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Paleoecology and paleoenvironmental analysis of the Upper Greenbrier Group (Upper Mississippian): West Virginia and western Maryland
WulfF, Julie Iris, Ph.D.
The Ohio State University, 1991
UMI 300 N. Zeeb Rd. Ann Aibor, MI 48106
PALEOECOLOGY AND PALEOENVIRONMENTAL ANALYSIS OF THE
UPPER GREENBRIER GROUP (UPPER MISSISSIPPIAN):
WEST VIRGINIA AND WESTERN MARYLAND
DISSERTATION
Presented in Partial Fulfillment of the Requirements for
the Degree Doctor of Philosophy In the Graduate
School of The Ohio State University
by
Julie Iris Wulff, B.S., M.S.
The Ohio State University
1991
Dissertation Committee: Approved by
Loren E. Babcock
James W. Coilinson William I. Ausich, Adviser
Terry J. Wilson Department of Geological Sciences Copyright by Julie Iris Wulff 1991 To Danielle Rose ACKNOWLEDGEMENTS
No dissertation can be completed without the help of numerous people.
I thank my advisor and friend, Dr. William I. Ausich, for his endless supply of advice, encouragement, ideas, good humor and, at times, financial support; Steven Riddle, my office mate and friend, for countless hours of discussion (not always dissertation reiatedi), study help and moral support; my fellow classmates, ail too many to mention, and the staff of the Department of Geological Sciences, in particular, Helen Hayes, Sue Shipley and Mary Hill.
This study was field intensive and could not have been carried out without the help of field assistants Brenda Lord Lasorsa, Barbara Schwimmer, Bill Ausich, Kelly Beattiey Grant, Mike Grant, Rob Corzatt, Ralph Bentley, Matt Karrer, Doug Ricketts, Bob Janosy and Elizabeth Ausich.
Dr. James Krug, of Aiderson, West Virginia, generously lent us the use of his turn of the century Victorian home while we were working in the area. The following people allowed us access to their quarries: Mr. Mike Hale and Mr. Steve Hinebaugh - Browning’s Deep Creek Quarry; Mr. Paul Schockey, Maryland Department of Transportation - Sang Run Quarry; Mr. C. K. Meadows - Kenton-Meadows Quarry; Mr. Patrick Adamson - Kermit Butcher Quarry; Mr. William Ryder - R. & R. Quarry; Ms. Diana Slater and Mr. Larry Simmons, Seneca Quarries - Slaty Fork Quarry; Acme Limestone Quarry and Mr. and Mrs. John E. Lane of Buckeye, WV.
Financial support was provided by the Appalachian Basin industrial Associates Fund and Friends of Orton Hail, both administered through the Department of Geological Sciences, Shell Oil Company, Arco Oil Company, and a Graduate Student Alumni Research Award.
Photographic assistance was provided by Beth Ann Daye and Bill Ausich. Drafting assistance was provided by Karen Tyler.
I thank my parents, Jerry and Helene Wulff, for their continued support and understanding throughout yet another degree.
Finally, I thank my husband and best friend, Eric Greenfield, who has only known me as a student. I am done, its finished, thanks for putting up with me through thick and thin. Lets get on with the rest of our iivesi
III VITA March 31, 1959...... Born - Chicago, Illinois 1982 B.S.,University of Illinois, Urbana, Illinois - Secondary Education, Physical Sciences 1986 ...... M.S., University of Illinois, Chicago, Illinois - Geological Sciences PUBLICATIONS Wulff, J. I. 1986. Ordination of paleocommunities in the Lodgepole Limestone of Central Montana. (Abstr.). IN The Geological Society of America, North-central section, 20th annual meeting. Abstracts with Programs, 18(4):331. Riddle, S. W., J. I. Wulff & W. I. Ausich. 1987. Biomechanics of flexibility in the Gilbertsocrinus column. Sixth International Echinoderm Conference. Abstr., 101. Riddle, S. W., J. I. Wulff & W. I. Ausich. 1988. Biomechanics and stereomic microstructure of the Gilbertsocrinus tuberosus column. IN Proceedings of the Victoria International Echinoderm Conference. Balkema Press, Rotterdam. Wulff, J. I. 1989a. Biostratinomy of Archimedes ; Use in paleoenvironmental interpretation. (Abstr.). IN The Geological Society of America, North-central section, 23rd annual meeting. Abstracts with Programs, 21(4):53. Wulff, J. I. 1989b. Ecophenotypic variability in Spirifer pellaensis. (Abstr.). IN The Geological Society of America, 101st annual meeting, St. Louis, November, 1989. Abstracts with Programs, 21 (6). Wulff, J. I. 1990a. Morphometries of Spirifer pellaensis; how many species are there? Second International Brachiopod Congress, University of Otago, Dunedin, New Zealand, February, 1990. Abstr., 103. Wulff, J. I. 1990b. An Upper Mississippian reef in southern West Virginia. (Abstr.) IN The Geological Society of America, North- Central section, 24th annual meeting. Abstracts with Programs, 22(5). Wulff, J. I. 1990c. Biostratinomic use of Archimedes in paleoenvironmental interpretation. Palaios, 5:160-166.
IV Wulff, J. I. 1990d. Tracking faunal and faciès changes across an uplift within a foreland basin. (Abst.). The Geological Society of America, 102nd annual meeting, Dallas, November, 1990. Abstracts with Programs, p. 62. Wulff, J. I. 1991. Intraspecific morphologic variability in Spirifer pellaensis. Greenbrier Group, (Upper Mississippian/Lower Carboniferous) USA. pp. 49-56 IN MacKinnon, D. et al., (eds.), Brachiopods Through Time. Balkema Press, Rotterdam. Wulff, J. I. & W. I. Ausich. 1991. Paleosols in the Greenbrier Group of central West Virginia: Evidence for extreme shallowing in the Greenbrier Sea. (Abst.). The Geological Society of America, North-Central section, 25th annual meeting. Wulff, J. I. & W. I. Ausich. 1989. Growth of the xenomorphic crinoid column (Taxocrinus, Late Mississippian). Journal of Paleontology, 63:657-661. Wulff, J. I., S. W. Riddle & W. I. Ausich. 1988. Columnal insertion and column growth in a Mississippian flexible crinoid. (Abstr.). IN The Geological Society of America, North-central section, 22nd annual meeting. Abstracts with Programs, 20(5): 395.
Fields of Study Major Field: Goelogical Sciences Minor Field: Paleoecology and Paleoenvironmental Analysis TABLE OF CONTENTS
DEDICATION ...... i i
ACKNOWLEDGEMENTS ...... i ü
VITA ...... iv
LIST OF TABLES • • ...... - - - ix
LIST OF FIGURES ...... x
CHAPTER PAGE
I. Introduction ...... 1
M e th o d s ...... 2 History & Geoiogic Setting of the Greenbrier G roup...... 4 Paieogeography & Tectonic Setting ...... 12
II. Sedimentology and Facies Anaiysis...... 21
Introduction ...... 21 Interpretation of Lithofacies ...... 23 Region 1 - Garrett Co., Maryland...... 25 Interpretation-Region 1 ...... 43 Region 2 - North-central West Virginia...... 54 Interpretation-Region 2 ...... 83 Region 3 - Southeastern West Virg in ia...... 84 Interpretation-Region 3 ...... 112 Regional Synthesis...... 116 Facies Relationships...... 119
III. Autecology . 125
Brachiopods • • ■ Bryozoans...... 142 Echinoderms ...... 149 Trilobite ...... 153 Foraminifera ...... 155
Vi G astro p o d s...... O s tra c o d e s ...... Algae ......
IV. Faunal Analysis and Paleoecology...... 170
Introduction ...... 170 Trophic S tr u c tu r e ...... 172 Tier Structure ...... 1/2 Other Factors in Faunal Association Development...... 174 Trophic Assemblages...... 175 Cluster Analysis of Localities and Taxa ...... 179 Region 1 - Western Maryland...... 179 Region 2 - North-central & Central West , ^ V irg in ia...... 189 Region 3 - Southeastern West Virginia...... 193 Taxa by Facies Cluster A n a ly s is ...... 197 S u m m a ry...... 197
V. Comparison Between the Eastern Interior Basin and the Appalachian B asin...... 198
Introduction ...... 198 Stratigraphie Correlation ...... 201 Faunal Comparison ...... • • • ^^1 Discussion ...... 211 Bangor Limestone...... 222 Conclusion ...... 223
VI. Autecology of Anthracosoirifer pellaensis ...... 224
Introduction ...... 224 D a t a ...... 225 R e s u lts...... • 226 Occurrence of A. pellaensis ...... 236 Discussion ...... 239 C o n c lu s io n ...... 242
VII. An Upper Mississippian Reef in South-Eastern West Virginia...... 243
Introduction ...... 243 Reef Definition...... 244 Location & Stratigraphie S e ttin g ...... 244 Description of R e e f ...... 244
v i i Reef Ecology & H is to ry ...... 253 Other Late Paleozoic Carbonate Buildups ...... 259 Conclusion ...... 262
VIII. Conclusion ...... 263
IX. Systematics ...... 266
Brachiopoda ...... 266 Echinodermata ...... 274 B ry o z o a...... 276 C n id e ria...... 278 Arthropoda ...... 279 M ollusca ...... 282 P r o tis ta ...... 283 P la n t a e...... 284
APPENDICES
A. Biostratinomic Utility of Archimedes in Environmental Interpretation...... 286
B. Archimedes Bedding Plane D a t a...... 294
C. Intraspecific Morphologic Variability in Spirifer pellaensis. Greenbrier Group (Upper Mississippian/Lower Carboniferous) USA ...... 299
D. Locality R e g is te r ...... 308
E. Pétrographie Descriptions ...... 311
F. Occurrence of Facies in All Localities ...... 339
G. Point Count D ata ...... 342
H. Faunal L is t...... 347
I. Cluster Analysis D a t a...... 355
J. Anthracosoirifer Pellaensis M easurem ents...... 358
REFERENCES ...... 365
v m LIST OF TABLES
TABLE PAGE
1. Evidence for existence of 38th Parallel Lineament Z o n e ...... 19
2. Some common Mississippian taxa In restricted shelves, bays and lagoons...... 46
3. Total organic carbon d a t a ...... 50
4. Characteristics of standard facies belts and environments . . . 51
5. Description of stages In Union Limestone and Aiderson Formation d e p o s itio n...... 123
6. Faunal associations and niche occupation ...... 176
7. Faunal associations and regional o c c u rre n c e ...... 182
8. Comparison of genera from the Eastern Interior Basin and the Greenbrier G rou p...... 202
9. Genera common to both basins - EIB and Greenbrier units (West Virginia and Maryland)...... 208
10. Genera common to both basins - EIB and Greenbrier units (West Virginia)...... 209
11. Genera common to both basins - EIB and Greenbrier units (M a ry la n d )...... 210
12. Comparison of genera from the EIB and Greenbrier Group (Limestone units only)...... 212
13. Genera common to both basins - EIB and Greenbrier Group (Limestone units only)...... 218
14. Chl-squared statistics ...... 230
IX LIST OF FIGURES
FIGURES PAGE
1. Location of measured sections in the Union Limestone, Greenville Shale and Aiderson Formation...... 3
2. Tectonic activity in the Appalachian Basin, Eastern Interior Basin and the Warrior Basin...... 5
3. Outcrop extent of Greenbrier units In West Virginia and Maryland...... 6
4. Currently recognized stratigraphie terminology...... 8
5. Thickness trends in the central Appalachian Basin ...... 9
6. , Outcrop view of entire section. Union Limestone, Greenville Shale and Aiderson Formation. R & R Quarry, Greenbrier Co., W V......
7. Outcrop view of Greenville Shale, dipping approximately 35° southeast. Near Greenville, WV; Monroe Co., W V......
8. Physiographic map of West Virginia and adjacent Maryland (Arkle et al., 1979) ...... 13
9. Position of West Virginia Dome and trend of the 38th Parallel Lineament Zone (from Heyl, 1972). 1°
10. Approximate boundaries of Regions 1, 2 & 3 based on faunal content _ and lithologie characteristics ......
11. Location of measured sections in Region 1 ...... 26
12. A. Sang Run Quarry; B. Deep Creek Quarry ...... 27
13. Qakland Q u a rry...... 28
14. A. Stratigraphie correlation by lithofacies and faunal content. B. Knobs-Union Road...... 29
15. Bloturbated Mudstone Fades ...... 23
16. Qstracode/Calclsphere Mudstone F a c i e s ...... 34
17. Fossiliferous Wackestone F a c ie s ...... 36
18. Foraminifera-rich Packstone ...... 38
19. Foraminifera-rich G rain sto n e ...... 40 20. Bryozoan rich G rain sto n e ...... 42
21. Fossiliferous Grainstone (Lag) ...... 44
22. A - Paieogeography of the open gulf and associated environments, Stage 2 (Chesterian); B - Paieogeography of the central Appalachian Basin following transgression of the Greenbrier Sea, Stage 3 (Chesterian). . 47
23. Inferred paleoenvironments of the central Appalachian Basin during deposition of the upper Greenbrier u n it s ...... 48
24. Location of measured sections in Region 2 ...... 55
25. A. Canaan Quarry; B. Roaring C r e e k...... 56
26. A. U.S. Route 33; B. Butcher Q u a r r y ...... 57
27. A. Monterviile Quarry; B. Kenton-Meadows Q u a rry...... 58
28. Arenaceous Fossiliferous M u d s to n e ...... 59
29. Fossiliferous Dolomitized M u d s to n e ...... 51
30. Arenaceous Micaceous M udstone ...... 63
31. Fossiliferous W ackestone...... 64
32. Arenaceous Wackestone ...... 66
33. Arenaceous Fossiliferous P a c k e s to n e ...... 68
34. Fossiliferous Packstone ...... ^ ...... 70
35. Qolitic P ackstone ...... 71
36. Arenaceous Hematitic P acksto n e ...... 73
37. Arenaceous Grainstone/Peloid Grainstone . * ...... 74
38. Oolitic Grainstone ...... 76
39. Paleosol ...... 78
40. Contact between Oolitic Grainstone & Paleosol...... 79
41. A. Drab-haloed root casts and mottled fabric on weathered surface of paleosol. B. Fitted-fabric on weathered surfaceof paleosol...... 80
42. Stratigraphie section at Canaan Quarry illustrating position of paleosols (CQ-4, CQ-7, CQ-9) and related lithologies...... 81
43. Siltstone, unit 3 3 - 8 ...... 82
44. Location of measured sections in Region 3 ...... 85
45. A. Slaty Fork Quarry; B. Swago C r e e k...... 87
XI 46. A. Renick Valley: B. Knobs-Union R o a d ...... 88
47. A. Sail Sulphur Springs Quarry; 8. Acme Q u arry ...... 89
48. Aiderson ...... flO
49. Fossiliferous M u d s to n e ...... 91
50. Arenaceous Fossiliferous Mudstone ...... ^8
51. Micaceous Mudstone ...... ^8
52. Mudstone; Dolomitized Mudstone • ...... ^8
53. Laminated M u d s to n e...... 98
54. Fossiliferous Wackestone ...... 190
55. Fossiliferous P a c k s to n e ...... 102
56. Oolitic Fossiliferous Packstone ...... 104
57. Qolitic Fossiliferous G ra in s to n e ...... 100
58. Foraminifera Peloid Grainstone ...... 108
59. Fossiliferous Intraclast G ra in s to n e ...... H O
60. Black Shale ...... I l l
61. Micaceous Siltstone ...... H O
62. Ideal depositional model: Cartwnate Platform with Frontal Hydrodynamic Build-up, Ste. Genevieve Limestone (Meramecian)...... 117
63. Correlation of measured sections showing basic facies relationships, shallowing event at the end of Union deposition and sharp lithologie change with deposition of Aiderson F o rm a tio n ...... 121
64. Changes in environmental conditions during deposition of Greenbrier units.. 122
65. A. Protoniella parvus; B. Ovatia elongata; C. Diaphragmas cesthensis; D. Echinoconchus sp...... 128
66. A. Inflatia Inflatus-, B. Orthotetes kaskasklensis ...... 131
67. A. Anthracosplrifer pellaensis-, B. Anthracosplrifer brecklnrldgensis-, C. Retlcularia sp...... 135
68. A. Composite subquadrata-, B. Clelothyn'dlnia sp.; C. Martlnia contracta . 138
69. A. Eumetria verneullana-, B. Eumetrla n.sp.; C. GIrtyella s p ...... 140
70. Brachiopod distribution per region and per fades...... 141
71. A. Archimedes sp.-, B. Fenestella sensu \a\o; C. Lyroporella sp.; D. Trepostome; E. cystoporate, f^stullpora sp...... 146
xii 72. A. Pentremites tulipaformis-, B. Pterotocrinus serratus; C. Paladin chesterensis . . . . i ...... 152
73. Foraminifera distribution per region and per facies...... 156
74. A. Endottiyrid foraminifera; B. Biserial foraminiferan ...... 157
75. A. Naticopsis (Natlcopsis) sp.; B. Straparollus (Euomphalus) sp.; C. Ostracodes ...... 160
76. Dasyciadaceans ...... 163
77. GIrvanella sp...... 165
78. Sphaerocodlum sp...... 166
79. General occurrence of calcispheres and associated aigae in ttie marine environment...... 168
80. Calcispheres ...... 169
81. Dendrogram for all regions, taxa by locality ...... 180
82. Dendrograms for taxa by locality ...... 181
83. Dendrogram for Region 1, locality by taxa ...... 188
84. Dendrogram for Region 2, locality by taxa ...... 192
85. Dendrogram for Region 3, locality by t a x a ...... 196
88. Location of Eastern Interior Basin and associated features ...... 199
87. Source areas of terrigenous elastics and general transport directions into the Eastern interior Basin and the Appalachian Basin...... 220
88. Morphotypes of Anthracosplrifer pellaensis...... 227
89. Morphotypes of Anthracosplrifer p e lla e n s is...... 228
90. External variables utilized in biometric anaiysis of Anthracosplrifer pellaensis. 229
91. Hinge by length plot for Anthracosplrifer p e lla e n s is...... 231
92. Cani X Can2 plot from Discriminant Function Anaiysis ...... 232
93. Transverse serial sections through each morphotype illustrating position fibrous nature and overall shape similarity of the cardinal process 233
94. Transverse serial sections through each morphotype illustrating position shape and overall similarity of the dental lamellae. 234
95. Transverse serial sections through each morphotype illustrating position orientation and shape of the bases of the spiraiium. 235
98. Documented occurrences of Anthracosplrifer pellaensis in the midcontinent and the Appalachian Basin...... 237
XIII 97. Occurrence of Anthracospirifer pellaensis morphotypes in the central Appalachian Basin...... 238
98. Occurrence of Anthracospirifer pellaensis morphotypes in Io w a...... 240
99. Summary of overall geographic distribution, morphotype geographic distribution and morphotype occurrence per type of substratum...... 241
100. Some currently recognized definitions of " r e e r ...... 245
101. Reef locaiity ...... 246
102. Schematic cross-section through the r e e f ...... 247
103. Reef Core facies ...... 249
104. infrareef f a c ie s ...... 250
105. Suprareef facies ...... 251
106. Reef Flank Facies A ...... 252 254 107. Reef Flank Facies B ......
108. Interreef Facies • ...... 255
109. Well preserved Afc/J/Vnedes zooaiium ...... 256 257 110. Oolite Shoal Facies * • • ......
111. Oolite Shoal Facies ...... 258
112. Paleoenvironmental reconstoiction of the reef en v iro n m e n t...... 260
113. Syringopolid coral ...... 280
114. Palaeacis s p ...... 281
XIV CHAPTER I
INTRODUCTION
Paleoenvironmental Interpretations provide a window Into the past, allowing us to see what a particular environment was like during a specific period of time. This ultimately gives us an Idea of what to expect for the future. Information Is derived from the rock units themselves, the fossils contained in them and the lateral and vertical relationships between adjacent rock units. Regional pictures are obtained by considering the relationships between stratigraphie packages from different areas.
This study of the Upper Greenbrier Group In the central Appalachian Basin (West
Virginia and western Maryland) provides a more complete history of the paleoenvironment than has previously been reported. Analysis of the sedimentology and facies distribution across the field area Indicates that depositional conditions varied considerably from north to south. The autecology of Individual organisms Is discussed and the Interpretations of their modes of life and environmental preferences further Illustrate the types of environments present. Finally, Identification of discrete faunal associations within each region of the field area support the Interpretation of changing environmental conditions throughout the field area.
This rich combination of lithologies and fossils represent a complex of depositional environments ranging from restricted marine or lagoonal to open marine, well circulated conditions, and from high to low turbulence conditions.
The purpose of this study was three-fold: 1) To evaluate the faunal associations of
Chesterian (Upper Mississippian) shallow marine environments represented In the Upper
Greenbrier Group of West Virginia and western Maryland, and compare them to coeval faunas
In continental Interior basins. This comparison would allow examination of fundamental distributional controls on Chesterian paleocommunities and. In particular, of Chesterian
1 2
brachiopods; 2) To compare the timing of marine events In the Appalachian Basin to those In
other cratonic basins in order to evaluate the dynamics of intracratonic environments; and 3)
To document complete faunal lists for the two youngest Greenbrier formations.
During the course of this study, several additional projects were carried out. Unusual
preservation of Archimedes axes and fronds provided the basis by which their use In
paleocurrent analysis could be shown. Analysis of morphologic variations In Anthracosoirifer
pellaensis illustrated how an organism can adapt to various environmental stimuli by varying
external features. Application of morphometric techniques to these brachiopods Illustrated the
presence of intraspeclfic morphologic variation. Finally, the presence of a reef In southeastern
West Virginia Indicates that organically-built framework structures do occur In the Late
Mississippian. These studies are Included as Appendices A, B and C and Chapters 6 and 7.
METHODS
Vertical sections of the youngest two formations, the Union Limestone and Aiderson
Formation, were studied at 19 localities along the length of the outcrop belt from western
Maryland to southeastern West Virginia (Figure 1; Appendix D). Field descriptions included
formation thickness, bedding thickness, lithologie characteristics, sedimentary structures, grain
size and fossil content. Each section was divided into units on the basis of vertical facies
changes.
Samples from each unit were collected, thin sectioned and analyzed for both lithologie
and faunal content. Point counts were made to more accurately describe and identify each
unit. The average grain size for each slide was determined by visual estimation. This was
then used as the Interval for grain counting. Because percentages were used for rock
identification, large grains such as shell fragments, that occupy a greater percentage of space, were counted more than once. Basic rock types were assigned using Dunham's (1962)
classification. Mudstones are mud supported and contain less than 10% grains.
Wackestones are also mud supported and contain greater than 10% grains. Packstones are grain supported and contain mud. Grainstones are grain supported and contain no mud. In ;I
,MD
f j
# Locations of measured sections \ 0 Approximate position of West Virginia Dome
^ j)p S O N & 3NION V
Figure 1; Location of measured sections in ttie Union Limestone. Grenville shale and Aiderson Formation.
CO 4 cases where a grain-supported rock had both mud and cement, It was classified as a
packstone. Modifying adjectives were added to further describe the specimens.
Fossil constituents were identified but usually not below the genus level. Faunal associations were identified based on recurring groupings. Environmental interpretations were
based on field and laboratory data collected during the course of this study and compared to
results obtained by such previous workers as Tissue (1986) and Carney & Smosna (1989).
Two statistical software packages, SAS and SYSTAT, were used in the analysis of
some data collected in this study. Cluster anaiysis of paieoecoiogicai data was performed
using SYSTAT. Using SAS, discriminant function anaiysis and principal component anaiysis were performed on morphometric data of Anthracosoirifer oeliaensis (Appendix C).
implementation of these statistical methods are more completely described in later sections.
HISTORY AND GEOLOGIC SETTING OF THE GREENBRIER GROUP
During the late Middle to Late Mississippian the Appalachian Basin and surrounding area (Figure 2) was tectonicaiiy active, undergoing subsidence to the south and uplift to the
east. This uplift shed terrigenous elastics westward (Arkie et al., 1979). The western edge of the Appalachian Mountain belt is a foreland foid-and-thrust belt, and the sedimentary rocks along the western edge of this belt provide an indirect record of this tectonic activity (Suppe,
1985). This tectonic regime was substantially different from settings elsewhere in the eastern
United States where other Mississippian (Chesterian) rocks and faunas are known. This is further discussed in Chapter 5.
The Greenbrier Group is a thick, fossiliferous, predominantly carbonate unit that was deposited in the Appalachian foreland basin, it crops out in a northeast-southwest belt approximately 170 miles long across south-central Pennsylvania, western Maryland and eastern West Virginia (Figure 3). The group was named by Rogers (1879) for exposures along the Greenbrier River in West Virginia (Lucke, 1939). According to Arkie et ai. (1979, p.
D12), "... little published work on the Mississippian of the State [West Virginia] is available . . . and most stratigraphie data in this paper are from West Virginia County Geoiogic Reports Sman I f EM - I* « I Large eubeidence • stable region mobile region
Neutral Area - Sman subsidence- stable region mobile region
SmaD subsidence 11 II SmaO uplift ■ stable region LLilI mobileI - region
Large subsidence Large iflift - stable region mobile region
Figure 2: Tectonic activity in ttie Appalactiian Basin, Eastern Interior Basin and ttie Warrior Basin. Summarized from Craig & Connor (1979).
cn ' • ' ' ■ - / I
Figure 3: Outcrop extent of Greenbrier units in West Virginia and Maryland. Redrawn from Arkie et ai. (1979). 7 published between 1907 and 1939." Most subsequent papers merely restate age relationships published in older reports (see Hickman, 1951; Leonard, 1968).
Reger (1926) described eleven formations from the thickest portion of the Greenbrier
Group in Monroe County, West Virginia. Later studies showed that several formations were local occurrences and stratigraphicaiiy useful only at southern localities (Lucke, 1939; Weils,
1950). Weils (1950) combined the Sinks Grove Formation, the Patton Limestone and the
Patton Shale Into the Denmar Formation, and the Taggard Limestone and laggard Shale into the Taggard Formation. The resulting seven formations currently recognized are listed in
Figure 4.
The Greenbrier Group is a time transgressive unit. Deposition began in southeastern
West Virginia during the middle Meramecian. Middle Taggard and younger formations are
Chesterian (Arkie et ai, 1979). The northern exposures are ail Chesterian In age (Weils, 1950;
Hickman, 1951; Youse, 1964). Exact ages of the Greenbrier units have yet to be determined.
Brachiopods, echinoderms, trilobites and foraminifera in the units indicate an upper
Mississippian age, but a finer delineation is not possible at this time.
The character of Greenbrier units varies northward and individual formations thin markediy (Figure 5). The Hilisdaie and Denmar Formations pinch out northward in
Pocahontas County, West Virginia. No lower Greenbrier units were deposited north of this point, and the remaining Greenbrier units thin substantiaiiy. The thinning is attributed to the presence of a structural hingeiine in Randolph County and the West Virginia Dome (Leonard,
1968; Yeiiding, 1984; Carney, 1987; Wuiff, herein). Both are discussed in detail later in this chapter. The stratigraphy is not well understood in north-central West Virginia where at least one worker recognized the presence of ail of the upper Greenbrier formations (Yeiiding, 1984).
Study of one section In that area did not result in stratigraphie conciusions similar to Yeiiding
(1984) (Wuiff, this study; D. Smosna, personal, commun.).
The Greenbrier Group is reduced to formationai rank in north-central West Virginia and western Maryland (Arkie et ai., 1979). Three members are recognized in north-central West
Virginia, and two have traditionally been recognized in western Maryland. However, results SYSTEM SERIES SW PA W MD NC WV SE WV
MORRO - PENN WAN POTTSVILLE FM. POTTSVILLE FM. POTTSVILLE FM. POTTSVILLE GP. ^ BLUESTONE FM. PRINCETON FM: UNDIFF'D UPPER MAUCH MAUCH CHUNK HINTON FM. MEMBER CHUNK FM. REYNOLDS LS. c BLUEFIELD FM, QC riLLVDALETHT LU H— to WYMPS ALDERSON FM. LU GAP LS. UPPER O u □C UPPER CL o LIMESTONE LIMESTONE GREENVILLE SH to MEMBER MEMBER to LOWER to UNION LS. to MEMBER MIDDLE MBR. MIDDLE MBR. PICKAWAY LS. LU TAéôAftb EM. LOYALHANNA LOYALHANNA LOYALHANNA MEMBER MEMBER MEMBER DENMAR FM.
HILLSDALE LS.
MACCRADY FM.
Figure 4: Currently recognized stratigraphie terminology (modified from Carney & Smosna, 1989). Note presence of middle member in western IVtaryland.
00 SOUTH PVG
NICG
NORTH
HF GG SHELF WEST VIRGINIA DOME MF POTTSVILLE GROUP POCONO GROUP HINGE LINE PG CF MAUCH CHUNK GROUP CHEMUNG FORMATION BASIN 1S00 40 0 GREENBRIER GROUP HAMPSHIRE FORMATION 1000 300 300 (Vert. exag. x 100) 500 MACCRADY FORMATION 100
Figure 5; Thickness trends in the central Appalachian Basin. Note erosional area near the West Virginia Dome and general southward thickening. Redrawn from Arkie et al., 1979. 10
from this study Indicate the presence of a thin middle member In western Maryland, and the
stratigraphy has been modified accordingly (Figure 4).
Greenbrier rocks reflect one of the last major marine Incursions of the Late Paleozoic.
The rocks are predominantly carbonates with substantial amounts of quartz sand and silt In
certain localities. Calcareous shales, shale, and slltstone are present In some sections.
Source areas of the terrigenous components have been Identified as the Canadian Shield and
exposed highlands to the east (RIttenhouse, 1949; DeWItt & McGrew, 1979; Yeiiding, 1984).
The faunal components represent a variety of environmental conditions ranging from high to
low energy and from open to restricted marine.
This study focused on the two youngest formations of the Greenbrier Group, the
Union Limestone and the Alderson Formation, and stratigraphicaiiy equivalent rocks northward.
Where it was exposed, the Greenville Shale was also sampled. Both the Union Limestone
and the Alderson Formation are recognized as far north as Randolph County. Just north of
the Tucker County line (In the Canaan Quarry), the Alderson Formation Is extremely, and the
presence of paleosols give evidence of subaerial exposure.
At the type section and surrounding localities In West Virginia, the Union Limestone Is
llthologlcally distinct (Figure 6). Reger (1926) described It as notably oolitic, very fosslllferous
and, at some localities, containing a middle red shaly unit. It generally has massive, lenticular
bedding and weathers white. The thickness in the south ranges from 30.5 meters to 119.5
meters (100 to ~ 392 feet). Blastolds, bryozoans, echinoderms, brachiopods, rugose corals and gastropods occur throughout the formation. This llthology Is continuous northward to
Canaan Valley. The Union Limestone Is not recognized north of this area.
The Alderson Formation contrasts sharply with the Union Limestone (Figure 6). Reger
(1926) described It as sandy and oolitic In places, dark gray weathering to a dirty yellow, and exhibiting very chippy weathering. The formation varies In thickness from 23 meters to 99 meters (75 to 325 feet). The abundant marine fauna Is not duplicated anywhere else In the
Greenbrier Group. Archimedes and Pterotocrlnus are the most common biotic components.
Brachiopods, other bryozoans, rare blastolds and other crinolds are also present. A plant 11
Figure 6: Outcrop view of entire section; Union Limestone, Greenviiie Shaie and Alderson Formation. R & R Quarry, Greenbrier Co., WV. Figure 7: Outcrop view of Greenviiie Shaie, dipping approximateiy 35“ southeast. Near Greenviiie, WV; Monroe Co., WV. 12 fossil zone occurs near the top. Typical Alderson llthologles are recognized as far north as
Greenbrier County and possibly southern Tucker County (at the top of the Canaan Valley section). No Alderson exposures were located In Pocahontas County. As with the Union
Limestone, the environmental changes In western Maryland resulted In stratigraphicaiiy equivalent units that are llthologlcally and faunally different from the type Alderson.
The Greenville Shale Is largely confined to Monroe County and, where present, occurs between the Union and Alderson Formations. Reger (1926) described It as black or dark, lenticular, fissile, calcareous and approximately 30.5 meters thick (-1 0 0 feet) (Figures 6 & 7).
Bivalves, gastropods and cephalopoda have been collected from It. The section of Greenville
Shale studied In this project Is an unfosslllferous, non-calcareous black shale. It Is at least 42 meters thick (Figure 7).
PALEOGEOGRAPHY AND TECTONIC SETTING
The sedimentation patterns and stratigraphie relations within the Greenbrier Group are a direct result of the paleogeographic position, structural configuration and tectonic setting of the Appalachian Basin during the early Chesterian.
Paleogeographic reconstructions of the Early Carboniferous by Scotese & Denham
(1988) place West Virginia and the central Appalachian Basin at approximately the paleoequator or slightly south of It. The tropical climate and warm waters formed excellent habitats for marine benthos, for the production of lime mud, and for the subsequent formation of thick limestone sequences.
Greenbrier rocks are situated on the Appalachian Plateau, the area of undeformed, sub-horizontal rocks just west of the highly folded Valley and Ridge Province (Figure 8).
Structural deformation of Greenbrier rocks occurred only In southeastern West Virginia where, as part of the Hurricane Ridge Syncline, they dip southeastward. Two structurally high areas existed during deposition of the Greenbrier Including the Cincinnati Arch and a possible area near the Blue Ridge Province In Virginia. Eustatic sea level rise In the Late Meramecian (Ross
& Ross, 1985), enchanced locally by tectonic movement In the area, caused the Greenbrier 13
I
APPALACHIAN PLATEAU
Figure 8; Physiographic map of West Virginia and adjacent Maryiand (Arkie et ai., 1979). Predominantiy horizontai rocks of the Greenbrier Group occur within the Appaiachian Piateau Province. 14
Sea to transgress northward. With advanced transgression, the sea split into two bays on
either side of the Cincinatti Arch. Southern West Virginia, eastern Kentucky and western
Virginia were submerged by the eastern bay; and western Indiana, western Kentucky and
Illinois were covered by the western bay.
Deposition of the Greenbrier Group occurred between two major orogenic events.
The Acadian orogeny occurred approximateiy 380 million years ago during the early Devonian,
it resulted from westward accretion of the Avalon terrane and was accompanied by large
scale thrusting (Windiey, 1984). The Alieghanian orogeny occurred aprroximately 300 to 250
million years ago during the Late Carboniferous - Early Permian. It was caused by the collision of Africa and North America and resulted in continent-directed folding and thrusting of the entire miogeociine along the western margin of the southern and central Appalachians
(Windiey, 1984). Tectonic activity during the relatively quiet time between these two events
(essentially the Mississippian) consisted of subsidence within the basin and uplift to the east
(Arkie et ai., 1979; DeWitt & McGrew, 1979; Carney & Smosna, 1989; Yeiiding, 1984). it is evident from the thick accumulation of limestone that terrigenous input was greatly reduced.
Paieotectonic reconstructions illustrate the subsidence history for the Late
Mississippian (Meramecian and Chesterian) (Craig & Connor, 1979, PI. 10). Three important factors affected the subsidence history: subsidence rate, the West Virginia Dome and the
38th Parallel Lineament.
Subsidence
Subsidence during the Meramecian was relatively slow along the length of the basin with one area of rapid subsidence in the southeastern-most corner. By the Chesterian, the axis of subsidence had shifted northwestward, and the entire length of the basin underwent rapid subsidence (Figure 2; Craig & Connor, 1979). The great increase in sediment thickness from north to south indicates that, although subsidence was rapid, the rate varied dramatically along the length of the basin. This is part of the explanation for the great changes in thickness from north to south. 15
West Virginia Dome
The thickness variation, plus the differences In sediment character and stratigraphie relations discussed earlier can also be explained by the presence of two structural features, the West Virginia Dome and the 38th Parallel Lineament. The West Virginia positive area, now called the West Virginia Dome (Kammer and Bjerstadt, 1986) Is situated just north of the 38th parallel lineament In Randolph County, West Virginia (Figure 9). Evidence for Its existence lies solely In sedlmentologic data. This topographic high was active from the latest Devonian through the Late Mississippian and was at times subaerlally exposed. Exposure resulted in erosion of the late Devonian Chemung Formation and was followed by an Interval of non- deposltlon of the latest Devonian/early Mississippian Price Formation (Kammer and Bjerstadt,
1986). Continued exposure resulted In erosion of older Greenbrier formations (Yeiiding, 1984;
Arkie et al., 1979), and the persistence of a topographic high resulted In severe thinning of younger Greenbrier units (Yeiiding, 1984; Carney, 1987; herein). Paleosols reported here at the top of the Greenbrier Group In Tucker County may Indicate uplift activity that occurred as late as deposition of the youngest Greenbrier units.
The West Virginia Dome also served as an effective barrier to southward transport of slllclclastic material that was being shed from the ancestral Appalachians to the northeast and from the Canadian Shield to the northwest. This material was deposited north of the dome and occurs within the basal member of the Greenbrier Formation (the Loyalhanna Limestone)
In north-central West Virginia and western Maryland (Figure 4). The Loyalhanna Limestone has a limited geographic distribution, and the West Virginia Dome as a barrier explains this restriction. The dome also served as an oceanographic barrier, restricting northward movement of water masses from the open ocean to the south. This Is discussed more fully
In a later section.
The 38th Parallel Lineament Zone
The second major structural feature Is the 38th Parallel Lineament, named by Heyl In
1972. This lineament zone extends from Pennsylvania and northern Virginia to Missouri
(Figure 9). North to south differences In sediment character and thickness of rock units 16
Figure 9: Position of West Virginia Dome and trend of the 38th Paraiiei Lineament Zone (from Heyl, 1972). 17 across this region can be expiained by the presence of the iineament which Heyi (1972) described as an "east trending zone of needy continuous fauits and intrusions that foiiow, approximateiy, the 38th Paraiiei from northeast Virginia to southcentrai Missouri."
Gardner (1915) recognized a "zone of disturbance" which ran for approximateiy 560
miies from Pennsyivania southwestward to Missouri. He recognized a series of faults and
uplifts that appeared to be connected, from the Warfield-Chestnut Ridge zone of folding in
Pennsyivania to West Virginia, through the Rough Creek Uplift in Kentucky to the
Shawneetown fault and Bald Hill Uplift in southern Illinois. Because some of these features are not prominent at the surface, Gardner concluded that the line of faulting was deep seated.
