40 cer mod 24-2-42 cy1 non

24-2-44 cer non

S trep telasma leemonens e

14-r-5 tr mod 15- 1- B tr mod

mod 20- 1- 10 cer non 20-r-L9 tr

20-3-7 tr mod UI C1448 tr non

23-2-32 tr mod 23-2-36 tr mod

23-2a-2 cer non 23-3-1 cer non

23-3-3 cyl non 23-3-4 cer non cyl mod 2 3- 3-B tr mod 23-3-11

'23- Iuu uJ r?-?.-1? cer mod, 5- L J cer -^

23-3-20 cer noïì 23a-I-2 cer mod

23a-I-3 cer mod

Streptelasma sP. cf. S leemonense

23-3-22 cer mod 23a-l-l tr non

Keelophylh¡n oklahomense

23-3-2 cer non 23-3-19 cer non 23-3-33 cer great 23a-l-I tr mod 25-t-2 cer non 209

APPENDIX 2: BIOMETRIC DATA n= nuilber of major sePLa. d= coral diameter, ín nm. l= length of major septa, as a fractÍon of the coral radius. l^7 = width of major septa at nidpoint of lengÈh, in mm. c1 = length of cardinal septum, as be1ow.

CIÀ7 = width of cardinal sepÈum, as belor^r. NoËe: 1 = less than other major septa. s = same as other major septa. g = greater than other major sePta.

SPECIMEN n d 1 T¡7 c1 cw

S trep tela sma subr are

3-2-11 2T 6 63 .30

3-2-12 27 I 89 .35

3-3-13 34 T2 .50 .20 S Þ

3- 3- 15 27 7 .93 .30

3- 3- 16 10 .60 .25 S

J-a J_a L+al, 1'1 1t E,L /,c ê S

3-3-27 T4 79 .35 S 1

3- 3- 30 2B B 1.00 .45 S 6

39 13 69 .45 s 6

UI C1560a 28 7 .50 .15 Þo S

30 10 .60 .20 g 1

37 13 54 .20 s S 2IO

UI C1581a 34 10 i. 00 .60 c S û o 41 15 80 .55 b ö

44 22 .50 1 I

o 4-r-2 26 7 .7r .20 Þ S

30 9 .61 .15 S S

4-L-3 35 I7

4-r-4 24 7

4-r-5 39 1B .67 .30 S 1

i3-1-1 27 7 .79 .40 ó S

13-r-2 22 I .94 .45 S S

33 15 .80 .25 1 I

13- 1-3 23 5 1.00 .25

35 13 .73 .60 1 1

13- 7-4 24 5 .70 .40

o 13-1-5 IB 4 I .00 .20 S Þ

14-r-2 24 7 1 .00 .50 e s

36 15 .53 .75 S 1

36 19 .42 .20 1 I

t4- r-3 32 T4 .39 .80 1 1

14- r-4 32 10 .65 .55 s S

37 T6 .69 .40 1

t4- r-7 31 11 .73 .70 S S

0 14- 1-B 37 9 .89 .15 S Ò

3B L2 .79 .15 c S

39 t7 .62 .15 S 2L7

14-r-9 23 8 1 .00 .40 S S

34 15 .80 .40 I S

14-1-11 33 1B .50 .65 S 1

L4-r-72 34 13 .85 .45 S I

14- 1- 13 37 T7 .62 .50 s S t4-t-14 30 11 .50 .70

14- 1- 15 3 I .00 S

5 .80 .35 S S

8 .63 .55 S S

L4_ T_ T7 72 .7r .55

14- 1- 18 28 I I .00 .50 s 6

14- 1- 19 33 10 .75 .50 S S

t4-t-20 7 .70 .50

14-t-22 32 8 .62 .50 S S

14-r-23 31 I4 .96 :60

14-1-26 27 11 .68 .35 S S

14-7-28 I 1. 00 .40 S S

14- 1- 30 20 4 .75 .2Ù b 6

33 9 .61 .65 S S

/,) 1^ .56 .50 ó S

15- 1- I i9 4 .87 .40 S S

30 t2 .58 .60

15- 1- 3 28 9 .89 .40 S S

û 15- 1-4 25 6 1 .00 .30 S Þ

15- 1-6 24 6 1.00 .30 s S

15- t-7 34 t1 212

15- 1-9 37 I2 1.00 .50 S 1

15- 1- 1 1 23 7 1.00 .50

15- 1- 14 29 9 1.00 .70 S s i5- 1- 15 24 6 .83 .50 s S

38 16 .72 .75 1 I

15-1-18 7 .71 .50

o 15- 1- 19 24 6 .83 .40 Þ S

15- 1-40 20 4 ,87 .35 S S uccvr, 45644 36 15 .97 .40 S 1

2Ib-2-3 2T 5 1 .00 .4s S S

24 8 1 .00 .55 1 1

21b-2-4 3 1. 00 .45

22 6 1.00 .15 S S

10 .50 1 S

2tb-2-8 30 9 .89 .60

34 T2 .67 .70

ot S 16- 1- 1 20 6 .50 S

11 .73 .4s i S

16-L-2 4 .50 .45

1^_1_1 33 9 .94 .45 S S

16-L-4 13 2 1.00 .20 S S

o 28 B .94 .50 Þ 6

37 L2 o, .75 S S

16- 1-5 13 3 .83 .40

22 5 .40 .50

32 8 .56 .65

L2 .75 .75 213

16-r-6 36 I7 .4r .15 s

16-r-9 18 6 1.00 .40 S S

25 8 1 .00 .35 g 1

16- 1- 10 44 16 .44 .50 s S

16- 1- 1 1 9 1.00 .65

T6-T-17 I .88 .50 s S

34 13 .50 .25 s I

16-1-19 27 I 1.00 .40 S S

30 T2 1.00 .35 S S t6-L-22 23 6 .75 .30 S S

1,6 .44 .65 S 1

t6-r-25 37 I2 .83 .55 s S

39 L4 .46 .70 1 s

16-r-26 32 11 1.00 .50

34 I2 .42 .40 I 1

T4 .50 .15 S S

t6-r-27 22 5 1. 00 .25 S S

27 10 .90 .45 s S

16-r-29 24 7 .7r .60 S S

28 8 .88 .55 S öt

34 T2 ot .60 S S

4T T6 .81 .50 S 1

16- 1-31 34 10 .90 .45 S S

L6-L-37 27 I 1.00 .25

32 9 .78 .30 S S

t6- r-47 2B B .62 .40 S E 214

o ( 17-o) 24-2-2s 26 7 .86 .50 ö S

o 33 10 .50 .40 ð 1

I 7-0- I 3B i0 .60 .40 S S

4I 13 .69 .40 c 1

42 I4 .71 .25 I 1

44 16 .75 .35 I 1 t7-a-2 27 10 I .00 .65

.25 S bo 1 7-0- 3 37 15 .80

o 17-0-4 36 10 1 .00 .50 e Þ

g 4I 13 .77 .30 Þ S

.30 S S 1 7-0- 5 32 B .50 o 4r 11 .63 .50 S b r7-o-6 5 .80 .40 S S

29 B ,56 .20 1 S

33 T2 .58 .25 S S

17-0-l 27 9 .67 .50 S S

31 i0 .60 .60 S S

.45 S 1 7-0- 8 24 7 .86 ó

29 T2 .75 .80 S 1

17-0-9 32 10 .65 .40

.20 S S 1 7-0- 10 T2 3 .33

1 T6 4 .75 .45 S

77 4 .62 .35 S S

27 7 .63 .45 s 1

34 11 .59 .50 I 1

17-0-11 33 9 .39 .25 S 1 215

17-o-14 24 7 1. 00 .50 c S

17-o-16 30 I2 I .00 .50 1 1

31 15 .67 .30 1 1

I7-O-17 2B 6 .58 .30 S 1

35 10 .50 .50 S 1

38 15 .50 .35 S 1

17-0-18 32 9 .56 .25 c S

I 7-0- 19 30 9 .83 .45 S 1

17-0-20 27 10 .75 .30

77-O-23 24 5 1 .00 .40 c S

27 7 .79 .35 S S

o 0 33 11 1. 00 .50 Þ Ò

17-o-24 I .50 .30 S S

77-0-25 23 B 1 .00 .4s s S

17-0-26 9 .61 .55

l2 .75 .55 S S

17-o-27 2B 10 .65 .35 I I

17-o-28 28 10 .80 .20 S S

17-o-29 2B 7 .86 .4s s S

32 13 .69 .35 i S

I 7-0- 30 31 9 .44 .55 s S

o 17-0-31 23 5 1. 00 .30 S Ò

17-0-32 18 3 1.00 .30 S S

26 5 1.00 .30 S S

36 10 .75 .35 c 6

L7-0-37 27 6 .75 .30 S 1 216

17-0-39 23 5 .70 .35 S 1

18- 1- 1 29 10 .40 .50