Woodward (1961) described a major fault scarp or "coastal declivity" in lower Cambrian rocks extending along a northeast-southwest trend for approximateiy 500 miles. The Cambrian rocks on the downside of this scarp are very thick. Woodward (1961) proposed the presence of a regional fault or major deformation break. Subsequent studies by Dennison & Dever
(1976), Heyi (1972) and Dennison & Johnson (1971) have confirmed these conciusions.
Regional gravity anomalies of basement rocks in Virginia, West Virginia and central and eastern Kentucky indicate a distinct and large right lateral shift along the 38th Paraiiei
(Heyi, 1972). These features delineate a wrench-fauit zone in the basement. Strike-siip faulting is the major component of movement and it appears that displacement was probably much greater in the Precambrian than later (Heyi, 1972). This fracture zone appears to have been present and sporadically active since at least 800 ga and may still be active today
(Dennison & Dever, 1976). Surficiai rocks above the zone contain igneous intrusions, flows and pyrociastic deposits of late Precambrian, Devonian, Triassic, Jurassic and Eocene age.
The alignment of these igneous rocks and the structural features discussed above mark the trend of the iineament (Dennison & Johnson, 1971, Dennison & Dever. 1976). Additionally, an examination of these volcanic rocks suggests that the iineament controlled or provided the pulses of voicanism (Dennison & Johnson, 1971). Sedimentary rocks, ranging in age from
Cambrian to Pennsylvanian, vary in distribution and thickness across the iineament. These variations are also indicative of tectonic activity along the trend (Dennison & Dever, 1976). 18
Table 1 summarizes new and previously described evidence used to support the existence of the iineament. Most important for this study are the features observed in West
Virginia. However, on a larger scale, ail are important in order to define the extent and overall effect of the 38th Paraiiei Lineament. Examination of the regional setting shows numerous domes and high points (anticlines) situated just north of the fauits in the iineament zone. The West Virginia dome Is one such high point and appears to be intimately related to the fault system. 19
Table 1: Evidence for Existence of 38th Parallel Lineament Zone
Malor Structural Features Involved (Heyl, 1972)
Stanley Fault - north-central Virginia Warfield Fault - southeastern Kentucky & southwestern West Virginia Irvine-Paint Creek Fault - eastern Kentucky Kentucky River Fault Zone - Kentucky Rough Creek Fault Zone - Kentucky Cottage Grove Fault - Illinois Big River Fault - Missouri Palmer Fault - Missouri Red Arrow Fault - Missouri (farthest west, small)
Virginia (Heyl, 1972)
1. Right lateral wrench faults cross the Blue Ridge Mountains and eastern Shenandoah Valley. 2. A swarm of Mesozoic and Tertiary Intrusions 70 miles long. 3. Tertiary Intrusions In Highland County are Interpreted to be the youngest expression of Igneous activity along the 38th parallel. 4. Stratigraphie changes across the Iineament. 5. Structural Irregularities across the Iineament.
Eastern Kentuckv and West Virginia (Calver & Hobbs, 1963; Heyl, 1972; Dennison & Dever, 1976; Colton, 1961; Woodward, 1961; Carovac and others, 1964; Arkie et al., 1979, Wuiff, this study)
1. Regional Bouger gravity anomaly patterns Indicate approximately 50 miles of right lateral offset In the basement. 2. Apparent early Paleozoic movement on the basement fault formed the northern boundary of the Rome Trough. 3. Deposltlonal thinning of Cambrian and lower Ordovician rocks northward across the Iineament zone 4. In east-central West Virginia - an east-west belt of non-deposltlon of the Price Formation; northward disappearance of Maccrady Red Beds, Hillsdale and Denmar Formations. 5. Recurrent basement fault movement In northeastern Kentucky Indicated by erosional removal of the St. Louis and Ste. Genevieve members of the Newman Limestone and upper Borden Formation members In areas on the upthrown side (northern block). 6. Continuation of an east-west sag, marked by patches of uneroded Mississippian rocks. 7. Stratigraphie changes across the structural line which Intensify westward. 8. Irregularities In the northeast-trending folds of the Cumberland Plateau as they cross the structural line. 9. Rocks of latest Precambrian age thicken south of the line (Colton, 1961). 10. Lower Cambrian rocks thicken markedly south of the line. 11. Upper Cambrian and Ordovician rocks all thin to form a stratigraphie trough along the Iineament trend between eastern Kentucky and the Warfield Fault in West Virginia. 12. Mississippian and lower Pennsylvanian rocks thicken abruptly south of the line. 13. Faults running parallel to Summerson’s Precambrian fault line (see Ohio 1.), lie to the north on trend with the Kentucky River Fault System In eastern Kentucky.
Southern Illinois (Heyl, 1972)
1. Surface fault pattern closely resembles the right lateral Osburn Fault In Idaho. 20
Table 1 (continued)
Ohio (Summerson, 1962)
1. Precambrian basement fault line runs paraiiei to the fault which cuts the Pennsylvanian. 2. Gay-Pink and Cabin Creek channel deposits in the Berea sandstone generally paraiiei the iineament and may represent westward drainage channelled along the sides of the uplift. CHAPTER II
SEDIMENTOLOGY AND FACIES ANALYSIS
INTRODUCTION
The Greenbrier Group represents one of the last major marine Incursions In eastern
North America during the Paleozoic. As described earlier, the units are predominantly carbonates with substantial amounts of quartz, calcareous shales, shales and siltstones in certain localities. As a result of the shallow shelf environment In the north, the West Virginia
Dome, and the normal marine sea to the south, the lithofacies and faunas change notably from north to south. Three regions are identified based on these changes, and the study was conducted with these three regions In mind. They are referred to as Region 1 (western
Maryland), Region 2 (north-central West Virginia) and Region 3 (southern and southeastern
West Virginia) (Figure 10).
At the localities studied, bedding In all units Is horizontal except at Greenviiie, West
Virginia where the Greenviiie Shaie dips approximately 35° southeast. The ubiquitous presence of algae (Regions 2 & 3), peloids and micritized grains Indicate deposition In shallow waters within the photic zone.
Based on pétrographie and hand specimen analyses, 62 subfacies were Identified. In an attempt to Interpret this unwieldy number. Individual subfacies were combined Into general facies based on overall similarity and abundances of aliochems and clastic grains. Care was taken to preserve all Information present In the Individual subfacles.
Several facies occur In more than one region. However when the aliochem component Is considered for ail subfacies within. It Is obvious that they do not compare environmentally or depositionaiiy and should not be combined. Additionally, the facies names are descriptive. Detailed pétrographie descriptions and original facies designations are listed
In Appendix E. The combined listing is in Appendix F. Point count data are listed in
2 1 22
n
I
h
2 W
ON
Figure 10: Approximate boundaries of Regions 1, 2 & 3. 23
Appendix G. The diagenetic aspects of these facies, inciuding euhedrai crystais of pyrite and
hematite and other non-carbonate minerais, are secondary and not important in facies
interpretations. Their presence is aiso noted in Appendix E. The term ’bioclast' refers to aii
fossil elements observed in thin section. A complete faunai listing is contained in Appendix H.
Within the overall transgression of the Greenbrier Sea, during deposition of the Union
Limestone and the Alderson Formation, only one significant change in sea level is recorded,
it occurred near the end of Union Limestone deposition and is recognized by a sequence of
paleosols at Canaan Quarry and by coarse grainstones and oolitic grainstones at other
localities. This is discussed in more detail in a later section. The development of mudstone,
wackestone, packstone and grainstone facies paraiiei to the shoreline is facilitated by local
variations in bottom topography and, to a certain extent, distribution of carbonate-producing
organisms. Washing of mud and finer particles may have been restricted in sheltered areas
(i.e., large depressions, in the lee of a shoal, etc.). in contrast, in less sheltered areas,
washing, transport and breakage of biociasts occurred. The degree of current turbulence
determined which facies types developed. Theoretically, physical parameters other than
substratum and current energy, such as salinity, temperature and oxygenation, were the same
in aii of these facies. For most of the fosslllferous facies within a region, the biociasts are
similar in thin section. Although more variation between facies occurs on the outcrop, in
general, this similarity indicates that environments were relatively uniform. As demonstrated in
the following discussions, this is important for the overall interpretation of the
paieoenvironments and history of the area. Differences in faunal abundance and diversity
from facies to facies within a region can be attributed to the original abundance of organisms
when alive, patchy distribution (common in modern environments), transport by currents and
preservational and sampling bias.
INTERPRETATION OF LITHOFACIES
Reworking of aliochems within a facies is pervasive in the marine environment. This is accomplished by bioturbation and wave and current action. However, transportation of aliochems by turbidites and storms is less common and can be more difficult to identify. 24
Distinguishing between reworking and transport can be difficuit, and the answer has great bearing on paieoecoiogic interpretation. The condition of the biociasts and the matrix and/or cement can be studied to heip in this determination.
Severai criteria may be combined in an attempt to separate reworked from transported grains, inciuding the foiiowing. The presence of micrite may indicate an absence of current transport. Ooiitic coatings, abraded grains and size sorting of abraded grains from various sources are aii indicative of current transport (Wiison, 1975). Weil sorted biociasts are aiso an indication of reworking and transportation. Terrigenous material may aiso suggest transport of the carbonate grains, although they may have been brought into the carbonate environment by wind or floating (Wiison, 1975). Rounded, abraded and broken biociasts have aii been transported to some degree. Ooids provide excellent information regarding transport and reworking. Well sorted ooids of uniform size are typically in situ. Ooiitic units with non- uniform ooids are composed of transported grains. Broken ooids are aiso indicative of transportation (Carozzi, 1989). Biociasts as ooid nuclei can cause some confusion. Few organisms live on the shoai itself but more commonly inhabit the flanks or live in the iee of the shoai (McKinney, 1979; Wuiff, 1989a, 1990c). Currents and progradation of shoals incorporate bioclastic debris into the shoai sediment, providing nuclei for ooid development.
Although they have not been transported very far, these biociasts are not representative taxa of the high energy, ooid-forming environment. The size relationship of the matrix relative to the aliochems is important. For mud deposition, low velocity currents or sheltered areas are required. This current velocity can only carry a certain grain size either in suspension or as bedioad. If the aliochems are notably coarser than the matrix, they must be relatively in situ.
Alternatively, the lateral change from a slightly shallower, higher energy environment to a mud-accumuiating facies is accompanied by a change in current velocity. Over the shoai, the current may be stronger, and the waves may rework some fossil material to adjacent areas. Baffling by grasses would result in a similar decrease in current velocity and deposition of fossils into muddy sediments. Bioturbation would incorporate these biociasts into the sediment. Thus, the fossil debris in a mudstone may not be in situ, it can aiso be 25
argued that bioturbation causes the breakage of in situ ciasts. However, the biociasts in the
mudstones studied are fairly well sorted, indicating transportation rather than just reworking.
The angularity of these biociasts can be expiained by suggesting that these siit-sized grains
were in equilibrium with the water energy and thus breakage and/or rounding did not occur
(Carozzi, 1989).
Micritization of grains is caused by the boring of biue-green aigae and subsequent
filling of the boreholes by micrite (Bathhurst, 1976). This clearly occurs within the photic zone
but, because micritized grains can be transported as any other grain, their presence must be
used with caution.
Sedimentary structures, such as cross-bedding and scour marks, are indicative of
current transport. Such structures were rarely encountered in this study. Those observed
occur only in the arenaceous units of Region 2. Because lateral facies changes are so
common in carbonate environments, key beds are not traceable or are not present and could
not be used for correlation in this study.
REGION 1 - GARRETT COUNTY, MARYLAND
Three localities are included in Region 1 ; Sang Run Quarry, Deep Creek Quarry and
Oakland Quarry (Figures 11, 12 & 13). Seven major facies are described from this region; a
detailed description of the subfacies is listed in Appendix E. The progressive change from
mudstone through grainstone to wackestone generally follows the stratigraphy of the
Greenbrier Formation and, in turn, continued transgression of the Greenbrier Sea. Lithologie
characteristics are fairly uniform at each locality. Figure 14a contains stratigraphie correlations
of the three sections sampled. Due to the extreme thickness of the section at Knobs-Union
Road, only the uppermost portion is illustrated in Figure 14a. The entire section is illustrated
in Figure 14b. Note the sharp lithologie change from the middle member to the upper member, and the differences between localities in the middle member. ' " ï V f ' è t
WJ MW • LOCATIONS OF HfASURED SECTIONS IN REGION I
O approximate POSITION OF WEST VIRGINIA DOME
%SON
V
Figure 11: Location of measured sections in Region 1. See text for details.
ro 27
t. ^ *
' V ' - s":,
-S
B
Figure 12: A. Sang Run Quarry; B. Deep Creek Quarry 28
Figure 13: Oakland Quarry Figure 14: A. Stratigraphie correiation by lithofacies and faunal content. Note grainstone at top of Union Limestone, position of paleosols, sharp change in Alderson Formation lithoiogy. B. Knobs-Union Road. Note interbedded siitstone units.
29 PLEASE NOTE:
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The following map or chart has been refilmed in its entirety at the end of this dissertation (not available on microfiche). A xerographic reproduction has been provided for paper copies and is inserted into the inside of the back cover.
Black and white photographic prints (17" x 23") are available for an additional charge.
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f- r — 9 _Q e z _2 0 0 0 a G » Q_ C (A T) T n T o T e T <* 'IT o — » » m üfiü 1 l it SI P T r k •!n i 7^5 y - » - — u . - r % - < ê .-_ o [ ï l 31 i m i x % n , k L r . , K l 7 ~ b'btr. h - 1- k P l - - - ^ - o Z T e S ■^r r h h ë z e K î b k l 3 E S H 1 S E E É E EEEEE I k l K l - k l - k b t-E E E E .r .r.h .kl 7 K - - - i FTTFKT hkbbb r b b k m I y : , h k h h ■ a o f f i S P r .r .E Z? 3 n Ç b ^ b .kb H t E E T ^ Figure 14b I u F )ta£atQ±i t t f j b ) ) ) ) ) ) j ) ) o ) ) ) ) ü r ) ) GO ) ) ) ) * ) ) lèni&hiiKtlii! « * ) ) HUIKMHI ) % ) > $ ) )_ ) )» ) ) ) » — ) Bififfli 32 MUDSTONES Bioturbated Mudstone (Figure 15) Description: This facies occurs in the middle member of the Greenbrier Formation. It is thinly bedded, weathers shaiy and chippy and is 1.5 m thick. The matrix is heavily bioturbated micrite with common silt to coarse silt-sized quartz. The swirled pattern of the grains is interpreted to be bioturbation. Rare bivalve molds were observed on outcrop, interpretation: The fine grained nature of the bioturbated mudstone facies indicates a low turbulence setting or deposition in a sheltered environment. The abundant quartz silt was most likely derived from reworked Loyaihanna Limestone directly beneath this unit. The homogeneity of the sediment is due to an active, soft-bodied infauna. The absence of a substantial shelly benthos is notable and suggests inhospitable conditions. This was most likely caused by the West Virginia Dome, which interfered with both the northward flow of nutrient-laden and normal salinity water masses and southward reflux off the shelf. This would have caused restricted circulation and possible fluctuations in salinity and temperature levels. An unstable substratum due to an active infauna may also have prohibited sessile benthos from settling successfully. This can be termed "biological bulldozing" (Thayer, 1983). Ostracode /Calcisohere Mudstone (Figure 16) Description: This facies occurs near the top of the middle member. It is thinly bedded, contains shale partings, weathers nodular and chippy and is 1.5 m thick. The matrix is a highly bioturbated, dense micrite. The unit at Sang Run has abundant microspar and possible pseudospar. Quartz sand is common to abundant in one unit. Disarticulated ostracodes and calcispheres are abundant to common, and benthic foraminifera are common. Brachiopod shells and spines, bivalves, triiobite fragments, peimatozoan debris, gastropods and algae are rare in thin section. These biociasts are sand to silt-sized and subanguiar. A sparse macrofauna is represented by one gastropod, fenestrate bryozoan fragments and brachiopods. Interpretation: This facies was also deposited in quiet waters. With the exception of the faunal change, the sedimentoiogic conditions under which this facies was deposited do not differ from that of the Bioturbated Mudstone Facies. The bioturbated matrix indicates the 33 Figure 15: Bioturbated Mudstone Facies, x 25; unit DC-0. Field of view for 25x magnification equals approximately 4.2 mm and for 63x magnification equals approximately 1.3 mm. 34 Figure 16: Ostracode/Caicisphere Mudstone Facies, x 25; unit DC-1. 35 presence of an active infauna. The appearance of biociasts impiies some change in physicai environmental conditions. Calcispheres are common to abundant in lagoonal settings (Wilson, 1975; Fiugel, 1987; Brasier, 1980; Wray, 1977). Ostracodes, although widespread, are commonly present in lagoonal settings as well. The combination of these two euryhaiine organisms, plus the general absence of non-ostracode shelly benthos representing a normal marine environment, gives ample evidence that this facies was deposited in an inhospitable environment. Conditions in such an environment imposed stress on the organisms present. Other invertebrate biociasts are rare and are equal to or slightly larger than the matrix. They may be the remains of eurytopic individuals capable of living in this environment or, as discussed above, may have been washed in from an adjacent facies. The infauna was most likely tolerant of these inhospitable physicai conditions. WACKESTONES Fossiliferous Wackestone (Figure 17) Description: This facies occurs throughout the upper member and is notably more fossiliferous in the uppermost portion of the Greenbrier Formation. Bedding is thick to massive. Units exhibit chippy, dimpled and nodular weathering, thin shaiy partings and range in thickness from 1.4 m to 4.0 m. The matrix is predominantly micrite and is dense and somewhat clotty where it is associated with clusters of biociasts. Microspar is rare to abundant and occurs around biociasts as well. Quartz silt is rare to abundant in the Sang Run units and polycrystaliine quartz is rare. Silt-sized pellets and peloids are common, and carbonate grains are abundant. Endothyrid foraminifera dominate the microscopic biota. They are second in abundance to the carbonate grains. Sand-sized brachiopod spines and shell fragments, bivalves, bryozoans, peimatozoan debris, tubular algae (abundant in one unit), calcispheres and ostracodes are common to rare and occur in one or more units. Macrofaunai elements collected on outcrop are productid brachiopods, gastropods, rare trilobites, scattered bryozoans and peimatozoan debris (large in upper Greenbrier units). Unit 0 0 -7 contains the most diverse fossil assemblage in western Maryland and contains eight 36 Figure 17: Fossiliferous Wackestone Facies, x 25; unit OQ-1. Note endothyrid foraminifera, and bivalve shells. 37 brachiopod species, Paladin chesterensls. fenestrate bryozoans (Archimedes^, trepostome, cystoporate and rhabdomesonid bryozoans, bivalves and echinoid spine base plates. Interpretation: This facies was deposited in moderately turbulent waters. Biociast breakage may be due to increased energy or bioturbation. Quartz silt was derived from the Loyaihanna units below and possibly washed in from shallower areas closer to the West Virginia Dome. The increase in endothyrid foraminifera may indicate additional changes in environmental conditions. However, endothyrids are hardy organisms and may have been tolerant of the somewhat stressful conditions under which they were living (McKay and Green, 1963). The increase in biociast abundance and diversity suggests a change in environmental conditions. Calcispheres and ostracodes still dominate the preserved biota, indicating that lagoonal conditions still prevailed. Organisms representing a more normal marine fauna are more abundant both in thin section percentage and on outcrop, but abundance is still quite reduced from what would be expected in a fully normal marine environment. The fauna in unit OQ-7 indicates a different scenario. The increase in abundance and size of upper-tier suspension feeders, such as bryozoans and pelmatozoans, in addition to the fauna already present in the older units, show that the environmental conditions were becoming more open marine. PACKSTONES Foraminifera-Rich Packstone (Figure 18) Description: This facies also occurs throughout the upper member. The units are either thin to medium bedded with shale partings or thick bedded to massive. They range in thickness from 0.7 m to 1.9 m. Weathered surfaces are littered with biociastic debris. The matrix varies among units and is coarse micrite with abundant quartz silt, or micrite or microspar with scattered areas of calcite spar as void fillings. Fine- to medium-sized crystals of caicite spar occur intergranuiariy in one unit. Another unit is highly bioturbated. Endothyrid and other foraminifera dominate the biociasts in ail but one unit where triiobite fragments dominate. Brachiopod shells and spines, fenestrate bryozoans, peimatozoan debris, trilobites, bivalves, tubular aigae and possible calcispheres are common to rare. These biociasts are gravel to 38 M# B Figure 18: Foraminifera-rich Packstone. A. Unit DC-4, x 25; foraminifera, bryozoan fragments, brachiopod sheiis and spines. B. Unit OQ-3, x 25; rare biserial foraminifer, caicispheres. 39 sand sized and are larger in the younger Greenbrier units. Macrofauna consists of abundant brachiopods (6 genera), gastropods, triiobites, fragments of fenestrate bryozoans and peimatozoan debris. Interpretation: Deposition of this facies occurred under conditions similar to those in the Fossiiiferous Wackestone Facies. Presence of limited caicite cement suggests some washing of mud in waters of either higher turbulence or in iess-sheitered areas. The faunai components are similar to those in the Fossiiiferous Wackestone Facies, further illustrating the similarity in environmental conditions. The large size of the biociasts indicates little or no transport. The lagoonai indicators are much reduced in abundance, although other invertebrates are not overly abundant. Again, the fauna suggests conditions that were less stressful than those that existed during middle member deposition. However, the absence of large, in situ upper tier suspension feeders such as peimatozoans, bryozoans and corals, indicate that conditions were still not completely open marine or that the conditions were sufficiently unstable so that a trophicaiiy diverse community could not develop. GRAiNSTONES Foraminifera-Rich Grainstone (Figure 19) Description: This thin- to thick-bedded facies also occurs in the upper member and has nodular weathering, individual units range in thickness from 0.35 m to 1.65 m. Caicite spar occurs as intergranuiar fine to medium mosaic crystals and as syntaxiai rims. Finer crystals surround the pellets and biociasts. Micrite intraciasts and translucent micrite peioids are common and carbonate grains are abundant. Foraminifera are abundant and dominant among the biociasts. Calcispheres are second in abundance and common. Brachiopod spines and shells, ostracodes, bivalves, peimatozoan debris, gastropods, triiobites, bryozoans and echinoid spines are rare to common. The calcareous algae Sohaerocodium sp. is rare. Ail biociasts are sand-sized and rounded, many have micrite envelopes. Macrofaunai components vary in diversity and abundance between units. Collectively they include 40 B Figure 19: Foraminifera-rich Grainstone. A. Unit DC-2, x 25; foraminifera, peimatozoan debris, peioids. B. Unit DC-3, x 25; foraminifera, dasycladacean aigae, peioids. 41 peimatozoan debris, brachiopods, gastropods and the trilobite Paladin chesterensls. All are abundant on weathered surfaces. Interpretation: This facies represents deposition In waters of high enough turbulence to wash away all mud. The Invertebrate fauna Is the same as that In the packstones and wackestones and In fact has a greater number of calcispheres and ostracodes than the previously described facies. The other biociasts are low In abundance, suggesting that overall conditions were not completely open marine and unstressed. Additionally, the rounded condition and micrltlzed edges indicate some reworking and possible transport from an adjacent facies. The dominance of the fauna by endothyrlds Is explained by the fact that although they are cosmopolitan, they are best adapted to higher energy environments (McKay & Green, 1963). Brvozoan-Rlch Grainstone (Figure 20) Description; This facies occurs In the uppermost portion of the Greenbrier Formation and Is one of the youngest units sampled in Region 1. It Is medium to thick bedded, 2.75 m thick and the thinner beds are essentially shell pavements sandwiched between thicker beds of bloclastic hash. Caicite spar occurs Intergranularly and syntaxiai rims are abundant. The cement In the entire unit has been heavily recrystalllzed to coarser cement. Quartz and pyrite silt are rare and fine-sand sized peioids are abundant. Bryozoans (non-fenestrate) dominate the bloclastic component and are abundant. Shell silvers and peimatozoan debris are abundant as well. Brachiopod spines are common; triiobites and foraminifera are rare. These biociasts are gravel to sand sized and subangular. Interpretation: Deposition of the facies occurred under conditions similar to units OQ-4 and 0 0 -7 . The unit is stratlgraphlcally equivalent to unit 0 0 -7 . This unit was deposited at the height of Greenbrier Sea transgression and the deposltlonal environment has been Interpreted as open marine (Carney & Smosna, 1989; Tissue, 1986; Wulff, this study). Here, under turbulent conditions, lime mud was washed while biociasts were broken and redeposlted as bloclastic hash. The shell pavements may be storm lags. Bryozoans are upper tier suspension feeders, and the large size of biociasts and bryozoan fronds on the outcrop 42 Figure 20: Bryozoan-rich Grainstone. Unit SR-5, x 25. 43 indicate that these are in situ. Rugose ocrais and rare crinoids have aiso been described from this facies (Tissue, 1986). The facies represents deposition in open marine waters. Fossiiiferous Grainstone fSheil iao) (Figure 21) Description: This facies is confined to Oakland Quarry and consists of thin (2 cm thick) layers composed entirely of whole shell and bloclastic debris. Unfossiiiferous green shale interbeds occur above and below these grainstones. Unit thicknesses range from 0.75 m to 1.2 m. Caicite spar is present as aphano- to fineiy-crystaiiine intergranuiar cement and as syntaxiai rims. Carbonate grains are abundant. Gravel to sand-sized non-fenestrate bryozoans, peimatozoan columnals and brachiopod spines are common to abundant. The macrofauna is diverse and moderately to poorly preserved. Six brachiopod species, plus many unidentified juvenile brachiopods, fragments of rhabdomesonid bryozoans, Archimedes sp. and other fenestrate bryozoans, large peimatozoan columnals and rare rugose corals were collected on outcrop. Interpretation: The grainstone-shaie couplets represent storm generated deposits (see Kreisa, 1981). The shale represents the waning phase of the storm and/or ambient conditions between storms. The grainstones are storm lags that were either deposited in the higher turbulence stages when only the coarser components could settle out, or they are composed of those biociasts that were not picked up and were just moved about on the sea floor as the fines were washed away. With the exception of the grading from grainstone to mudstone, no other sedimentary structures are present. The fossil material both in thin section and outcrop is the same as that in younger units at Oakland and Sang Run quarries indicating that the depositionai conditions prior to storms were the same as for the Fossiiiferous Wackestone Facies. Foraminifera are absent from this higher energy facies, possibly because as light particles, they were carried away during the storm and redeposited elsewhere. INTERPRETATION - REGION 1 - WESTERN MARYLAND The depositionai conditions of the Greenbrier Sea in Region 1 represents a gradual change from a shelf lagoon or restricted shelf environment to slightly less restricted and then 44 Figure 21 : Fossiiiferous Grainstone (Lag). Unit OQ-4, x 25. Fenestrate & other bryozoans, peimatozoan debris, brachiopod sheiis and spines. 45 to open marine. The mudstones of the middle member represent the most restricted phase when the environment was quiet and inhospitable to most marine organisms. The second phase, deposited in a slightly less restricted environment, is represented by the various fossiiiferous wackestones, packstones and grainstones of the upper member. The wackestone, packstone and grainstone facies appear to represent the same depositionai conditions with variations in bottom topography accounting for the differences in mud accumulation and bioclast distribution. Therefore, the facies of the upper member described above do not represent any significant environmental or sea level changes but simply differences in local topography. The iithofacies described above suggest that these limestones formed in a shallow, open marine environment. But the fauna suggests that some modification needs to be applied to this interpretation. Organisms that inhabited open marine/normal marine environments include brachiopods, echinoids, crinoids, nautiloids and ammonites plus individual genera from other fossil groups (Wilson & Jordan, 1983). The fauna in these rocks is dominated by ostracodes, calcispheres and endothyrid foraminifera. it is not until deposition of the youngest Greenbrier units that abundant upper tier suspension feeders appear in addition to the fauna already described. This biota represents a restricted shelf facies or shelf lagoon (see Wilson, 1975; Enos, 1983). Table 2 is a list of Mississippian organisms that commonly occur in lagoonai settings. The biota from Region 1 is clearly comparable (Appendix H). Carney & Smosna (1989) presented one interpretation of Greenbrier paieoenvironments, illustrating a restricted gulf for early Greenbrier units such as the Loyaihanna and open marine conditions for later Greenbrier units (i.e., upper member) (Figure 22). However, based on the lithologie and faunai evidence discussed above, this area is here interpreted to have remained restricted until deposition of the youngest units in the Greenbrier Formation (Figure 23). The restricted setting can be attributed to two factors, the West Virginia Dome and the broad, shallow carbonate platform upon which the Greenbrier Formation was deposited. As a 46 Table 2: Some common Mississippian taxa in restricted shelves, bays, and lagoons. (James, 1983). Organisms in parentheses are groups or genera with broader écologie ranges but which are common In restricted environments. Algae Blue-green aigae Oncoids (Glrvanella) Dasyciads Foraminifera Parathurammlna (Endothyrlds) Stromatoporoid Amphlpora Sponge Chaetetes Bryozoan (Cryptostomes) Brachiopods Lingula Orbiculoldea Chonetes Composlta Molluscs (Gastropods) (high spired) (Euphemltes) (Bellerophon) (Aviculopecten) (Schlzodus) (Megaiodonts) Arthropods Rhabdostlchus ostracodes Trace Fossils (Rhizocorallum) (Chondrites) 47 LOWLANDS LOWLANDS TIDAL MUD FLAT A RESTRICTED GULF RESTRICTED GULF J OPEN GULF OOID SHOAL BASIN 100 OPEN MARINE FLOODED OOID SHOAL BASIN 100 Figure 22: A. Paleogeography of the open gulf and associated environments, Stage 2 (Chesterian): B. Paleogeography of the centrai Appalachian Basin following transgression of the Greenbrier Sea, Stage 3 (Chesterian). Redrawn from Carney & Smosna, 1989. LOWLANDS APPALACHIAN HIGHLANDS Extent of field area PALEOSHORELINE West V irginia Dome Region 1 - restricted to sem i-restricted shelf lagoon Region 2 & 3 - open marine normal marine conditions T id a l mud f l a t Figure 23: Inferred paieoenvironments of ttie centrai Appalachian Basin during deposition of the upper Greenbrier units. (Tidal mud flat enviroment information from Carney & Smosna, 1989; western boundary of basin estimated). .p» 00 49 topographic high, the West Virginia Dome served as a barrier to southward transport of quartz sand, thus iimiting the areai distribution of the Loyaihanna Limestone (see discussion in Chapter 1). it is possibie that the Dome aiso restricted northward movement of water masses from the open ocean to the south thus iimiting the exchange of normai saiinity waters with the water on the sheif. Southward refiux of water was aiso iimited. The frictionai effects of iarge water masses over shallow wide shelves aiso caused restriction in circuiation (see Wiison, 1975, Enos, 1983). These two factors are interpreted to have caused a severe restriction in circuiation, which. In turn, may have caused an increase in temperature followed by an increase in evaporation rates and a rise in saiinity. A depletion in oxygen may aiso have occurred. Any influx of water in a sea this shallow and restricted would aiso have caused fluctuations in both saiinity and temperature, adding further to the stress imposed on the local fauna. The exact nature of the stress to organisms in the Greenbrier Sea is not easily determined. Depleted oxygen was a reasonable first hypothesis based on the discussion of restricted circuiation above. Shales from the middle member at Deep Creek Quarry are dark, but an analysis of the total organic carbon yielded low values, suggesting abundant aerobic activity (see Barker, 1979) (Table 3). Therefore, oxygen was readily available In this environment. The absence of primary evaporites such as dolomite or anhydrite indicates that hypersaiinity was not the cause of the environmental stress. The available evidence is consistent with the hypothesis that environmental stress was simply due to a moderate fluctuation of temperature and saiinity caused by the shallow sheif and the West Virginia Dome, as discussed above. A contributing factor may aiso have been an active infauna and resulting instability of the substratum (Rhodes & Young, 1970). Open circuiation shelf lagoons and restricted lagoons were described In detail by Wiison (1975) and Enos (1983). Table 4 contains a summary of the important points of these two environments. The iithofacies and fauna in Region 1 are very similar to these idealized models. Comparison of Table 4 to the sedimentoiogic and biologic characteristics of the 50 Table 3: Total Organic Carbon Total Carbon C02 TOC % Bioturbated Mudstone (DC-0) 0.74 0.27 0.47 Ostracod/Calcisphere Mudstone (DC-1) 4.56 4.22 0.34 Greenville Shale (G-1) 1.54 0.02 1.52 Greenville Shale (RR-1) 2.21 0.51 1.69 51 Table 4: Characteristics of standard facies belts and environments Shelf Lagoon (Wilson, 1975) Location: Behind the outer piatform edge Water Depth: 10’s of meters Salinity: Normal to slightly higher Circuiation: Moderate Sediment: Texturally varied; large amounts of lime mud. Limestone & lenses or thin beds of iand derived ciastics; Grainstones to mudstones; Light to dark in color; Lenses of lime sand commonly contain sheliy and anguiar fragments; Bioclastic wackestone & biostromes may develop; Medium to platy bedded, may be nodular or wavy; Burrowing and peiieting common; If terrigenous ciastics are present, usuaiiy in weii defined beds & are intercaiated with limestone units Fauna: *Biota generally abundant molluscs, sponges, arthropods, foraminifera, algae *Patch reefs ^Marine grasses *Stenohallne forms, other than normal marine organisms, are absent ^Normal salinity organisms are present but reduced in number brachiopods, cephaiopods, echinoids, red algae Restricted Shelf (Enos, 1983) Location: Any part of a continental shelf or island Water depth: "Shallow" Saiinity: Abnormal - higher or lower Circuiation: Slow; Depletion of oxygen & nutrients, temperature fluctuation; Low energy - littie mechanical abrasion & reworking; Causes of restriction: Reefs, isiands, skeletai or ooid shoais or damping effect of vast expanses of shaiiow water Sediment: Dominantiy muddy & contains organics, pyrite & evaporites; Limited number of grain types; Carbonate or terrigenous mud; Fecal pellets, peioids, grapestones, intraciasts & limited range of skeletal components Environmental Interpretation: Facies Mosaic: Random lithologie changes, very shaiiow water where minor changes in sea level or depositionai topography can cause significant changes in environments Facies Prosaic: 10’s to 100’s km wide, 1000’s km^ with very little internal facies differentation; lime mudstones, muddy peioidal packstone & wackestone, foraminifera wackestone Fauna: ♦Depauperate ♦Low diversity, high abundance Benthic foraminifera, ostracods, gastropods (particularly high spired), bivalves, algal oncoids, serpulid worms, lingulld brachiopods ♦Reduced size, aberrant growth forms 52 Table 4 (continued) Standard Microfacies 1. Whole sheiis in micrite 2. Bloclastic wackestone* 3. Coated grains in micrite 4. Foraminifera-dasyciad grainstone* 5. Peioidal grainstone (locally with ostracods & foraminifera)* 6. Grapestone-peioid-intraciast grainstone 7. Foraminifera or dasyciad grainstone with peioids* 8. Laminated to bioturbated pellet mudstone or wackestone (locally with fenestrai fabric) 9. Homogeneous, unfossiiiferous mudstone (with possible gypsum crystals) * occurs in Greenbrier Units Winnowed Edge Sands (Wilson, 1975) Location: At the edge of the piatform, shoreward of the foresiope Water Depth: 5-10 meters Circuiation: High energy, weii oxygenated Sediment: Grainstones - calcareous or doiomitic lime sands; Predominantly light colored; Often cross bedded, small unconformities common (due to periodic exposure) Aiiochems: rounded biociasts, fairly well-sorted, some coated, oolitic, quartz sand may be present Fauna: *worn/abraded coquinas of organisms which lived in adjacent facies (le: foresiope, reef) *Few indigenous organisms, shifting substratum makes it very inhospitable to benthic organisms Standard Microfacies 1. Coated & weii worn bloclastic grainstones * 2. Coquina shell hash 3. Onkoidai bloclastic grainstone 4. Lag breccia 5. Oolites * Open Shelf/Open Marine Neritlc+ (Wilson, 1975) Location: Seaward of the foresiope and reef Water Depth: 10’s to 100’s of meters; below normai wave base but intermittentstorms affect bottom sediments Saiinity: Normai marine Circuiation: Good current circuiation, generally weii oxygenated Sediment: Very fossiiiferous limestone, interbedded with marl, weii segregated beds. Siitstone & shale commonly interbedded with limestones in clearly segregated layers. Range in color from gray, green, red & brown, due to variable oxidizing & reducing conditions. Quartz silt common. 53 Table 4 (continued) Much pelleting of micrite matrix, bloclastic & whole fossil wackestone, winnowed bloclastic grainstone & coquinas, some caicisiltite. Sediment thoroughiy burrowed, beds homogenized, thin to medium, wavy to nodular beds, ball & flow structures common in argiliaceous limestone, surfaces often show diastems, lag concentrates of fossils; mud mounds & pinnacle reefs occur. Fauna: Very diverse, shelly fauna indicating normal marine salinity. Infauna & epifauna present. Notable presence of stenohallne forms such as: brachiopods, corals, cephaiopods & echinoids. May not be abundant in piaces but generaiiy present. Standard Microfacies 1. Microbiociastic caicisiitite 2. Whole shells In micrite 3. Biociastic wackestone* 4. Coated grains in micrite* + No modern environment for this type of sedimentation exists. Interpretation is based mainly on the rock record. The facies is very similar to Beit 7 which occurs "inside" a shelf margin barrier. Distinction between the two is important but at present, Wilson (1975) Is unclear. 54 Greenbrier Formation in western Maryiand supports the piacement of these facies in an environment somewhat transitionai between these two iagoonai facies. REGION 2 - NORTH-CENTRAL WEST VIRGINIA Region two contains six localities: Canaan Quarry, Roaring Creek, U. S. Route 33, Butcher Quarry, Monterviiie Quarry and Kenton-Meadows Quarry (Figures 24 - 27). Stratigraphie correlations are illustrated in Figure 14a. Ail are situated close to the West Virginia Dome. With the exception of the shoreline to the north, this area represents the shallowest part of the Greenbrier Sea. Few body fossils, abundant ooids and quartz sand suggest high energies and shaiiow water. As discussed previously, this localized shallowing was a direct result of the presence and periodic uplift of the West Virginia Dome. The inferred provenance of most of the quartz and associated minerals was the exposed highlands to the east (Rittenhouse, 1949; Youse, 1966; Arkie et al., 1979). Secondary sources were reworked sediments on the West Virginia Dome and from the sandy Pickaway Formation below the Union Limestone. The Canadian Shield may aiso have supplied siiiciciastics. However, it is unlikely that any would have been transported south of the West Virginia Dome. An unconformity was described at the base of the Greenbrier Formation (Kammer & BJerstedt, 1986), and the Greenbrier sits directly on the early Mississippian Price Formation. Thirteen diverse facies from this region are described herein. Detailed pétrographie descriptions and point counts are listed in Appendices E & G. In contrast to Region 1, these facies do not occur in any order and the same stratigraphie interval may contain different facies suites. MUDSTONES Arenaceous Fossiiiferous Mudstone (Figure 28) Description: This facies exhibits medium to thick bedding with styioiites, cherty concretions and cross-bedding (where quartz is more abundant) in some units, individual units range in thickness from 0.62 m to 4.13 m. The micrite matrix is abundant, massive and bioturbated. Microspar and scattered dolomite rhombs occur in nearly ail units. Dolomite has completely LOCATIONS OF MEASURED SECTIONS IN REGION 2 a #O APPROXIMATE POSITION " OF WEST VIRGINIA DOME V Figure 24; Location of measured sections in Region 2. See text for details. C Jl U1 56 B Figure 25: A. Canaan Quarry; B. Roaring Creek 57 A 1 # 6 3 : B Figure 26: A. U.S. Route 33; B. Butcher Quarry 58 B Figure 27: A. Monterviiie Quarry; B. Kenton-Meadows Quarry 59 B Figure 28: Arenaceous Fossiiiferous Mudstone. A. Unit M-1, x 25; B. Unit KM-2, x 25, note ostracodes. 60 replaced the micrite In two units. Angular to subangular, silt- to sand-sized quartz Is common to abundant In all units. Pyroxene, hematite, rock fragments, pyrite and zircon are rare to common in one or more units. Rare micrite Intraciasts, carbonate grains, peioids and stringers of pellets occur In the Monterviiie and Butcher Quarry units. Invertebrate biociasts are of low diversity and of variable abundance, except at Kenton-Meadows Quarry where they are rare. Brachiopod shells, peimatozoan debris, ostracode valves, foraminifera, calcispheres and tubular algae, are rare to common In one or more units. These biociasts are gravel to sllt-slzed and subangular to angular. Macrofauna Is only notable In unit M-1 where abundant, articulated brachiopods from three genera, 1 bivalve genus and fenestrate bryozoans were collected. Interpretation: This facies was deposited In a low energy, quiet environment. The fauna Is similar to that of the lower portion of the upper member In Region 1 and seems to represent a somewhat open marine environment. Low density particles such as calcispheres and ostracodes may have easily been transported southward from Region 1. Upper tier suspension feeders are absent. The abundance of fine lime mud and lack of a suitable substratum may have prevented these organisms from successfully colonizing. However, modern brachiopods such as Notosarla nlorlcans and Waltonia Inconsolcua are able to live at the sedlment/water interface In rather turbid conditions (M. Rhodes, personal commun.). The brachiopods present In these facies were most likely capable of the same. Fossiiiferous Dolomitlzed Mudstone (Figure 29) Description: This facies is distinguished from the previous one by the absence of quartz and an increase In bloclast diversity. Bedding Is thin to thick and Individual units are 0.15 to 1.6 m thick. The matrix, originally micrite, has been diagenetlcally altered to dolomite. It Is common to abundant and massive. Sand-sized bloclastic Intraciasts are rare to common. Peimatozoan debris, fenestrate bryozoans, brachiopod shells, ostracodes? and foraminifera are abundant to common. The biociasts are all broken and subangular. Abundant peimatozoan debris was collected from one unit on outcrop. 61 B Figure 29: Fossiiiferous Dolomitized Mudstone. A. Unit M-4, x 25; B. Unit M-2, x 25. 62 interpretation: This facies was deposited under conditions simiiar to those of the Arenaceous Fossiiiferous Mudstone. The mud matrix indicates that environmentai turbulence was low. The source of siiiciastic material may have been temporarily shut off, thus explaining the absence of quartz sand in these units. Alternatively, a barrier may have prevented its transport into the area at this time. As in the previous facies, the substratum may not have been conducive to successful colonization. The low abundance and relatively small size of biociasts in these units, plus the general low diversity, suggests that they were transported in from an adjacent fossiiiferous facies. Arenaceous Micaceous Mudstone (Figure 30) Description: This facies is restricted to the uppermost portion of Canaan Quarry in what is probably oldest Aiderson Formation. The unit has very thin bedding, is laminated, weathers chippy and fissile and is approximately 3 m thick. The matrix is micrite with very abundant quartz and hematite silt. Mica flakes are abundant and, in a general way, are aligned parallel to bedding. No biociasts were observed in thin section nor collected on outcrop. Interpretation: The lithoiogy represents continuous deposition in a quiet environment. The undisturbed laminae indicate the complete absence of any infauna, and the paleosoi facies directly below suggests that this facies was probably deposited in very shaiiow water. The Greenbrier Sea was at its shallowest during this time and erosion may have been extensive. WACKESTONES Fossiiiferous Wackestone (Figure 31) Description: The units in this facies are thin to massively bedded and in piaces, lumpy. The matrix is either dense, fine, clotty dismicrite or microspar, it is abundant and bioturbated. Anguiar to subangular, silt-sized quartz is common to rare. Silt-sized pyroxene is common to rare in one or more units. Micrite intraciasts with sparry grains and algal coatings are abundant to rare; peioids are common. Sand-sized endothyrid foraminifera, biseriai foraminifera, trilobite fragments, peimatozoan debris, bryozoans, shell silvers, tubular aigae and brachiopod spines are abundant to common. Many biociasts have micrite envelopes and 63 Eaassiïiï Figure 30: Arenaceous Micaceous Mudstone. Unit CQ-10, x 25. Eiongate grains are mica, bright grains are quartz. 64 Figure 31 : Fossiliferous Wackestone. Unit M-7, x 25. Foraminifera, ostracodes, peioids. 65 most are broken and subangular. Brachiopods, rare gastropods, rugose corals, rare triiobltes, tiny pelmatozoan debris and bivalves were collected on outcrop. Interpretation: Deposition occurred in waters of moderate to low energy. Bioturbation produced the ciottiness and caused the formation of the dismicrite fabric and possible breakage of biociasts. Dismicrite may be formed by bioturbation and subsequent void filling by caicite cement (Folk, 1959). Quartz is lower in abundance than in the Arenaceous Mudstone and may represent restriction of source area or simply less quartz supplied to the area. Due to the possibility of transportation, it can not be determined whether the algal encrustation of the intraciasts occurred before or after deposition in this environment. The biotic component is slightly more diverse than the mudstone units in Region 2, and the iagoonai forms are absent. The eurytopic nature of endothyrids is illustrated by their abundance in this lower turbulence environment. Because iagoonai and restricted shelf faunas are absent from this facies, a normal marine environment is inferred. However, the absence of upper tier suspension feeders suggests that this facies can best be compared to the middle member fauna of Region 1. Arenaceous Wackestone (Figure 32) Description: The bedding in this facies ranges from thin and somewhat flaggy, to thinly laminated with limestone nodules and concretions, to massive with cross bedding. Thickness of individual units ranges from 0.6 m to 2.2 m. Much of the reddish brown coloration in some units is due to weathering and alteration. The matrix is predominantly microspar with variable amounts of micrite In some units. The matrix of one unit is ail micrite whereas another has a pseudospar matrix, in ail units, the matrix is abundant and massive. Abundant, angular to subangular quartz sand is the most dominant non-carbonate grain. Piagiociase, poiycrystaiiine quartz, pyroxene, pyrite, zircon, augite and hematite are abundant to common in one or more units. Peioids are abundant to common in most units, micrite pellets are very abundant in one unit. Sand-sized foraminifera, bryozoan fragments, pelmatozoan debris and shell silvers are abundant to rare. One unit (33-7M) contains elongate ovals (burrows?) filled with sediment that is finer material than the surrounding 66 Figure 32: Arenaceous Wackestone. A. Unit B-8, x 25; B. Unit 33-7m, x 25. 67 matrix. No macrofauna, except for tiny pelmatozoan debris in one unit, was collected. Interpretation: This facies is predominantly from U.S. Route 33 and Butcher Quarry, localities that are almost directly over the West Virginia Dome. The amount of mud suggests that environmental turbulence was relatively low. As in the fossiliferous mudstone, the faunal abundance and diversity is so low that little, if any, fossil material is likely to be in situ, it appears that the increase in siliciclastic material may have prevented organisms that were sensitive to increased turbidity from successful settlement. PACKSTONES Arenaceous fFosslllferousi Packstone (Figure 33) Description: Bedding in this facies ranges from medium to thick with variously occurring cross-bedding, undulose beds, shale interbeds and ripple marks. Individual unit thickness ranges from 0.26 m to 5.5 m. Caicite spar is dominant as intergranular mosaic crystals and syntaxial rims. Microspar, micrite and hematite cement are rare to common in some units. Abundant, subangular, sand- and silt-sized quartz grains dominate the non-carbonate component in all units. Zircon, pyroxene, piagiociase, augite and hematite are rare to common in one or more units. Poiycrystaiiine quartz and rock fragments are rare. Peioids, oolds and intraciasts are abundant to rare. Sand-sized foraminifera, pelmatozoan debris, bryozoans, shell slivers, sponge fragments, brachiopod spines, echinold spines and trilobite fragments are abundant to common in one or more units. Trace fossils were observed on outcrop. Interpretation: This facies was deposited under higher energy conditions than previously described Region 2 facies. Cross-bedding, ripple marks and the decrease in mud all indicate increased turbulence in shallower water. The diversity and abundance of the fauna indicates normal marine conditions although the absence of fossils on the outcrop may imply transportation of various bioclasts into this facies. It is also possible that the high siliclastic component may have limited certain benthos from becoming established. 68 B Figure 33: Arenaceous Fossiliferous Packstone. A. Unit B-10, x 25. Foraminifera, pelmatozoan debris, peioids. B. Unit RC-5, x 25. Foraminifera, peioids. 69 Fossiliferous Packstone (Figure 34) Description: Bedding In this facies ranges from thin to massive, and one unit has abundant calclte-fllled fractures. Thickness of Individual units ranges from 0.25 m to 4.2 m. Dense, somewhat clotty micrite Is present and caicite spar occurs as blotchy to clear Intergranular cement. Detrltal hematite Is present as vein filling and rare sllt-slzed grains. Peioids are common In one unit, micrite pellets and Intraciasts are rare. Foraminifera dominate the bloclastic component and are followed In abundance by pelmatozoan debris, brachiopod shells and spines, shell silvers, fenestrate bryozoans and possible calcispheres. These biociasts are rounded to subangular and many have micrite envelopes. No fauna was collected on outcrop. Interpretation: Deposition occurred In waters of moderate turbulence where washing removed some of the mud and finer particles. The clotty micrite can be attributed to bioturbation and the rounding of biociasts Is attributed to reworking by waves and currents. It Is also possible that they were reworked elsewhere and transported to this facies. The distinct absence of quartz In this facies may be attributed to a periodic cessation of the terrigenous supply much like the situation described for the Fossiliferous Dolomltlzed Mudstone facies. Unabraded and uncoated foraminifera suggest that they are in situ. Their preference for higher turbulence environments (McKay & Green, 1963) supports this Interpretation. The remaining faunal components Indicate somewhat open marine conditions, thus the calcispheres were most likely transported from the north. The condition of the biociasts suggests that they have been reworked prior to burial and may have been transported. Oolitic Packstone (Figure 35) Description: This facies Is medium to thick bedded, occurs In only one unit and is 0.77 m thick. The matrix Is an abundant, massive micrite with common quartz silt. Intergranular caicite cement Is common to rare. Quartz sand Is common, and rock fragments, pyroxene, pyrite, zircon and microcllne are rare. Oolds are the most abundant non-skeletal allochems; peioids and Intraciasts are common. All biociasts are broken and foraminifera, brachiopods. 70 Figure 34: Fossiliferous Packstone. A. Unit CQ-1, x 25; foraminifera, shell slivers. B. Unit M-5, X 25; pelmatozoan debris, shell slivers. 71 Figure 35: Oolitic Packstone. Unit KM-7, x 25. Golds, both true and superficial; more visible in hand specimen. 72 bryozoans, pelmatozoans, triiobltes and ostracodes are abundant as oold nuclei. Many non- oolitlcally coated biociasts have micrite coatings. Pelmatozoan debris was collected on weathered surfaces. Interpretation: Most traditional models of oold formation require an environment of higher energy where wave agitation facilitates calcium carbonate precipitation around a nucleus. This wave energy necessariiy prevents any mud from settling. The amount of mud In this facies contradicts this model and suggests that the oolds were transported from a nearby oold producing shoal. The abundance of quartz silt in such a fine matrix Implies a nearby source as well. As nuclei of transported oolds, none of the biota are in situ. Arenaceous Hematitic Packstone (Figure 36) Description: This facies is limited to unit 33-9 and is 1.5 m thick. It Is thinly bedded, laminated, cross-bedded and weathers chippy. The binding agent Is a complex mix of micrite and hematite cement with abundant siit-sized grains of quartz, caicite and hematite. Transiucent hematite grains are widely disseminated, and sand to silt sized augite, pyroxene and quartz are also abundant. Unidentifiable carbonate grains are common. Interpretation: This facies is unusual in that it preserves very fine (4 mm?) ripple marks in a micrite matrix. Unit 33-8 may be a paieosoi. If this Is the case, this facies probably corresponds closely In environmental regime to the finely laminated facies above the second paieosoi at Canaan Quarry. The Iron staining and hematite formation may indicate subaeriai exposure. GRAINSTONES Arenaceous Grainstone: Peloidal Grainstone (Figure 37) Description: This facies occurs in 18 units making it the most common facies In region 2. Units range in thickness from 0.7 m to 7 m thick. Overail, bedding ranges from thin to massive with nodular surfaces, cross-bedding, thin laminae, mottiing and ripple marks. Caicite spar occurs as simple Intergranular cement or sparry mosaic and syntaxiai rims. Cement is abundant, poikiiotopic In places, and crystal sizes range from aphanocrystailine to coarseiy 73 Figure 36: Arenaceous Hematitic Packstone. Unit 33-9, x 25. 74 Figure 37: Arenaceous Grainstone; Peioid Grainstone, x 25. A. Unit 33-1L; B. Unit 33-2L. 75 crystalline. Hematite cement occurs In some units. Quartz silt and sand is very abundant to abundant in ail but one unit and is concentrated in distinct bands in the cross-bedded units. Rare to common poiycrystaiiine quartz, pyroxene, hematite, pyrite, augite, zircon, microcllne and rock fragments occur in one or more units. Abundant peioids, encompassing a wide size range, are present in many units. Most of them are probably micritized foraminifera and other biociasts. Bloclastic and aigaiiy coated intraciasts, some of which are grapestone-iike, are abundant to rare in some units. Rare oolds, many of which are recrystaiiized, are also present. Foraminifera, pelmatozoan debris, shell silvers, bryozoans, echinold spines, sponge fragments, trilobite fragments, dasyciadacean algae, gastropods, bivalves, brachiopods and ostracodes, occur in varied abundance and diversity within these units. Many biociasts have algal coatings or micrite enveiopes. The outcrop fauna consists of brachiopods (abundant in M-6), fenestrate and other bryozoans, peimatozoan debris and one biastoid. Interpretation: Deposition occurred in a high energy setting, that wash away mud, broke biociasts and produced intraciasts. Faunal diversity and abundance is moderate and simiiar to the other facies within this region. The biotic component is more limited when some units are considered individually. Unit RC-2, for example, contains a low diversity and low abundance fauna and may represent siightiy different conditions of deposition, it is the northernmost locality in Region 2 and may have been affected by the same stressful conditions as facies in Region 1. The combination of biociasts and outcrop fauna suggests normal marine conditions. The absence of corals and more pelmatozoans may be due to a shifting substratum in high turbulence waters. Most of the biociasts are in situ but the breakage may indicate some transport. Oolitic Grainstone (Figure 38) Description: The only true oolitic grainstone occurs in unit KM-10. it is also the top of the exposure and quite possibiy the uppermost Union Formation. The unit is massively bedded and is 1.7 m thick. Sparry caicite occurs intergranuiariy as fine to coarse crystals. Golds are abundant and exhibit a wide size range (fine to coarse sand), intraciasts are rare and are ooiiticaiiy coated. Ail microscopic faunal components occur as odd nuclei. Common 76 Figure 38: Oolitic Grainstone. Unit KM-10, x 25. 77 pelmatozoan debris, shell slivers, foraminifera and rare gastropods are present. Small brachiopods and pelmatozoan debris were the only macrofaunal elements collected, interpretation: The facies was deposited In high energy, agitated waters under conditions conducive for oold formation. The size distribution of the oolds Indicates that they are both autochthonous and allochthonous (see CarozzI, 1989). The constantly shifting substratum would not have been conducive for benthic invertebrates. Thus, most of the bloclastic material was transported from the environments adjacent to the shoal. MISCELLANEOUS FACIES Paieosoi (Figure 39) Description: This facies is part of the paieosoi referred to in Chapter 1 and described by Wulff & Ausich (1991). The unit is very thinly to thinly bedded, weathers chippy and shaiy, is poorly cemented and is mottled reddish brown to grayish yellow. The paleosols range in thickness from 1.4 m to 1.7 m thick. The lower and upper contacts are well defined. Caicite and hematite cement occur intergranuiariy as aphano- to finely crystalline in size. Sand-sized grains of quartz, piagiociase, hematite and pyroxene are common. Peioids and intraciasts are rare. Sand-sized, angular to subangular shell silvers are abundant. Interpretation: This facies is interpreted to be a very weakly developed paieosoi and therefore represents the shallowest episode of Greenbrier deposition and subaeriai exposure. Reddish/brown oxidized sediments, fitted fabric, drab-haioed root casts and an erosionai contact at the base (Figures 40 & 41) support the interpretation that this iithofacies is a paieosoi (see Retaliack, 1990). The environment was poorly drained and swampy, and numerous plants grew on the recently developed soil. Three Individual paieosoi horizons have been identified In the Alderson Formation in this area (Wulff & Ausich, 1991) (Figure 42). Siitstone (Figure 43) Description: Four units are included in this facies. They are ail thinly bedded, weather either fissile or chippy and range in thickness from 0.15 m to 2.35 m. One unit, CQ-7, is finely laminated. Quartz is common to very abundant as coarse silt- to sand-sized grains. Silt-sized 78 B Figure 39: Paieosoi, x 25. A. Unit CQA-4; B. Contact between unit CQA-3 & CQA-4 (paieosoi). Up Is to the left. 79 Figure 40: Contact between unit CQA-3 (oolitic grainstone) and unit CQA-4 (paieosoi). 80 B Figure 41 : Paieosoi features on outcrop. A. Drab-haioed root casts and mottied faabric on weathered surface of paieosoi. B. Fitted-fabric on weathered surface of paieosoi. 81 CQA-9 W E h ü Ë i CQ-9 COA 8 CQ-8U COA-7 CQ-8L COA 6 COA 5 CO -7 CQA-4 CQ-6 ------p -sM a CQA-3 1 1 |o Ti=n 1 01 CQA-2 CO 5 ---- 5 0 o -X COA-1 o e ra Figure 42: Stratigraphie section at Canaan Quarry iliustrating position of paieosols (CQA-4, CQA-7, CQA-9) and reiated iithologies. Canaan Quarry was resampied on a finer scaie to better document the paieosols. The stratigraphie columns reflect this. The overall thickness remains the same as does the general breakdown into units, the units rom both sections are cross-referenced on the columns, (i.e., CQ-6 = CQA-4). 82 Figure 43: Siitstone. Unit 33-8. Quartz silt, siiiciciastic mud. 83 elongate grains of mica are abundant In three units, and In CQ-7, are aligned parallel to bedding. In three units, the matrix consists of hematite stained siliclastic mud and a small amount of lime mud. Slightly coarser lime mud constitutes the matrix In the fourth unit. The matrix Is massive, bloturbated and abundant In all examples. There are no biociasts In thin section, and no macrofauna was collected on the outcrop. Interpretation: The units In this facies are from localities that are near the shallowest part of the Greenbrier Sea. At least one unit Is directly above a paieosoi, and It Is possible that the hematite Is a product of subaeriai exposure. The red coloration Indicates abundant oxidation and the absence of fauna suggests that the other units may have been partly subjected to exposure at some time. In portions of 33-4 and 33-8, the mica appears to be an alteration product, surrounded by the background hematite matrix. INTERPRETATION - REGION 2 - NORTH-CENTRAL WEST VIRGINIA The Iithofacies and fauna in Region 2 represent a shallow open marine environment, similar in part to Region 3. By the time upper Greenbrier units were deposited In this area, the sea had transgressed far enough northward that the shoreline and nearshore processes of the Greenbrier Sea Itself did not affect this area. The shallowness of the water In Region 2 was caused by the presence of the West Virginia Dome. The generally subaqueous highpoint experienced nearshore and shoreline processes around It and served as a locus for oold development, bioclast accumulation, more turbulent waters and paieosoi development. The wide variety of Iithofacies both laterally and vertically Is attributable to periodic Influx of slliclastlcs, washing and movement of allochems by waves and tidal currents, as well as variations In bottom topography. An explanation for the limited faunal abundance and diversity Is problematic. Some sessile benthic organisms such as pedlcally attached brachiopods, stalked echinoderms, corals, etc., are capable of living in high turbulence environments. If the substratum were mobile however, as Is the case In some turbulent settings, they would not likely survive. The wave action In such settings would cause breakage of shell material, thus decreasing the 84 amount of identifiable whoie-fossil debris. Additionaiiy, as illustrated by McKinney (1979) and Wulff (1989a, 1990c), some benthos may live in the lee of shoals. Upon death, their remains would become incorporated into shoal sediments by reworking, transport and progradation. This situation may explain the faunal occurrence in Region 2. The mobile substratum undoubtedly prevented many organisms from successfully settling. Those that were successful were probably broken and moved by the processes listed above. in general, the influx of quartz sand does not seem to have had an adverse effect on the biota. Both arenaceous units and fossiliferous units contain broken biociasts in thin section and limited fauna on outcrop. The fossils that are present suggest normal marine conditions. Because a great deal of aiiochem movement would have occurred on these shoals, it is nearly impossible to separate in situ from transported biota. This environmental setting can, more or less, be compared to winnowed platform edge sands or facies belt 6 of Wilson (1975) and adjacent facies (Table 4). These are known to occur on shoals and, although the model does not include a topographic high like the West Virginia Dome, several lithologie and biologic features of Region 2 can be compared, in such shallow waters, small unconformities due to periodic exposure are common. These unconformities are represented by the paieosoi development in this Region. The depositional environment of Region 2 is inferred to have been an open marine weii-circuiated shoal area. Episodic uplift of the West Virginia Dome resulted in exposure, swampy conditions and paieosoi development. Turbulent conditions dominated and, due to the shifting substrata and wave action, a limited association of in situ and transported fauna Is present. REGION 3 - SOUTHEASTERN WEST VIRIGNIA The Union Limestone and Alderson Formation were examined at nine localities in this region which begins just south of the West Virginia Dome in Pocahontas County (Figure 44). The localities are Slaty Fork Quarry, R & R Goal Company Quarry, Swago Creek, Renick Valley, Knobs-Union Road, Sait Sulphur Springs Quarry, Acme Limestone Quarry, Alderson n L p m m f # LOCATION OF MEASURED SECTIONS IN REGION 3 O APPROXIMATE POSITION OF WEST VIRGINIA DOME ] t L V Figure 44: Location of measured sections in Region 3. See text for details. CO CJl 86 and Greenville (Figures 6, 7, 45-48). Stratigraphie correlations are Illustrated in Figure 14a. Because Knobs-Union Road is a very thick section, only the uppermost portion is included in Figure 14a. The entire Knobs-Union Road section is illustrated in Figure 14b. The amount of quartz sand Is notably reduced; however, the source was still most likely from the east and northwest. The number and diversity of brachiopods is decreased as well. Fenestrate bryozoans fArchimedes in particular), increase dramatically in number. The lithologie characteristics and biotic component in the Union and Alderson Formations in this southern section differ dramatically from the rocks previously described. Thirteen major facies were described from these units; the subfacies within them are described in detail in Appendix E. These facies do not occur in any order, or at any given stratigraphie level and there Is substantial variation from locality to locality. After careful analysis of the fauna and Iithofacies at Swago Creek and comparison to units at other localities, it was determined that this section is not within the Union Limestone or the Alderson Formation. Price (1929) reported the section at Swago Creek to be within the Hillsdale Formation of the Greenbrier Group. Although this assignment can not be confirmed at the present time, this section is most certainly not correlative with the other sections sampled. Therefore, aside from the facies analysis of the Swago Creek units in this chapter, there is no further consideration of the rocks at Swago Creek. MUDSTONES Fossiliferous Mudstone (Figure 49) Description; This facies is medium to thick bedded with external Iithologies varying from highly weathered and chippy to rough and dimpled surfaces to heavily bloturbated. Individual units are 1.2 m to 13 m thick. Micrite dominates the matrix, and it is abundant and dense. Microspar and dolomite occur in some units. Rare to common quartz silt is present in several units. Abundant sand-sized peioids and pellets occur in some units. Endothyrid and other foraminifera are unbroken and are common in some units. Pelmatozoan debris, aigae, calcispheres (abundant in one unit), brachiopod spines and shell silvers, bryozoan fragments 87 Figure 45: A. Slaty Fork Quarry; B. Swago Creek 88 I B Figure 46: A. Renick Valiey; B. Knobs-Union Road 89 ... B Figure 47: A. Sait Suiphur Springs Quarry; B. Acme Quarry 90 Figure 48; Aiderson 91 Figure 49: Fossiliferous Mudstone. Unit RV-4. Biociasts predominantiy brachiopod shelis. 92 (fenestrates abundant in one unit), ostracodes, triiobites, bivaives and burrows are common to rare and occur in one or more units. These biociasts are gravai to siit-slzed and rounded to subanguiar. The macrofaunai component is notabie oniy at Renick Vaiiey where brachiopods and fenestrate bryozoans are abundant, trepostome, cystoporate and rhabdomesonid bryozoans are common and bivaives are rare. Peimatozoan debris occurs everywhere, and part of a syringoporid corai coiony was coiiected at SC-1. Interpretation: This facies was deposited in a quiet environment. Bioturbation was caused by an active infauna. The presence of caicispheres and ostracodes suggests a iagoonai environment as in Region 1. However, the remaining fauna is representative of more open marine conditions. Because many of these biociasts are iarger and subanguiar, indicating iittie transport, this environment was not restricted and stressed. Additionaiiy, seaward transport of iight particies such as caicispheres is very common (Carozzi, 1989). Thus, this facies is a mixture of in situ and transported biociasts. Bioclast abundance and diversity in individual units is much lower than the combined list above. The possible lack of attachment sites on a muddy substratum may have prevented some benthos from successful settlement. The Renick Vaiiey unit is in the Aiderson Formation and differs substantially in faunai composition from the other units in this facies. Here, the fauna reflects normal marine conditions, and the organisms present were adapted for life on a muddy, possibly soupy substratum (Wuiff, 1989a, 1990c). Arenaceous Mudstone: Arenaceous Fossiliferous Mudstone: Ostracode Mudstone (Figure 50) Description: This facies exhibits bedding that ranges from thinly laminated to thin bedded to massive. The individual units range from 0.4 m to 15.6 m thick. Where present in the Aiderson Formation, weathering is chippy. The matrix is dominantly micrite, dense and bioturbated. Quartz silt and hematite are scattered throughout the matrix. Microspar occurs in one unit. Abundant, angular to subanguiar quartz sand and silt dominate the non carbonate component. Mica silvers and shards are rare to common. Carbonate grains and intraciasts are rare. Faunai components are not significant in the arenaceous sub-facies. Peimatozoan debris, ostracodes, caicispheres, fenestrate bryozoans, shell silvers, brachiopod 93 Figure 50: Arenaceous Fossiliferous Mudstone. Unit A-3, x 25. Fenestrate bryozoans, peimatozoan debris, quartz silt. 94 shells and spines, tubular algae, other bryozoans, bivalves, triiobites, endothyrid foramlnlfera and echlnoid spines are abundant to rare (in the order listed) and occur In one or more of the units In the other two facies. Macrofaunai abundance varies greatly and consists of peimatozoan debris, brachiopods, encrusting and fenestrate bryozoans and rare rugose corals. Interpretation: This facies was deposited In quiet waters In conditions fairly similar to the previously described facies. The amount of quartz sand Is greater here and may have been brought In during a higher energy pulse or carried westward by wind. The fossil material In thin section and on the outcrop is very similar to that In the Fossiliferous Mudstone Facies and are probably a mixture of transported and In situ clasts. The small size and abraded condition of some of the clasts indicates some reworking. It appears from the diversity that the siliciastic input did not have an adverse effect on their growth and survival. Micaceous Mudstone (Figure 51) Description: This facies occurs in one unit, sandwiched between two calcareous siitstones. It Is medium bedded, faintly laminated, has nodular weathering and scattered chert and is 2.84 m thick. The matrix is brown, dense micrite with common quartz silt and hematite. Abundant, silt-sized mica grains are aligned parallel to bedding. Peimatozoan debris, blastoids and rugose corals were present on outcrop. Interpretation: The stratigraphie position of this unit, indicates deposition during some sort of erosional event outside of the basin, which supplied terrigenous materials to the lime mud already present. The waters were relatively calm allowing deposition of fine grained sediments. The absence of infauna is illustrated by the parallel alignment of the grains and the laminae. The absence of Invertebrate biociasts In thin section implies that the macrofauna was most likely transported from an adjacent facies during influx of the elastics. This facies is part of the terrigenous pulse recorded at Knobs-Unlon Road and Acme Quarry (Figures 14a & 14b). Dolomitized Mudstone: Mudstone (Figure 52) Description: The units included In this facies exhibit a wide range of physical characteristics. Bedding ranges in thickness from medium to massive. Units weather chippy and flaggy and 95 B Figure 51: Micaceous Mudstone. Unit KU-13.2. A. x 25; B. x 63 96 B Figure 52: Mudstone; Dolomitized Mudstone, x 25. A. Unit SC-3; B. Unit AQ-11. 97 some have slit wisps. They are 0.6 m to 4.5 m thick. The matrix is micrite (or originally micrite where It Is now dolomitized), which is generally massive and bioturbated. Dolomite rhombs are rare to abundant In some units. The presence of Intraciasts creates a dlsmlcrlte- like fabric. Angular to subanguiar quartz and pyrite silt are common; mica, plagloclase and hematite are rare. Non-skeletal allochems are limited to two units and are common micrite pellets and abundant, clotty micrite Intraciasts. Biociasts are limited In distribution as well. Rare to common peimatozoan debris, bryozoans, shell slivers, ostracodes and caicispheres are subanguiar to rounded. Rare Inarticulate brachiopods, Pentremltes. peimatozoan debris, rugose corals, Pterotocrlnus serratus. fenestrate bryozoans and burrows were collected on outcrop. Interpretation: This facies was also deposited In quiet waters. An active infauna Is Indicated by the extensive bioturbation. Comparison of faunai composition between thin-sectlon and outcrop provides conflicting Information. The thin section component Is very similar to the limited fauna In the lower upper member of Region 1. The outcrop fauna, however. Is more representative of open marine conditions. Because transportation of light particles Is very common, tidal currents could easily have transported the caicispheres and ostracodes from their Iagoonai environment to the north (Carozzi, 1989). Because there is no evidence of restricted circulation in any other facies In Region 3, the dolomite Is secondary and open marine conditions prevailed. Laminated Mudstone (Figure 53) Description: The beds in this facies are thick to medium and thin laminae are prominent on both weathered surfaces and In thin section. Individual units are 1.25 m to 4.5 m thick and contacts between units are generally sharp. Nodular weathering, uneven partings and chert stringers are present. The matrix Is micrite In all but one unit where it has been altered to microspar. Quartz silt Is a secondary matrix component. Quartz sand Is abundant In coarse layers and rare to common In fine layers. Hematite, pyrite, zircon and mica are rare to common in one or more units. Carbonate grains are common in two units; peimatozoan debris and shell silvers are rare In other units. Rare brachiopods were described on outcrop. 98 Figure 53: Laminated Mudstone, x 25. A. AQ-2; B. AQ-14. 99 Interpretation: This unit was deposited in quiet waters that received an influx of quartz sand from an outside terrigenous source or erosion of underlying sandy units. Continuous, undisturbed deposition is indicated by the sharp laminae and grading of quartz. The sharp contacts above and below suggest dramatic changes in conditions prior to and after deposition, particularly at Acme Quarry where the overlying unit is an oolitic grainstone. Bioclastic debris is so rare that it appears this abundance of elastics interfered with successful inhabitation. Of all the arenaceous units, this one contains the most siliciastic material and represents a different depositionai environment. The small fossils that are present were most likely transported in. This facies is also part of the terrigenous pulse recorded in units at Knobs-Union Road and Acme Quarry (Figures 14a & 14b). WACKESTONES Fossiliferous Wackestone (Figure 54) Description: Four sub-facies are included under this heading and differ mainly in their non- skeietai aiiochem component. Twenty seven units are included in this facies making this the most commonly occurring facies in the region. Bedding thicknesses range from thin and shaiy to thick to massive. Individual units are 0.55 m to 8.2 m thick. External surfaces exhibit mottled and puckered weathering, siit-wisps (particularly common at Knobs-Union Road), styloiites, stromatactis, chert nodules and caicite-fiiied fractures. Micrite is the dominant matrix component and is generally dense and bioturbated. The presence of quartz silt, peioids and intraciasts creates grainy, dismicrite and/or clotty textures in some units. Microspar matrices are present in some units as are scattered dolomite rhombs. The matrix is somewhat coarser and lighter colored in some units. Quartz is the most common non carbonate grain. Angular, silt- to sand-sized grains are abundant to common in many units. Non-skeietai aiiochems consist of rare to abundant bioclastic micrite intraciasts. Many are large (1-2 mm), some contain iarger biociasts (sand-sized) and many are encrusted with Sohaerocodium. Ooids and superficial ooids are common, many are micritized and/or broken. Siit-sized pellets are rare to abundant as intergranular clusters and fracture filling. 100 B Figure 54: Fossiliferous Wackestone, Unit S^-3, x 25. A. Triiobite fragment. Fenesteiia sensu lato, peimatozoan débris; B. intraciast of aigae (Glrvaneila). shell slivers. 101 The microscopic faunai component is abundant and diverse and varies substantiaiiy from unit to unit. In approximately decreasing abundance, the biociasts are peimatozoan debris, fenestrate bryozoans (gravel sized at one locality), brachiopod shelis and spines, other bryozoans, endothyrid foramlnlfera, caicispheres, dasycladacean aigae, tubular aigae, syringoporid coral and others, Sohaerocodium sp., triiobites, echlnoid spines, ostracodes, gastropods and bivaives. These biociasts range in size from gravel to sand and many are subanguiar indicating little or no transport. Macrofaunai components are just as diverse and varied in distribution. Peimatozoan debris, rare rugose corals. Archimedes sp., Fenesteiia sensu iato, brachiopods (9 genera), Pentremltes sp., other bryozoans, gastropods and rare triiobites were coiiected from one or more units on outcrop. Interpretation: The increased faunai diversity suggests deposition in a substantiaiiy different environment than the mudstones described above. The major difference was most likely the substratum, a point that is discussed later. The iarger aiiochems imply less transport than in previous facies. The silt wisps at Knobs-Union Road may have had the same source as the quartz silt in other units. The faunai diversity and composition in both thin section and outcrop is representative of normal marine conditions (Wilson & Jordan, 1983). The co occurrence of various groups in both thin section and outcrop suggests that they are part of the in situ fauna and are representative of the environmental conditions at the time of deposition. Overall, shallow, moderately energetic, well circulated waters characterize the depositionai environment. PACKSTONES Fossiliferous Packstone (Figure 55) Description: Four subfacies are included within this general packstone facies and together they occur in 12 units. Bedding is thin with silty interbeds or thick to massive, individual units range in thickness from 0.7 m to 10.5 m. Styloiites, lenses of ooids, hashy fossiliferous lenses and interbeds, silty interbeds and rare cross bedding occur on outcrop. Micrite matrix is abundant in some units and is massive, clotty and/or has a dismicrite texture, it has been 102 Figure 55: Fossiliferous Packstone. Unit SF-9, x 25. Brachiopod shells, bryozoan fragments. 