û 18-I-2 25 7 .7r .35 Þ 6

18- 1-5 B .56 .55 S S

1B- 1-6 37 10 .90 .55

18-1-7 26 B 1.00 .55 S I

18-1-10 23 6 1.00 .50 S

18-1-12 37 I4 .57 .20 1 S

18-1-18 26 .50 .25 1 I

18-1-19 28 10

18-1-25 31 11 B2 .50 S 1

37 15 .87 .15 1 1

TB-I-26 31 11 .82 .60 S 1

t8-r-27 40 I6 .66 .4s 1 1

18- 1-28 26 6 1 .00 .45 S I

32 10 .80 .4s 1 1

10 ô a S LO_ L_ L a1 1? .85 .50

4I I4 .86 .55 S S

LB-2-4 34 I9 .68 .40 S S

I 8-2-5 21 6 .75 .50 S S

27 11 .63 .50 S S

tB-2-7 20 4

30 .14 .20 Þo S

iB-2-B 29 t4 .57 .65 -: S

rB-2-9 2T 6 .75 .30 c 6

29 7 .36 .15 c S 217

o 1B-2- 10 27 6 .50 .25 ó r8-2-12 2L I .50 rB-2-15 32 11 .82 .75 S S

35 I4 .63 .55 g 1

18-2-16 19 4 1 .00 .30 c S

31 B .s6 .40 1

1B-2-18 7 .43

o rB-2-79 10 1 .00 .70 Þ

1B-3-1 29 10 1 .00 .70 c S

40 T7 .97 .30 1 S

42 25 1 .00 .15 S S

18-3-2 35 T2 1.00 .65 S 6

44 22 .63 .25 c S

18- 3- 3 29 10 I .00 .50 S s

30 11 .95 .40 S 1

34 13 .85 .25 s 1

18-3-5 3s 11 1 .00 .60 S S

1 1 1 8- 3-B 33 T4 .50 .40

o 18-3- i0 31 7 .86 .40 S Þ

18-3-15 40 1B .86 .30 S S

42 2L 1. 00 .20 s s

1B-3- 16 30 8 1 .00 .20 S 6

30 9 1. 00 .55 S s

40 15 1.00 .60 S 1

43 22 .93 .70 c S

18-3-17 2I 5 .90 .35 s S 2t8

35 11 1. 00 .65 1 s

42 2T 1.00 .45 òo S

43 2I .86 .4s S S

18-3-18 4T 25 .96 .20 1 1

18-3-19 32 10 .85 .55 S S

q 18-3-20 26 9 .67 .25 õ S

18-3-21 9 .78 .40 S S

18-3-22 27 11 .63 .20 S S

18-4- 1 2B B 1.00 .55 S S

43 20 1.00 .30 S 1

47 30 .73 .25 I s

UCGM 45618 29 10 .70 .45 S S

40 1B .61 .10 c S

46 29 .48 .10 1 1

UCGM 45619 36 15 .47 .20 S 1

40 2I .52 .10 S S

UC0,L"I. 45622 29 8 1 .00 .40 S s

36 15 .60 .15 I 1

USNM 365918 32 16 .69 .30 bo S

40 22 .48 .10 1 1

4l 29 .52 .10 1 S

t 19- r-2 20 7 .71 .15 Þ S

25 9 .50 .15 bo S

19- r-4 32 13 .73 .75 c 1

40 22 .68 .10 1 1

19- r-7 29 10 .40 .10 S S

31 13 .31 .15 1 1 279

19- 1- I 27 10 .35 .10

14 .33 .15

33 T7 .47 .15 S s

L9-r-9 25 6 .83 .40 bo S

37 t6 .69 .30 s S

19-1-10 31 10 .95 .50 1 1

36 18 .72 .15 S S

19-1-11 33 I .75 .25 öo S

11 .68 .20 1 S

39 2T .45 .10 S S

19-r-72 23 5 1.00 .40 óo S

39 13 .85 .15 S S

43 22 .55 .35 1

19- 1- 13 3B 24 .s4 .35 1

19- 1- 14 15 5

18 10

2B 18 .50 .10 S S

19- 1- 15 34 10 1.00 .60 1 1

42 23 .72 )^ S 1

44 32 .66 .15 1

L9-2-r 26 9 )) 10 S

13 .50

19-2-5 25 8 .50 .15 öo S

19-2-6 24 9 .72 .40 c S

33 15 .40 .20

19-2-7 6 .25 .35 0o öo

9 .28 .10 S S 220

L9-2-lr 22 6 .50 .10 öo s

27 10 .35 .15 6o 1

û 33 I7 .53 .10 b S

19-2-16 20 4 .62 .20 g s

27 9 .56 .20 S 1

31 11 .55 .20 s 1

o T9-2_IB 19 6 .83 .25 S

32 I6 .69 .30 öo S

19- 3- I 23 7 .50 .20 s S

32 I4 .50 .35 S S

39 20 .67 .i5 1 s

19-3-2 31 T2 i.00 .30 S S

4T 27 .4s .15 S S

44 27

19- 3- 3 22 6 .75 .40 S ¡i

37 18 .56 .20 1 1

3B 27 .38 .15 1 1

L9-3-4 T9 7 1. 00 .35

29 B 1.00 .40 S S

1Ê 40 I' .74 D 1

19- 3- B 22 B .50 .10 S S

o 23 9 .56 .15 6 b

29 13 .58 .15 1 I

19-3-12 33 10 .20 .05 g S

3B 15 .47 .15 g s

40 2I .33 .10 1 S 22r

t9-3-14 14 .2t .15 s S

34 16 .34 .15 c S

19-3-1s 10 .55 .25 s 1

15 .33 .15 S 1

T7 .47 .10

û S 19- 3- 16 15 5 .50 .15 b

2l 6 .33 .10 g s

o 29 10 .45 .10 Ò S

19-3-17 15 5 .60 .15 S S

to S 22 7 .20 E,

25 9 .50 .20 S S

o 19- 3- 19 18 4 .31 .30 Þ 6

û 23 7 .57 .30 s ö

19-3-20 2l 5 .30 .05 c S

19-3-21 T7 5 .70 .20

20 9 .50 .25 s

26 13 .42 .20 s S

L9-3-23 19 5 .40 .25 c S

25 8 .31 .15 1 S

19-3-24 29 t4 .57 .25 1 1

33 19 .66 .20 S S

t 19-3-26 29 13 .46 .20 Þ 1

L9-3-32 24 10 .50 .10 c S

S 19- 3- 39 2B T2 .42 .20 S

19- 3-40 28 T2 .75 .60 S I

o 19-3-41 3B 15 .67 .35 Þ 1 222

19-3-42 t7 5 .30 .05

1 USNM 3659I9 4B 27 .5.2 .10

20-I-I 44 13 .46 .15 s S

54 1B .58 .15 S S

S 20-L-2 3B 11 .77 .15 6

38 T2 .75 .15 S S

20-t-3 24 6 .92 .25 c S 1 30 9 1.00 .40 1

1 3B t4 1.00 .30 S

20-r-5 49 15 .60 .25 c 1

o 20-l-7 36 11 .68 .25 ó S

44 I7 .6s .25 S 1

20-1-11 35 B .44 .10 I S

o 4l 10 .70 .05 ô S

o 20-1-13 26 6 1. 00 .40 Þ S

25 .82 .05

20-l-16 25 .82 .05

g ü 20-2-I 34 9 .94 .45 Þ b