103 recrystallized to microspar and pseudospar In some units. Dolomite rhombs are abundant In one unit. Calcite cement is common and occurs intergranulariy, as sparry mosaic and syntaxial rims. Quartz is notably rare in this facies as compared to the wackestones described above. Micrite Intraciasts with biociasts and carbonate grains are generally common and occur In all but one unit. Micrite pellets and peioids are rare to abundant and occur either intergranulariy or In sheltered areas beneath biociasts. Golds are common to rare In a few units. The microscopic biotic component Is abundant and diverse. In approximately decreasing order of abundance It consists of peimatozoan debris; fenestrate and encrusting bryozoans; endothyrid foramlnlfera; bIserial and unlserial foramlnlfera; shell fragments; bivalves; ostracodes?; brachiopod shells and spines; corals; dasycladacean algae; tubular algae; gastropods; triiobites and echlnoid spines. The biociasts are sand-sized and subanguiar although most have micrite envelopes. Macrofauna collected on the outcrop consists of peimatozoan debris, rugose corals, Pentremltes sp., Pterotocrlnus serratus. fenestrate bryozoans (Archimedes sp. is abundant), trepostome bryozoans, brachiopods (4 genera), triiobites and syringoporid coral. Interpretation: Depositionai conditions of this facies were not much different from those of the wackestones. Environmental energy was moderate, allowing deposition of mud. The Intraciasts represent episodic times of higher turbulence when biociasts and matrix were ripped up and redeposlted. They may be from within this particular facies or transported. Some transport of biociasts is indicated by the small size in thin section. However, the abundance of corresponding macrofauna on outcrop suggests that the majority of these biociasts are In situ. The fauna contains both upper and lower tier suspension feeders and Is representative of a normal marine faunai assemblage. Oolitic Fossiliferous Packstone (Figure 56) Description; This facies has medium to thick bedding and units range In thickness from 0.2 m to 1 m. Dense patches of Intergranular micrite and sparry calcite cement are common In one or more units. Sand to sllt-slzed quartz Is common. Polycrystalline quartz is rare. Golds are common to abundant and In one unit are highly weathered with micritized nuclei. 104 B Figure 56: Oolitic Fossiliferous Packstone, x 25. A. Unit S^2; coated triiobite fragment, intraciasts and peimatozoan debris; B. Unit AQ-IO; brachiopod shelis, ooids. 105 Bioclastic micrite intraciasts, some with aigai encrustations, are common. In thin section, large bryozoan fragments, brachiopod shells, peimatozoan debris, tubular aigae, foramlnlfera, coral, triiobites and gastropods are rare to abundant in one or more units. Fossils coiiected on outcrop are limited and consist of abundant peimatozoan debris, rare gastropods, small brachiopods, and rugose corals. Interpretation: This facies differs from the Fossiliferous Packstone by the presence of ooids and slightly more quartz. This can be accounted for by a slight increase in environmental energy and subsequent transport of aiiochems and quartz from the north. The ooids were derived from the shoal facies in the area. The non-uniformity in size and weathering of some is indicative of transport (Carozzi, 1989). The intraciasts are also indicative of higher energy and transport. The faunai component both in thin section and on outcrop represents open marine conditions, and their large size indicates iittie or no transport. GRAiNSTONES Oolitic Fossiliferous Grainstone (Figure 57) Description: Four subfacies are included in this facies encompassing 17 units. Bedding ranges from thin to massive and exposures contain cross bedding, styloiites and silt wisps. Thickness ranges for individual units range from 0.43 m to 7.7 m. Calcite cement occurs as both interlocking mosaic crystals and simple sparry calcite. Crystals range in size from very fine to coarse and exhibit typical aggrading growth toward the center of voids. Ooids dominate the non-skeietai aiiochem component. They have biociasts as nuclei, many have oniy superficial coatings and many have micrite envelopes. Oncoiites are common to rare in some units, and the ooids at Greenville do not have radial fabric. Clotty bioclastic intraciasts are common to rare, and many have oolitic or aigai coatings. Micrite pellets and peioids are common. The microscopic biotic component is diverse and abundant, although most are oold nuclei. Bryozoans and peimatozoan debris are abundant; endothyrid and biseriai foramlnlfera, shell fragments, bivaives, dasycladacean aigae, brachiopod spines, gastropods, triiobites, tubular algae, Sohaerocodium sp.. and corai are common to rare. Most biociasts 106 m B Figure 57: Oolitic Fossiliferous Grainstone, x 25. A. Unit S -9; B. Unit SF-15; uniseriai foraminiferan. 107 not encased in oolitic coatings have micrite envelopes. Rare peimatozoan debris, brachiopods, encrusting bryozoans, bivaives, gastropods, blastoids, rugose corals and Pterotocrlnus serratus wing plates were coiiected on outcrop. Interpretation: included within this subdivision are oolitic grainstones and oolitic pellet grainstones. The presence of ooids, coated grains, bioclastic intraciasts and the absence of mud indicates turbulent conditions. The fossils coiiected on outcrop, although representative of an open marine fauna, are rare in abundance and fragmented. The presence of abundant ooids indicates a shoaling environment and, with progradation of the shoal (as at the Sait Suiphur Springs quarry, see Chapter 7), or simply reworking by currents, organisms living on the fringes of the shoal were incorporated into the facies (Wuiff, 1990c; McKinney, 1979). This, then, would be the source for both the few, broken fossils collected on the outcrop and the oold nuclei. True oolitic grainstones occur at the top of the sections at Acme Quarry, Slaty Fork Quarry and the R & R Quarry and at the base of the Aiderson Formation at Greenville. The Aiderson Formation is not of quarrying quality in these areas and is usually removed, it is probable therefore, that these oold grainstones are, stratigraphicaiiy, the uppermost part of the Union Limestone. This suggests that Union deposition ended with a shoaling event, with production and widespread transport of ooids across Region 3 (Figure 14a). This scenario is further discussed in a later section. Foramlnlfera Peloid Grainstone (Figure 58) Description: The units included in this facies differ in the amount of peioids and foramlnlfera, but the overall combination of aiiochems and cement warrant this grouping. Bedding is thick in ail units and individual unit thicknesses range from 0.5 m to 1.45 m. Calcite cement occurs as both sparry mosaic and simple spar, and syntaxial rims are common. Rare hematite occurs as indistinct "smears" between grains. Clotty bioclastic intraciasts are common and are medium sand to coarse sand sized. Round to oval peioids are common. Endothyrid foramlnlfera are abundant, peimatozoan debris, brachiopod shells, echlnoid spines and dasycladacean algae are common. Triiobite fragments are rare. The biociasts are coarse silt to sand-sized and rounded to subanguiar. No fauna was coiiected from outcrop. 108 B Figure 58: Foramlnlfera Peloid Grainstone, x 25. A. Unit SC-5; B. Unit 80-2. 109 Interpretation: A highly turbulent environment Is Indicated by the absence of mud and the presence of Intraciasts. The fauna, with the exception of the foramlnlfera, Is limited In abundance and diversity and the small size and abraded condition Indicates much reworking and possible transportation. Fossiliferous Grainstone fIntraclast Fossiliferous Gralnstonel (Figure 59) Description: The units In this facies are classified together even though the non-skeletal aiiochems differ substantially. The units are thickly bedded. Thickness of Individual units ranges from 0.8 m to 4.5 m. Calcite cement Is common and occurs as fine to coarse Intergranular crystals and syntaxial rims. Clotty, large (sand to gravel sized) bioclastic, quartz bearing, micrite Intraciasts are very abundant to rare. Sllt-slzed micrite pellets and sand-sized peioids are common In one or more units. Ooids are rare to common. Peimatozoan debris Is abundant In all units, large bryozoan fragments, brachiopod shells, foramlnlfera, triiobites, dasycladacean algae, bivalves, and tubular algae are rare to common in one or more units. Macrofauna consists of abundant peimatozoan debris and fenestrate bryozoans; with rare gastropods, brachiopods (4 genera) and numerous small, unidentified brachiopods, and rugose corals. Interpretation: High environmental energy Is Indicated by the abundant calcite cement, Intraciasts and transported ooids. The moderately diverse faunai assemblage, both In thin section and on outcrop represent a normal marine environment. The co-occurrence In both thin section and outcrop, plus the large bloclast size, suggests In situ occurrence and little transport. MISCELLANEOUS FACIES Black Shale (Figure 60) Description: This facies occurs only In the Greenville Shale. It Is very thin to thinly bedded and weathers Into large chips. It Is black, unfosslllferous and approximately 42 m thick at Greenville. Inarticulate brachiopods are present at R & R Quarry where the unit Is 1 m thick. The Greenville Shale Is comprised basically of sand and sllt-slzed quartz grains and organlcs. 110 Figure 59: Fossiliferous intraciast Grainstone. Unit SF-13U, x 25. Cystoporate, peimatozoan debris, fenestrate bryozoan fragments. 111 Figure 60: Black Shale. Unit G-1, x 25. 112 Interpretation: The black shale collected both at Greenville and the R & R Quarry records an anaerobic environment. Total organic carbon values are high, reflecting little, if any, aerobic activity (Table 3; see Barker, 1979). This unit is sandwiched, both vertically and horizontally, between limestones of normal marine character. The sharp lithologie and biologic change Indicates a major local change In environmental conditions. The Greenville Shale Is confined largely to Monroe County, although Its presence in Greenbrier County suggests greater distribution than previously reported. The significance of this unit is discussed in a later section. Micaceous Siltstone (Figure 61) Description: This facies Is Interbedded with an Arenaceous Mudstone facies described from Knobs-Unlon Road and is approximately 1 m thick. It Is non-calcareous, unfosslllferous and consists of laminated quartz silt. Fine sllt-slzed elongate grains of mica are common throughout. Large (1 cm) intraciasts are present In hand specimen, interpretation: A terrigenous pulse, resulting from uplift and erosion, may have caused this Influx of non-calcareous material and blockage of carbonate production. The depositionai environment was quiet, however, allowing this fine-grained material to settle out into finely laminated layers. The large Intraciasts In hand specimen appear to be rip-ups of material similar to the matrix and were washed in during this ciastic influx. Just as in the arenaceous mudstone facies, the siiiciastic content most iikeiy interfered with successfui settiement of the benthos. iNTERPRETATiON - REGiON 3 - SOUTHEASTERN WEST ViRGiNIA Stages in the transgression of the Greenbrier Sea can not be as easiiy deiineated in Region 3 as in Region 1. This is due to the establishment of a reiativeiy stable environment with respect to circuiation, salinity and temperature ieveis during deposition of the upper Greenbrier units (Union and Aiderson), and the reiativeiy constant water depth as transgression was near its maximum. As mentioned above, the shaiiowing event recorded in upper Union units was the only large scale fluctuation In water depth in this region. 113 i Figure 61: Micaceous Slltstone. Unit KU-12.2, x 25. 114 Additionally, no recognizable pattern of facies distribution exists. No physical barrier would have blocked passage of northward or southward moving water masses. With a direct link to the open sea toward the south, a constant flow of nutrlent-rlch, normal salinity waters existed. The iithofacies described record deposition in shallow, open marine waters. With the exception of the oolitic grainstones, siitstones and shales, the physical parameters of the environments appear to have been fairly constant. The fossils present In these facies further confirm an open circulation, normal marine environment. Throughout this discussion, bottom topography and sheltered areas have been used to explain the variations in iithology and faunal content, i have pointed out that physical conditions, except for water turbulence, were the same for the wackestone, packstone and grainstone producing environments. It seems unlikely that the physical conditions of a mudstone facies and a fossiilferous facies would have been that different if they were immediately adjacent to each other. The absence of benthic fauna must be attributable to something else. One explanation may be the concept of taphonomic feedback (KIdweil & JabionskI, 1983). Benthic larvae need a hard substratum on which to settle, and the mudstone facies offer few places for attachment. Thus, the muddy substratum environments remained relatively fauna free, unless skeletal debris were Introduced either through physical transportation or migration of organisms adapted to a muddy substratum. The formation of oolitic grainstones in the Union Formation was due, in most instances, to development of local highpolnts (Wulff, 1990b). Here, Increased turbulence enhanced conditions for oold development. The shoreline was many miles northwest of most Greenbrier oold bodies. In places where It Is not possible to demonstrate shoaling, traditional models for oold formation can not be utilized. Tucker & Wright (1990), for example, summarized studies that suggest that some ooids form in quiet environments with coating accomplished by processes other than agitation (p. 6). The Greenville Shale formed in what appears to be the deepest part of the basin and represents an anoxic event that, as indicated by the great thickness of accumulation In Monroe County (42.7 m), lasted a long time. Significant subsidence occurred along the 115 central portion of the Appalachian Basin during this time (Figure 2). Because the Greenville Shale Is confined to a narrow belt within the center of this region, it is suggested that this area was undergoing the greatest subsidence of all. Unlike the areas to the east and west, stagnation or restriction occurred, resulting in the development of anoxic conditions and deposition of the shale. It Is also possible that while the surrounding area was experiencing normal marine conditions, oxygen-poor bottom waters flowed Into this trough during this time. GIrty (1926) Identified a limited fauna of bivalves and cephalopoda from various localities In southern West Virginia Indicating fluctuation In oxygenation levels during deposition. Subsequent Iithofacies and blofacles, which developed during post-Greenville deposition, differ sharply at the two localities studied. At Greenville, faunal turnover Is slight with similar biota In both the upper Union Limestone and the lower Alderson Formation (Appendix H, Figure 14a). It appears that the displaced benthos was able to re-lnhabit the area once this anoxic event ended. Northward, at the R & R Quarry, the Iithofacies and blofacles changed greatly from an oolitic unit In the upper Union Limestone to muddy, fossiilferous units In the lower Alderson Formation. This thin exposure (~1 m) represents the last remnants of Greenville Shale deposition. Thus, following Greenville Shale deposition, environmental conditions changed significantly and were accompanied by development of different faunal assemblages. Ongoing uplift to the east and northeast provided enough terrigenous material to cause cessation of carbonate deposition producing the siitstones and, as noted above, records some sort of tectonic pulse. Thus, the overall Interpretation for this region Is an open marine "basin" with shallow waters and sedimentation that kept pace with the high rate of subsidence. Wilson (1975) described an open shelf environment whose characteristics compare with those of Region 3. Table 4 contains a summary of the Important points. This corresponds to Facies Belts 2 and 3 of Wilson’s (1975) Idealized facies sequence. 116 REGIONAL SYNTHESIS The regional picture for the central Appalachian Basin during deposition of upper Greenbrier units shows that deposition occurred under a variety of environmental conditions stemming from the paleogeographic position, structural configuration and tectonic setting of the Appalachian Basin. In the north, shelf lagoon conditions prevailed, controlled by a shallow sea, wide shelf and barrier to the south. The biotic component Is one of primarily eurytopic organisms capable of living under stressful or variable conditions. Marine environmental conditions In the central areas were generally of higher turbulence. The abundance of slllclclastic material and cross-bedding and the presence of paleosols Indicates shallow waters with significant terrigenous Influx. The general absence of fauna suggests environmental turbulence and substrata too mobile for successful habitation. To the south, open marine conditions prevailed, due to a broad connection to the open sea to the south and blockage of southward transport of terrigenous elastics that might have Interfered with carbonate production. The biota reflects organisms adapted to life In open marine, normal salinity conditions. A similar environmental gradient was described by CarozzI (1989) for the development of a carbonate platform with a "frontal hydrodynamic build-up" (p. 539). He used the Ste. Genevieve Limestone In the southern part of the Illinois Basin to Illustrate this sequence. The model's environments range from subtldal to Intertidal and consist of a seaward slope, discontinuous oolitic bars and shoals, a lagoon and a delta or estuary (Figure 62). This Is considered a Type 4 platform (CarozzI, 1989) with a well developed frontal build-up of a hydrodynamic nature. Such a build-up, as represented by the oold shoals of the Ste. Genevieve Limestone, results from the mechanical concentration of various bloclasts, oolds, llthic pellets and Intraclasts, all of local origin. Dispersal of these constituents Is mainly by tidal currents. In both landward and seaward directions. Thus, the protected and quiet lagoon behind the build-up receives most of Its bloclasts from the build-up. Oolds also are subject to transport and dispersal. Conditions for precipitation of calcium carbonate are fairly localized on the platform. Oolds are penecontemporaneously distributed as detrltal particles along 117 MEAN SEA lEVEl WAVE BASE Subtidal Intertidal ^ lnt -CalcisillKe matrix Clear Calclte Cement ______| Calcisiltite I Pure Quartz Sandstone f Matrix I Clear Calcite Cement Influx of Detrltal Quartz Transported Fauna Fauna in Place I Transported Fauna BIP ^ BTR ■3 ORS BIO PEP M ------— ^ LPI ^ - ^ OOl ------o ------DO SPA Figure 62: ideal depositional model: Carbonate Platform with Frontal Hydrodynamic Build-up, Ste. Genevieve Limestone (Merameclan). SIP = Benthic fauna In situ & ecologically zoned; BTR = Benthic fauna transported by traction; ORS = Organisms transported by suspension; BIO = Bloturbatlon; PEP = Fecal pellets; LPI = LIthIc pellets (P) & Intraclasts (I); OOL = oolds; DO = Detrltal quartz; SPA = Interparticle sparlte cement or primary porosity. After Rao & CarozzI (1978). 118 depositional strike from hundreds of feet to several miles (CarozzI, 1989). Additionally, ooids and quartz are transported into the shallowest and deepest facies. The size and shape of the hydrodynamic buildups is very important in its ability to interfere with tidal currents. Some buildups remain below low tide level and barely become subaeriaiiy exposed. Others reach sufficient heights to remain exposed long enough for paleosols to develop. The lagoonai environment is also important in settings such as these. It ranges from fairly open marine to low turbulence and well protected. If considerable reworking is present, the llthic pellets, Intraciasts and fecal pellets are generally dispersed seaward. Such seaward transport of lagoonai allochems is very common (CarozzI, 1989). Plant debris, oogonia of calcareous algae and delicate lagoonai organisms may be carried in suspension to the platform slopes where they eventually settle in deeper water. Finally, the Influx of sand- to silt-sized quartz varies as a function of the geological composition, morphology and climate of the source areas. Silt-sized eollan quartz Is deposited In the more shoreward portion of the lagoon and the coarser quartz tends to concentrate at the hydrodynamic build-up Itself. If the West Virginia Dome Is considered as a locus for accumulation of bloclastic debris and terrigenous elastics. It may be analogous to a frontal hydrodynamic build-up. The entire study area may be compared to Carozzi’s model, keeping In mind that the situation was brought about by tectonic activity, not just the Influence of the hydrodynamic build-up. Transportation of bloclasts to the inhospitable environment of the middle member of Region 1 might have been accomplished by landward dispersal via tidal currents. The presence of oolds In facies that developed far from a shoal can be explained by noting the transportability of oolds from their place of origin. Calclspheres within Region 3 were most likely transported In suspension southward from the lagoon to open waters. Finally, the quartz sand In the Loyalhanna Limestone was most likely trapped behind and directly at the West Virginia Dome. Overall, the general setting of the Appalachian Basin toward the end of Greenbrier deposition was similar to conditions In the Eastern Interior Basin. This similarity Is treated further In Chapter 5. 119 FACIES RELATIONSHIPS A regional shallowing event is recorded at the end of Union Limestone deposition In Regions 2 and 3 (Figure 63). As noted earlier, the youngest Union beds collected at several localities In Region 3 are oolitic grainstones. Correlative units In Region 2 are either oolitic grainstones or arenaceous and bloclastic grainstones. Such facies represent deposition In shallow, highly turbulent waters. Above these units in Region 2 are the paleosols and oxidized facies described earlier. Combined, these facies represent a low point In the depth of the Greenbrier Sea Indicating that, although tectonic uplift of the West Virginia Dome may have played some part In the exposure at Canaan Quarry, a widespread lowering of sea level also occurred at this time. This depositionai environment did not extend north of the West Virginia Dome, Indicating yet another influence the Dome had over the sedimentation and circuiation patterns to the north. In summary, three stages, based on lithologie and faunai changes, can be delineated In the depositional sequences of the Greenbrier units studied (Figures 63 & 64, Table 5). Because the units are diachronous, the stage transitions are not time correlative. In Region 1, the three stages correspond to the middle, upper and uppermost members of the Greenbrier Formation (Figures 14, 63 & 64). In Regions 2 and 3, stages 1 and 2 can not be Identified stratigraphicaliy. This is due to the stable environments already established In these regions at the time rocks were being deposited in Region 1 and also to the small effect a rise in sea level had on these areas. Stage 3, however. Is marked by the extreme shallowing at the end of Union time and by the grainstones and paleosols described above. The similarity in lithoiogies above this horizon enables correlation to the stage 3 boundary in Region 1 (Figures 14 & 63). Figure 63: Correlation of measured sections showing basic facies relationships, shallowing event at the end of Union deposition and sharp lithologie change with deposition of Alderson Formation. Facies numbers refer to numbers assigned to general facies in Appendix F. 120 PLEASE NOTE: Oversize maps and charts are filmed in sections in the following maimer: LEFT TO RIGHT, TOP TO BOTTOM, WITH SMALL OVERLAPS The following map or chart has been refilmed in its entirety at the end of this dissertation (not available on microfiche). A xerographic reproduction has been provided for paper copies and is inserted into the inside of the back cover. Black and white photographic prints (17" x 23") are available for an additional charge. University Microfilms International Figure 64: Correlation of measured sections showing basic facies relationships, shallowing event at the end of Union di and sharp lithologie change with deposition of Alders Formation. Facies numbers refer to numbers assignee general facies listed in Appendix F. N Canaan Quarry Oakland Quarry Sang Run Quarry Deep Creek Quarry Roaring Creek — M or 5 icies m deposition derson gned to Butcher Quarry U. S. Route 33 Slaty F( Kenton Meadows 11 Quarry 16 10 18 16 15 13 12 14 13 12 Monterville Quarry 13 W 20 12 13 11 R & R Coal Co. Renick Valley Slaty Fork Quarry Knobs-Unior Alderson S Greenville Salt Sulphur Springs Acme Quarry Deep Creek Quarry Roaring Creek Montervi KEY Litliology Facies Number Mudstones 1, 2, 8, 9. 10, 21, 22, 23, 24, 25 Wackestones 3 ,1 1 ,1 2 ,2 6 Packstones 4, 13, 14, 15, 16, 27, 28 Grainstones 5, 6, 7, 18, 19, 29, 30, 31 Siitstones 20, 33, 34 Shale 32 Paleosol 17 Ü U lc n e r K iu m iy y s. KOUte Kenton Meadows Quarry 16 15 14 X Monterville Quarry 13 18 12 11 10 8 29 V 14 26 29 10 U. S. Route 64 12 33 12 22 26 26 27 27 26 26 U V ^ 122 2 Open Marine Restricted Marine Seml-restrlcted M a rin e West Virginia Dome Approx. extent of fie ld a re a Figure 64: Changes In environmental conditions during deposition of Greenbrier units. 123 Table 5: Description of stages in Union Limestone and Alderson Formation deposition. Region 1 can be divided into three time slices (Ti, Tg, Tg) representing the middle member, upper member and uppermost upper member of the Greenbrier Formation. As environmental conditions remained relatively stable in Regions 2 and 3, there is no clear division to be made. However, based on faunai evidence and comparison to Region 1, the Alderson Formation can be said to have been deposited during Time Tg. The occurrence of wackestones, packstones and grainstones at approximately the same stratigraphie interval may not represent significant environmental differences. Carbonate environments exhibit a great deal of lateral variation and these differences may be attributed to variations in bottom topography or to deposition in sheltered versus non-sheitered areas. T i - Region 1 : Semi-restricted shelf lagoon * Combined effect of the West Virginia Dome blocking northward transport of normal marine water masses plus the wide shallow platform produced a damping effectreduced circuiation —>• increased evaporation and salinity and fluctuation in water temperature. Fluctuations in these factors may also have been caused by influx of fresh water from the north where the Mauch Chunk delta complex was being deposited. * The fauna is depauperate and dominated by forms indicative of lagoonai conditions. Normal marine faunai components are absent. Region 2: High energy, open marine shoal * Extensive reworking of sediment plus substantialinflux of siiiciciastic material * The bloclasts are broken, coated, not in situ, limited macrofauna probably lived in sheltered areas within the shoal environment. Region 3: Open marine, shallow shelf * Connection to open ocean to the south facilitated circuiation and normal marine conditions. * Normal marine biota Tg - Region 1 : Semi-normal marine * increase in circuiation creating more stable marine conditions. * Fauna consists of opportunistic organisms in simple assemblages. Major normal marine groups still absent (ie: corals, echinoderms, bryozoans) Region 2: As in T j Region 3: As in T^ Tg - Region 1: Open marine - well circulated waters * Lithoiogies similar to those in Region 3, "Aiderson-type" lithoiogies * Fauna approximates normal marine composition with appearance of bryozoans, peimatozoan debris, etc. 124 Table 5 (continued) Region 2: High energy, open marine shoai * Locally extremely shallow and periodically emergent as Indicated by development of a paleosol in Alderson-equlvalent strata * Biota representative of marine and non-marine conditions (ie: bivalves, plants) Region 3; As In CHAPTER III AUTECOLOGY Autecology Is the study of the relationship among Individual organisms and their environment (Bates & Jackson. 1980; Dodd & Stanton, 1981). Because modes of life differ within and between individual groups of organisms, it is essentiai to understand their ecology before an Interpretation of the community as a whole can be developed. This chapter discusses the modes of life and inferred paleoenvironmental preferences for the major fossii organisms present in the Greenbrier rocks studied. Preservational and sampiing biases are important factors in observed faunal occurrences and they have been accounted for in the foliowing interpretations. BRACHIOPODS External morphologic variations have aiiowed brachiopods to iive in many different environments and on different substrata. Varying degrees of aiation, thickening of the umbonal region, width of the interarea, perimeter size and spine development are morphologic variations that enabled Paleozoic brachiopods to successfuiiy inhabit various environments. It Is possible to use overall brachiopod shell shape to Interpret some aspects of the environment in which a particular brachiopod lived (Muir-Wood & Cooper, 1960, Copper, 1966b, Alexander, 1975, Fursich & Hurst, 1974). Because brachiopods are epifaunal benthic organisms, two factors play an important role in their distribution: nature of the substratum, and physical conditions immediately above the substratum. Brachiopods of the order Strophomenida are represented by individuals belonging to the suborders Productidina, Strophomenidina and Chonetidina. Living habits of productid brachiopods were Intimately linked to the arrangement and type of spines, because each genus possessed a specific pattern (Muir-Wood & Cooper, 1960). The spines permitted colonization on soupy and muddy bottoms and also provided support against flipping in 125 126 increased currents or In turbulent waters. The following summary of productid brachiopod paleoecology Is adapted from Mulr-Wood & Cooper (1960), except where noted. Protonlella oarvus (family Buxtonlldae) had strongly curved umbones and swollen umbonal slopes (Figure 65). This Indicates that the shells were not cemented or anchored to the substratum (Mulr-Wood & Cooper, 1960) and the Increased weight served to anchor the shell on the substratum. As with most genera in this family, P. oarvus had short thin spines on both valves. These delicate spines probably did little In the way of shell stabilization. The ears, however, had numerous, long, thin spines. These probably could have held the valve firm and steady on the substratum with the anterior margin at an oblique angle upward. Protonlella Is abundant In the wackestone, packstone and grainstone facies of Region 1, which Indicates that P. oarvus successfully colonized a variety of substrata and environments. Because It Is present only In the stressful environments of Region 1, it may have been a more eurytopic species. Ovatia (family Llnoproductidae) was also stabilized by spines, it lived with the visceral disk of the dorsal valve on the mud, stabilized by the spines along Its ears and flanks. The genlculated margin grew up and away from the sea floor keeping the commissure well above the sediment-water Interface (Figure 65). Ovatia eionaata is present in mudstone, wackestone, packstone and grainstone facies of all three regions. In the grainstone facies. It Is squashed flat and was probably transported In. The occurrence of this brachiopod In a variety of lithoiogies suggests that although it was well adapted for life on muddy substrata in presumably quiet environments. It was able to colonize substrata deposited under different environmental conditions such as ones of greater turbulence, or In less sheltered areas. The mode of life of Diaphraomus (family Productldae) Is not as clearly understood. It probably lived seml-lnfaunally, stabilized by spines, with Its long trail extending upward away from the sedlment-water Interface. The brush of ear and flank spines and possibly trail spines would have helped hold the shells steady. Dlaohraomus cestrlensis Is widespread In upper Greenbrier units of ali three regions in the mudstone, wackestone, packstone and grainstone facies (Figure 65). It Is usually disarticulated and the ventral valve Is commonly preserved Figure 65: A.1 - A.3 - Protonlella parvus, x 1.1.; B.1 - B.6 - Ovatia elonoata. x 1.1; C.1 - C 8 ÇLIaphraqmus cestrlensis. x .9: D.1 - D.3 - EchinoconchiiR sp. y i 127 128 2 Figure 65 129 interior-up. Occurrences in the ostracode/calclsphere mudstone, (arenaceous, fossiilferous) mudstone and oolitic grainstone facies are rare, and it is assumed that they are not in situ. Distribution of Diaohraomus in the other facies suggests an ability of this brachiopod to survive in a variety of environments as the productids discussed above, its occurrence in lithoiogies representative of higher energy and/or unsheltered conditions is counter that of the Productldae of Muir-Wood & Cooper (1960). it seems clear, however, that adaptation for one environment would not necessarily preclude this brachiopod from living elsewhere. Echinoconchus sp. (family Echinoconchidae) is assumed to have lived in a manner similar to representatives of the Buxtonlldae such as Protonlella. Shells have broad umbonal slopes and massive umbones for posterior weighting on the substratum. There is no evidence of cementation in adults. Whether or not juveniles were attached by clasping spines can not be answered at the present time. Both valves have dense prostrate spines. Echinoconchus sp. occurs only in Region 2 in the fossiilferous mudstone facies (Figure 65). From this distribution, it appears that it may have been stenotopic for both substratum and other factors and lived most successfuiiy on muddy substrata in quiet environments. infiatia inflatus (family Marginiferidae) was also a free-living productid. it did not have abundant spines and probably lived as did other unattached productids, resting on the dorsal valve visceral disk, steadied by the umbo and a few spines, infiatia inflatus occurs in Regions 2 and 3 in the mudstone, wackestone and grainstone facies (Figure 66). it is particularly abundant in the (Arenaceous, Fossiilferous) Mudstone and Fossiilferous Mudstone subfacies in the southern portion of Region 2 and northern portion of Region 3. This brachiopod probably was stenotopic for factors other than substrata, and was most successful on muddy marine substrata. Strophomenids are represented in the Greenbrier Group by Orthotetes kaskaskiensis (family Orthotetidae). Alexander (1977) described O. kaskaskiensis as cemented to the substratum during youth stages. The small deithyriai chamber is filled with secondary shell material, eliminating the possibility of a pedicle in adult forms (Muir-Wood & Williams, 1965). Thus, O. kaskaskiensis was free living on the sea floor, it is found in wackestone, packstone Ftoure 66; A.1 - A.6 - InBMIa Inllalus. x .75; B.1. B.2 - 0flhslifisja§!as! 130 131 Figure 66 132 and grainstone facies of Region 1 and mudstone and grainstone facies of Regions 2 and 3 (Figure 66). In these environments of higher energy and possibly shifting substrata, the broad fiat shape of Q. kaskaskiensis most likely served to balance the shell on the substratum, in the case of the muddier facies, the large surface area created a "snowshoe effect" for buoyancy (see Thayer, 1975). Life orientation of £ . kaskaskiensis was concave side up (ventral valve), thus creating a space beneath its shell edge and the substratum, if O. kaskaskiensis inhabited waters of higher turbulence or were episodically disturbed by storm waves, such an orientation would have been ecoiogicaiiy unsound because a large current could easily flip the shell over to the more hydrodynamicaiiy stable concave down position, in a depositional environment such as one depositing grainstones and packstones, this may explain the high number of O. kaskaskiensis preserved dorsal valve up. Ruaosochonetes sp. (family Chonetidae) occurs in abundance in Region 3 in mudstone, wackestone and grainstone facies. Muir-Wood (1962) described the inferred life habits of the Chonetoidea and the following is a summary for chonetids in general. The shells have spines along the posterior margin which were probably for attachment or entanglement with other organisms. Additionally a minute foramen indicates the presence of a functional pedicle in juveniles. After attachment, the shell rested on the sea floor, ventral valve up with the spines acting as stabilizers or attachments. Larger chonetids with thickened convex dorsal valves were probably unattached and free living throughout life. This posterior thickening may have served as umbonai weighting, keeping the anterior margin directed upwards and free of mud. Chonetid-dominated paleocommunities were described by Koch (1981) and Boucot (1975). Associated iithoiogies were muddy, and Koch (1981) suggested that the turbidity may have been too high for other brachiopods. Thus, chonetids, in general, were more tolerant of muddy environments than other brachiopods. Their inferred mode of life was similar to that of Orthotetes in that quiet waters were necessary to avoid flipping into a more hydrodynamicaiiy stable position by a strong current. The predominance of Ruaosochonetes sp. on muddy substrata in this study suggests a preference for quieter environments and confirms Koch's (1981) hypothesis. 133 Spiriferld brachiopods are represented In the Greenbrier Group by Anthracosoirlfer oellaensls. A. breckinridaensis and Retlcularla sp (Figure 67). Alexander (1977) described the mode of life of members of the Splrlferacea and Reticuiariacea as stabilization on a rather wide interarea with or without a functional pedicle. The commissure would then necessarily be vertical. Specimens of Anthracosoirlfer from the Greenbrier Group have medium-sized interareas with small "deitidial" plates. The delthyrium and notothyrium are open which Indicates that a functional pedicle tethered this brachiopod to the substratum. Reticuiaria sp. has a small pedicle opening and narrow interarea and was also pedically attached throughout life (Alexander, 1977). A. oeiiaensis occurs in abundance in grainstone, packstone and wackestone facies in Region 1, in high abundance in fossiiiferous mudstone facies in Region 2 and in lower abundance in mudstone, wackestone, packstone and grainstone facies of Region 3. Region 1 abundance is highest in iithoiogies that are indicative of higher energy conditions. Shifting of the sediment on the sea floor was probably common under such conditions, but the pedicle attachment and interarea stabilization were apparently quite efficient for insuring successful colonization. The attachment also raised the commissure above the sea floor which may have helped to avoid smothering by fine sediment in the muddier facies. Morphologic variation In response to environmental conditions is extremely common in Anthracosoirlfer oeiiaensis and is exhibited in ail occurrences of this geographically widespread species, both within the Greenbrier and age-equivalent rocks elsewhere (Wulff, 1989b; 1990a; 1990b; 1991a; Chapter 6). Anthracosoirlfer breckinridaensis is confined to Region 1 in the Triiobite/Foraminifera rich packstone subfacies. An explanation similar to that for the A. oeiiaensis distribution can be applied to this brachiopod's occurrence. It fits into the round morphotype of Wuiff (1989b, 1990a, 1991a) and would most commonly occur on substrata with little or no mud. Reticuiaria sp. occurs only in Region 3 in wackestone and grainstone facies. The pedicle attachment may have helped to keep the brachiopod stable on the shifting substratum of the higher energy environment and also to raise the commissure above the sediment-water interface in the muddier facies. Figure 67: A.1 - A.24 - Anthrar.nspirifer peilaensis. x .6; B.1 - B .5 - A. breckinrldqenais, x .9; C.1 - C.6 - Reticuiaria sp., x 1.1. 134 135 # e # w » Figure 67 136 Brachiopods belonging to the genus Composite (family Athryldacea) are represented In the Greenbrier Group by numerous, moderately morphologically diverse Individuals of subouadrata (Figure 68). Alexander (1977) described members of the Athyrldacea as either unattached with the commissure horizontal or tethered by a functional pedicle. The pedicle foramen of Composite Is large relative to the shell size and lacks any sort of closing plates. A functional pedicle was therefore presumably present throughout life. Composite subouadrata Is present In every brachlopod-bearing facies, Indicating a eurytopic, very adaptable brachiopod. The genus Is more abundant and larger In the coarser grained facies In Region 1, where abundant bloclastic debris and carbonate grains provided ample attachment sites. The abundance may also suggest a preference for coarser substrata and higher energy conditions. Clelothvridlna sp. (family Athyrldacea) Is a rare brachiopod In the Greenbrier Group (Figure 68). The pedicle foramen of this genus Is relatively small suggesting a small, yet functional pedicle. The mode of life can be Inferred to have been similar to that of Composita. Clelothvridlna occurs In fossiiiferous wackestone facies where raising above the sedlment-water Interface may have kept It from getting smothered by mud and fine particles. The exterior ornamentation is characterized by concentric lamellae which extend anteriorly Into flat spines. These spines may also have served to raise the shell above the sedlment-water Interface or they may have been a protective device against shell-crushing predators. A third possibility Is that the lamellae, as ridges along the surface, might have functioned as pathways for sediment removal. Alvarez et al. (1987) described a similar situation In Athvrls camoomanesl. In which micro-frills on the shell exterior function as "rain gutters" and with the help of gravity, funnel accumulating sediment downward and off the shell. Martlnia contracta (family Martiniidae) has a similar distribution to the splriferlds and athyrlds, occurring In mudstone, wackestone, packstone and grainstone facies In all three regions (Figure 68). It Is Interpreted to have been stabilized by a functional pedicle and Interarea stabilization (Alexander, 1977), and lived similar to the splriferlds and athyrlds. Figure 68: A.1 - A.10 - Composite subouadrata. x 1.1; B.1 - 8.3 -ÇleIgthyrIdiDg sp., x 1.4; C.1 - C.4 - Martinia contracta, x .95. 137 138 B Figure 68 139 Brachiopods belonging to the genus Eumetrla (family Retzildae) occur in wackestone, packstone and grainstone facies (Figure 69). Eumetrla verneuliana is present in ail three regions and co-occurs with Eumetrla n. sp. in Region 1. They are interpreted to have lived tethered to the substratum by a fully functional pedicle (Alexander, 1977). Because this genus occurs in a variety of facies representing a variety of environmental conditions, particularly in Region 1. Eumetrla is interpreted to have been eurytopic for both substrata and conditions above the substratum. Although the mode of life is well suited for high environmental energies, it was able to live in quieter environments as well. The order Terebratuiida is represented by the rare occurrence of Girtveiia sp. (Figure 69). All terebratuiids were tethered to the substratum by a functional pedicle (Alexander, 1977; Muir-Wood et ai., 1965). These small, ovate brachiopods occur in the triiobite/foraminifera-rich packstone facies illustrating the need for a functional pedicle in this moderately energetic environment. As discussed above, the brachiopod fauna consists of seventeen species with individuals adapted for life on substrata ranging from muddy and soupy to coarser-grained and mobile. Although transportation, sampling and preservationai bias have altered the distribution to some extent, the numerous articulated specimens and degree of preservation indicate that most brachiopods are in situ (although not in life position). Seven species occur In ail three regions in a variety of facies (Figure 70). These brachiopods are interpreted to have been eurytopic and able to deal successfully with variations In substratum character, salinity and nutrient levels. It has been shown that the morphologic variability exhibited by Anthracosoirlfer oeiiaensis enabled it to live on various types of substrata (Wuiff, 1989b; Chapter 6). This study Indicates that A oeiiaensis was also able to deal successfully with changes in the physical factors listed above. Although the other brachiopod species associated with A. oeiiaensis may not exhibit morphologic variation, it is assumed that their adaptive capabilities were similar. Two species are limited to two regions (Figure 70). The distribution of Girtveiia sp. in the wackestone and packstone facies of Regions 1 and 3 suggests a tolerance for the 140 B é '- S M r i a v e m m i t a . x 1.1; B.1 - 8.2 - Eumetria n.sp., x 1.4; C.1 I I § § i ! l a i .1 :S .S I !s- ,! k. I ; 5 ! .? 2i & c = % I t) I t E < I ly Uî i I ill !!1 I REGION 1 X X XXX XXX X XX REGION 2 XX X X X XXXX REGION 3 XX XX XX XXXXX OSTRACOD/CALCISPHERE MUDSTONE XX X X X ARENACEOUS FOSSIUFEROUS MUDSTONE XXX XXX FOSSTUFEROUS MUDSTONE XX XXX AREN./AREN. FOSS./OSTRACOD MUDSTONE XXX X FOSSIUFEROUS WACKESTONE XXX X XX X XX XX XX FORAMINIFERA PACKSTONE XXX X X X XX XX FOSSIUFEROUS PACKSTONE XX X X OOUTIC FOSSIUFEROUS PACKSTONE XX FORAMINIFERA GRAINSTONE X X X XXXX FOSSIUFEROUS GRAINSTONE ILAGI XXXX ARENACF.OUS/PRI.OID GRAINSTONE X X X X X XX O O U TIC FOSSIUFEROUS GRAINSTONE XX FOSSTINTRACLAST FOSS. GRAINSTONE X X X Figure 70: Brachiopod distribution per region and per facies. 142 environmental conditions of both regions and perhaps an intolerance to the higher energy waters of Region 2. its functional pedicle may have served to raise the commissure of the brachiopod above the sediment-water interface rather than anchor it in a high energy environment. Alternatively, since its occurrence is rare, sampling or preservationai bias may have caused its ommission from the Region 2 collection, infiatia infiatus occurs in Regions 2 and 3. It occurs most commonly in mudstones but is also present in wackestones and packstones. This suggests an ability to live on a variety of substrata. It probably was stenotopic for factors other than substrata and was not capable of living in the semi-restricted waters of Region 1. Seven species are limited to a single region (Figure 70). The three confined to Region 1 occur in such low abundance that interpretation is difficult, it is assumed, at the very least, that these three species were tolerant of semi-restricted conditions. In Region 2, Echinoconchus sp. occurs in a mudstone. Because other productids are numerous elsewhere, and their mode of life is basically similar, Echinoconchus sp. is interpreted to have been stenotopic and limited to lower energy, well circulated waters. The three species limited to Region 3 occur mainly in mudstones and wackestones and are interpreted to have been stenotopic organisms adapted for life in open marine waters on soft substrata. Much of the Union Limestone in Region 3 was deposited in high energy waters. The absence of abundant brachiopods in the Union Limestone in this region (compared to the muddier Aiderson Formation) may be due to an inability to live in more turbulent waters. This compares to the brachiopod distribution in Region 2 where they only occur in the muddier facies of this high energy depositional environment. BRYOZOANS Bryozoans are locally abundant in the Greenbrier Group but rare to common overall. Diversity is low and the fenestrate genus Archimedes is dominant. Rhabdomesonid, trepostome and cystoporate bryozoans are rare to common. 143 The relationship between zooarium morphoiogy and environmentai energy has been recognized by numerous workers. Stach (1935, 1936) stated that the varying morphologies exhibited by bryozoans were phenotypic responses to the environment. Schopf (1969) reinforced this by noting that morphologies could be influenced by direct mechanical injury in a current, by the transport of abrasive sediment and/or by the transport of nutrients to and away from bryozoans. He stated "If a structural grouping Is to be considered ecoiogicaiiy significant, then a definite environmentai influence should be shown on the structure" (p. 235). In other words, a relationship shouid be determinabie between the actuai shape and form of the coiony and the environmentai conditions in which it iived. Physical disturbances may be caused by waves, currents, sedimentation and extreme fluctuations in salinity or temperature (Sverdrup et al., 1942 cited in McKinney & Jackson, 1989). The overall effect of such disturbance varies and is dependent on other factors. For example, the effect of strong water movement depends on the size and stability of the substratum. Aigae and seagrass that are relatively short-lived are essentially unstable substrata and more easily moved about than more permanent substata (i.e., coral) (McKinney & Jackson, 1989). Disturbance may have a biologic origin in the form of predation and/or bioturbation. However, both of these factors decrease with depth and the overall effects vary locally. For example, predation by grazers drops within 100 - 200 meters of the surface (Jackson & Winston, 1982). Deposit feeders that disturb and turn over the substratum are less effective below a few hundred meters (Thayer, 1983). Paleozoic bryozoan faunas are numerically dominated by erect species. Rigidly erect species were dominant grovt/th forms throughout epicontinental seas (McKinney & Jackson, 1989), averaging 10 - 30 cm in height. Archimedes sp., Fistulioora sp. and Tabuilpora sp. built large colonies on the floors of lagoons and shoals (McKinney, 1979, 1983). Most erect bryozoans in high turbulence settings were flexible and able to passively elastically deform in currents (McKinney & Jackson, 1989). This elasticity may also have benefitted colonies in areas of higher sedimentation. Fenestrate bryozoans are notably abundant in wackestone 144 facies where substantial mud was deposited. The weight of the accumulating sediment may have caused the coiony to bend, essentially passively shaking off sediment accumulating on the fronds. The most successful Paleozoic fenestrate bryozoans were the fenesteiiids (McKinney & Jackson, 1989). Fenestrate bryozoans are the most common bryozoans in the Greenbrier Group and Archimedes. Fenestella and Lvroooreiia have been described from these rocks (Figure 71). Small pieces of axial screws are numerous and axes with fronds still attached are common. Fenestrate morphoiogy is interpreted to have been an adaptive strategy for life in both vigorous and quiet water (McKinney & Gault, 1980). Fenestrates are uniiaminate rigidly erect colonies. They have narrow branches (averaging 2 mm wide) that can easily be broken in strong currents. The growth of dissepiments, linking the vertical branches together helps to decrease breakage. Genera with abundant dissepiments are more common in rocks interpreted to have accumulated in higher turbulence settings. Penniretepora. for example, has unlinked branches and, where in situ, is in mud-dominated deposits representing quiet conditions. Where more than one morphoiogy occurs, colonies with dissepiments are larger and more numerous (McKinney & Jackson, 1989). Archimedes was apparently restricted to relatively quiet water environments, and remains of Archimedes meadows are common in the lee of shoals (McKinney, 1979; McKinney & Gault, 1980; Wuiff, 1989a; 1990c) where water depth is interpreted to have been at or below normal wave base. Colonization in waters of higher energy was difficult for two reasons. Because the point of coiony origin is only about 1/5-1/10 the diameter of the higher portions of the coiony, stress on the base was high and breakage most likely occurred there (McKinney & Jackson, 1989). This weakness probably made life in turbulent settings difficult. Secondly, axes are much more durable than the fronds themselves, and naked axes present in grainstones and other iithoiogies indicating higher turbulence were transported from quieter settings. Unabraded fronds in Greenbrier rocks occur in the greatest abundance in various fine-grained facies. Figure 71: A.1 - A.3 - Archimedes sp., x .9; B.1 - Fenestella sensu iato, x 1.1; C.1 i=yi QRorella; D.1 - D.3 - trepostome, x 1.1; E.1 - cystoporate, Fistuiioora sp., x 1.2. 145 146 Figure 71 147 This location was ideal from a nutritional standpoint as well. As turbulent water washed over the shoal, it slowed sharply upon entering the lagoon waters. This decrease in flow would have allowed the plankton and other suspended nutrients to settle out (McKinney, 1979). Secondary spirals have been described as originating from whorl peripheries. It appears that at least In some localities, Archimedes reproduction was by fragmentation, not by larval recruitment (McKinney & Jackson, 1989). Archimedes was an opportunistic bryozoan, which must have reproduced rapidly In order to survive on unstable, shifting substrata such as In front of a migrating shoal. Fenestella occurs In a variety of Iithoiogies and was adapted to live In a number of environments and on a variety of substrata (McKinney & Gault, 1980). Fenestrate fronds that were not associated with Archimedes axes were Identified as Fenestella sensu lato. Lvroooreiia Is Interpreted to have lived In areas of unidirectional currents and shifting bottoms (McKinney, 1977). It lay on the sea floor, with the thickened margin facing upcurrent and the fan extending downcurrent. The zooeclal feeding surface faced away from the substratum. Lvroooreiia Is present In Iithoiogies that Indicate a close proximity to a shoal. It has the smallest fenestrules and lived In the most turbulent waters of all the fenestrates. This relationship suggests that fenestrule size may correlate with water energy and movement (McKinney, 1977). Non-fenestrate bryozoans In the Greenbrier, trepostomes, cystoporates (Figure 71) and rhabdomesonlds are not as abundant as the fenestrates. Some relationships between non- fenestrate bryozoans and their environment were discussed by Schopf (1969) and McKinney & Jackson (1989). The percentage of erect forms Increases relative to encrusters with Increasing depth. In addition, the ratio of flexible to rigid species changes sharply at about 35 meters depth, with more flexible forms being present In shallower water. Flexibility may be due to Jointing among the branches or a lightly calcified skeleton. These adaptations are directly related to water turbulence. The type of preferred substratum also changes with depth, with rocks and shells used more often In deeper waters. 148 In Region 1, units from the uppermost Greenbrier Formation contain the most abundant bryozoans. Archimedes, trepostomes, cystoporates and rhabdomesonids are common. Archimedes was present in float blocks from the upper Greenbrier at Sang Run. Large fragments plus axes occur in the uppermost Greenbrier Formation at Sang Run and Oakiand Quarries. In addition to Archimedes (axes and axes with fronds), rhabdomesonids, trepostomes and cystoporates were aiso coiiected at Oakiand Quarry. Rhabdomesonids are smali, stick-iike bryozoans. Fragments coiiected are no more than 0.5 cm in iength and oniy approximately 2 mm in diameter. The fragiiity of these thin-branched coionies aimost ensured breakage upon exposure to stronger than normai currents. The trepostomes and cystoporates are far iess common and occur as smaii fragments. The increase in bryozoan diversity in unit 7 at Oakiand Quarry accompanies a change to more normai marine conditions near the end of Greenbrier deposition. Their absence in older Greebrier strata indicates an intolerance of the stressful conditions that prevailed. No bryozoans were coiiected from localities in Region 2. Oniy the Union Formation was sampled in this area. The overall water turbulence remained high during deposition of the upper Greenbrier units and this, coupled with the increased siiiciastic component, may have prevented bryozoans from successfully inhabiting this area. in Region 3, bryozoans are abundant in the wackestone facies of the Aiderson Formation and in certain units of the Union Limestone that represent quieter environments. Archimedes dominates the bryozoan fauna in the Aiderson Formation, occurring mostly as axes with fronds. Qne locality contains bedding plane exposures that are covered with well preserved Archimedes coionies. Their biostratinomic utility was described by Wulff (1989c; 1990c). Trepostomes and cystoporates are iess common, usually occur as smali fragments of larger coionies and seem to occur mostly in muddy facies at Renick Valley and at R & R Quarry, it appears that these bryozoans were able to tolerate somewhat turbid environments. The bryozoan abundance in Region 3 reflects normai marine conditions as discussed in Chapter 2. 149 ECHINODERMS Echinoderms are moderately abundant In the Greenbrier units although most fossil material consists of columnal and other skeletal debris. All echinoderms, both modern and ancient, are exclusively marine and require normal marine conditions for successful habitation. They occur In association with other normal marine organisms such as corals, brachiopods and bryozoans. They are suspension feeders and the nature of their food gathering system requires some current or water agitation (Brelmer & Lane, 1978). For the sessile benthic echinoderms, a suitable substratum was also required. This explains their general absence from muddy environments where the absence of a firm substratum may have prevented settling. Modern crinolds have tissues that hold the skeleton together. Upon death and decomposition of these tissues, disaggregation rapidly occurs (Liddell, 1975; Meyer & Meyer, 1986). It Is assumed that ancient crinolds and blastolds had the same types of tissues, thus rapid decomposition and disarticulation must also have occurred. BLASTOIDS In 1957, Cline & Beaver wrote that very little had been published on the paleoecology of blastolds. In preparation for their manuscript on blastold paleoecology, 110 manuscripts were reviewed and no significant reference to life mode or character was noted. Very little has been published on this subject since then, and It Is still necessary to follow Cline and Beaver's suggestion that, "since blastolds typically occur with crinolds. It can be assumed that their life mode and character was similar to crinolds" (p. 955, Cline & Beaver, 1957). With no modern analog, comparison to crinolds Is the most desirable alternative. The Chesterlan of the Midcontinent and the Appalachian Basin Is known for the abundance of fenestrate bryozoans, and It was also the acme of development for the blastold genus Pentremltes. This blastold Is probably the most abundant and diverse blastold known (Waters et al., 1982). It Is common In shelf deposits mainly from North America (Waters et al., 1982) although It has been described from Columbia, South America as well (Fay & Wanner, 1967). Early and middle MIsslsslpplan Pentremltes Inhabited carbonate platforms with a few species capable of living In more clastic, deltaic environments. By the upper Meramecian, Pentremltes lived on 150 both carbonate platforms (l.e., Ste. Genevieve Limestone, Monteagie Formation) and deltaic environments (Floyd Shale). Waters et ai. (1982) noted that the morphologies of Pentremltes in the Floyd Shale were more diverse than those of the carbonate platform communities. With the onset of cyclic sedimentation and increased ciastic influx in the Chesterian of the midcontinent, Pentremites expanded and became the dominant echinoderm in both carbonate platform and deltaic communities. Morphologic diversity expanded as well, and the genus developed aimost the entire morphologic spectrum known for blastolds (Waters et ai., 1982). Three species of Pentremites. P. puicheiius. P. tuiioaformis and P. codoni were identified from Greenbrier rocks coiiected in this study (Figure 72). They occur aimost exclusively within the Union Limestone, and ail were coiiected in Region 3. The occurrence of Pentremites in the Union Limestone is divided among wackestones, packstones and grainstones. The associated fauna indicate that the environment was normai marine. As discussed in a previous chapter, the variations in mud and abundance of biociasts may be attributed to patchy distribution and bottom topography. Thus, the differences in overall environment may actually have been very slight and the overaii turbulence was moderate. Blastolds were coiiected at two horizons in the Aiderson Formation and they contrast sharply. At the R & R Quarry, Pentremites are rare and smaii. The facies is a fossiiiferous wackestone dominated by fenestrate bryozoans. Because bryozoans require essentially the same conditions as blastolds, this blastold may aiso have iived in this environment. However, the somewhat muddy substratum may have iimited the biastoid settlement. At Greenville, Pentremites occurs in moderate abundance at the base of the Aiderson Formation. The facies is an oolitic grainstone, and, as noted in a previous section, this depositional environment was not very different from the uppermost Union Limestone at this locaiity. The more turbulent waters and increased circulation were dearly beneficial to the blastolds and other normai marine organisms within this facies. GRiNOiDS The crinoid genus Pterotocrinus is present in the Greenbrier Group. Pterotocrinus is a morphoiogicaiiy unusual crinoid, and its paieoecoiogy is not weii understood. At least three Figure 72: Pg^remltes, A.1 - A.3, x 1.4: Pterotocrinus serratus. B.1, x 1.6; Paladin chesterensis - C.1 - 0 .3, x 1.55; 0.4 - 0.5, x 1.5; 0.6, x 2.8. — 151 152 B.1 'y. A .>rr Figure 72 153 different hypotfieses have been proposed for the function of the tegmen wing piates. Chestnut & Ettensohn (1984) suggested that aduit specimens of Pterotocrinus lived with their calyces on the substratum. The wing plates served as stabilizers on the sediment surface and prevented foundering and smothering. Welch (1978) proposed that the wing piates may have originally served a protective function. They later served as vanes, tunneling water and nutrient flow through the arms to the ambuiacrai side. Baumiiier & Piotnick (1989) proposed a completely different interpretation, it was assumed that this crinoid had a parabolic filtration fan feeding posture as described by Macurda & Meyer (1974). its outstretched arms formed a circular filter with the concave (aborai) side facing into the current. Accepting the rheophiiic nature of crinolds (Brelmer, 1969) and a parabolic filtration fan feeding posture, Baumiiier & Piotnick (1989) suggested that the wing piates of Pterotocrinus deoressus served as a rudder mechanism for passive reorientation and gave it rotational stability in the current. Pterotocrinus serratus Weiier is the only identifiable crinoid coiiected. It was identified by its distinct wing piates which occur in moderate abundance in Region 3 (Figure 72). The wing piates occur in ail four major facies, and the degree of preservation indicates that some are relatively in situ while others were transported. By comparison with other crinolds, it can be assumed that Pterotocrinus serratus iived in moderately agitated, clear, normai marine waters. Several additional crinoid genera from the Greenbrier Group have been coiiected and described by other workers. These are noted in the tables in Chapter 5. TRiLOBiTE One triiobite species. Paladin chesterensis. was recognized from the Greenbrier rocks studied (Figure 72). Brezinski (1983) discussed the paieoecoiogy of P. chesterensis and interpreted it to have been a mobile, benthic, eurytopic, deposit feeder (Brezinski, 1983). Some workers now feel Paladin may have been more of a filter feeder (Schmalfuss, 1981). Characteristics that are present in £ . chesterensis that are supportive of a benthic, filter feeding habit include, position of the terrace lines [most of which are on the doublure] and presence of a weak anterior arch which facilitated development of ventral feeding currents. 154 The short preglabellar area and inflated glabella are also indicative of plowing in the substratum. The absence of splnoslty and lack of exceptional reduction of pleural areas suggests that f . chesterensis was not a strong swimmer (Fortey, 1985). In Pennsylvania, P. chesterensis co-occurs in abundance with infaunal deposit feeding bivalves and, to a lesser extent, productid brachiopod-dominated associations (Brezinski, 1983). Based on studies by Bretsky (1969) and Stanley (1970) on moliuscan-dominated faunas in nearshore environments, Brezinski (1983) suggested that P. chesterensis was preferentially a nearshore, muddy bottom dweller. Brezinski (1983) attributed the decreased triloblte abundance In the more offshore, productid brachiopod associations to the decrease in nutrients in the substratum. Paladin chesterensis occurs in Upper Mississippian rocks throughout the Appalachian Basin (Easton, 1942; Tissue, 1986; Brezinski, 1983, 1989; Wulff, this study), the midcontinent (Chamberlain, 1969; Weller & Weller, 1936) and Utah (Chamberlain, 1969). it has been coiiected from calcareous shales and shaiy limestones in Pennsylvania (Brezinski, 1983, 1988) and from fossiiiferous wackestones, packstones and grainstones in western Maryland and West Virginia (Tissue, 1986; Wulff, this study). P. chesterensis occurs In moderate abundance in Maryland and West Virginia. Specimens are preserved as isolated scierites and are either pygidia or cranidia with no free cheeks. Oniy one complete cephaion was coiiected (Figure 72). Occurrences are essentially limited to Region 1 where. In agreement with Brezinski (1983), they are associated with productids and other brachiopods. The iithofacies ail contain a mud component, and the substratum was most likely stable. As described in a previous chapter, this environment was a shallow shelf and certainly offshore compared to the bivalve dominated communities in the overlying Mauch Chunk deltaic complex. The rare occurrences off. chesterensis outside of Region 1 can not be addressed. Too little information is available to determine whether or not they are in situ. Thus, based on the environmentai interpretation discussed in chapter 2, and the discussion presented above, P. chesterensis is interpreted to have been a relatively eurytopic triloblte capable of living under a variety of conditions and on various substrata. 155 FORAMINIFERA Endothyrid foraminifera (family Endothyracea) are widespread across the field area. They are present in virtually every major tithofacies (mudstone, wackestone, packstone and grainstone) and in several environmental settings (Figures 73 & 74). Numerically, they are more abundant In wackestone, packstone and grainstone facies. McKay and Green (1963) described endothyrlds and related foraminifera as commonly occurring with crinolds, corals, brachlopods, bryozoans, molluscs, gastropods, ostracodes and algae In rocks of shallow water origin. Environments In which they occur are Interpreted as shoals and represent Initial stages of deposition in environments of restricted circulation. They are absent from lagoonai and evaporlte environments (McKay & Green, 1963). Their occurrence In Greenbrier rocks other than gralnstones Indicates a more eurytopic nature (c.f. McKay and Green, 1963) and an ability to tolerate muddy substrata and possibly turbid waters. The endothyrlds occur In ail llthologles In Region 1 (Figure 73). In Region 2, their occurrence In basically ail major llthologles Indicates that apparently the Influx of quartz sand was not detrimental to their survival. Endothyrlds are restricted to the Union Limestone In Region 3. They are rare or absent In the Alderson units. In this area, they represent the standard endothyrid distribution, being more abundant In packstone and grainstone units. The endothyrid distribution Illustrates two situations; presence across a changing environmental gradient and presence-absence across a change In llthoiogy. BIserlal foraminifera have a limited distribution (Figures 73 & 74). They are are absent from the mudstone facies of all three regions. This may suggest a low tolerance to muddy substrata or amount of suspended sediment. Unlserial foraminifera were identified In a fosslllferous packstone In Region 3 (Figure 73). The scarceness of these foraminifera do not allow for any paleoecologlcal Interpretation. In general, foraminifera decrease In abundance with a corresponding Increase In ostracode abundance (Benson, 1961) and thus can be used to Indicate changing environmental conditions. The appearance of foraminifera at the base of the upper Limestone Member of the Greenbrier Formation In Region 1 Illustrates this point. It signals the beginning 156 £ I ÜiI 03 D REGION 1 # REGION 2 ## REGION 3 # • • OSTRACOD/CALCISPHERE MUDSTONE • ARENACEOUS FOSSILIFEROUS MUDSTONE • FOSSILIFEROUS MUDSTONE • MUDSTONE/DOLOMITIZED MUDSTONE • AREN./AREN. FOSS./OSTRACOD MUDSTONE • FOSSILIFEROUS WACKESTONE • • ARENACEOUS WACKESTONE • FORAMINIFERA PACKSTONE • FOSSILIFEROUS PACKSTONE • • • AREN. (FOSSILIFEROUS) PACKSTONE OOLITIC FOSSILIFEROUS PACKSTONE • FORAMINIFERA GRAINSTONE • BRYOZOAN GRAINSTONE • ARENACEOUS/PELOID GRAINSTONE • OOLITIC FOSSILIFEROUS GRAINSTONE • • FORAMINIFERA PELOID GRAINSTONE • Figure 73; Foraminifera distribution per region and per facies. 157 Figure 74: A. Endothyrid foraminifera, x 25. B. Biseriai foraminifer, x 25. Field of view for 25 X magnification equals approximately 4.2 mm and for 63 x equals approximately 1.3 mm. 158 of gradational change to more open marine conditions from the restricted conditions recorded in the middle member stratigraphicaiiy beneath it. GASTROPODS Three gastropod genera have been reported from the Greenbrier Group and two were collected in this study fNaticoosis (Naticopsis) and Straoaroilus (Euomohaiusl) (Figure 75). They occur only in Region 1 where they are rare to common. Yocheison (1971) described gastropods belonging to the family Euomphaiacea as living a sedentary life, resting with their apertures perpendicular to the substratum. He argued that an animal with open coiling such as euomphaiacids would have difficulty balancing the shell during locomotion. They apparently adopted an unusual gastropod posture, that of lying fiat on the sediment and rarely raising the aperture above the cephaiopedai mass (Linsiey, 1977). The open coiling would increase the area of contact with the substratum, and the aperture would necessarily be raised above the sediment. For a coiled, sedentary animal living on a mud bottom, this shape change would be a natural response (Yocheison 1971). Euomphaiids may have been deposit feeders rather than herbivores, and open coiled forms may have become further specialized toward ciliary feeding (Yocheison, 1971; Linsiey, 1977). McLean (1981) compared Euomphaiids with modern gastropods in support of the filter-feeding hypothesis and noted that discoidai or open-coiied shells with radial apertures are different from those of motile gastropods which have tangential apertures and thus the capacity to balance their shells over the cephaiopedai mass. The gastropods at Deep Creek Quarry occur only in the upper units. The matrix filling their shells is muddier and lighter in color than the surrounding matrix and may indicate transport prior to burial. This would indicate lower faunai diversity yet in this region. OSTRACODES Ostracodes are present In every type of habitat where water is present (Benson, 1961; Pokorny, 1978). interpretation of ostracode paieoecoiogy includes among other things. Figure 75: Naticopsis (Naticoosls) sp., A.1 - A.3, x 1.4; Straoaroilus (Euomohaius) sp., B.1 B.2, X 1.1; Ostracodes, 0.1, x 25. 159 160 B Figure 75 161 consideration of their association with other organisms. Some ostracodes are usefui as paieoecoiogicai indicators of brackish or fresh water sediments (Benson, 1961). Species may be benthic, nektobenthic, peiagic, commensai or parasitic. Saiinity is a fundamentai factor in the distribution of ostracodes. Nearshore species are typicaiiy euryhaiine aiiowing for accommodation to fluctuating saiinity levais typical of shallow lagoonai waters. Species diversity in the nearshore environment is low compared to that of less brackish settings. Brackish water ostracodes are sometimes present in hypersaiine lagoons. Because of their tolerance to fluctuating saiinity levels, they commonly live in waters that are too saline for most normal marine ostracodes (Benson, 1961). As salinity decreases in a given environment, ostracodes become dominant as foraminifera and other major marine groups disappear. The opposite relationship is exhibited in the sequence of DC-0, DC-1, DC-2, in these units, the ostracode abundance decreases as foraminifera abundance increases. Since endothyrlds are most commonly present in waters of normal or near normal saiinity, this suggests changing saiinity levels in the area. Texture and stability of the substratum also play a role in ostracode distribution and diversity. Smooth shelled forms commonly occur in fine-grained muddy sediments whereas rougher, more ornate forms occur In coarser, more calcareous sediments. Because the ostracodes in this study are described only from thin section and the nature of their tests can not be determined (Figure 75), a detailed paieoenvironmentai interpretation utilizing ostracodes can not be made. ALGAE Wray (1977) provided a detailed analysis of calcareous algae and the points pertaining to algae identified in the Greenbrier are summarized below. CALCAREOUS GREEN ALGAE Dasyciadaceans (family Dasyciadaceae) have both living and fossil genera. Extant genera are tropical to subtropical marine plants that live in shallow, warm marine waters. A few genera do live in warm temperate environments. The plants waters of normal saiinity, and 162 their depth range Is from Just below low tide to approximately 30 meters. Dasyclads grow upright in sand and mud bottoms and many attach their rhizolds to firm objects, such as shells, In the loose sediment. These plants occur only In quieter regimes, either below fair- weather wave base or In protected areas. They are the typical algal flora In modern marine lagoons. Elliot (1968) determined that the ecological requirements of fossil dasyclads were essentially the same as those of living descendants. Thus, we can use the extant genera as analogs for Interpreting the paieoecoiogy of the fossil genera. The dasyclads Identified In this study occur almost exclusively In Region 3 where normal marine conditions prevailed throughout deposition of the Greenbrier (Figure 76). Two rare occurrences In units from Region 2 suggest that they were probably present to the north as well. They are most common In fosslllferous and oolitic grainstone and are common to rare In the packstone and wackestone facies. This distribution contradicts the normal distribution described above and the only explanation is that these tiny fragments were transported prior to burial. Because lateral variations In llthoiogy and faunai components are so common In this study area, even a short distance may have taken the plant remains from Its sheltered environment to a more turbulent one. BLUE GREEN ALGAE Margulls & Schwartz (1982) have recently assigned Blue-green algae to the Kingdom Monera, Phylum Cyanobacteria. Most paleontologists still recognize these organisms as algae and I have kept them In the Kingdom Plantae to avoid confusion. These organisms are characterized by simple filaments and coccold forms and are generally of microscopic size. Most living species are enclosed in a mucllagenous sheath, and It Is believed that CaCOg, when precipitated. Is deposited In this sheath. These calcified sheaths are the principal kinds of skeletal carbonate produced by blue-green algae. Living blue-green algae usually secrete CaCOg In subaerial, brackish and freshwater environments and only rarely In normal marine waters. Because fossil forms are widespread In marine rocks. It Is possible that unlike the dasyciadaceans, a modern example Is not an appropriate analog for paleoecologlcal Interpretations. 163 Figure 76: Dasyciadaceans, x 25. 164 GIrvanella is characterized by flexible, tubular filaments of uniform diameter. The filaments have relatively thick calcareous walls, are unsegmented and rarely branch. Individual filaments may occur, but groups are more common, twisting together to form nodules. GIrvanella Is a very common algal component and has a worldwide distribution. It Is most common In the Paleozoic and Is unrecorded In the Cenozolc. It has been suggested that GIrvanella may actually be the remains of numerous taxa which may belong to several families of blue-green algae (Wray, 1972). Because of this. It Is not possible to set limits on Its depth. GIrvanella (and GIrvanella-llke algae) occur most commonly In Region 3 with a few recorded from Region 2. It occurs In a wide range of llthologles from mudstone to grainstone (Figure 77). Both clumps of filaments and single filaments are common. Wray (1977) makes no statement as to the apparent environmental preferences of GIrvanella. Based on the distribution and co-occurrence with other algae. It Is assumed that they had similar écologie preferences and that substantial transport of the Individual masses and filaments has taken place. Sohaerocodlum Is an encrusting algae that Is restricted to marine sediments and commonly occurs In reef settings (Wray, 1972, 1977). It actually represents a symbiotic relationship between the red alga Rotholetzella and the encrusting foraminifera Wetheredella (Wray, 1977). It occurs In moderate abundance In Region 3, particularly at the Salt Sulphur Springs Quarry and roadside reef (Figure 78). The most obvious occurrence Is Its encrustation of a syrlngoporld coral colony (Chapter 7). It appears to encrust nearly the entire surface of each coralllte In the colony and In places. Is so massive that It joins corallltes together (Figure 78). In places, the algae appears to encrust the substratum as well. If the coral were alive at the time of encrustation, this association may be an example of mutualism. Additionally, It would have contributed to the reef core framework as It did In the Devonian reef complexes of western Australia (Wray, 1972). Because It was also described from two other localities. It Is likely that the distribution was wider and occurrences were overlooked or not represented In thin section. 165 Figure 77: GIrvanella sp., x 25 166 Figure 78: Sphaerocodlum sp., A. x 25; B. x 63 167 CALCISPHERES Calcispheres are calcareous, hollow spherical bodies with well defined walls. The walls may have several layers and some have radially arranged spines on the outer surface. They average between 75 and 200 microns In diameter (Wray, 1977; Brasier, 1980). Calcispheres are widely known from upper Paleozoic limestones, especially the Devonian and Carboniferous (Wray, 1972). The origin of calcispheres Is unclear and workers have referred them to both plant and animal origin (Stanton, 1963; Rupp, 1967). The generally accepted interpretation is that they are oogonia of calcareous algae. Rupp (1967) noted that the non ornamented fossil calcispheres resemble the reproductive cysts of living dasycladacean algae (subfamily Acetabularlae). Additionally, Marszalek (1975) described a modern calclsphere- produclng alga Acetabularla In south Florida. As a whole, the Acetabularleae can tolerate salinities ranging from hypersaiine to brackish. They can also withstand wide variations In temperature (Wray, 1977). Thus, their occurrence In lagoonai or restricted settings Is to be expected. Fossil calcispheres commonly occur In lagoonai limestones from the Devonian onward (Brasier, 1980; Scholle, 1983; Pokorny, 1978). They occur In rocks interpreted to have been deposited in shallow environments of restricted circulation (CarozzI, 1961b; Wray, 1972). For example, the shelf facies of Devonian reef complexes in western Australia and western Canada, which formed In lagoons or back reef environments, are characterized by three main faunai elements. They are radlosphaerld calcispheres, Vermlporella segments and GIrvanella (Figure 79) (Wray, 1972). This fossil distribution is similar to that of living Acetabularla. The calcispheres from the Greenbrier rocks occur most commonly In Region 1, and are most abundant In the calclsphere/ostracode mudstone facies (Figure 80). They also occur in other mudstone facies In Region 1 and it may be suggested that they reflect restricted lagoonai conditions. They have micrltlzed tests and faint walls. Their association with ostracodes and the absence of normal marine fauna also reflects restricted lagoonai conditions. b a s in l a g o o n lA REEF Ba c k reef Figure 79: General occurrence of calcispheres and associated algae ii in the marine environment. Modified from Wray. 1972. cn 0 0 169 Figure 80: Calcispheres, x 25. CHAPTER IV FAUNAL ANALYSIS AND PALEOECOLOGY INTRODUCTION In any setting, the survival of the fauna Is based not only on the ability of Individual organisms to Interact with their environment but also on each Individual’s ability to live successfully among other organisms In its Immediate surroundings. This includes both members of the same species and members of different species. This paieoecoiogicai anaiysis of the Greenbrier fauna reveais trends in faunai distribution that mirror the facies and environmental conditions discussed in Chapter 2. This chapter discusses the paieoecoiogy of individual groups of organisms as they occur In the Greenbrier Formation of north-central West Virginia and western Maryland and In the Union Limestone and the Alderson Formation of southeastern West Virginia (Figure 3). The faunai content and lithologie character of these units, indicate that environmentai conditions across the region ranged from semi-restricted, lagoonai in the north to open marine and weii circulated In the south (Wulff, 1990d; this study). The field area was subsequently divided into three regions based on these environmental Interpretations (Figure 10). Variations in bottom topography and the presence of sheltered areas (i.e., large depressions, lee side of mounds, etc.) resuited in a great deai of iithoiogic variabiiity within each region. Because many of the lithofacies contain the same or simiiar bioclastic associations, it was determined that aside from differences in turbulence, physical conditions above the sediment-water interface, such as temperature and salinity, did not differ greatiy between the wackestone, packstone and grainstone facies. Thus, the differences In faunai diversity in these lithofacies is better attributed to deposition in sheitered versus non-sheltered areas, in addition to preservation and sampiing bias (Wuiff, 1990d; this study), in contrast, highly fosslllferous mudstones were interpreted to have formed under different environmental conditions. 