o S 3B 10 .80 .50 Þ

LQ 2./, .10 õo 1 ¿v- J- ¿ .69

o, S S 20-3-3 25 6 .15 o 20-3-4 31 7 .64 .25 ö S o 40 13 .73 .30 b S

1 20-3-5 20 6 .83 .10 6

S 20-3-6 39 13 .81 .60 c

1 45 16 .81 .60 S 223

20-3-7 44 T2 ,54 .20 S S

54 18 .47 .15 S S

S 20- 3- B 36 11 1.00 .60 c

20-3-9 4I iB 1 .00 .10 S

20- 3- 10 37 I4 1.00 .15 S S

20-4-r 39 13 .65 .20 S s

48 26 .35 .10 S S

20-5-2 34 I2 .54 .30 öo s

o ù 20-5-3 35 9 .67 .20 ö õ

20- 5-5 26 6 .92 .50 S S

2B 7 .79 .50 S S

42 I2 .63 .50 öû 1

20-5-6 21 6 1. 00 .30 öo S

30 9 .28 .25 1 S

20-5-7 2T 4 1. 00 .05 óo S

UI ENT-I 36 13 .88 .20 S 1

2r-7-r 11 2 1. 00 .15

o T9 5 .80 .30 Ò S

o 24 7 .7r .40 6 s

2I-La-I 22 6 I.UU .JU S Ð

32 11 .82 .25 6 1

t 37 1B .69 .10 ö S

2I-Ia-2 26 1 .t9 .45 g S

32 t2 .75 .60 s 1

o 2l-Ia-3 26 7 .43 .40 c ó o 2I-Ia-4 22 6 .75 .45 Þ 1

2I_Ib-T 23 I .BB .50 S S 224

31 t4 .57 .4s e 1

2I-Ib-2 T7 5 .40 .25

o o 2L-rb-4 24 5 .60 .4s b Ò

2I-Ic-I 33 72 .79 .40 S 1

39 18 .56 .80 1 1

o 2I-lc-2 26 7 .71 .4s c Ò

31 10 .55 .50 S S

2I-Ic-3 36 13 .92 .50 Þû 1

g 2I-Ic-4 20 4 1.00 .50 Þo ó

2I-7c-7 17 5 .90 .40 S S

o 23 7 .86 .50 S ô

2L-Ic-9 T4 3 1. 00 .20 S öo

21-1c-10 22 4 .38 .10 Þo S

21-1c-13 T7 4 .7s .15 öo 6

23-r-l 15 4 1.00 .40 Þo S

23-2-4 33 9 .39 .25 òû S

23-2-8 28 9 .67 .50 öo 1

33 15 .47 .15 S S

23-2- 17 34 T2 1 .00 .65 S S

37 I6 .81 .70 S 1

23-2-20 27 7 1.00 .70 S ôo

30 10 .95 .65 bo S

23-2-24 9 1.00 .35 1 I

32 11 .4s .50 S S

o 23-2-28 29 9 .44 .20 c Ò

35 i3 .50 .25 S S 225

23-2-29 4 1.00 .35 S

6 .50 .25 c S

23-2-3r 9 I .00 .50

23-2-37 22 4 1.00 .30 c

23-2-39 6 .50 .25 ø S

7 .43 .50 û Þç

23-2-40 43 2T ,76 .40 S I

23-2-4Ia 23 6 .63 .40 s I

33 t2 .50 .25 1 S

1tr 23-2-43 28 B .50 1 S

23-2-45 31 9 1.00 .60 bo Þo

35 I7 .94 .40

23-2-47 2B B 1. 00 .35 1 s

23-2-50 T4 2 1 .00 .10 c 6o

25 5 .30 S S

23-2-52 I9 4 .75 30 c S

23-2-54 I2 .77 .65 S 1

23-2-55 30 10 .90 .25 S 1

23-2a-I 26 7 .86 20 öo s

,1-r..-? 33 't) lnn .50 S S

23-2a-5 23 7 .86 .40 S S

26 9 .67 20 S s

23-3-6 32 t2 .75 70 S 1

34 13 .77 .60 S 1

23-3-9 11 .82 .15

23-3-14 23 6 1. 00 .50 S 1 226

25 7 .93 .50 S I

29 11 .73 .50 S 1

23-3-17 T7 7 1 .00 .70 c 6

36 I4 .93 .70 S 1

23-3-18 37 I4 .46 .10 S I

23-3-25 24 6 I .00 .60 s S

3l 13 .77 .50 S S

23-3-29 7 1.00 .40

10 .80 .40 s S

33 T2 I .00 1 1

23-3-3r 31 11 .59 .40 S 1

23-3-35 9 .89 .50

1., ÕE 23-3-36 25 9 Þo S

23-3-40 25 7 .71 30 Þo S

23a-I-4 38 I6

23a- 1-B 30 T2 83 .55 Þo

25-I-I 23 7 86 30

25-r-4 3B 15 80 .40

45 23

S treptelasma amsdgní

ô OGS_ 3 16 4 r.00 .15 ú S

26 8 .69 .15

27 10 .70 .15 s s

29 13 .69 .15 s S

OGS-4 9 2 I .00 .10

l2 3 .83 .10 227

OGS-5 t2 2 I .00 .10 c

16 5 I .00 .10 g S

OGS-6 33 I1 .68 .10 S S

OGS- 8 2B T2 .63 .10 s S

OGS-9 31 T7 .68 .10 S S

Ocs- 1 1 t7 4 r.00 .10 s

I9 7 1.00 .10 S S

OGS- I 3 31 18 .44 .10 c S

31 19 .58 .10 óo S

Ocs- 14 27 7 .64 .05 S S

27 I .88 .i0 S S

31 10 .80 .20 S S

o 24-r-r 24 10 .85 .10 S Þ

25 12 .67 .15 bo s

24-2-r 23 6 I .00 .20 bo S

34 19 .95 .10

24-2-5 23 B .75 .25 Þo S

., .7 'tl ,)\ R? _q S

24-2-7r 22 7 1 .00 .35 S S

o 2B 11 .68 .15 Ò S

31 I2 .54 .10 S S

24-2- 17 29 10 1. 00 .15 S S

36 2T .43 .05 öo S

24-2-r8 I7 4 .88 .10 S S

23 B .63 .10 S S

24-2-24 10 2 1.00 .20 S S

10 3 1. 00 .15 S s 228

o 24-2-27 35 I7 .35 .05 Þ S

24-2-29 2B 9 .55 .10 c S

31 13 .69 .15 S S

24-2-3r 26 .44 .10 c s

q 28 1I .45 .15 b S

24-2-34 32 15 .73 .15 S S

32 1B S S

24-2-36 20 5 .90 .10 c S

25 9 .33 .10 c s

31 13 .73 .15 6 S

34 18 .44 .10 c s

24-2-38 27 9 .67 .15 S S

27 9 .20 S S

24-2-39 I7 4 .88 .10 S S

o 23 7 .43 .10 ó S

24-2-40 1B 5 .80 .10 s S

o 24-2-47 T6 5 .60 .10 Þ S

27 6 .42 .IU öç s

24-2-54 18 4 .63 .10 öo S

19 4 .50 .10 6 S

Streptelasma leemonense

1 d SPECIMEN n d SPECIMEN n

uccl"I, 45614 32 9 UCGM 45615 24 7

B 14- 1-5 31 B 14-1-31 30

13 15- l- 12 36 19 20- 1- 10 3B 'NumbersI in parentheses indícate continuation of daÈa from the same índ ívídual 229