170 171 METHODS Appendix H contains a listing of ail taxa identified in this study and the localities where they occur. Autecology was discussed in Chapter 3. A qualitative separation into "faunai associations" was made based on examination of the faunai diversity and relative abundance in each region and in each stratigraphie horizon. Each region, because it had particular environmental conditions (i.e., lagoonai, high turbulence or open marine), contained an overall faunai assemblage that was not present in either of the other two regions. The members of the Greenbrier Formation in Region 1 each contain one unique faunai association. In Region 2, the faunai associations occur throughout the section. The faunai associations in Region 3 are unique to either the Union Limestone or the Alderson Formation. Thus, the overall differences between these units reflect regional and environmental variabiiity. Cluster anaiysis was applied to this data set to explore patterns of faunai associations. SYSTAT version 3.2 was employed on a Macintosh lici computer. Presence-absence data was clustered using euclidean distance and complete linkage. Dendrograms created by this analysis are illustrated in Figures 81 through 85 and are discussed below. Because presence-absence data were used, no distinction Is made between rare and abundant constituents. Additionally, because of the equal ranking rare occurrences receive in cluster analysis, the dendrograms that result from analysis of taxa per unit by locality do not accurately represent the faunai distribution. Thus, cluster anaiysis was performed utilizing taxa per region subdivisions. Raw data are listed in Appendix I. It was not possible to sample sufficient material from laterally adjacent facies for paleocommunity anaiysis. Rather, faunai associations that could be collected are time- averaged because they occur vertically throughout the section. They are interpreted in terms of the faunai component and their ability to live under specific conditions and in certain types of environments as represented by the variety of facies in which they occur. These faunai associations are unique to each region. Trophic structure anaiysis and relationship to the substratum are used to interpret the paieoecoiogy of these associations. The term "faunai association" rather than 172 "paleocommunity" is used to refer to the fossils present for the following reason. Paleocommunity analysis assumes that all associations were collected from laterally equivalent units and are therefore age equivalent as well. Interpretations are made for specific points In time. As discussed above, these faunai associations occur throughout the Greenbrier units and are not necessarily laterally equivalent. Thus, a traditional community paleoecologic Interpretation can not be made. Troohlc Structure Trophic structure refers to the various food gathering strategies employed by the organisms In question. Two trophic strategies are common In the Greenbrier units, suspension feeding and deposit feeding. Both of these can be further Interpreted using the tiering Ideas of Ausich and Bottjer (1982). Tiering Is "the establishment of a community structure In which different organisms are distributed vertically In space" (Ausich & Bottjer, 1982). Primary tierers are suspension feeders whose bodies or burrows Intersect the sea floor (Bottjer & Ausich, 1986). Secondary tierers are suspension feeders that live at some level above or below the sedlment-water Interface but do not maintain contact with the sediment- water interface. These may be epizoans living on primary epifaunal tierers or plants, or they may be living In the burrows of primary infaunal tierers (Bottjer & Ausich, 1986). In areas with high population density, this distribution In elevation above the sea floor allows organisms to maximize their feeding potential and may lessen direct competition for food and space. Tier Structure Maximum tier structure In the Greenbrier faunai associations consists of two epifaunal tiers and one Infaunal tier. The first epifaunal tier is 0 to 5 cm above the sedlment-water Interface and the second Is greater than 5 cm. The infaunal tier Is 0 to -5 cm below the sedlment-water Interface. Suspension feeding, deposit feeding and possibly grazing strategies were all present In these faunai associations. Although tiering was originally described for suspension feeders, it can also be applied to deposit feeding organisms. Trophic strategies in the first epifaunal tier Include both suspension and deposit feeding. Suspension feeders include brachlopods, some bryozoans (i.e., rhabdomesonids) 173 and solitary corals. Deposit feeders may Include trilobltes, gastropods and benthic foraminifera. Trophic strategies In the second epifaunal tier consisted solely of suspension feeders. These are colonial corals (I.e., syrlngoporaceans), some bryozoans (I.e., Archimedes. Fenestella. branching trepostomes, etc.) and pelmatozoans. Because stalked echlnoderms grew to different heights within the second tier. It was actually subdivided further perhaps creating a third epifaunal tier. Benthic foraminifera and some ostracodes may also have occupied this tier as secondary tierers by attaching to the blades of marine grasses. Gastropods may have become secondary tierers when they attached themselves to sea grass, octocorals or other elevated organisms. Feeding off algae that may have been growing on these organisms, the gastropods would then be classified as grazers. Trophic strategies In the Infaunal tier were either suspension or deposit feeding. In this study, bivalves were the only occupants of this tier. Suspension feeders are the most common In these associations. They may be either active suspension feeders In which ciliary action Is used to draw food particles Inward to the food gathering apparatus; facultative suspension feeders In which the ambient current Is used alone or with ciliary action; or passive suspension feeders In which the ambient current Is solely relied upon to bring food particles to the food gathering apparatus (LaBarbera, 1984). Some brachlopods may have been facultative suspension feeders, whereas others may have been active suspension feeders. The same was likely true for bryozoans (LaBarbera, 1984). Brachlopods and bryozoans used ciliary action to enhance the flow of nutrients toward their mouths (Boardman, 1983; Rudwick, 1965). Some pedically attached brachlopods were rheophlllc and could orient themselves In the current (LaBarbera, 1978; Richardson, 1981a). Brachlopods, although selective In the material actually Ingested, take Into their systems a wide variety of particles In a wide size range (Rudwick, 1965). Undigested material and particles that are too large for the food groove of the lophophore are passed back out via mucous strands. It Is probable that Paleozoic brachlopods fed In the same manner. Crinolds are passive suspension feeders. Most Paleozoic crinolds were rheophlllc and actively oriented In the current with their aboral sides facing upstream (Macurda & Meyer, 174 1974; Warner, 1977). Because crinolds usually fed from horizontally flowing currents, occupation at different heights above the sedlment-water Interface decreased direct competition for food (Lane, 1963, 1973). Size selectivity for food further reduced any competition (Ausich, 1980, Lane, 1973). It can be assumed that this same situation applied to blastolds as well. Some bivalves were also suspension feeders. Living partly to entirely burled In the substratum, they extended their siphons slightly up Into the water column. Deposit feeders are not diverse In these associations. Like modern benthic foraminifera. It Is probable that Greenbrier foraminifera fed on small bacteria, algae, protlsts and Invertebrates (LIpps & Valentine, 1970). Some even scavenge for dead organic particles. Trilobltes present In the Greenbrier probably established feeding currents along their ventral sides. Organic materials entrained In the currents may have been from stirred-up deposits or from suspension. Some bivalves were deposit feeders. Rather than extending siphons In the water column and passively filtering, they probably used their siphons to browse the sediment around their burrows for food. OTHER FACTORS IN FAUNAL ASSOCIATION DEVELOPMENT Crowding or space competition might also have been a factor In faunai association development. Some sessile benthos are able to make room for themselves by growing over other organisms or poisoning them by stinging (I.e.. Montastrea annularis: Scatterday, 1977). It Is unlikely that any organisms In these associations had that capability. Corals and bryozoans may have changed their growth vectors to move away from the crowded areas and brachlopods developed unusual morphologies In order to better fit Into a crowded area. No aggressive or active competition for space was documented In this fauna. Predation plays an Important role In any analysis of faunai associations. Of the fauna present In the rocks studied, only the cephalopod collected at the R & R Quarry, can be confidently classified as a predator. However, Paladin and ostracodes could have been predators as well. Mobile organisms such as fish and other cephalopoda were predators and their absence In these rocks may be explained by two factors. First, as a function of the 175 food chain and energy transfer, larger predators naturally occur In lower abundance. Second, mobile organisms have a lower chance of being preserved In a given environment. Opportunistic species might also be considered In a paleoecologic study. Such species can be recognized by the following criteria (Dodd & Stanton, 1981). Opportunistic species are very abundant within a faunai assemblage and are widespread over a given Isochronous horizon. They may occur In several horizons between barren Intervals. They are present In a variety of facies and external morphologies can be variable. Finally, they are abundant In easily distinguishable fossil associations. These criteria should be combined with sedlmentologic evidence for transportation and sorting to Insure that In situ faunas are being analyzed. Two brachlopods In this study, Anthracosolrlfer oellaensls and Comooslta subauadrata. are probably opportunistic species. A discussion of their occurrences Is Included In the description of Faunai Association 2. TROPHIC ASSEMBLAGES Trophic assemblages, as defined In this study, refer to the combination of feeding strategies (trophic structure) and tiering arrangement. Two simple trophic assemblages are present In the units studied. Trophic Assemblage 1 contains organisms that occupy the first tier. It contains any combination of the first tier dwellers discussed above. Trophic Assemblage 2 contains organisms that occupied both the first and second tiers. This contains any combination of the fauna discussed above with at least one taxon from tier 2. Food resource partitioning In both trophic structures was fairly well developed based on particle size preference, type of nutrients and elevation In the water column. The algae and calcispheres do not figure Into either structure because they are the base of the food chain and do not compete for space or food. Another way to look at the faunai distribution Is by niche occupation. Because this Is Intimately related to tiering and trophic strategies, an In- depth discussion Is not Included. A summary of niche occupation per region Is contained In Table 6. TABLE 6: FAUNAL ASSOCIATIONS & NICHE OCCUPATION REGION/ TROPHIC FREE FREE ATTACHED ATTACHED FAUNAL ASSOC STRATEGY IMMOBILE MOBILE LOW HIGH 1/ SUSPENSION/ D'taphragntus cestriensis Ostracods Anlhracospirifer Fenestella sensu lato FA-1 FILTER Oyuiiadongata Bivalves pellaensis PnXonieUa parvus Compositasubquadrata Orthotetes kaskaskiensis M artinia contracta DEPOSrr/GRAZERS Endothyraceans PHOTOSYNTHESIS Girvanella? Calcispheres 1/ SUSPENSION/ Dii^hragmus cestriensis Ostracods Anthracospirÿer pellaensis Pelmatozoan debris FA-2 FILTER Ovaliaelongata Bivalves Anirhacospirifer Biyozoan fragments Orthotetes kaskaskiensis Paladin chesterensis breckinridgensis Protoniella parvus Compositasubquadrata Rugose corals M artinia contracta Pahieacissp. Banetriavemeuliana Eumetriansp. Girtyellasp. DEPOSrr/GRAZERS Endothyraceans Naticopsis (Naticopsis) Straparollus (Euomphalus) PHOTOSYNTHESIS Calcispheres 1/ SUSPENSION/ Orthotetes kaskaskiensis Bivalves Anthracospir^er Pelmatozoan debris FA-3 FILTER Protoniella? parvus Paladin chesterensis pellaensis Archimedessp. Rugose coral Compositasubquadrata Fenestella sensu lato Fistidiporasp. Trepostomes Rhabdomesonids Cystoporates Trepostomes LyroporeUasp. Cystoporates comulitellid DEPOSrr/GRAZERS Endothyraceans TA B LE 6 (continued) REGION/ TROPHIC FREE FREE ATTACHED ATTACHED FAUNAL ASSOC STRATEGY IMMOBILE MOBILE LOW HIGH 2 / SUSPENSION/ Echinoconchiasp. Ostracods Anthracospirifer Pelmatozoan debris FA-4 FILTER Ir^ a tia ii^latus pellaensis Ovatia elongala 2/ SUSPENSION/ Diaphragmus cestriensis Anthracospirifer FA-5 FILTER Ir^latia U^latus pellaensis Orthotetes kaskashensis Compositasubtptadrata Rugose coral Eumetria vemeuliana M artinia contracta DEPOSIT/GRAZERS Endothyraceans 2 / SUSPENSION/ Ostracods FA-6 FILTER DEPOSrr/GRAZERS Endothyraceans PHOTOSYNTHESIS Calcispheres Dasyciadaceans 2 / SUSPENSION/ Bivalves FA-7 FILTER Avicitlopectensp. DEPOSrr/GRAZERS ■ PHOTOSYNTHESIS Plants (unident.) TABLE 6 (continued) REGION/ TROPHIC FREE FREE ATTACHED ATTACHED FAUNAL ASSOC STRATEGY IMMOBILE MOBILE LOW HIGH 3/ SUSPENSION/ Cleioth^idinasp. Ostracods Anihracospirÿer pellaensis Archimedessp. FA-8 FILTER Diaphragmus cestriensis Bivalves Composilastdrquadrata Pelmatozoan debris Injlatia inflatus Paladin chesterensis Eunulria vemeuliana Pterotocrinus serratus Orthotetes kaskaskiensis Girtyellasp. Pentremilessp. Reticulariasp. M artinia contracta Rugose coral Trepostome bryozoans? Syringoporid coral DEPOSrr/GRAZERS Endothyraceans Biseriai forams Uniserial forams Gastropods Cephalopod PHOTOSYNTHESIS Calcispheres Dasyciadaceans Girvanella? 3 / SUSPENSION/ Diaphragmus cestriensis Bivalves Anthrace^irifer pellaensis Archimedessp. FA-9 FILTER I i ^ t i a inflatus Con^xailasiéquadrata Trepostome bryozoans Orthotetes kaskaskiensis Eumetria vemeuliana Pterotocrinus serratus Rugosochonetes sp. Girtyellasp. Pentremilessp. Rugose coral RhWidomesonid bryozoans Pelmatozoan debris Trepostorae bryozoans? DEPOSrr/GRAZERS Endothyraceans PHOTOSYNTHESIS Dasyciadaceans C3 179 CLUSTER ANALYSIS OF LOCALITIES AND TAXA Figure 81 contains a dendrogram of localities clustered by taxa for all three regions. Three major clusters are noted and, with the exception of a few localities, confirms the division of the field area Into three regions. Ciuster 1 contains ail three localities from Region 1. Cluster 2 contains Region 3 localities plus the Region 2 locaiity Monterville Quarry. It Is Included because of the diverse brachiopod fauna present there. Cluster 3 contains the remaining Region 2 localities plus the region 3 localties Slaty Fork and Acme Quarry. A comparison of the faunai components from both localities iiiustrates their simiiiarity to the Region 2 localities. Reiationships of locaiities per region are iliustrated in Figures 82a-c. They depict, for the most part, the same relationships as depicted in the dendrogram for all three regions. REGiON 1 - WESTERN MARYLAND Three faunai associations (FA1 - FA3) were identified from the Greenbrier Formation in this area (Figure 10; Table 7). The transgression of the Greenbrier Sea, can be divided into three stages with noted environmentai changes accompanying each stage (Wuiff, 1990d). A record of this transgression is recorded in the lithofacies and biofacies. Accordingly, each stage contains one faunai association that Is unique to that part of the section. FAUNAL ASSOCIATION 1 - TROPHIC ASSEMBLAGE 1 (TABLE 7) This suspension and deposit feeding association occurs in the middle member of the Greenbrier Formation In Region 1. Ostracods and calcispheres dearly dominate the association with endothyrid foraminifera second in abundance. Rare in abundance are brachiopods, aigae, fenestrate bryozoans and bivalves. Normal marine biota, as defined by Wiison & Jordan (1983), are notabiy absent. The lithofacies that contain this association are bioturbated and fossiiiferous mudstones and were deposited in a semi-restricted, shelf lagoon setting (Wulff, 1990d; Chapter 2). Salinity and temperature fluctuations caused by high evaporation resulted In stressful conditions. Ostracods, although widespread environmentaiiy, commoniy occur in restricted environments, in either brackish or hypersaiine waters. 180 TREE OIRGRRtl DISTANCES 0.000 1.000 Saig Run - Ook I end - Dm p C r#«k - Nontarul 11# R R Quarry Knobs-Un Ion Or##nul 11* Rmick Val RIdarson SSS Quarry Rcma Quarry Kan ton Maad Roaring O k U.S. 33 Cenaen Q. Buichar Slaty Fork ' Figure 81; Dendrogram for all regions, taxa by locality. See text for explanation. 181 TFEE DIflGRfln DISTANCES 0.600 0.800 deep creek - scng run ook I Old TREE DIRGRRN DISTANCES 0.000 1.000 B montervi lie - ken ton mead roaring crk U.S. 33 ccnacn quarr- butcher quar- TREE DIRGRRN DISTANCES 0.000 1.000 greenvl I le - slatyfork knobs-un ion alderson renIck val le- r r quarry - SSS quarry - acme quarry - Figure 82: Dendrograms for taxa by locality. A. Region 1 ; B. Region 2; C. Region 3 182 Table 7: Fauna! Associations Fauna! Association 1 Ostracods Dominant Calcispheres Endothyrld foramlnlfera Common Anthracosplrifer pellaensis Rare Composita subquadrata Martlnia contracta Diaphragmas cestrlensis Ovatia elongata Orthotetes kaskasklensis Protonlella parvus GInranella sp. Fenestella sensu lato Bivalves Fauna! Association 2 Calcispheres Abundant Endothyrld foramlnlfera Anthracosplrifer pellaensis Anthracosplrifer brecklnrldgensis Composite subquadrata Diaphragmas cestrlensis Eumetrla verneullana Eumetrla n.sp. GIrtyella sp. Martlnia contracta Ovatia elongata Orthotetes kaskasklensis Protonlella parvus Paladin chesterensis Common Natlcopsis (Natlcopsis) Straparollus (Euomphalus) Ostracods Pelmatozoan debris Rugose corals Rare Palaeacis sp. Bivalves Bryozoan fragments Fauna! Association 3 Endothyraceans Abundant Pelmatozoan debris Anthracosplrifer pellaensis Common to Composite subquadrata Abundant Orthotetes kaskasklensis Protonlella parvus 183 Table 7 (continued) Archimedes sp. Common Fenestella sensu lato FIstullpora sp. Cystoporates Trepostomes Rhabdomesonlds Paladin chesterensis Rare Lyroporella sp. Rugose coral Bivalves comulltellld Faunal Association 4 Echlnoconchus sp. Common to Inflatia Inflatus Abundant Ovatia elongata Anthracosplrifer pellaensis Rare Pelmatozoan debris ostracods Faunal Association 5 Anthracosplrifer pellaensis Common to Composita subquadrata Abundant Eumetrla verneullana Martlnia contracta DIaphragmus cestrlensis Inflatia Inflatus Orthotetes kaskasklensis Rugose coral Rare Endothyraceans Paladin chesterensis Faunal Association 6 Endothyraceans Abundant Calcispheres Rare Ostracods Dasycladaceans Faunal Association 7 Bivalves Common Aviculopecten sp. Plants (unldent.) Faunal Association 8 Anthracosplrifer pellaensis Rare to 184 Table 7 (continued) Clelothyrldlna sp. Abundant Composita subquadrata DIaphragmus cestrlensis Eumetrla verneullana GIrtyella sp. Inflatia Inflatus Martlnia contracta Orthotetes kaskasklensis Retlcularla sp. Pentremltes sp. Pelmatozoan debris Archimedes sp. Abundant Trepostomes Rare Endothyraceans Abundant BIserlal foramlnlfera to Rare Unlserlal foramlnlfera Calcispheres Rare to Ostracods Common Dasycladaceans GIrvanella sp. Sphaerocodlum sp. Trace Fossils Gastropods Rare Paladin chesterensis Pterotocrlnus serratus Faunal Association 9 inartlculates (rare) Anthracosplrifer pellaensis Rare to Composite subquadrata Abundant DIaphragmus cestrlensis Eumetrla verneullana? GIrtyella sp. Inflatia Inflatus Orthotetes kaskasklensis Rugosochonetes sp. Pelmatozoan debris Archimedes sp. Rhabdomesonlds Trepostomes Pterotocrlnus serratus Common Trace Fossils Pentremltes sp. Rare Rugose coral Bivalves Dasycladacean 185 Calcispheres most commonly occur In lagoonal settings although they are often transported seaward by tidal currents (Wray, 1972). The brachiopods In this semi-restricted setting are varied both In abundance and mode of life. Anthracosplrifer pellaensis. Composite subquadrata. and Martlnia contracta were all pedlcally attached, and the bloclastic material In these facies might have provided some attachment sites. DIaphragmus cestrlensis. Ovatia elongate. Protonlella parvus and Orthotetes kaskasklensis utilized either spines or a broad flat outline for stabilization on muddy substrata. Brachiopods are rare to common In occurrence, and their presence Is attributed to both transportation (some of the valves are abraded and disarticulated) and the presence of rare hardy Individuals that were able to withstand the stresses of such an environment. Grant (1981) noted that some brachiopods are able to withstand more variable conditions than has previously been thought. This association does not occur In any other llthology nor does It occur at any other stratigraphie Interval. The fauna consists of organisms that were not restricted to a particular facies but were capable of living under stressful, fluctuating conditions. FAUNAL ASSOCIATION 2 - TROPHIC ASSEMBLAGE 1 (TABLE 7) This association differs sharply from Faunal Association 1 by the Increase In abundance and diversity of the fauna. It occurs In the upper member of the Greenbrier Formation In Region 1. Brachiopods, endothyrlds and calcispheres dominate the assemblage. Trilobltes, ostracods, gastropods, pelmatozoan debris and trace fossils are common. Bryozoan fragments, rugose corals and bivalves are rare. Once again, the normal marine biotic component Is absent. Associated llthofacles are fossillferous wackestones, packstones and gralnstones. The continued occurrence of ostracods and calcispheres and the paucity of bryozoans and crinolds suggests that the environment was still Inhospitable to most organisms. However, the Increase In faunal diversity implies that changes In the physical parameters of the environment created less stressful conditions. For example, foramlnlfera tend to Increase In abundance relative to ostracods as the waters become more normal In salinity (Benson, 1961). The 186 brachiopod diversity is notabiy increased, and their preservation and abundance, in contrast to those in FA 1, indicates that they are in situ. The increase in biociastic material provided ample attachment sites for Anthracosplrifer pellaensis. A. breckinridoensls. Composite subquadrata. Martlnia contracta. Eumetrla verneullana. Eumetrla n. sp. and Girtvelia. Muddier areas provided suitable substrata for DIaphragmus cestrlensis. Ovatia elonoata. Orthotetes kaskasklensis and Protonlella parvus. Endothyrld foramlnlfera are best adapted for life in coarse-grained sediment deposited in turbulent waters (McKay & Green, 1963). Their abundance in these facies is consistent with this interpretation. As benthic deposit feeders, Natlcopsis fNaticopsis^ and Straparollus (Euomphalus) grazed about on the substratum. Recent work suggests that the gastropods may even have been ciliary filter feeders (Linsiey, 1977). Preservation of the pelmatozoan debris and bryozoan fragments, the transportability of the light fragments, and the inability of both to live in non-normal marine conditions, implies that they are not in situ. This faunal association is not restricted to a particular facies, and the variety of iithoiogies indicates that these organisms were eurytopic for both substratum conditions and conditions above the sediment-water interface. Composita subquadrata is present in high abundance at Sang Run Quarry in the upper member of the Greenbrier Formation, its presence In this facies, which has been interpreted as being stressful to most organisms, and not normal marine, plus its occurrence throughout the field area in a variety of facies, implies that it was opportunistic and eurytopic. Anthracosplrifer pellaensis does not occur in high abundance, but it meets several of the other criteria for identification as an opportunistic species, it is also widespread throughout the field area, occurs in a variety of facies and exhibits wide external variations in morphology (Wuiff, 1989b, 1991). The paieoecoiogy of A. pellaensis is more thoroughly discussed in Chapter 6. FAUNAL ASSOCIATION 3 - TROPHIC ASSEMBLAGE 2 (TABLE 7) This association occurs in the uppermost upper member of the Greenbrier Formation in Region 1. The increase in faunal diversity changes the trophic structure as compared to FA1 and FA2. Brachiopods, endothyrlds and pelmatozoan debris dominate this fauna. 187 Bryozoans, of which Archimedes is most abundant, occur second in abundance. They are iarger and more diverse than the few fragments in faunal associations 1 & 2. Archimedes are preserved with fronds attached to the axes. Trilobites, echinoid debris, rugose corais, bivaives and a singie cornuiiteiiid are rare components. The increased diversity and presence of crinoids and bryozoans impiies environmentai changes toward more normal marine conditions. The ostracode-caicisphere component is absent and foramlnlfera are abundant. Llthofacles associated with these fossils are fossillferous gralnstones and packstones. The modes of life of the brachiopods and endothyrlds have already been discussed, it is sufficient to say that they were well suited for these substrata. The condition, size and abundance of the pelmatozoan debris suggests that they may be in situ. Co-occurrence with well preserved bryozoans indicates hospitable environmentai conditions. Because both crinoids and bryozoan colonies require suitable substrata for initial attachment of larvae, these iithoiogies were ideal. It is puzzling that no crinoid cups or cup plates were collected and it is possible that the plates were transported away. The presence of Paladin chesterensis in FA 2 and the fact that it was a normal marine dweller suggests that its decrease in abundance in these facies may be attributed to the increase in skeletal debris and subsequent decrease in the amount of organic detritus in the substratum, individual scierites may also have been washed away. The other organisms occur too rarely to interpret their role in this association. The continued presence of genera and species from the somewhat stressful conditions represented by FA2 to the more open marine conditions represented by FA3 illustrates the eurytopic nature of these organisms. The presence of stalked echinoderms and bryozoans suggests that more open marine, normal salinity conditions developed toward the end of Greenbrier deposition in Region 1. Figure 83 is a taxa by locality dendrogram for Region 1. Cluster 1 contains organisms that are in FA3. They are mostly bryozoans and required normal marine conditions. Cluster 2 contains organisms that occur in ail three Faunal Associations in this region. Their abundances vary greatly and increases toward FA3. Opportunistic brachiopods and endothyrlds are present, and, as indicated by their occurrence in ail three faunal associations. 188 TPEE D l AOAAM DISTANCES 2.000 BI8ERI a £ * ° ° ° —I n U O O S A N B A H R B D O nC C V 8T O P O R TREAS A R C H iriE D B IU A L U E 8 E rO O T H V R P E LM A O E B P A L A D IN ORTHOrET CONPOe IT P E U L A CALCIBP O IR V A N E L O STR RCO D S T R A P S O V A T IA M A R T IN I A U E R H E U L D IA P H P A L flE A C OIRTV EUNETRIA BRCCK MAT I OOPS PROTON IE LVROPOR Figure 83: Dendrogram for Region 1, locality by taxa, see text for explanation. 189 they are environmentally widespread. The fauna In Cluster 3 occurs mainly In FA2. None of these organisms are abundant. The brachiopods In FA1 are rare and are Interpreted to have been transported In to this setting. Organisms In Cluster 4 are rare In FA1 and FAS. This cluster really represents FA2 and those organisms which settled when the change to less stressful conditions occurred. REGION 2 - NORTH-CENTRAL AND CENTRAL WEST VIRGINIA Four faunal associations (FA4 - FA7) are present In Region 2 (Figure 10, Table 7). The diversity and abundance appears to have been affected by three factors; 1) high energy due to the West Virginia Dome and shallow areas around It; 2) Influx of slllclclastlcs from the exposed highlands to the east; and 3) possible restriction of circulation In the vicinity of the Dome Itself (Wulff, 1990d; this study). Because there Is no barrier to the south limiting circulation In this region, open marine conditions would have been expected. However, the faunal components do not reflect this, and It appears that the factors listed above Influenced the faunal distribution more than the normal marine component. FAUNAL ASSOCIATION 4 - TROPHIC ASSEMBLAGE 1 (TABLE 7) This association Is restricted to the Union Limestone at one locality In Region 2. It Is composed entirely of well presen/ed and In situ brachiopods. This association Is confined to a fossillferous mudstone that was probably thixotropic prior to llthlflcatlon. Three productid brachiopods, Inflatia Inflatus. Echlnoconchus sp. (present only at this locality) and Ovatia elonoata occur at this locality. All three used their spines for stabilization on this substratum (Mulr-Wood & Cooper, 1960). An Intermediate morphotype of Anthracosplrifer pellaensis (Wulff, 1989b; 1991a, Chapter 6) Is the rarest of the four brachiopods here and probably attached Its pedicle to the small amount of bloclastic material present. This Is a simple association consisting of one brachiopod that was restricted to a quiet, low turbulent environment and three eurytopic brachiopods, all of which were adapted 190 for muddy substrata. Mudstones such as this are rare in this region. The occurrence reflects a brief, but sharp change in environmentai conditions that ailowed a different fauna to become established. FAUNAL ASSOCIATION 5 - TROPHIC ASSEMBLAGE 1 (TABLE 7) This association also occurs at only one locality in the Union Limestone In Region 2. Brachiopods also dominate this association, yet the diversity and iithoiogy contrasts sharply to that of FA4. The facies is a fossillferous grainstone deposited in a turbulent environment that was much more similar to those in which the rest of the llthofacles in this region were deposited. if they were pedicaiiy attached to iarger objects such as cobbles, Anthracosplrifer oeiiaensis. Composite subouadrata. Eumetrla verneullana and Martlnia contracta, probably remained relatively stable even though the surrounding substratum may have been unstable or the water turbulence high. DIaphragmus cestrlensis and inflatia inflatus, although adapted for muddy environments, were also able to live on this substratum by virtue of weighted umbos (Muir-Wood & Cooper, 1960). Free living Orthotetes kaskasklensis most likely rested on the substratum and shifted with currents. Endothyrlds are rare, which is unusual, considering they are best adapted for environmentai conditions such as these. It Is possible that as light particles, the tests were carried away by the high energy currents. This association consists of brachiopods, that, although as a group are restricted to this locality, also occur in the semi-restricted environments of Region 1 and the open marine environments of Region 3. This further exemplifies the adaptability of these brachiopod genera to live in a variety of environments. FAUNAL ASSOCIATION 6 - TROPHIC ASSEMBLAGE 1 (TABLE 7) This simple association consists almost entirely of endothyrld foramlnlfera. Rare dasycladacean algae and pelmatozoan debris occur at only a few stratigraphie levels. The 191 association occurs at numerous iocaiities in Region 2 and in a variety of iithoiogies ranging from arenaceous, fossiiiferous and peioidai wackestones, packstones and grainstones. It Is unusual that no other organisms are present in these units. However, turbulent water and possibly the amount of suspended quartz sand may have made this environment unsuitable for habitation by many other invertebrate benthos. Endothyrlds are present in nearly every unit of the Union Limestone in Region 3. The low diversity in this faunal association may be due to the inability of the co occurring organisms in Region 3 to live under the environmentai conditions present in Region 2. FAUNAL ASSOCIATION 7 - TROPHIC ASSEMBLAGE 1 (TABLE 7) Confined to the top of the Alderson Formation at one locality, this association differs sharply from the other faunal associations in this study, it consists of bivaives and plants. The iithofacies is a micaceous mudstone, and the environment has been interpreted as a swampy, poorly drained area that was periodically subaeriaiiy exposed due to either tectonic movement of the West Virginia Dome, possible eustatic sea level change (Wuiff & Ausich, 1991), or both. Aviculooecten sp. lived on this muddy substratum utilizing its fiat shape for stabilization, much like the snowshoe effect described by Thayer (1975). The plant material indicates subaerial exposure in this area and development of a paieosoi (Retaiiack, 1990). The occurrence of this association is directly related to the environmental conditions in the area (Wuiff & Ausich, 1991). it is not representative of the general overall conditions during Greenbrier deposition in Region 2. Figure 84 is the taxa by locality dendrogram for Region 2. Because both pelmatozoan debris and endothyrld foramlnlfera are rare in FA4 and FAS, Cluster 1 essentially represents FA6. Because bivaives are rare in FAS, Cluster 4 essentially represents FA7. Clusters 2 and 3 are not as clear-cut. Cluster 2 contains fauna from from FA4, FAS and FAS. However, those in FAS are rare and not truly representative of the faunal association. Cluster 3 contains fauna from FAS, and ail are rare except Composita subouadrata and Anthracosplrifer 192 TREE DinORntI OISTAMCES 0.000 1 .0 0 0 _ EMD01HVR -I ■ PELMfiOEB -T DIRPH CRLCISPH BISERIRL OURTIR ORTHOTET MRRTIMIR irF L R T IR UERtCUL ECHIHO OSTRRCOD PRLRDIN 0 IRVRMEL 3 RUOOSRMS COMPOS IT PELLR RUIOULO i| BIURLUES ORYSCLHO Figure 84: Dendrogram for Region 2, locaiity by taxa, see text for explanation. 193 pellaensis In FA5. These two clusters represent the brachiopod rich faunal associations but again, because of the presence-absence data set, do not accurately represent each one. REGION 3 - SOUTHEASTERN WEST VIRGINIA Two faunal associations (FA8 & FA9) are present In Region 3 (Figure 10, Table 7). The faunal components and lithologie characteristics here indicate that this area experienced normal, open marine conditions during deposition of the upper Greenbrier units (Wulff, 1990d; Carney & Smosna, 1989). Lithologie differences between the Union Limestone and Alderson Formation Indicate a change from turbulent, shallow conditions to lower energy, somewhat deeper or quieter waters. This difference alone supports the development of different faunal associations. Lithologie and faunal changes within the Union Limestone also suggest more turbulent waters to the north and less turbulent conditions to the south (Figure 14). Because the area was open marine, we might expect the faunal distribution to be fairly constant throughout. The wide variations in llthology and bioclast accumulation have been attributed, in part, to differences in the bottom topography (Wulff, 1990d, this study). Thus, as noted earlier, sheltered versus non-sheltered areas may explain the contrast between richly fossillferous units and depauperate ones. The reef fauna described in Chapter 7 has been included In this discussion. In contrast to the faunal associations discussed In this chapter, the facies and fossil components present in the reef are all laterally equivalent and age- equivalent. Thus, it was not appropriate to discuss these as separate faunal associations. Additionally, because all of the fossil components can be shown to occur elsewhere in the Greenbrier, the reef fauna Is included In the already defined faunal associations. FAUNAL ASSOCIATION 8 - TROPHIC ASSEMBLAGE 2 (TABLE 7) This association occurs In Region 3 In the Union Limestone and at one basal Alderson Formation locality. The association is the most diverse studied and overall, is not dominated by any one group. Locally, units are dominated by brachiopods, Sphaerocodlum and corals. 194 Brachiopods are the most numerous component in the south (Sait Suiphur Springs and Knobs-Union Road), yet they are iimited to a few beds. Archimedes, other bryozoans, pelmatozoan debris, Pentremltes. Pterotocrlnus serratus. endothyrld foramlnlfera, algae and rugose corals are common to abundant. Rare components Include biserlal and unlserlal foramlnlfera. Paladin chesterensis. ostracods, calcispheres, gastropods and bivalves. The llthofacles associated with this association range from fossillferous, oolitic, and In places arenaceous, mudstone, wackestone, packstone and gralnstones. Modes of life of all organisms present have been discussed In earlier sections and their overall adaptability to various substrata Is exhibited In this association as well. The association Is composed of normal marine dwelling organisms that were eurytopic for substrata and both eurytopic and stenotopic for environmental conditions. FAUNAL ASSOCIATION 9 - TROPHIC ASSEMBLAGE 2 (TABLE 7) This faunal association Is restricted to the Alderson Formation In Region 3. Although two of the localities are at the base of the Alderson and the third Is at the top of the formation, the faunal diversity and llthology Is consistent throughout. Brachiopods dominate the assemblage and one genus, Rugosochonetes. does not occur elsewhere. Archimedes. trepostome bryozoans, and pelmatozoan debris are second In abundance. Blastolds, rugose corals, algae, bivalves and foramlnlfera are rare. Near normal marine conditions are Indicated by the diversity of the fauna and presence of stenotopic organisms such as pelmatozoans and bryozoans. Associated llthofacles are arenaceous and fossillferous mudstones, wackestones and packstones. The presence of mud In all of the facies suggests lower turbulence and quiet conditions. As previously discussed, the brachiopods’ modes of life were such that they were well suited to the conditions under which these llthofacles were deposited. The success of all of the suspension feeders suggests that the water must have been relatively clear. The rarity of blastolds and the presence of disarticulated pelmatozoan debris suggests that the pelmatozoans did not thrive as well In this environment. 195 One of the most notable features of this association (and of the Alderson In general) Is the near absence of foramlnlfera. They are rare which contrasts sharply with the Union Limestone In Region 3 and the faunal associations to the north. One possible explanation is the amount and type of mud In these Iithoiogies. It Is browner In color than the mudstones and wackestones to the north, suggesting a different source for this fine-grained carbonate component. Although the endothyrlds survived In the muddier environments to the north, perhaps this change In the source of the mud or in the abilities of the foramlnlfera to tolerate this change, prevented them from successful habitation. The remaining faunal components occur In numbers too few to accurately Interpret their role in the association. The organisms In this assemblage are eurytopic for both substratum and conditions above the sediment-water Interface. This Is particularly true for the brachiopods, as several genera are present in the northern associations as well. Figure 85 Is the taxa by locality dendrogram for Region 3. Open marine conditions prevailed and the separation of the two faunal associations represents differences In environmental turbulence rather than other physical parameters. Cluster 1 contains organisms that occur in FAB. None of these are common in the units, and the rhabdomesonid bryozoan from FA9 may be included in this cluster because It Is rare as well. Inflatia Infiatus is fairly common at RenIck Valley and its presence in this cluster seems to be a function of the presence-absence data set. Cluster 2 also contains organisms that most commonly occur in FAB with some overlap of FA9. These are clustered because of the greater similarity between the two faunal associations. Cluster 3 consists of organisms that occur in both fôunal associations of this region. This basically reinforces the point that environmental conditions were stable with respect to salinity, temperature and nutrient availability. Thus the differences between these two formations and faunal associations appear to be due to environmental turbulence and the inability of some organisms to Inhabit a higher or lower energy regime. 196 TREE o imonmn g.ooo_ D I8TRNCE8 INFLRTI PHRBOOM CHL C I 8 P H OSTRRCOD OIRUPMEL PRLRDIN SVff INDOP CLEIOTH UNI8ERIR PTBROTO BISERIRL DRSVCLRD B IVRLVES OIRTV MRRTIMIR PROTON IE SPHRERO RETIOULR ORTHOTET RUOOSOCH UERNEUL RRCHIMED ErOOTHVR DIRPH PELLR PENTREM PELMRDEB RU008RN8 COMPOS IT Figure 85: Dendrogram for Region 3, iocaiity by taxa, see text for expianation. 