26 B ( 20- 1- 10) 40 l5 20- 1- 15

20-t-19 28 6 (20- 1- 19) 3B 11

(20-1-19) 40 t7 20-3-Ia 2T 5

(20- 3- la) 23 6 ( 20- 3- la) 25 7

(20-3- la) 26 9 (20-3- ia) 30 10

(20-3- 1a) 32 T2 (20- 3- 1a) 36 t4 i8 (20-3- la) 39 17 (20-3- 1a) 39

19 ( 20- 3- 1a) 39 t9 ( 20- 3- la) 39

( 20- 3- 1a) 39 20 20- 3- lb T9 5

(20-3- lb) 22 6 (20-3-1b) 23 6

(20-3-lb) 24 1 (20-3- lb) 25 7

(20-3- lb) 26 7 (20-3-lb) 2B I

20-4-2 28 9 UI C1448 37 l2

23-2-32 29 10 23-2-36 34 11

23-2a-2 29 7 23-3-l 26 B

(23-3-1) 30 10 23-3-3 40 15

(23-3-3) 42 76 23-3-4 32 10

23-3-B 26 7 23-3-i0 ¿J 5

(23-3-i0) 27 7 23-3-11 28 1l

/^a a 11\ 2^ 26 7 \L J'J_ L L' t2 23-3-12 t2 (23- 3- 12) 35 I2 23-3-13 32

23-3-20 32 i1 23a-I-2 35 T2

23a-l-3 30 9 (23a-1-3) 33 10

Streptelasma s p. cf. S . leemonense

23-2a-4 28 5 (23-2a-4) 34 9 230

(23-2a-4) 35 10 (23-2a-4) 37 11

(23-2a-4) 38 12 23-3-22 19 4

(23-3-22) 2I 4

Streptelasma sP. A

( 1) L7 3 15-0- 1 T6 2 5 1s-o-

( r4 2 15-0- 1A I2 2 1s-0- 1A)

15-0- lc I2 2 ( 1s-o- 1c) 13 2 5

Grewin ekia s p. A

14-2-7 22 7 (r4-2-7) 31 10

(14-2-7) 32 11

Keelop hvllu m oklahomense

23-3-2 29 20 23-3-19 32 13

(23-3-1e) 32 T4 (23-3-re) 32 T7

23-3-30 31 t7 23-3-33 20 3

(23-3-33) 30 T2 23a-I-I T4 4

11 (2-qa- !.- 1) 20 5 (23a-I-t) 28

(23a-1-1) 30 1B 25-l-2 30 T2

(25- r-2) 30 l2 (2s-r-2) 30 T7

Rhesmaphyllum

17-Ia-4 18 4 (17-Ia-4) t9 5

r7-2b-5 2L 7 (17-2b-s) 22 B

17-3-5 L9 5 ( I 7- 3-s) 22 6

Dínophyllum

77-2-3 21 4 (17-2b-3a) 29 9 231

17-3-1 23 5 ( 17-3- 1) 36 9

(17-3-1) 4T 15

Dalmanophyllum

6- 1-5 24 I 10-2-5 24 B

2 ( 10-2-s) 30 11 17-1-10 T2

(17-1-10) 15 3 ( 17- 1- 10) 20 5

(17-1-10) ?20 ?6 17-2a-2 2B 11

UCGM 45639 30 t2

Phaulactís

9-7-6 30 13 (e- 1-6) ?35 22

17-2-l 30 t2 (L7-2-r) 3B 23

Unassigned specímens belongíng to Silurian assemblage

17-l-2 20 5 ( 1 7- 1-2) 23 7

17-1-3 15 4 (17-1-3) 24 7

L7-r-4 t7 3 (r7 - r- 4) 20 5

23 6 17-1-B T2 J 17-1a-1

5 ( 17- 1a- 1) 29 10 17-Ia-5 1B

17-Ia-6 22 5 17-la-7 LW 4

(17- La-7) 25 B (17-Ia-7) 25 9

24 6 17-2-2 27 B 17-2- 4

(17-2-4) 25 7 17-2-9 L6 4

5 (17-2-e) 24 7 17-2-t4 20

17-2-15 31 9 17 -2-16 25 8

I7-2a-3 26 6 232

17-2a-4 27 7 17-2a-6 20 5

17-2a-7 2T 5 1 7-0 (2a) -38 24 6

L7-2b-r 2l 7 17-2b-2 19 6

L7-2b-3 26 7 17-2b-4 t4 3

(17-2b-4) 1B 4 17-3-2 20 4

(17-3-2) 22 6 (r7-3-2) 30 13

(r7-3-2) 30 15 17-3-3 2t 6

(17-3-3) 26 10 (t 7- 3- 3) 27 T2

17-3-4 17 4 (t7-3-4) l9 6

( 17- 3- 4) 2L 8 t7-3-6 23 7

17-3-7 25 7 17-3-8 32 10

17-3-9 20 6 17-3-10 15 4

17-3-11 18 6 (17-3-11) 18 7

17-3- 12 2I 7 L4-2-2 1B 4

(t4-2-2) 22 5 r4-2-B 20 6

( 14-2-8) 24 7 233

APPENDIX 3: CARDINAL FOSSULA I,\'IDTH AND SHAPE

i,Iidth of cardinal fossula (fw) \raa measured in mm beÈ\^Ieen median lines of septa immediaËe1y adjacent to the fossula, midway between axíal and peripheral ends of septa bounding the fossula. Shape (ft) is according to the types descríbed ín SYSTEI'IATIC PALEONTOLOGY under

Streptelasma subregulare. Two numbers separated by a slash índícate the shapes on either síde of a fossula. Coral diameter (d) was measured in mm on the transverse thin sectíon. Specimen numbers in parentheses indicate contínuation of daÈa from the same indívidual.

SPECIMEN fw ft d SPECIMEN fw ft d

S trep telama subregulare

3-3-13 1.7 1 T2 3-3- 16 1.8 4 10

3-3-24 1 5 2 l2 3- 3- 30 r.4 4 I

( 3- 3-30) 1.8 4 13 UI C1560a 1.1 4/s 7

(rrr n1 qÁ,n.\ 1â l_0 (L1r C1560a) 1.6 5 13 \ u! v¿Jvvsl -?