197 TAXA BY FACIES The relationship between taxa and facies was also analyzed with cluster analysis. The dendrograms for taxa by facies contain clusters that are very similar to those In the taxa by locality analysis. This can be attributed to the fact that each facies occurs In a specific region and contains only the taxa In that region. Thus the data are essentially the same. No pattern exists In the dendrograms for facies by taxa. Clusters contain mudstones, wackestones, packstones and gralnstones In no specific order. This confirms that the Individual taxa and faunal associations are not restricted to any particular facies. SUMMARY Nine faunal associations were defined from Greenbrier rocks. Distinctions among faunal associations were based on fossil content and relative abundances of taxa. Confirmation was supplied by resuits of cluster analyses. These associations represent the different environmentai conditions that existed during deposition of Greenbrier rocks. It Is clear from their distribution throughout the Greenbrier, that Iithofacies piayed a smaii role in their occurrence and that physicai parameters other than nature of the substratum were the iimiting factors. Such factors probabiy inciuded saiinity, temperature and water turbulence. CHAPTER V COMPARISON BETWEEN THE EASTERN INTERIOR BASIN AND THE APPALACHIAN BASIN INTRODUCTION The Eastern Interior Basin (EIB) provides an excellent feature for comparison to the Appalachian Basin from both a tectonic/structural and a faunal viewpoint. Both basins were connected at various times during the Mississlpplan, and age-equivalent strata are present in the basins. Although the depositlonal environments may have been similar at any given moment In time, overall, the processes occurring In each basin were quite different. The tectonic setting, for example, differed markedly and resulted In the development of different environmental conditions and the deposition of different Iithoiogies. Faunal composition shows some Interesting trends as well. Endemism, the restriction of organisms to a particular region or environment. Is not particularly strong In either basin, and numerous genera and several species are common to both areas. These widespread distributions provide a great deal of Information on the adaptability and paieoecoiogy of these organisms. The structural setting and tectonics of the Appalachian Basin have aiready been discussed and wiil not be reviewed here. The foiiowing discussion of the EIB was summarized from Sabie (1979) unless otherwise noted. The region encompassed by the EIB Includes much of Missouri, Illinois, western and southern Indiana, west-central Tennessee and Kentucky (except the eastern subsurface). Numerous structural features surround and define the outiine of the basin (Figure 86). Chesterian rocks of the EIB are characterized by cyclic deposits of limestones and detrital, clay-rich units. The ciastic units contain varying amounts of mudstone and quartz sand and silt with minor limestone. The overall thickness and proportion of clay to quartz 198 199 ILLINVOIS INDIANA MISSOURI EASTERN INTERIOR BASIN JESSAMINE DOME OZARK UPLIFT KENTUCKY TENNESSEE a = LINCOLN ANTICLINE b = DUPO ANTICLINE (. NASHVILLE DOME C = STE. GENEVIEVE FAULT 40 100 MILES Figure 86: Location of Eastern interior Basin and associated features. Modified from Sable, 1979. 200 vary substantially laterally. Carbonate units consist of relatively pure limestones with varying amounts of bloclastic material, colds, pellets, and terrigenous elastics. Overall, these Iithoiogies are not very different from the Greenbrier units of the Appalachian Basin. All Chesterlan-aged rocks In the EIB have been eroded by Pennsylvanian, Cretaceous or Holocene processes. The thickest sequences preserved are In southern Illinois ( >411 meters (-1350 feet) and In western Kentucky (-3 6 5 meters or 1200 feet). Most units thin to the north and east. This Is most easily demonstrated In widespread units such as the Glen Dean Formation. Chesterian formations are also thinner marginal to the Cincinnati Arch. The main source areas of the elastics are thought to have been eastern Canada, from either the Shield or northward extensions of the Appalachian Mountain belt. These sediments are thought to have been brought Into the area via the Michigan River (Swann, 1964). Lateral shifts In the river’s course produced belts of sand and mud In different parts of the region at different times (Swann, 1964). Provenance of additional terrigenous material was most likely from the northeast, within or beyond the Acadian tectonic belts of the northeastern United States and eastern Canada and possibly northern Canada; from the east, within or beyond the Piedmont province of the eastern United States; and possibly from the south In the areas between the Ouachltas of Arkansas and the Warrior Basin of Alabama and Mississippi (Thomas, 1974). Major northeastern and southwestern oscillations In the shoreline resulted In the deposition of carbonates In the basin and surrounding areas. The depth of this sea Is estimated to have been 50 to 75 feet with a minimum and maximum of 30 to 100 feet (Swann, 1964). Widespread emergence and southward tilting at the end of the Chesterian caused deposition to cease. A low lying landmass was produced over much of the EIB region. Tectonic activity was restricted to the arches and basin. Epelrogenic uplift affected the transcontinental arch and the stable shelves adjacent to It. The Cincinnati Arch was mildly uplifted and the eastern margin was alternately emergent and submerged (Rice et al., 1979). Much of Missouri and Iowa was a stable submerged platform. Mild subsidence characterized 201 broad areas of the basin region and the iaterai persistence and smaii thickness variations within the formations indicate that subsidence across the basin was fairly uniform. Within the basin, discrete regions contain evidence of tectonic activity, it appears that many of these can be linked to the continuation of the 38th paraiiei lineament zone (Figure 9). In northeastern Kentucky, for example, there are distinct thickness variations in upper Mississlpplan units along the trends of the Kentucky River Fault System and the Waveriy Arch (Dever et ai., 1979). STRATiGRAPHiC CORRELATION Stratigraphie correlation between basins was determined based on the COSUNA charts for the Northern Appalachian Basin and the Midwestern Basin and Arches Region (Lindberg, 1985). The Union Limestone, Greenville Shale and Alderson Formation are ail Chesterian in age. Equivalent strata in the EIB include the Renault Formation - Paoli Limestone through the Gien Dean Formation (and age-equivaient strata in the region). It is not possible with currently available data to subdivide EIB units into Union and Alderson equivalents. FAUNAL COMPARISON Faunal lists for the EIB and the Appalachian Basin were compiled from numerous sources (Weller, 1931; Weller, et al., 1952; Tissue, 1986; Girty, 1926; McFarlan, 1942; Chestnut & Ettensohn, 1984; Utgaard & Perry, 1960; Perry & Horowitz, 1963; Kelly, 1984; Waters, 1977; herein). Table 8 contains comparative listings for both basins at the generic level. Kammer & Ausich (1988) reported that, in regional paleoecoiogic studies, faunal comparisons at the generic level may be complete enough to provide ample information for interpretation. They noted that, in cases where species-ievei determination is not possible or where taxa have been overly split, generic-level data might be more desirable. Because species level identifications were not possible for several taxa in the Appalachian Basin and species-ievei systematics may not be comparable among ail data, genus-level comparisons were used. 202 TABLE 8: COMPARISON OF GENERA FROM THE EIB AND THE GREENBRIER GROUP Renault Fm. = B; Rldenhower Shale (IL)/Paint Creek Fm. (KY) = C; Gasper Oolite = D; Golconda Fm. = E; Glen Dean Limestone » F; Indian Springs Shale - G; EIB General = H; Union Limestone (County Reports) = I; Alderson Formation (County Reports) = J: Union Limestone (This study) » K; Alderson Fm. (This study) = L; Greenbrier Fm.-MD (This study) = M; Greenbrier Fm.-MD (Tissue, 1984) = N; Bangor Limestone-AL (Waters, 1977) = 0 CORALS Rueoae coral (unid.) Svringopora Svrineoporicse ThyanophyUum__ Triplophvilum ECHINODERMS Ampelocrinu» Penuramininiu Pentnmite» Phacelocrinm Ramuiocrinm Talarocrinm Zeacrinui ______Unidentified debris 203 TABLE 8 (continued) Renault Fm. = B; Rldenhower Shale (1L)/Palnt Creek Fm. (KY) = G; Gasper Oolite = 0; Golconda Fm. = E; Glen Dean Umestone = F; Indian Springs Shale » G; EIB General = H; Union Umestone (County Reports) = I; Alderson Formation (County Reports) = J; Union Umestone (This study) = K; Alderson Fm. (This study) = Greenbrier Fm.-MD (This study) = M; Greenbrier Fm.-MD (Tissue, 1984) = N; Bangor Umestone-AL (Waters, 1977) = 0 BRYOZOANS X X X Archimede: XX XXXXXXXXXXX Ascopora XX RatnMomplla X X CheilotrvDa X X rhîrtniryp» X Coeloconui X Cvsiodiava XXXX Cy«tojiorali* X Eiiasojpora X Eridooora XXXX Fenesiella XXXXXXX X X X XX R jtu lip o ra XX XX XXXXXXX Glyntnpora XX X X HedeiellB X LvroDora XX X XXXX l.VTopmella XXX Meekooora X XX XXX X Polvnora" XXXXXXX X PrismoDora X X X Pivlnpora X X Rliabdomejonids X X X X X Rhabdomeson X Rhombopon XXXX X Rhvnchooora X Sepifvpon XXX X XXXX StênojjoiB XXXXX X X Siomâloeora X Streblotrypa XXXX X Tabuliporâ XXXXX Thamniscii» X X Treposicme ____1 X Z3Z BRACHIOPODS Anthracosoirifer Brachythiu------Camaroroechia (K Y I Piaphnemiu Dielsrms __ Eumetria lin e uls- Maitinia Orfaiculoidea Orthotete» Proloniella Pugnoides 204 TABLE 8 (continued) Renault Fm. = B; Rldenhower Shale (IL)/Palnt Creek Fm. (KY) = G; Gasper Oolite = D; Golconda Fm. = E; Glen Dean Umestone = F; Indian Springs Shale = G; EIB General = H; Union Umestone (County Reports) = I; Alderson Formation (County Reports) • J: Union Umestone (This study) = K; Alderson Fm. (This study) = L; Greenbrier Fm.-MD (This study) = M; Greenbrier Fm.-MD (Tissue, 1984) = N; Bangor Umestone-AL (Waters, 1977) = 0 R c D RF G HIJKI. M M o Pundospirifer XX X Pustula XX X YY XX X Y X X RuEOSochonetes X X .Schiicheitell» XX S o iiife r X XXX XX XXXXX Y X Torvnifer X TîisonoEloïu ...... X BIVALVES Anniilirnnehii Rivalvci (unid.) Canevella Conocardium ParaUclodon Schizodm GASTROPODS Relleiphon XXX Borestuj Riicannp^ii X Ruiimofpha X X Cvclonema X Cvpricardella Cvpricardina Donalina? X Eotrochui X X 205 TABLE 8 (continued) Renault Fm. = B; Rldentiower Shale (IL)/Palnt Creek Fm. (KY) = G; Gasper Oolite « D; Golconda Fm. = E; Glen Dean Limestone = F; Indian Springs Shale ° G; ElB General = H; Union Limestone (County Reports) = 1; Alderson Formation (County Reports) = J; Union Limestone (This study) = K; Alderson Fm. (This study) = Greenbrier Fm.-MD (This study) = M; Greenbrier Fm.-MD (Tissue, 1984) = N; Bangor Umestone-AL (Waters, 1977) = 0 B ç D E F Q H I J KLM N o Huconospira X Euomphâlus X Y Funhemus X Holooea X X trp m p yg m a X Loxonerna X X M ourionia X Naticoosis XX X X X Neilaonia X PaleozvBOpIeura X Pateliilabiâ X Platvcetaa XXXX X Plaivzona X Plnimtnmari» X Ptvchomphalui X SoIenosDira X Steyocoelia X SwâDarollu» XX X X X .Simphmtviuj • X Zyggpltun------X FORAMINIFERA Climacammina X Endothvraceana XXX X Biierial forami X X UniKrial forann______X TOILOBITES nrifrnhiitM XXXX Paladin XXXXX Ehylüeâs______XX X OSTRACODA B ollia X Paraoarchiiea X Prim itia X üüdmtifiedMinsod:__ XXX CEPHALOPODS CyrtDcera» X Dolontioceraj X Endolobus X Onhoceras X Reticvcloceras X 9tmbocera< X Unidentified cephalopod X ALGAE Caleispherea X Dasvcladaceana X G itvanella XXX Sphaerocodium XX 206 TABLE 8 (continued) Renault Fm. = B; Ridonhower Shale (IL)/Palnt Creek Fm. (KY) = G; Gasper Oolite = D; Golconda Fm. = E; Glen Dean Limestone = F; Indian Springs Shale = G; ElB General = H; Union Limestone (County Reports) = I; Alderson Formation (County Reports) ■ J; Union Limestone (This study) «= K; Alderson Fm. (This study) = L; Greenbrier Fm.-MD (This study) = M; Greenbrier Fm.-MD (Tissue, 1984) = N; Bangor Umestone-AL (Waters, 1977) = 0 L M N MISCELLANEOUS Chiton X Comulitell» lOrtonlai X C o m iilîte i X X Laevidentalium X X X Phoiphamiului X Scolëcodonts X SniiQThi» Y X X 207 Total generic diversity for the hvo basins is 220. The EiB contains 150 genera; 6 corals, 30 echinoderms, 26 bryozoans, 29 brachiopods, 28 bivalves, 16 gastropods, 3 triiobites, 3 ostracodes, 2 cephalopoda and 7 miscellaneous genera such as cornuiiteiiids and conuiariids. No data are available on the presence or absence of foraminifera and algae. The Greenbrier units contain 73 taxa. Most have been identified to genus but in several cases it was not possible to do so. There are 5 corals, 4 echinoderms, 12 bryozoans, 25 brachiopods, 11 bivalves, 2 gastropods, 2 triiobites, 2 cephaiopods, 4 algae, 1 conuiariid and unidentified ostracodes. Forty three genera co-occur in both basins, and they are mainly brachiopods, bryozoans, and, to a lesser extent, bivalves, it is important to note that because of the inability to classify to lower taxonomic levels, plus other factors discussed below, this number is only approximate. Table 9 contains a listing of the genera common to both basins. Because the Union and Alderson formations of central and southern West Virginia represent environments different from those recorded in the Greenbrier Formation of western Maryland, a comparison was also made of the EiB fauna to the West Virginia fauna and to the western Maryland fauna. Co-occurrence between the EiB and West Virginia is high, with the greatest similarity in the brachiopods, bryozoans and bivalves (Table 10). it is likely that the factors controlling the distribution of the fauna in the West Virginia Greenbrier units and the EiB were similar. Comparison of the EiB fauna to the western Maryland fauna illustrates the environmental differences between these two areas (Table 11). Twenty-six genera co-occur, and, again, the brachiopods are most numerous with bryozoans second in abundance. The more stenotopic brachiopods such as Echinoconchus sp.. infiatia infiatus. Ruoosochonetes sp. and Chonetes sp. (as discussed in Chapter 3) are absent in Maryland. Echinoderms are nearly absent as well. The environmental requirements of these organisms and their presence in the open marine waters of the EiB, point to sharply different settings in these two areas as has been argued for differences between the Greenbrier units in western Maryland and West Virginia. TABLE 9: GENERA COMMON TO BOTH BASINS-EIB & GREENBRIER UNITS (WEST VIRGINIA & WESTERN MARYLAND) CORALS ECHINODERMS BRYOZOANS BRACHIOPODS BIVALVES GASTROPODS TRILOBITES Syringopoticae Pentremites A rc h im e d e s Anthracospirifer Aviculopecten N a tic o p s is GriffttMdes Triplopl^llum Pterotocrinus F e n e s te lla Brachythyris E d m o n d ia Straparollus P a la d in Zaphrentoides Fistulipora C h o n e te s M y a lin a G ly p to p o ra Cleiothyrùüna Parallelodon L y ro p o ra C o le tU im Sanguinolites P o fy p o ra C o m p o s ita S ch izo d u s Rhabdomesonids G r a m a S p h en o tu s R h o m b o p o ra Diaphragmas S te n o p o ra D ie la s m a T a b u lip o r a Echinoconchus E u m e tria G ir ty e lla In f ia t ia M a r tin ia Orbiculoidea O rth o te te s O v a tia P o s tu la Reticularia S p ir ife r Spiriferina r o o 00 TABLE 10: GENERA COMMON TO BOTH BASINS-EIB & GREENBRIER UNITS (WEST VIRGINIA) CORALS ECHINODEF BRYOZOANS BRACHIOPODS BIVALVES TRILOBITES Syringoporicae Pentremites A rc h im e d e s Anthracospirifer Aviculopecten Griffithides Triplophyllwn Pterotocrinus F e n e s te lla Brachythyris E d m o n d ia P a la d in Fistulipora Chonetes Myalina Glyptopora Cleiothyridina Parallelodon Poiypora Coledium Schizodus Rh^omesonids Composita Sphenotus Rhombopora Diaphragmas Stenopora Echinoconchus Tabulipora Eumetria G ir ty e lla In f ia t ia M a r tin ia O rth o te te s O v a tia P o s tu la Reticularia S p ir ife r Spiriferina ro o VO TABLE 11 : GENERA COMMON TO BOTH BASINS-EIB & GREENBRIER UNITS (MARYLAND) CORALS BRYOZOANS BRACHIOPODS BIVALVES GASTROPODS TRILOBITES Zaphrentoides A rc h im e d e s Anthracospirifer Aviculopecten N a tic o p s is P a la d in F e n e s te lla Cleiothyridina Sanguinolites Straparollus Fistulipora C o m p o s ita S ph en o tu s L y ro p o ra C r a m a Rhaixlomesonids Diaphragmas R h o m b o p o ra D ie la s m a T a b u lip o r a E u m e tria G ir ty e lla M a r t in ia Orbiculoidea O rth o te te s O v a tia ro I—» o 211 Finally, because the faunal diversity In the shale formations In the EIB Is so high and because fosslllferous shale formations were not sampled In the Greenbrier, a comparison between the EIB limestones and the Greenbrier units was made (Tables 12 & 13). No significant difference was detected In this comparison as compared to the total comparisons. The only differences are the following: the absence of Orbiculoidea (a thin shelled brachlopod more commonly preserved In shales and possibly overlooked). Paladin chesterensis (possibly misclassifled as discussed below) and Sanguinolites sp. (which might have been better adapted to life In muddy environments). DISCUSSION The above comparisons discussed which taxa co-occur in both basins. The results suggest that similarities exist between the two. It Is equally Important to point out which taxa are not present, because this Illustrates the differences that exist In the basins. Whereas crinolds are abundant and well described from the EIB (Kelly, 1984), they are virtually absent from the Greenbrier rocks of the Appalachian Basin. During a time when crinolds were on the rise evolutlonarlly, this absence Is notable. Bryozoans exhibit nearly the same situation. The list of EIB taxa Is diverse, although that for the Appalachian Basin Is not. Brachiopods, however, are diverse In both basins. The same relationships can be seen If the Bangor Limestone (Warrior Basin) Is compared to the Greenbrier Group (see below). The EIB and the WB contain similar faunal diversities and abundances. Essentially, every major taxon In the Greenbrier rocks, with the exception of the brachiopods. Is reduced In number and diversity. Yet all three basins were connected during some point In the deposition of these units. Thus, as discussed In previous chapters, conditions In the Appalachian Basin must have been distinctly different during this time. Two questions can be addressed with regard to the comparisons. First, what processes affected the widespread distribution of similar taxa? Second, although similar In both basins, why Is the generic diversity higher In the EIB In light of the widespread distribution? 212 TABLE 12: COMPARISON OF GENERA FROM THE EIB AND GREENBRIER (UMESTONE UNITS ONLY) Renault Fm. = B; Gasper Oolite = D; Golconda Fm. = E; Glen Dean Limestone = F; EIB General = H; Union Limestone (County Reports) = I; Alderson Fm. (County Reports) = J; Union Limestone (This study) = K; Alderson Fm. (This study) = L; Greenbrier Fm.-MD (This study) = M; Greenbrier Fm.-MD (Tissue, 1984) = N; Bangor LImestone-AL (Waters, 1977) = O B D E F Hi I J KLIm n Io CORALS CamDODhvllum X Chaetetes? Cladochonus so. Cvstelasma Lithostrotion MenoDhvlIum Michelinia Palaeacis X Rueose coral (unid.) XX X SvrinEODora X SvrinEODoricae X Thvsanonhvllum X TrioIcDhvllum X X X X X X Zaohrentis ZaDhrentcides XXX ECHINODERMS AllaEecrinas X Acrocrinus X Ampelocrinus X Aohelecrinus X Archaeocidaris Armenocrinus X AEassizocrinus X XXX Batocrinus CamDtocrinus X CrvDhiocrinus X Culmicrinus Cvmbiociinus X Dlchocrinus XX Diplobastus X Discocvstis X DizvEOcrinus Eunachvcrinus XX Haitnostocrinus Hvrtanecrinus Leoidesthes Leoidodiscus Mesoblastus X NeoisoroDhusella X Neopalaester 213 Table 12 (continued) Renault Fm. = B; Gasper Oolite = D; Golconda Fm. = E; Glen Dean Limestone = F; EIB General = H; Union Limestone (County Reports) = I; Alderson Fm. (County Reports) = J; Union Limestone (This study) = K; Alderson Fm. (This study) = L; Greenbrier Fm.-MD (This study) = M; Greenbrier Fm.-MD (Tissue, 1984) = N; Bangor LImestone-AL (Waters, 1977) = O BDE FHIi j K L I m n Io Onvchocrinus Passalocrinus Pentaramicrinus Pentremites X X X X X X XX XX Phacelocrinus X Phanocrinus X PhosDhanulus X Platvcrinus Pterotocrinus X X X X X X Ramulocrinus X Talarocrinus XX Taxocrinus Tholocrinus Tremataster Zeacrinites Zeacrinus Unidentified debris X X X BRYOZOANS Anisotrvna X X X Archimedes X X X X X X X X XXX Ascopora X Batostomella X X CheilotrvDa X Chirlotrvna X Coeloconus X Cvstodictva X X X Cvstoiwrate X EliasoDora X Encrusting forms X X Eridoirara X XX Fenestella XX X X X X X X XX Fistulitwra X X X X X X X XX GlvntoDora XX X Hederella Lvrotrora X X X X X X Lvrooorella X X Meekooora X X X XX Pennireteoora X PolvDora X X X X X X Prismormra X XX PtvIODora X X Rhabdomesonids X X X X 214 Table 12 (continued) Renault Fm, = B; Gasper Oolite = D; Golconda Fm. = E; Glen Dean Limestone = F; EIB General = H; Union Limestone (County Reports) = I; Alderson Fm. (County Reports) = J; Union Limestone (This study) = K; Alderson Fm. (This study) = L; Greenbrier Fm.-MD (This study) = M; Greenbrier Fm.-MD (Tissue, 1984) = N; Bangor LImestone-AL (Waters, 1977) = 0 B D E F hIi j KLIm n Io Rhabdomeson X Rhombotrora XX X X Rhvnchooora X SeotoDora XXXX XX StenoDora X XX XXX StomatODora X Streblotrvoa XXX X Tabulitrara X X X X Thamniscus X Treiwstome XX BRACHIOPODS Ambocoelia? Anthracospirifec Antiouatonia? Beecheria Brachvthris Camarotoechia (KY) Chonetes Cliothvridina Coledium Composita Crania Diaohraemus Dictvoclostus Dielasma Echinoconchus Eumetria Flexaria Girtyella Infiatia Lingula Orbiculoidea Orthotetes Ovatia Perditocardinia Protoniella Pugnoides Pustula Reticularia Reticulariina 215 Table 12 (continued) Renault Fm. = B; Gasper Oolite = D; Golconda Fm. = E; Glen Dean Limestone = F; ElB General = H; Union Limestone (County Reports) = i; Alderson Fm. (County Reports) = J; Union Limestone (This study) = K; Alderson Fm. (This study) = L; Greenbrier Fm.-MD (This study) = M; Greenbrier Fm.-MD (Tissue, 1984) = N; Bangor LImestone-AL (Waters, 1977) = O B D E F H I I J K L I M N I O Rusosochonetes XX Schuchertella X Soirifer XXXXX Soiriferina XXXXXX Streotorhvncus Torvnifer X Trigonoelossa BIVALVES Acanthooecten X Allerisma X Annuliconcha X Astartella Aviculioecten X X X X XX BelIeroDhontacean Bores tus Bivalves funid.) XX X Canevella X Conocardium X X X Cvoricardella X X Deltopecten X Donaldina Edmondia X X Eoistroboceras Glossites X Grammvsia X Leda X Leotodesma X Meekosoira Mvalina XXX Nucula XX NuculoDsis X Parallelodon XX Permophorus Phestia X Pteria X Sanguinolites X Schizodus X X X Seotimvalina X Sohenotus XXX Stegocoelia Streblochondria X Stroboceras 216 Table 12 (continued) Renault Fm. = B; Gasper Oolite = D; Golconda Fm. = E; Glen Dean Limestone = F; ElB General = H; Union Limestone (County Reports) = I; Alderson Fm. (County Reports) = J; Union Limestone (This study) = K; Alderson Fm. (This study) = L; Greenbrier Fm.-MD (This study) = M; Greenbrier Fm.-MD (Tissue, 1984) = N; Bangor LImestone-AL (Waters, 1977) = O B D E F H I I J K lIm nIo Sulcatopinna Triptoceroides Turrilepas Wilkineia X GASTROPODS Bellerphon Bores tus Bucanopsis Bulimoroha Cvclonema CvDricardella Cvpricardina Donalina? Huconospira Euomphalus Euphemites Euphemus Meekospira Mourionia Naticopsis Neilsonia Paleozygopleura Patellilabia Platvceras Platvzona Pleurotomaria Ptvchomphalus Solenospira Stegocoelia Siraparoilus Strophostvlus Zveooleura FORAMINIFERA Climacammina Endothviaceans Biserial forants 217 Table 12 (continued) Renault Fm. = B; Gasper Oolite = D; Golconda Fm. = E; Glen Dean Limestone = F; EIB General = H; Union Limestone (County Reports) = I; Alderson Fm. (County Reports) = J; Union Limestone (This study) = K; Alderson Fm. (This study) = L; Greenbrier Fm.-MD (This study) = M; Greenbrier Fm.-MD (Tissue, 1984) = N; Bangor LImestone-AL (Waters, 1977) = 0 BDEF H IK L L m J l l i L Tuberitina X Uniserial forams X TRILOBITES Griffithides XX X Paladin XX X X Phvlliosia XX OSTRACODA Bollia X Paraoarchites X Primitia X Unidentified ostracods XXX CEPHALOPODS Cvrtoceras X Dolorthoceras X Endolobus X Orthoceras X Reticvcloceras X Stroboceras X Unidentified ceohalooo X ALGAE CalcisDheres X Dasvcladaceans X Girvanella X X X Sohaerocodium X X MISCELLANEOUS Chiton Comulitella fOrtonial X Comulites X Laevidentalium X Paraconularia X Phosohannulus Scolecodonts Spirorfois X X TABLE 13: GENERA COMMON TO BOTH BASINS-EIB & GREENBRIER (WEST VIRGINIA & MARYLAND) (LIMESTONES ONLY) CORALS ECHINODERMS BRYOZOANS BRACHIOPODS BIVALVES GASTROPODS TRILOBITES Syringoporicae Pentremites A rc h im e d e s Anthracospirifer Aviculopecten N a tic o p s is Griffithides Triplopfiyllum Pterotocrinus F e n e s te lla Brachythyris E d m o ru ü a Straparollus Zaphrentoides Fistulipora C h o n e te s M y a lin a G ly p to p o ra Cleiothyrùüna Parallelodon L y ro p o ra C o le d iu m S chizo du s P o iy p o ra C o m p o s ita S ph en o tu s Rh^omesonids C r a n ia R h o m b o p o ra Diaphragmas S te n o p o ra D ie la s m a T a b u lip o r a Echinoconchus E u m e tria G ir ty e lla In f ia t ia M a r tin ia O rth o te te s O v a tia P u s tu la Reticularia S p ir ife r Spiriferina ro »—» 0 3 219 The widespread distribution of the fauna is explained by the presence of the connective seaway and overlapping environmental conditions between the two basins (Figure 87). Many pelagic larvae can float long distances before settling, thus migrating in both directions from each basin. Over time and given a sustained ability to interbreed, species as well as genera were distributed widely. Generic diversity is much higher in the EiB (Table 8). Part of this may be an artifact of out-of-date taxonomy. For example, Griffithides and Phiiiiosla were both described from the EiB (Weiier, 1920; Butts, 1917) but not from the Appalachian Basin. Griffithides mucronatus has since been reassigned to Paladin mucronatus (Chamberlain, 1969), a genus that is present in the Upper Mississippian of the Appalachian Basin, it is possible that other species of Griffithides described from the EiB may also belong to species of Paladin occurring in the Appalachian Basin. Soirifer peiiaensis described from the EiB (Weiier, 1914) has since been reassigned to Anthracospirifer peiiaensis (Tissue, 1986; Wuiff, this study). Other species assigned to Soirifer in the EiB may also belong to Anthracospirifer. Preservation of bryozoans in the Greenbrier is such that, with the exception of the fenestrates, identification to order was the lowest taxonomic level possible. This limited the ability to compare Greenbrier bryozoans to those from the EiB. Even though lists from the West Virginia County Reports were used (Girty, 1926), the old taxonomy further prevented an accurate comparison. It is clear, however, that overall diversity in the Greenbrier was substantially lower than that of the EiB. Lastly, as In all studies such as this, the bias created by selective preservation and sampling must be noted. Simple comparison of this study's faunal list to the larger and more diverse listings in the West Virginia County reports (i.e., Girty, 1926) illustrates this point. The question as to why the diversity is so much greater in the EIB can be considered in four parts, corresponding not to stratigraphie divisions but to geographic divisions. For most of the late Meramecian and the Chesterian, the EiB experienced open circulation and normal marine conditions. Correspondingly, a diverse and abundant, normal marine fauna flourished, in Chapter 2, it was noted that Region 1 of the Appalachian Basin was an area of 220 mm Paieoshoreline Small amount of uplift Neutral Area - stable region I Fine load | | Areas of subsidence ^ Coarse load || | [ | Uplift - mobile belt or region Figure 87: Source areas of terrigenous elastics and general transport directions into the Eastern Interior Basin and the Appalachian Basin. Modified from Craig & Connor, 1979. 221 restricted circulation, fluctuating temperature and salinity levels and nutrient deficiencies. The faunal diversity and abundance is, not surprisingly, low. Some of those organisms present in Region 1 were eurytopic and able to live in both open marine and stressful conditions. Region 2 was described as a high energy, somewhat turbid environment and the depauperate fauna reflects an inability of many of the marine organisms to live under such conditions. Although the organisms in both basins were eurytopic and adapted to a variety of environments, it appears that the high energy conditions of Region 2 were not hospitable for some of the genera that flourished in the EiB. The comparison between Region 3 and the EiB is more complicated, it has already been established that open marine conditions prevailed in Region 3 during Greenbrier deposition. Given similar conditions in each basin and the connective waterway, comparable taxonomic diversity would be expected. The westernmost extent of the shoreline and overall tectonic activity may have been important factors (Figure 87) controlling faunal distribution. In the Meramecian, the shoreline extended as far west as the Transcontinental Arch (Craig & Connor, 1979, Pi. 11). Tidal fiats occupied the eastern flank of the arch in places and open ocean conditions prevailed on the western side. A connection to the open ocean was also present in southern Texas. By the Chesterian, the seas had receded from much of the west. Areas of non-deposition and presumably erosion now flanked all borders of the seaway east of the Transcontinental Arch. An open ocean connection was present to the south in Texas, Louisiana and Mississippi. One possibility for the difference in diversity and abundance may be that organisms flourishing in the westernmost parts of the sea contributed to the increased diversity of the EIB. Perhaps due to either the great distance separating them from the Appalachian Basin or an Inability to successfully Interbreed with individuals from the Appalachian Basin, they are not represented farther east. Alternatively, or In addition to the above scenario, the ongoing influx of terrigenous materials may have restricted some genera to specific regions, in the Chesterian, the Transcontinental Arch was a relatively stable feature, undergoing small amounts of uplift. 222 Neutral areas existed due north of the EIB, and the EIB Itself was undergoing considerable subsidence (Craig & Connor, 1979, PI. 10). Terrigenous Influx was relatively small with low amounts of coarse sediment and large amounts of fine sediment being shed southward Into southeastern Iowa, northern Illinois and northern Indiana. Most of this material did not make It to the southern portions of the EIB. The Appalachian Basin region was vastly different (Figure 87). Western West Virginia remained stable and experienced small amounts of subsidence. Eastern West Virginia was part of a large mobile belt, undergoing large amounts of subsidence while regions due east were being uplifted (Craig & Connor, 1979, plate 10). Erosion resulting from this uplift caused smali volumes of coarse sediment and large volumes of fine sediment to be transported westward Into the Appalachian Basin. This Is represented as the sandstones, slltstones and silty limestones in Region 3. It Is probable that some genera that were restricted to the EIB were simply not able to live in waters that were even slightly turbid. Finally, differences In larval migration ability most likely played a role In the development of different populations. With the Information available In this study. It was not possible to determine which of the above discussed factors was most likely responsible for the organism distribution. BANGOR LIMESTONE A comparison to the Bangor Limestone (Chesterian) provides a larger regional picture and further exemplifies the contrast in environmental conditions between the EIB and the central Appalachian Basin during the late Mississippian. The Bangor Limestone was deposited In the Warrior Basin (approximately northern Alabama and Mississippi) under shallow marine, normal circulation conditions (Figure 2) (Craig & Connor, 1979, Plates 11, 12). This sea was connected to open ocean towards the south and to the Greenbrier Sea to the northeast. The area was fairly stable tectonically with mild subsidence occurring to the southeast and southwest (Craig & Connor, 1979, Plate 10). The fauna Is very similar to, but more diverse than, that of the EIB (Table 8) (Waters, 1977). Generic composition Includes 1 coral, 18 echinoderms, 22 bryozoans, 16 brachiopods. 223 11 bivalves, 17 gastropods, 1 trilobite, 2 cephaiopods, 1 cornulltellld and 1 conuiariid. Generic co-occurrence between the Bangor and the Greenbrier Is 22 and, as In previous examples. Is greatest for the brachiopods and bryozoans. This pattern suggests that environmental conditions during Bangor deposition were more similar to the open marine stable conditions of the EIB than to the more variable conditions of the Appalachian Basin. CONCLUSION The co occurrence of faunas from the EIB and the Appalachian Basin Illustrates the eurytopic nature of numerous genera, the effect a connective seaway can have on organism distribution and the limitations on distribution due to sediment Influx and varying environmental conditions. The comparison shows that although shallow marine conditions existed across North America during the late Mississippian, the paleodeposltlonal conditions In the study area were unique and that many factors were Important In the eventual development of faunal abundance and diversity. CHAPTER VI AUTECOLOGY OF ANTHRACOSPIRIFER PELLAENSIS INTRODUCTION Variations In external morphology among Individuals of the same species can be deceiving. Organisms are commonly classified as different species based simply on these external characteristics. MIsclassiflcatlon often occurs because poor characters were chosen to define the species. Some Jurassic ammonites with different external morphologies that were assigned to separate species are now recognized to be sexual dimorphs (Callomon, 1963). Early workers of batocrinlds erected separate species based on arm number and arrangement. Lane (1963) however, revised this taxonomy by recognizing that arm number and arrangement varied Intraspeclflcally. Growth form and colony size of bryozoans are typically not useful for species classification because they may be profoundly Influenced by environmental parameters. Internal structures such as zoold morphology are most commonly used for both calcified living and fossilized byrozoans (McKinney & Jackson, 1989). McGugan & May (1965) studied a population of morphologically diverse splrlferlds from the Tunnel Mountain Formation of British Columbia. Utilizing simple biometric statistics on external characters, they concluded that the Individuals In the population belonged to the same species Anthracospirifer curvllateralls (Easton). They did not, however, discuss possible mechanisms for the external variations. Anthracospirifer peiiaensis is another brachlopod species that has a variable external morphology. It Is known from Mississippian rocks (Meramecian and Chesterian) and Is widespread geographically. The pronounced variations In external morphology of Anthracospirifer peiiaensis can potentially be attributed to two factors, genetic or ecophenotyplc. 224 225 All sexually reproduced organisms possess some genetic variation between Individuals. This Is due to recombination In the gene pool and the number of combinations available. Some of the variability has no special adaptive significance, but others will result In Individuals that are slightly better adapted for a given habitat or environment. This follows the course of natural selection and the survival of best fit organisms. Studies of genetic variability within popuiations indicate that more genetic varlabiiity occurs In stable environments than in unstable environments (Ayala et al., 1973, 1975). The reasons for this are unclear, but it has been suggested that the morphologic variabiiity within popuiations of invertebrates is due more to phenotypic than genotypic causes (Dodd & Stanton, 1981). Non-geneticaliy Induced variability is caused by phenotypic effects. Muitiple choice variabiiity was discussed by Bonner (1965). it ailows for two or more morphotypes per species. Each morphotype is calied an ecophenotype, and the one that develops is determined by the environmental conditions under which it Is growing. Environmental stresses that may Influence brachlopod morphology could be substratum characteristics, water energy or crowding. Numerous studies have addressed the possible relationships between Intraspecific morphologic variation and adaptation to substrata (e.g. Alexander, 1975; Copper, 1966b; Elias, 1988; Foster, 1974, 1989). The results of the present study Indicate that external variations exhibited by Anthracospirifer peiiaensis are due to both genetic factors (inferred from the individual) and ecophenotyplc factors. The geologic setting and methods utilized In this study are discussed In detail In Wulff (1991a) and In Appendix 0, and are briefly described below. DATA Intraspecific morphoiogic variation in brachiopods is not limited to spiriferids. Alexander (1975) determined that external variations in the Ordovician brachlopod Raflnesaulna alternata. allowed this strophomenid to Inhabit a wide variety of substrata with one morphotype per substratum type. Morphologically diverse Devonian brachiopods from 226 Utah, such as Cleoithvrldlna devonlca. Trifldorostellum dunbarense. SInotectlrostrum banffense and CvrtosDlrlfer montlcola also exhibit variations in external morphology. Studies indicated that ail morphotypes of a species apparently inhabited the same type of substratum (Alexander, 1977). Copper (1966b) determined that ail morphotypes of the Devonian atrypid, Kerpina vineta. inhabited the same types of substrata. The specimens of Anthracospirifer peiiaensis available for this study were from 9 localities across the Midcontinent and the Appaiachian Basin (Appendix 0, p. 56). They were separated into four groupings based soieiy on externai morphotype, with the initial assumption that each group was a separate species. These morphotypes are aiate, intermediate, notched and round (Figures 88 & 89). Oniy aduit specimens were used because many juveniies are morphoiogicaiiy simiiar, and it is oniy through aiiometric growth that different morphotypes arise. Current taxonomic practice on brachiopods reiies heaviiy on the character of internai structures for species designation. This is particuiariy important in groups such as the terebratuiids whose externai features are simple and extremely simiiar for many genera (M. Sandy, 1989, personal commun.). Thus, both internal and externai characters of Anthracospirifer peiiaensis were studied. Several variables were measured in an attempt to quanitify these morphoiogic differences (Figure 90). The data were subjected to simple bivariate statistics, principai component analysis (RCA) and discriminant function analysis (DFA). RESULTS Resuits from Chi-squared analysis show that four discrete morphotypes are present in the coiiections studied (Tabie 14). However, Length by Width and RCA piots indicate too much overlap to suggest that each morphotype represents a single species (Figures 91 & 92). Thus, based on these morphometric results, the individual brachiopods were considered to beiong to one species, Anthracospirifer peiiaensis. Analysis of serial sections and comparison of the dentai iameiiae, cardinai processes and spiraiium bases confirms that these morphotypes beiong to a single species (Figures 93 - 95). it is clear, therefore, that the 227 ’ r > l k ■ -"' 4# Figure 88: Morohotvoes of Anthracospirifer peiiaensis. A. Aiate, x .6; B. intermediate, x .8. 228 B Figure 89: Morphotypes of Anthracospirifer oeliaensis. A, Notched, x.75; B. Round, x .7. 