UI C15BIa 1.5 2 10 (ur c15Bla) 1.9 3 15

(ur c1581a) 2.6 5 22 4-r-2 1.1 4 6

(4- r-2) 9 4/5 B 4-r-6 2.0 5/4 7

13-1-1 I 5 5/2 7 13-r-2 1.6 4 B

( 13- 1-2) I B 5 15 13- 1-3 7 4 5

( 13- 1-3) 1 7 3 13 1 3- 1-5 I 4 4

14-r-2 1.0 2 7 (14-t-2) 1 4 5lI 15

(14-r-2) 2.4 L/3 I9 14- 1- 3 2 2 5 t4 234

t) t4-r-4 1.1 s/r 10 (r4-r-4) 4 16 t4-r-7 r.2 3/L 11 14- 1- B 1 2 4/s 9

( 14- 1- 8) t.7 3 T2 ( 14- 1-8) I 5 2 t7

14-r-9 I.2 4 I ( 14- 1-9) 1 B 4 15

14-1-11 r.7 4 18 t4-l-12 9 5 13

14-1-13 2.8 3 I7 14- 1- 15 7 I 3

1 J 1 8 ( 14- 1- 1s) o 1 5 ( 14- 1- ls)

1 4 10 14- 1- 1B 1.1 2 8 14-L-t9 3

11 14-1-22 r.4 2 B t4-r-26 2 0 1

14- 1- 30 .7 5 4 ( 14- 1- 30) 7 5 9

4 ( 14= 1- 30) 1.9 4 16 15- 1- 1 8 2/s

( 1s- 1- 1) r.4 s/3 I2 15-r-2 9 4 J

15- 1- 3 1.3 5 9

15-L-4 I.2 4/3 6 15- 1-6 I.2 4 6

15-I-7 1.8 5 11 15- 1-9 1.3 2 t2

15-1-11 1.0 2 7 15-1-13 1.3 2/4 L7

15- 1- 14 1.4 4 9 15- 1- 15 .8 5 6

11õõrà l.ÉL L l, i5- i- i6 i.0 2 6 UUUI'l qJU+1 !.4 1 1:q

2Lb-2-3 1.0 I 5 (zrb-2-3) .8 I 8

27b-2-4 1.1 4 7 (2rb-2-4) .B 1 10

2rb-2-B I 4 ( 2 lb-2-B) 1 9

(2rb-2-B) I L2 16- 1- I 1.0 2/4 6

( 16- 1- 1) I.2 5/4 11 16- 1- 3 1.1 2 9

( 16- 1-3) 1.2 2 T2 16-r-4 7 4 2

1 2 2 12 ( 16- 1-4) 1 5 1 B ( 1 6- 1-4)

5 16- 1-5 8 1 3 ( 16- 1-s) 7 1 235

( 16-1-5) 1.3 1 B ( 16- 1-s) r.2 1 10

( 16- 1-s) 1.3 1 I2 16-1-6 2.L 4 T7

16-I-9 r.2 1 6 ( 16- 1-e) 1. I 1 B

16-1-10 2.0 1 16 16-1-11 1.8 4 9

(16-1-1i) 2.I 1 9 16- 1-19 r.4 4 8

( 16- 1- 1e) )) r/4 T2 t6-r-22 .9 1 6

(16-7-22) 2.0 4 16 L6-r-25 1.1 5 I2

(16-L-2s) 1.5 2 T4 16-r-26 1.3 1 10

(16- 7-26) 1.6 rl2 t2 16-r-27 1.0 1 5

(16- r-27) r.4 I 10 16-r-29 1.6 1 7

(16-r-2e) 1.0 2 B (t6-r-29) r.4 4 T2

(16- r-29) 1.5 2/s I6 16-1-31 1.0 I 10

L6-r-37 1.5 2 9 16-r-47 t.6 3 B

77-0- (24-2-2s) 1.0 2 7 Irz-o-( z4-z-2s)r.r 2 101

1 7-0- 1 r.2 2/r 10 ( 17-o- 1) r.4 5 13

( 1 7-0- 1) 1.3 4/s T4 ( 17-o- 1) 1. s s/2 16

17-0-2 1.5 I 10 17-0-3 1.0 2/s 15

17-0-4 7.4 2 10 ( 17-0-4) r.7 2 13

1 7-0-5 1.0 3 8 ( 17-o-s) 1. s 3 11

i ( t7-a-6 .B 5 \rr 11-n-6\e v/ l..3 4 8

( 1 7-0-6) 1.5 2 72 r7-o-7 1.1 1 9

(17-o-7) 1.1 1 10 17-0-8 1.1 2 7

( 1 7-o- 8) 1.1 2 L2 17-0-9 .9 3 10

1 7-0- 10 I 3 ( 17-o- 10) .8 1 4

( 1 7-o- 10) .9 2 7 ( 17-o- 10) r.2 2 11

17-0-11 1.3 r/3 9 17-0-13 r.7 1 9 236

r7-o-L4 r.2 4 7 17-0-16 1.8 I T2

( I 7-0- 16) ')) 4 15 t7-0-17 1.1 2 6

(17-o-17) t'L 3 10 (17-o-17) 2.5 I 15

17-0- 1B 1.8 2 9 17-O-19 7.2 4 9

17-o-20 1 3 1 10 17-o-23 9 2 5

(17-o-23) 1.2 2 7 (17-0-23) 1 4 4 11

17-0-25 r.4 I I 17-0-26 2 0 r/s 13

17-o-27 1.1 1 10 t7-0-28 1 1 1 10

L7-O-29 9 2 7 (17-O-2e) I 3 2 T2

1 7-0- 30 1 0 4 9 i7-0-3i I 0 2 5

17-0-32 7 2 3 (17-o-32) ,9 2 5

(17-o-32) 1 4 2 10 17-0-34 1 0 I 6 r7-o- 36 1 3 3/r 7 17-0-37 ,8 4 6

18-1-2 2 0 4 7 l8- 1-5 1 ,4 412 B

1B-1-6 2 3 2 10 18- 1- 7 2 I 5 I

1B- 1- 12 2 1 2 T4 18-1-16 I ,3 2 3

,) (t8-1-16) 1 6 5 6 18- 1-25 2 5 11

(18-1-2s) 2 0 5 15 1B- 1-26 1 ,7 2 ii

18-r-27 5 0 4 L6 18-1-28 3 ,0 4 6

1 13 I R- L1-?R\ ae/ 3 10 L8-2-2 ,9 I \Le 3 0

(rB-2-2) 1 6 1 T4 18-2-7 ,9 2 2

,) (rB-2-7) 2 0 4 4 ( 1B-2-7) 2 J 7

1 8-2- 8 3 6 3/s T4 18-2-9 1 .5 5 6

( 18-2-e) 2 5 3 7 18-2- 10 1 .B 5 6

LB-2-15 I 2 4/L 11 ( 18-2-1s) I .7 5 t4

18-2-16 1 I 2 4 (18-2-16) I .0 2 237

18-2-19 I .0 4 10 18-3-1 2.2 2 10

(18-3-1) 1 .B 2/r I7 ( rB- 3- 1) 2.4 2 25

,) 1B-3-2 3 4/2 T2 ( i8- 3- 2) 5.1 2 22

18-3-3 2 .6 4 10 (18-3-3) 3.5 2 11

18-3-3 3 .0 2/s 13 18-3-8 2.2 J T4

18-3-10 o 2 7 18-3-1i 1.5 4 5

18-3-15 2 .3 s/2 1B ( 1B-3- 1s) 1.9 5 2T

1B-3-16 1 ) 4 B ( 1B-3- 16) r.2 4 9

( 18-3-16) 1 .6 5 15 (18-3-16) 2.0 5 22

18-3-17 .9 2 5 (18-3-17) 1.6 4 11

( 18-3-17) 2 .6 2 2T ( 18-3-i7) 2.6 2ls 2L

i8- 3- 19 1 .2 412 10 1B-3-20 2.3 2/s 9

18-3-22 1 .6 1 11 18-4- I 1.1 4 8

( 18-4- 1) I ') 2 20 ( i8-4- 1) 3.1 2/s 30

USNM 365918 I o 3ls I6 ( 36se 1B) 3.2 3 22

( 36se 1 8) 5 .3 3 29 UCGM 45618 3.9 3 10

,) (uccu 456i8) 3 2 18 (uccM 45618) 1.8 3/2 29

f rr^^i. / E/ l^\ ô1 UUUI'I 4]O IY I .7 I I) \ uuul't 1)u L7 ) 2 LL

19-r-2 1 .4 5/r 5 ( 19- 1-2) )) 2/5 6

(re- r-2) I .5 4/2 I ( 19- 1- 2) 1.5 2/4 11

19-7-4 1 .3 5 13 ( le- 1-4) 3.6 3 2l

19-7-7 I .B s/4 10 ( le- 1- 7) 3.0 3 13

19- 1-B I .8 1 L0 ( le- 1- 8) 2.4 r/5 13

L9-I-9 1 .0 4/2 6 ( 1e- 1-e) r.6 s/4 16

19- 1- 10 1 .4 4 10 ( i9- 1- 10) 2.4 2 1B

19-1-11 1 .0 1 B (19-1-11) 1.0 1/4 11 238

,, o (1e-1-11) 9 3lr 2I t9-t-12 r/4 5

(re- r- 12) ) I 2/4 13 ( 19- 1- 12) 4.4 3 22

19-1-13 4. 0 3 24 19- 1- 14 2.1 s/2 T7

19- 1- 15 1. 2 4 10 ( le- 1- ls) 2.7 4/3 23

( ie- 1- 1s) 4. 3 3 32 19-2-r 1.3 5 13

t9-2-5 1. 3 4 B L9-2-7 1.7 3 6

(re-2-7) 1. I s/4 9 t9-2-rr t.7 4/r 6

(19-2-i1) ) 4 4 10 (re-2-rr) 2.r 5 I7

t9-2-16 1. 6 4lr 4 (te-2-16) 2.4 4/L 9

(Le-2-16) 1. 6 4/s 11 19-2-18 1.0 2 6

( 1e-2-18) ') 5 2/3 T6

19- 3- 1 1. 5 3/2 7 ( le- 3- 1) 2.5 4 L4

( 1e- 3- 1) 3. I 2 20 19-3-2 r.4 1 I2

(re-3-2) 3. 3 3/r 27 19- 3- 3 1.0 4/r 6

( le- 3- 3) 2 B 3/L 18 ( le-3-3) 2,8 J 2I

t9-3-4 5 2 7 ( 1e- 3-4) 1.2 2 I

( 1e- 3-4) 1 5 s/4 t9 19- 3- 8 t.l 3 B

f 1^ I O\ 1l ( 1A ( rv- J- ö/ _t o )/L+ Y \ rr- J- o,, l.l

rg-3-12 2 2 1 10 (re-3-t2) 2.6 2 15

(r9-3-12) 3 3 5/3 2I 19- 3- i5 r.7 5 10

(le-3-15) 2 5 4 15 19-3-16 1.9 1 10

L9-3-17 1 3 1 10 19- 3- 19 1.0 1 4

( le-3-le) I 2 214 7 19-3-20 r.7 2 5

L9-3-2r 1 8 3 5 (19-3-21) r.6 I 9

( 19-3-2 1) 2 0 i 13 t9-3-23 1.8 I 5

(re- 3-23) 2 0 3 8 19-3-24 2.7 4/3 T4 239

(re-3-24) 2.8 2 79 19-3-26 r.6 5 13

L9-3-29 1.5 2 6 t9-3-32 r.2 5/2 10

19- 3-40 I.9 5 l2 t9-3-4I 2.1 2 T4

( le- 3-4 1) 2.0 3/L 15 USNM 365919 1.3 5 13

13 ( 36se 19 ) 2.0 I I6 20- 1- I 1.5 2

(20- 1- 1) 2.3 J 1B 20-2-2 1.5 3/4 11

(20-2-2) 1.8 3 T2 20-t-3 .6 5 6 aa (20- 1-3) .9 5 9 ( 2o- 1- 3) s/4 t4

20-L-5 3.0 3 15 20-I-6 ,o 2 27

20-r-7 r.4 4/s i1 (2e-r-7) 2.1 3 T7

20-1-11 1.1 3 B (20- 1- I 1) r.2 2 10

20-1-13 1.5 4 6 20-2-L r.2 4 9

(20-2-r) 1.3 3 10 20-3-3 .8 5 6

20-3-4 1.5 3 7 (20-3-4) r.6 3/s i3

20-3-5 1.3 s/3 6 20-3-7 1.5 3 T2

(20-3-7) 1.8 2 18 20-3-8 1.5 2 11

20-3-9 2.r 2/s iB 20- 3- 10 1.8 2 T4

/ , r \ a1 ) .L 20-4-i 2.0 ¿14 IJ \ ¿v-+-^^ L ) J. J. J

20-5-2 1.6 2 I2 30-5- 3 1.0 s/2 9

20-5-5 1.0 3/4 6 ( 2o-s- s) 1.3 3/r 7

( 20-s-s) 2.0 3 I2 20- 5- 10 2.5 4/2

UI ENT- 1 t.7 2 13 2I-I-3 1.1 2 5

(21-1-3) 1.1 3 7 2I-la-7 1.1 3/4 6

(21-la-1) 1.6 3 11 (21-la-1) 2.5 3 1B

2L-Ia-2 1.1 3 7 (21-la-2) 1.3 2 t2

2I-la-3 r.2 2 7 2L-Ia-4 .B 2 6

2r-Lb-1 1.1 2/4 8 (2 1- lb- 1) 1.9 2 t4 240

2L-]-b-3 .7 1 4 2r-Ib-4 .9 2 5

2r-rb-g .7 2 4 2I-lc-I I .1 5 T2

(21-lc-1) 2.3 3 1B 2I-Ic-2 1 .1 3 7

(2r- Lc-2) 1.1 5 10 2l-Ie-3 1 .9 413 13 ) 2I-Ic-4 1.1 2 4 2l-Ic-7 I 2 5

(21-tc-7) r.2 4 7 21-1c-8 .6 4 3

21-1c-10 .9 2 4 21-1c-13 i .0 2 4

1 4 9 23-L-r .6 1 4 23-2-8 .5

(23-2-B) 1.3 3 15 23-2-17 2 .3 2 l2

o (23-2-t7) 1.5 4 I6 23-2-24 1 4 12

23-2-28 1.3 3lr 9 (23-2-28) I .3 3/s 13

23-2-29 .8 I 4 (23-2-29) 1 .1 3/s 6

23-2-37 1.0 2 4 23-2-39 I 2 3 6

23_2_40 1.8 2 2I 23-2-47a i 0 3 6

(23-2-4La) 1.3 2 I2 23-2-45 1 2 4 9

23-2-47 .B 5 B 23-2-50 B 2 3

(23-2-50) o 2 5 23-2-52 B r/4 4

1.1 ¿J- ¿- J+ l. t- Jl + LL

23-2-55 1.3 2 10 23-2a-L 1. t 2 7

23-2a-3 1.3 4 12 23-2a-5 1.3 4/2 7

(23-2a-5) r.6 2 9 23-3-6 r.2 413 L2

23-3-t4 .7 2 6 (23- 3-14) 7 2 7

(23-3-14) r.2 2 11 23-3-17 2 0 4/2 15

23-3-18 2.2 3 I4 23-3-24 1 5 1 10

23-3-25 .9 2 6 (23-3-2s) 1 8 4 13

10 23-3-29 .9 1 7 (23-3-2e) 7 5 241

23-3-31 r.4 3 11 23-3-36 r.7 3 9

23-3-40 1.1 2 7 23a-I-8 1.6 r 12

25-1-4 2.7 3 23

Streptelasma amsdeni

OGS-3 1.0 r/s 4 (ocs- 3) r.4 I 10

(ocs- 3) 1.3 5 l2 OGS-5 1.0 5 4

OGS-6 1.6 2 11 OGS-B 2.2 5 11

OGS-9 2.2 5/2 I7 ocs- 1 1 7 r/2 4

(ocs- i 1) 1.6 4 7 Ocs- 13 2 J 5 I7

( 0Gs- 1 3) 3.1 1 18 ocs- 14 1 2 1/2 10

24-r-L 1.5 I 10 (24-r-r) I 9 5 I2

24-2-r 1.1 4 6 24-2-5 1 1 4/r 7

(24-2-s) r.4 5 10 24-2-tL I 2 4 6

(24-2- rr) r.4 5 11 (24-2-rr) I 9 I L2

24-2-17 I.2 5 10 (24-2-77) 2 7 4 2T

24-2-18 1.0 2/r 4 (24-2-rB) I 6 s/4 8

24-2-24 .6 1 2 (24-2-24) 9 1 3

24-2-27 2.7 4 18 24-2-29 2 0 3 9

(24-2-29) 1.8 5/2 9 (24-2-2e) 1 6 5/r L2

(24-2-22) 2.1 4/s 13 24-2-31 1 6 1 I

24-2-34 1.8 L/5 15 (24-2-34) 2 9 1 1B

24-2-36 1.0 I 5 (24-2-36) 2 9 I 18

(24-7--36) 1.6 5lr 13 24-2-38 1 6 4/r 10

(24-2-38) r.6 2/r 10 24-2-39 I 2/r 4

(24-2-39) 1.9 t 7 24-2-40 I 3 2 5

1 24-2-47 r.4 5 4 24-2-54 r/4 4

(24-2-s4) r.2 I 4 242

APPENDIX 4: TASULAE PER UNIT LENGTH

Tabulae/cm r¡ras calculated by counting the number of tabulae aË the coral axis in a longitudinal thin section, and divídíng by the

total length of the interval examíned.

SPECIMEN Tabulae/cm SPECIMEN Tabulae/cm

S trep telasma subregulare

13-r-2 2.0 14- 1- 3 2.9

14- 1- B 11. I 14-1-13 9.0

14- 1- 30 4.8 15-1-15 6.0

16- 1- I 5.0 16- 1- 3 5.3

16- i-5 4.7 16- 1-6 9.3

I 7-0- 3 20.0 r7-0-6 15.7

1 7-0- 10 7.5 17-0-11 27 ,2

1 7-0- 16 r0 .7 t7-0-17 7.0 r7-o-20 14.7 1B-2- 15 5.0

18- 3- 1 6.8 1B-3-15 4.4

1B-3-17 4.7 1B-3-18 8.3

I 8-4- I 3.9 UCGM 45619 4.6

UCGM 45628 4.4 19_T-12 9.5

19-3-4 5.6 20-3-7 8.0

20-3-9 8.1 2I-Ia-l 6.5

2I-Ic-3 4.0 21-1c-18 5.0 243

S trep telasma ams dení

OGS- 7 4.8 ocs- 10 5.1 ocs- 12 4 0 ocs- 13 4.3

24-2-7 5 0 24-2-r0 5.1

24-2-rr 4 0 24-2-12 4.r

24-2-36 4 7

S t rep telasma leemonense

20- 1- 10 9.3 23-3-I 11. 4

23-3-11 20.0