229 MAXIMUM WIDTH HINGE LENGTH LENGTH ALATION = HINGE/WIDTH AT MID-LENGTH Figure 90: External variables utilized in biometric analysis of Anthracospirifer oeliaensis 230 Table 14: Chi-squared statistics for measurements on Anthracospirifer pellaensis HINGE 144.86 OF 4 PROS > X^ = 0.0001 MAXIMUM WIDTH X^ 125.75 DF 4 PROS > X^ = 0.0001 LENGTH X^ 28.14 DF 4 PROB > X^ = 0.0001 HINGE/LENGTH X^ 183.45 DF 4 PROB > X^ = 0.0001 MAXWIDTH/ LENGTH X^ 157.98 DF 4 PROB > X^ = 0.0001 ALATION x^ = 145.55 DF 4 PROB > X^ = 0.0001 HINGE * ^ + 11 13 15 17 19 21 23 25 27 29 LENGTH Figure 91: Hinge by length plot for Anthracospirifer pellaensis. Each moiphotype was plotted separately and the field of distribution outlined as follows: Alate = asferisks, Intermediate = dashed line, Notched = diamonds, Round = solid line. Note, although initially appears allometric, overlap of all morphotypes and range of size indicates it is not. ro w CAN 2 5 4 3 2 1 0 1 -2 •3 4 5 6 - 5.4 - 4.2 - 3.0 - 1.8 - 0.6 0.6 1.8 3.0 CAN 1 Figure 92: Cani x Can2 plot from Discriminant Function Analysis. Plotting and symbols as in Figure 35; note overlap among the morphotypes. ro CO ro oo Oc, ALATE 1.8mm NOTCHED 3.8mm ROUND 3.6mm IN TER M ED IA TE 0.9mm Figure 93: Transverse serial sections through each morphotype illustrating position, fibrous nature and overall shape similarity of the cardinal process. ro w w 234 ALATE 2.2mm NOTCHED 2.6mm ROUND 1.8mm IN TE R M ED IA TE 1.5mm Figure 94: Transverse serial sections through each morphotype illustrating position, shape and overall similarity of the dental lamellae. ALATE 1.9mm NOTCHED 3.9mm W ROUND 3.8mm INTERMEDIATE 0.9mm Figure 95: Transverse serial sections through each morphotype illustrating position, orientation and shape of the bases of the spiralium. ro CO CJl 236 mechanism causing these externai variations is intraspecific and whether geneticaiiy or non- geneticaiiy controiied, must be attributed to something other than species differentiation. OCCURRENCE OF ANTHRACOSPiRiFER PELLAENSiS Anthracospirifer oeiiaensls occurs in the Peiia Beds of iowa (Johnson & Vondra, 1969; McKay et ai., 1987), the Pitkin Limestone in Arkansas (Easton, 1942), Chesterian strata in indiana, iiiinois (Weiier, S., 1920) and Kentucky (Butts, 1917), the Greenbrier Group in West Virginia and western Maryiand (Tissue, 1986; herein) and Greenbrier equivaient rocks in southern Pennsyivania (Carney, 1987) (Figure 96). The presence of the connective seaway between the Appaiachian Basin and the Eastern interior Basin during the Late Mississippian probabiy enhanced distribution of marine organisms between the Greenbrier Sea and the waters to the west. Given comparabie physicai conditions, one would expect to find the same species in the basins on either side of the Cincinnati Arch. This would explain the widespread occurrence of A. pellaensis and other Mississippian fossils. An intimate relationship exists between turbulence and substratum characteristics. Muddy, soupy bottoms are indicative of lower energy conditions and mudstones and wackestones are typically deposited in these environments. Conversely, areas with abundant carbonate grains generally reflect higher energy waters where packstones and grainstones are typically deposited and fine grained sediments are winnowed. The distribution of & pellaensis morphotypes can be described in terms of three relationships: 1) iithoiogy and locality; 2) morphotype and locality; and 3) morphotype and iithoiogy. These are considered in the discussion below. APPALACHIAN BASIN Anthracospirifer pellaensis occurs in southern Pennsyivania and western Maryiand in units dominated by packstones and grainstones (Carney, 1987; herein). Morphotypes present are intermediate, notched and round (Figure 97). Aiate forms are notably absent. Southward, 238 PA A MD X w v f \ OCCURRENCE OF ANTHRACOSPIRIFER PELLAENSIS MORPHOTYPES IN THE CENTRAL APPALACHIAN BASIN PACKSTONES & GRAINSTONES WACKESTONES Figure 97: Occurrence of Antfiracospirifer pellaensis morphotypes In the central Appalachian Basin. Paleoshoreline Figure 96: Documeraed occurrences of AnlhracospHer pellaensis In the mkJcontlnent and Ihe Appalachian Basin. ro CO 238 PA # OCCURRENCE OFANTHRACOSPIRIFER PELLAENSIS MORPHOTYPES DSf THE CENTRAL APPALACHIAN BASIN PACKSTONES & GRAINSTONES WACKESTONES Figure 97: Occurrence of Anthracospirifer pellaensis morphotypes In the central Appalachian Basin. 240 OCCURRENCE 0¥ ANTHRACOSPIRIFER PELLAENSIS MORPHOTYPES IN IOWA n CALCAREOUS MUDSTONES Figure 98: Occurrence of Anthracospirifer oeliaensis morphotypes in iowa. 241 Frequency 140 120 100 80 60 40 20 IA-1 IA2 IA3 PA-4 IA-5 MD6 MD-7 WV-8 PA-9 cm cm cm g/p cm g/p g/p ws g/p Locality A late Notched Round Intermediate * Calcareous Mudstone cm Wockestone ws Groinstone/Pockstone g/p Figure 99: Summary of overall geographic distribution, morphotype geographic distribution and morphotype occurrence per type of substratum. Locality notation, I.e., IA-1, refer to localities listed In Appendix C, (Appendix 1, p. 56). 242 lithologies and may have been the least stable on such substrata. This may explain their overall smaller size as well. Because all four morphotypes do co-occur In muddy lithologies, an equally plausible viewpoint may be that the presence of alae restricted A. pellaensis from the packstone and gralnstone forming environments. One possible explanation may be the amount of torque exerted on a wider shell In higher energy waters. Schumann (1991) reported the occurrence of morphologic variability In the modern brachlopod Terebratalla transversa. Where water turbulence Is low (without strong currents), wide, well-ribbed shells predominate (splrlfer-type). Where stronger currents occur, rounded more rostrate shells dominate (atrypid-type). Finally, In very strong currents, only round, smooth thick- shelled individuals occur fTerebratula-tvoe). Additionally, some brachlopods are rheophlllc and orient themselves In the current for feeding (LaBarbera, 1978; Richardson, 1981). If an Individual were constantly trying to reorient In the current. It would have had little time to do anything else. Thus, the development of wide shells (alate) or the suppression of alae formation Is an ecophenotypic response by these modern brachlopods to their environment. This example may serve as an analog to fossil brachlopods, oartlcularlv Anthracospirifer pellaensis. CONCLUSION This study demonstrates that, at least, for Anthracospirifer peiiaensls. external characters and Internal structures are Important for proper taxomonic assignment. The morphologic varlablity exhibited by Anthracospirifer pellaensis can be attributed to ecophenotypic responses to the environment. Intermediate, notched and round Individuals were able to Inhabit a variety of substrata whiie the alate forms were not. The development of alae can be explained as a phenotype that could only be expressed In muddler and/or quieter environments. CHAPTER VII AN UPPER MISSISSIPPIAN REEF IN SOUTHEASTERN WEST VIRGINIA INTRODUCTION The construction and faunal composition of carbonate buildups differ markedly from the Early and Middle Paleozoic to the Late Paleozoic. During the Early and Middle Paleozoic, buildups were dominated by framework building organisms, such as corals, archaeocyathlds or stromatoporolds (James, 1983). These organisms gave these buildups topographic relief and wave reslstence. However, most of the carbonate buildups formed during the Mississippian do not have rigid frameworks. For example, the Early Mississippian is dominated by Waulsortlan buildups (Smith, 1972; Lees et al., 1985; Lees & Miller, 1985, Auslch & Meyer, 1990), which are enigmatic carbonate buildups with no visible framework structure. Thrombolltic carbonate bloherms have been described from Late Mississippian rocks (Webb, 1987). The distinction between these Early to Middle Paleozoic buildups and the Mississippian buildups came about near the end of the Devonian (Frasnlan-Fammenian extinction event) when many framework building organisms either became extinct or were severely reduced In number. In contrast to the Mississippian buildups, reef mounds of the Upper Carboniferous (Pennsylvanian) tend to have definite organic frameworks. Many Pennsylvanian and Permian carbonate buildups are dominated by calcareous phylloid algae (James, 1983; West, 1988). Thus, the presence during the Late Paleozoic of carbonate buildups with structural frameworks or reefs (as they will be referred to hereafter). Indicates that the conditions that supported such growth and the organisms capable of producing It, were not completely wiped out at the end of the Devonian, just merely suppressed. An Upper Mississippian reef In the Greenbrier Group of West Virginia Illustrates that some Middle Paleozoic reef builders survived Into the Late Paleozoic. The reef described here Is a small 243 244 patch reef consisting of a definite centrai framework and associated facies. Another possible Mississippian reef, that has been reported as a Lithostrotion. bed has been described from the Hiiisdaie Formation at Valley Head, West Virginia, it is described in a geologic quarry report and further study is needed to determine whether it is part of a reef complex. REEF DEFINITION Much controversy has centered on the definition of reefs. The past several decades have witnessed the development of many classification schemes and definitions of reefs and reef-iike structures (Dunham, 1970; Heckei, 1974). Several of these definitions are listed in Figure 100. i follow Wilson (1975) after Dunham (1970) and refer to a reef as any carbonate buildup that contains an organically built rigid framework. LOCATION AND STRATiGRAPHIG SETTING A small patch reef is exposed in a road outcrop on the north side of U.S. Route 219, approximately 1.3 miles northeast of the town of Salt Sulphur Springs, West Virginia (Figure 101). The outcrop is directly across the road from the Sait Sulphur Springs quarry locality discussed in Chapter 2. The entire exposure is situated in the uppermost Union Limestone and is at approximately the same stratigraphie level as the Archimedes-rich strata described by Wuiff (1989a, 1990c; Appendix A). DESCRIPTION OF THE REEF Figure 102 is a schematic representation of the reef outcrop and associated facies. The total length is approximately 48.7 m and the height through the reef core is approximately 1.65 m. The reef complex can be described in terms of seven facies; reef core (2), infrareef (2a), suprareef (2b), reef flank (1) & (3), interreef (5) and oolite shoal (4) & (2c). Because Facies 2b (suprareef) is in gradational contact with Facies 2 (reef core), and because the oolite facies occurs both lateral to the core and above it, it is assumed that the measured height of the reef core is close to the actual depositionai height. The following section contains lithologie and faunai descriptions of each facies. Detailed descriptions are contained in Appendix E. 245 REEF: "Any biologically Influenced buildup of carbonate sediment which affected deposition In adjacent areas (and thus differed to some degree from surrounding sediments), and stood topographically higher than surrounding sediments during deposition" (Longman, 1981) "A ridgellke or moundllke structure, layered or massive, built by sedentary calcareous organisms, especially corals and consisting mostly of their remains; It Is wave résistent and stands above the surrounding contemporaneously deposited sediment" (Bates & Jackson, 1980) "A buildup that displays 1) evidence of a) potential wave reslstence or b) growth In turbulent water which Implies wave reslstence & 2) evidence of control over the surrounding environment" (Heckei, 1974) "A buildup formed. In part, by a wave-resistant framework constructed by organisms - - this framework exerts some control over Its surrounding environments" (Wilson, 1975) Figure 100: Some currently recognized definitions of "reef. 246 Monroe County, West Virginia . SAIT SULPHUR SPRINGS Figure 101: Reef locality -1.3 miles northeast of Salt Sulphur Springs, WV on U.S. Route 219. 1m Figure 102: Schematic cross-section through the reef. Facies numbered as follows: 1 = Reef flank facies 1; 2 = Reef core; 2a = infrareef facies; 2b = suprareef facies; 2c = ooid shoal; 3 = Reef flank facies 2; 4 = ooid shoal and 5 = interreef facies. ro 248 Reef Core (Facies 2) (Figure 103) The iithoiogy is best described as a syringoporid boundstone. The core consists of a syringoporid coral coioriy. The matrix is composed of massive micrite and microspar. Ubiquitous sand-sized quartz and caicite grains are present. Major biotic components are the syringoporid corai framework and the caicareous aioae Sohaerocodium. This taxon is actuaily a symbiotic reiationship between the red aigae Rothoietzelia and the encrusting foraminifera Wetheredeiia (Wray, 1977). The aigae encrusts aii the coraiiia and in places, as masses, connects the coraiiites (Figure 103). if the corai were aiive at the time of encrustation, this may be an exampie of mutuaiism. This unusuai occurrence is discussed further in Chapter 3. infrareef Facies fFacies 2a) (Figure 104) This facies is at the base of the core and represents the substratum on which the corai coiony grew, it is a wackestone with a massive micrite and microspar matrix. There are no major biotic components, and the interstitiai biota consists of biociastic hash. The debris was probabiy derived from within this facies and from iateraiiy adjacent facies. Corai debris is notabiy absent from the facies. Suprareef Facies fFacies 2b) (Figure 105) The suprareef facies is in gradationai contact with the reef core beiow. it is an aigai wackestone with a massive and coarse microspar matrix. Pods of micrite are scattered throughout. Abundant carbonate grains are present as ciusters in the coarser matrix and scattered in the finer matrix. They are probabiy derived from reworking of the corai in Facies 2. Pyroxene and pyrite are common components as weli. The singie major biotic component is Sohaerocodium. it encrusts aimost everything, even the matrix. Reef Fiank Facies A fFacies 11 (Figure 106) This facies is a fossiiiferous wackestone. it is situated in the iee of the reef. The matrix is composed of massive micrite and fine microspar that contains scattered sand-to silt- sized quartz grains. Major biotic components are rugose corals, the fenestrate bryozoan Archimedes and peimatozoan debris. Biociastic hash, similar to that in Facies 2b, makes up the interstitiai biota. 249 Figure 103: Reef Core Facies. Unit 219-2, Syringoporid coral, x 25. 250 Figure 104: Infrareef Facies. Unit 219-2a, biociastic hash, absence of corai debris, x 25. 251 Figure 105: Suprareef Fades. Unit 219 2b, A. Sphaerocodium sp., corai debris & bryozoan fragments, x 25. B. Sphaerocodium sp. encrusting bryozoan fragment, x 63. 252 Figure 106: Reef Flank Facies A. Unit 219-1. Dasyciadaceans, fenestrate bryozoans, peimatozoan debris. 253 Reef Flank Fades B fFacles 3) (Figure 107) This facies is notabiy different from the fiank facies described above, it occurs in a higher energy zone on the stoss side of the reef core and contains a substantialiy different faunai component. It is a fenestrate-rich wackestone with a massive, coarse microspar matrix. Scattered areas of micrite are present. Ooids are common and were washed in from the iateraiiy adjacent shoai (Facies 4). The major biotic components are Archimedes, encrusting bryozoans and peimatozoan debris. The encrusting bryozoans are larger and more abundant than in previously described facies. The conditions of this environment were ideal for development of Archimedes colonies (see below). Interreef Facies (Facies 51 (Figure 108) The interreef facies represents background depositionai conditions and is similar in character to stratigraphicaiiy equivaient units in nearby localities, it is a fenestrate and echinoderm wackestone with a microspar matrix and scattered areas of micrite. Major biotic components are Archimedes and peimatozoan debris. Archimedes is particularly abundant in this facies and, as in ail other Archimedes bearing units in this area, are very well preserved (Figure 109). There are no minor biotic components. Oolite Shoal fFacies 4 & 2c) (Figures 110 & 111) The oolite facies occurs both lateral to (Facies 4) and above (Facies 2c) the reef core. Pétrographie and hand specimen analyses confirm that these two facies are correlative. They are oolitic grainstones with medium-grained to coarse-grained sparry mosaic cement. Intergranular crystals exhibit typical aggrading growth toward centers of voids. The aiiochems consist aimost exclusively of well formed ooids with biociasts as nuclei. Non-ooid aiiochems also have oolitic coatings. Facies 2c differs from Facies 4 by the presence of abundant, intergranular clusters of pellets. REEF ECOLOGY AND HISTORY The presence of the syringoporid boundstone and associated facies described from this outcrop are consistent with the interpretation that this is a patch reef complex. The 254 B Figure 107: Reef Fiank Facies B. Unit 219-3, x 25. A. Fenestelia sensu iato; B. Cystoporate. 255 Figure 108: Interreef Facies. Unit 219-5, x 25. A. Archimedes sp.; B. Cystoporate (upper 1 /2 of photo), large intraclast in lower center. 256 ë ) ;.. ' ' Figure 109: Well preserved Archimedes zooarlum, Salt Sulphur Springs Quarry. 257 Figure 110: Ooid Shoal Facies, Unit 219-4, x 25. 258 Figure 111: Ooid Shoai Faciès, Unit 219 2c, x 25. Note abundant peiiets, biociasts as ooid nuciei. 259 ecology and history of this reef can be summarized in the following scenario. Figure 112 has been modified from McKinney (1979) to illustrate the reef's position compared to the oolite shoai and Archimedes colonies. The water was shallow as indicated by the calcareous algae and shallow water dwelling organisms. With the exception of the shoai area, depth was most likely below normal wave base. The shoai created a sheltered environment conducive for grovyth of initially fragile organisms such as young bryozoa or coral colonies. Leeward of the shoai, colonization on the muddy substratum was facilitated by the abundant biociastic debris of the infrareef facies. This provided a hard substratum for larval settlement. The syringoporid colony grew in a manner similar to that of other organisms adapted for life on a somewhat muddy substratum. Archimedes colonies flourished both in the lee of the shoai (as depicted by McKinney, 1979) and in front of it. Water turbulence was probably higher on the stoss side of the shoai. The presence of Archimedes in more turbulent waters indicates that it was equally able to flourish successfully in both environmental settings. Ooids were formed in the higher energy waters of the shoal environment. As water masses passed over the shoal, friction generated by waves touching the bottom caused the masses to slow down. Suspended nutrients settled out, essentially raining down on the Archimedes and passing along to the benthos behind. Eventually, progradation of the shoai caused cessation of coral growth and a new facies developed on top of the reef core. Further progradation resulted in smothering and burial of the reef. OTHER LATE PALEOZOIC CARBONATE BUILDUPS The reef described above contains an interreef fauna dominated by fenestrate bryozoans and pelmatozoans with minor rugose corals. The actual core consists of one or more syringoporid coral colonies. As noted above, other Mississippian carbonate buildups do not have such frameworks and distinct facies development. Early Mississippian Waulsortian mounds have been described from Ireland (Sevastopuio, 1982), England (Miller & Grayson, 1982) Montana (Cotter, 1965; Smith, 1977), New Mexico (Lane, 1982); the southern midcontinent (Manger & Thompson, 1982) and Kentucky (Ausich & Meyer, 1990). The major lithology is a wackestone to mudstone. Major j » (B> i ^ Figure 112; Paleoenvironmental reconstruction of ttie reef environment. Numbers at base correspond to facies discussed in text and listed in Figure 102. Modified from McKinney, 1979. ro cn o 261 biotic components are fenestrate bryozoans and crinoids. Minor components inciude brachiopods, moiiuscs, Amoiexis (a soiitary ruoosanl. Svrinaooora (a tabuiate corai), ostracods, foraminifera, triiobite fragments and caicispheres (Wiison, 1975). There are no preserved frame-buiiding organisms. The abundant peimatozoan debris and fenestrate bryozoans have indicated to some workers that they may have served as sediment bafflers and trappers (King, 1986; Horowitz, 1987 et ai., in West, 1988). in situ crinoid hoidfasts in the wackestones of the Fort Payne Formation support this interpretation (Ausich & Meyer, 1990). Thromboiitic mounds have been described from the upper Mississippian Pitkin Limestone in Arkansas (Webb, 1987). Thromboiites (cryptaigai structures with obscureiy dotted, rather than a iaminated, internai structure (Bates & Jackson, 1980) are the most common biotic constituent foiiowed by fenestrate and encrusting bryozoans, encrusting foraminifera, "spicuiar" aigae, Asohaitina sp., rhodoiithic aigae, crinoids (with hoidfasts in piace) and brachiopods. Aigae are apparentiy the framework buiiders for these buiidups (Webb, 1987). A third exampie of carbonate buiidups are the (upper Pennsyivanian) phyiioid aigae reefs described by James (1983) and West (1988). They have a wackestone matrix and an abundant fauna. The main faunai component and frame builder is phyiioid aigae, consisting of carbonate encrusted leaves that grew upright in thickets, in some buiidups, encrusting bryozoans and foraminifera also contributed to the framework, commonly in equal abundance to the aigae. Minor biotic consituents inciude red and green aigae, fusiiinids, caicispheres, crinoids, rugose corals and brachiopods. These buiidups are much smaller than Waulsortian mounds and, as in other well defined reefs, there are skeletal flanking beds. There is a zonation of biota as well, with red aigae, fusiiinids, caicispheres and crinoids occurring more oceanward, and green aigae, rugose corals and brachiopods occurring leeward. 262 CONCLUSION The important points of this study can be summarized as follows: 1) The usual onshore-offshore progression of facies Is not recorded In the reef of this study. Not only was the shoreline hundreds of miles to the northwest, but the trend of the facies from backreef to forereef Is northeast-southwest. It Is clear that this shoal and small reef were a localized occurrence. 2) With the exception of the Pennsylvanian phyiioid algae mounds, few other Late Paleozoic buildups have definite frameworks. Most Mississippian carbonate buildups are considerably different from other buiidups in the Paieozoic. 3) The presence of this patch reef of Late Mississippian age provides proof that, despite the extinctions at the end of the Devonian, the habitats in which reefs form in were stiil avaiiable. Those organisms capable of producing frameworks managed to do so. Compared to their predecessors, however, reef formation and growth was subdued. With additionai carefui fieid work, it is possibie that more Late Mississippian reefs wiil be found. CHAPTER VIII CONCLUSION This study of the Upper Greenbrier Group and equivalent strata provides new Information allowing for a more complete understanding of Greenbrier depositional history and Appalachian Basin mechanics. Whereas previous studies have Illustrated the Appalachian Basin as an open marine northern extension of the seas to the south and west (see Carney & Smosna, 1989), analysis of the sedimentology, faunai components and tectonics reveals that this was not the case In the Late Mississippian. The recognition of distinct facies suites across the field area resulted In the division of the field area Into three regions (Figure ). The following discussion presents these findings as a summary of the more detailed work contained within this document. Sedimentologlcally, the Greenbrier Group consists of a wide variety of carbonate rocks. They range from clean oolitic sands to biociastic oolitic grainstones to fossiliferous packstones and wackestones to mudstones. With the exception of the fossils within the mudstones, ail others were Interpreted to be relatively In-situ. Disarticulation and breakage of bioclasts were interpreted to have been caused by minimal transport and bioturbation. The great number of micritized grains indicates a water depth within the photic zone. Formation of the grainstones, packstones and wackestones was not due to great changes in water turbulence or environmental conditions. Rather, they were likened to the normal distributional patchiness seen In modern oceans. The lateral variations were Interpreted to have been the source of these different rock facies. The West Virginia Dome, a generally subaqueous, topographic high within the Greenbrier Sea, Interfered with the southward transport of siiiciciastics and other terrigenous materials. This resulted In a concentration of quartz sand and silt around the Dome and a decrease in siiiciciastics 263 264 southward. Pulses of erosion and influx of terrigenous material is represented in southern sections where thin but prominent layers of siitstone and calcareous siitstone occur. Paleontological analysis Indicated that open marine conditions did not exist along the length of the basin during deposition of the upper Greenbrier units. A depauperate fauna of ostracodes, caicispheres, gastropods, triiobites and brachiopods dominates the Greenbrier Formation in Region 1. The absence of upper tier suspension feeders, such as crinoids, bryozoans and corals implied environmental conditions far from normal marine. Upper tier suspension feeders do occur In the uppermost Greenbrier Formation In Region 1 indicating changes toward more normal marine conditions. The highly turbulent waters around the West Virginia Dome in Region 2 appear to have limited the successful habitation of certain organisms even though the waters may have been of normal marine salinity and temperature. The increase in sliiciciastic material and thus increase in turbidity may also have contributed to the low diversity and abundance of organisms. Region 3 contrasts sharply with Regions 1 and 2. it contains a diverse and abundant faunai assemblage consisting of organisms best adapted for life in open marine conditions. These inciude brachiopods, bryozoans, crinoids, biastolds and corals. This north to south distribution of fauna indicates changing environmental conditions from iagoonai with restricted circulation to high turbulence and increased turbidity to open marine. These differences were caused, in part, by the presence of a wide, shallow shelf in the north, the West Virginia Dome and the 38th Parallel Lineament Zone (Figure 9). interpretation of the autecoiogy of the organisms present indicates that some were highly adaptable and capable of living under a variety of conditions and on a variety of substrata. Others were quite limited and restricted to particuiar waters and substrata. Brachiopods appear to have been the most fiexibie with regard to these environmentai conditions while corals, bryozoans and echinoderms were the least fiexibie. Faunai associations based on recurring groupings of organisms were quaiitativeiy described. They closely follow the paleoenvironmental interpretations and divisions of Chapter 2. Cluster analysis was empioyed to confirm the quaiitative separation into distinct groupings. 265 Tier structure and trophic strategies were used to further characterize the faunai associations. They are simple associations with iittie or no evidence of complicating factors such as presence of predators or large scale transport. Because the paieoenvironments change southward, and the organisms reflect this change, each faunai association occurs in one region only. Because the Eastern interior Basin was episodically linked to the Appalachian Basin via the connective seaway to the south (Figure # ), a comparison of age-equivaient strata was conducted to see what similarities, if any, existed in faunai composition. Overall, the tectonics of the two basins differed notably and faunai make-up was expected to differ as well. This was found to be the case. At the generic level, diversity within individual phyla was much higher in the EiB. The most notable differences were in the echinoderms, bryozoans, corals, bivalves and gastropods (Table 8). Environmentai differences due to clastic influx, water circulation and tectonic movement were interpreted to have been the cause for this large difference in diversity. intraspecific morphologic variation was analyzed usina Anthracosoirifer oeilaensis. This brachiopod exhibits great external variation in shell morphology, it has a wide geographic distribution and occurs on a variety of substrata. Multivariate statistics and analysis of internal structures were utilized to confirm that ail morphotypes in the collection studied belonged to the same species. Analysis of the relationship to the substratum, morphotype distribution on various substrata and geographic distribution indicated that the external variations could be attributed to ecophenotypic responses to the environment. These results provide a basis by which other morphologically variable brachiopods can be done can be analyzed. Reefs are relatively rare in the Upper Mississippian. A patch reef and associated facies was described from the Union Limestone in southern West Virginia. This occurrence indicates that such reefs do occur in the Upper Mississippian. However, they are smaller and less complex than, for example, those In the Early or Late Paieozoic. CHAPTER IX SYSTEMATICS PHYLUM BRACHIOPODA Dumerii, 1806 Fourteen genera were Identified from the Greenbrier Rocks studied. Species designations were not made in ail cases due to lack of information on internal structures and degree of preservation. Unless noted otherwise, identification was based on comparison to written descriptions and photographs from Williams et ai. (1965). in cases where only this reference was used, the description is short and paraphrased from the appropriate section. Ranges and occurrences outside of the field area were compiled from Carter and Carter (1970) and Williams et ai. (1965). Order Terebratuilda Waagen, 1883 Family Cranaenidae Cloud, 1942 Subfamily Girtyeiiinae Stehii, 1965 Genus Girtyeiia Weller, 1914 Range: Mississippian Occurrence: Deep Creek Quarry, R & R Quarry, Sait Sulphur Springs Quarry; North America - Europe Girtveiia sp. Figure 69 Remarks - - These small, ovate brachiopods were assigned to Girtveiia sp. They were distinguished by their small size, faint fold and sulcus and straight anterior margin. No umbonai features were well enough preserved to help in the identification. Several species of 266 267 Girtveiia have been Identified In the Mississippi Valley and the Appalachian Basin (Weller, 1914; Reger, 1926) but a lower taxonomic designation was not possible with the material available. Order Splrlferlda Waagen, 1883 Family Retzlldae Waagen, 1883 Genus Eumetrla Hall, 1864 Range: L Mississippian - U. Mississippian; L Carboniferous - L Permian Occurrence: Sang Run Quarry, Deep Creek Quarry, Montervllle Quarry, R & R Quarry, Knobs-Unlon Road, Alderson, Greenville; North America; Europe, USSR Eumetrla verneullana (Hall, 1883) Figure 69 Remarks - - Identification was based on comparisons to written descriptions and photographs In Weller (1914). Three species of Eumetrla are common In the Mississippi Valley region. Eumetrla verneullana Is more elongate than oval. The costae are similar In spacing and number to E. vera. but the shell Is more elongate than E. vera or E. costata. Eumetrla n. sp. Figure 69 Description - - Shell small, subequally biconvex, greatest width approximately mid-length. Dimensions of complete specimen are, shell width approximately 12 mm, shell length approximately 11.8 mm; finely costate with approximately 25 costae In 10 mm; umbo dominated by large circular foramen, umbo very weakly Incurved toward brachial valve. Remarks - - This brachiopod Is nearly Identical to E verneullana except the umbo Is less Incurved and the pedical foramen can not be seen from the brachial side (as Is the case In all other species of Eumetrla). Two specimens were collected at Deep Creek Quarry. 268 Family Splrifericlae King, 1846 Genus Anthracosplrifer Lane, 1963 p. 387 Range: U. Mississippian - Pennsylvanian Occurrence: Sang Run Quarry, Deep Creek Quarry, Oakland Quarry, Montervllle Quarry, Butcher Quarry, R & R Quarry, Renick Valley, Knobs-Unlon Road, Salt Sulphur Springs Quarry, Alderson, Acme Quarry, Greenville; North America Anthracosoirifer oeilaensis (Weller, 1914) Figure 67 Remarks - - Numerous specimens were collected throughout the field area. Originally Identified as Solrifer oeilaensis by Weller (1914) and other early workers; Dutro (personal commun., 1990) and comparison to specimens of Solrifer and Anthracosoirifer Indicated that these brachiopods should be assigned to Anthracosoirifer. The shells are small to medium with a well defined fold and sulcus, 9 to 14 costae on each flank and 1 to 5 costae In the sulcus. There Is a central costa in the fold and a complimentary depression In the sulcus. Shell morphology ranges from transverse to round. These variations have been linked to ecophenotypic responses to environmental conditions (Wulff, 1989, 1990, Chapter 6). Appendix J contains the measurements taken on Anthracosoirifer oeilaensis to determine this relationship. Pertinent photographs and diagrams are Included In Chapter 6. Anthracosoirifer brecklnrldoensls Weller. 1914 Figure 67 Remarks - - The shell Is small and round with sharp, well defined costae. Maximum width occurs at about mid-length. It has fewer lateral costae than A. oeilaensis. The shell Is smaller than round morphotypes of A. oeilaensis. and it Is narrower In overall outline. Five specimens were collected at Deep Creek Quarry. Range: Occurrence: Deep Creek Quarry; North America (Chester) 269 Family Athyrldldae M’Coy, 1844 Subfamily Athyridlnae M’Coy, 1844 Genus Composita Brown, 1849 Range: U. Devonian (Fammenlan) - Permian Occurrence: Sang Run Quarry, Deep Creek Quarry, Oakland Quarry, Montervllle Quarry, Butcher Quarry, Slaty Fork Quarry, R & R Quarry, RenIck Valley, Knobs-Unlon Road, Salt Sulphur Springs Quarry, Alderson, Greenville; Europe - North America - Australia Comooslta subauadrata (Hall, 1858) Figure 68 Remarks - - Comooslta subauadrata Is abundant throughout the field area. Within the range of variation In the fold, sulcus and number of growth lines, all specimens exhibit essentially the same morphology. The sulcus develops about half-way between the posterior and anterior margins. Length and width are approximately equal, and the posterior margin makes an approximate 90“ angle at the umbo. When turned 45“ and viewed, the shell approximates a subquadrate shape. The anterior margin may be slightly to strongly llnguold. It Is my opinion that Comooslta Is highly overspllt throughout its occurrence. All specimens In this study area have been identified as Ç. subauadrata based on the umbonai angle and the overall shell shape. Genus Clelothvrldlna Buckman, 1906 Range: U. Devonian - Permian Occurrence: Knobs-Unlon Road; Cosmopolitan Clelothvrldlna sp. Figure 68 Remarks - - Clelothvrldlna Is subequally biconvex and transversely suboval. Growth lamellae are distinct and extend Into short flat spines. The shell Is small, and because no internal features were observed a species designation could not be made. 270 Family Martiniidae Waagen, 1883 Genus Martlnia M’Coy, 1844 Range: L Carboniferous, ?U. Carboniferous Occurrence: Sang Run Quarry, Deep Creek Quarry, Montervllle Quarry, Knobs-Unlon Road, Salt Sulpfiur Springs Quarry; Cosmopolitan Martlnia contracta (Meek & Worthen, 1861) Figure 68 Remarks - - The shell is small to slightly larger, biconvex and nearly equldlmenslonal with broadly rounded cardinal extremities. The hingellne Is well defined across the ventral valve creating a "shleld-llke" shape to the overall outline. The umbo Is Incurved, and there Is no external ornamentation of note. Overall, It looks similar to Comooslta with the exception of the well-defined hingellne and shallower fold and sulcus. Family Retlcularlldae Waagen, 1883 Genus Retlcularla M’Coy, 1844, Range: ?Devonlan, L. Carboniferous Occurrence: RenIck Valley, Salt Sulphur Springs, Alderson; Europe, Asia Retlcularla sp. Figure 67 Remarks - - Retlcularla Is rare In the Greenbrier rocks studied. It Is small and unequally biconvex, slightly transverse with a weak fold and sulcus. Concentric growth lamellae are conspicuous and there are unlramous spines along the lamellae. No spines were preserved In the specimens collected. Because no Internal features were observed, a species designation could not be made. Order Strophomenlda Qplk, 1934 Suborder Productlnlda Waagen, 1883 Family Productldae Gray, 1840 271 Genus Diaphragmas GIrty, 1910 Range: Upper Mississippian (Meramec - Chester) Occurrence: Sang Run Quarry, Deep Creek Quarry, Monterviiie Quarry, Kenton-Meadows Quarry, R & R Quarry, Renick Vaiiey, Knobs-Union Road, Sait Sulphur Springs Quarry, Aiderson, Acme Quarry; North America Diaohraomus cestriensis fWorthen. 1860) Figure 65 Remarks: This brachiopod is abundant in the study area. Specimens were identified by comparison to photographs and written descriptions in Weiier (1914), Muir Wood & Cooper (1960) and Wiiiiams et ai. (1965). Most of the specimens are disarticuiated vaives and neariy aii the ventrai vaives are preserved interior up. Species identification was based on the characteristics of ventrai vaive interiors. There is a medium septum that runs about haif the iength of the vaive, adductor muscie scars are branching/dendritic and iobate. Oniy the exterior of the dorsai vaives was observed, it is eiongate, with a short viscerai disk, curving traii, few rugae and fine spines which occur as a iarge group on the flanks and scattered on the costae. Whoie sheiis are often broken at the diaphragm, in which case no traii is preserved. Where a traii is present, it is never entire. Famiiy Linoproductidae Stehii, 1954 Subfamiiy Linoproductinae Stehii, 1954 Genus Ovatia Muir-Wood & Cooper, 1960 Range: L. Carboniferous (L Mississippian - U. Mississippian) Occurrence: Sang Run Quarry, Deep Creek Quarry, Monterviiie Quarry; North America - Europe - (USSR) - Asia (Kazakhstan) Ovatia eionoata (Muir-Wood & Cooper, 1960) Figure 65 Remarks: identification was confirmed by J. Carter (Carnegie Museum). The brachiopod has a medium-sized, eiongate sheii with distinct irreguiar costae and rugae on flanks, it has a 272 tapering umbo and the dorsal valve Is gibbous. All of the collected specimens are articulated thus no Information on Internal features was available. Species designation was based on overall shell shape and number of rugae (approximately 8 near the hinge and on the flanks). The trail curves so that the visceral disk Is at approximately right angles to It. Ovatia eionoata Is distinguished from (). ovata by Its longer trail, steep flanks, massive Incurved umbo and more numerous spines (Mulr-Wood & Cooper, 1960). Ovatia Is commonly confused with Llnooroductus. which Is a Pennsylvanian genus of this subfamily (Carter, personal commun.). Family Buxtonlldae Mulr-Wood & Cooper, 1960 Subfamily Buxtonllnae Mulr-Wood & Cooper, 1960 Genus Protonlella Bell, 1929 Range: U. Mississippian (Meramec - Chester), ?L Pennsylvanian (Morrowan) Occurrence: Deep Creek Quarry, Oakland Quarry, Salt Sulphur Springs Quarry; North America Protonlella parvus? (Meek & Worthen, 1860) Figure 65 Remarks - - This brachiopod was Identified by J. Carter (Carnegie Museum). The shell Is small, subcircular to subpentagonal In outline and finely costate. The visceral disc and the trail are short. The flanks spread or flare. No Internal structures were observed. These specimens are easily confused with small Diaohraomus specimens, and because only a few were collected, the Identification Is tenuous. Family Echlnoconchldae Stehii, 1954 Subfamily Echinoconchlnae Stehii, 1954 Genus Echlnoconchus Weller. 1914 Range: L. Carboniferous (Mississippian) Occurrence: Montervllle Quarry, Europe, N. Africa, Asia, North America 273 Echlnoconchus sp. Figure 65 Remarks - - This brachiopod Is distinct. The shell is medium sized, and concentric growth lines with double rows of spines are on both valves. A shallow sulcus Is present In the dorsal valve. The shell Is concavo-convex, or the brachial valve Is geniculate. No Internal structures were observed, and species designation was not possible. Family Marglnlferidae Stehii, 1954 Subfamily Costlsplnlferlnae Mulr-Wood & Cooper, 1960 Genus Inflatia Mulr-Wood & Cooper, 1960 Range: Upper Mississippian (Chester) Occurrence: Montervllle Quarry, R & R Quarry, RenIck Valley, Knobs-Unlon Road; North America Inflatia Inflatus McChesney, 1860 Figure 66 Remarks - - This brachiopod has a distinct shell with a well defined sulcus In the dorsal valve. It Is medium sized, elongate-quadrate, and the dorsal valve Is spirally curved. Rugae are present on the posterior of both valves. Spines are scattered and also occur in a row near the dorsal valve hinge. No Internal structures were observed and the species designation was based on the descriptions from Weller (1914) and Mulr-Wood (1965). Family Orthotetldae Waagen, 1884 Subfamily Orthotetlnae Waagen, 1884 Genus Orthotetes Fischer de Waldheim, 1829 Range: M. Carboniferous - Permian Occurrence: Sang Run Quarry, Deep Creek Quarry, Oakland Quarry, Montervllle Quarry, RenIck Valley, Salt Sulphur Springs Quarry; Cosmopolitan 274 Orthotetes kaskasklensis (McChesney, 1860) Figure 66 Remarks - - The shell Is medium to slightly larger In size and concavo-convex. The outline Is round to oval with a straight, well defined hingellne. Most of the kaskasklensis specimens collected were disarticulated. A median septum extends about 1/4 of the length of the dorsal valve. The dental ridges are fused by secondary shell substance that defines a small delthyrlal chamber. This Is commonly filled with secondary shell material as well. The ventral valve Is convex and Is rarely preserved whole In the study area. Family Chonetldae Bronn, 1862 Subfamily Rugosochonetlnae Mulr-Wood, 1962 Genus Rugosochonetes Sokolskaya, 1950 Range: L. Carboniferous - U. Carboniferous Occurrence: RenIck Valley, Knobs-Unlon Road, Alderson; Europe, Asia, Australia, North America, Africa? Rugosochonetes sp. Remarks - - Rugosochonetes has a small, piano- to sightly concavo-convex shell. It Is caplllate with numerous splnules. A dorsal medium septum Is approximately one-half the valve In length. Phylum Echlnodermata Laske, 1878 Subphylum Pelmatozoa Leuckart, 1848 Class Blastoldea Say, 1825 Order Eublastoldea Bather, 1899 Family Pentremltldae d’Orblgny, 1852 Genus Pentremltes Say, 1820 Range: Mississippian - Pennsylvanian Occurrence: R & R Quarry, RenIck Valley, Knobs-Unlon Road, Salt Sulphur Springs Quarry, Acme Quarry, Greenville; North America, South America 275 Remarks - - Pentremltes aodoni (Defrance), P. Duichellis Ulrich, and P. tulloaformls Hambach (Figure 72), were Identified by comparison to photographs and descriptions In Waters et al. (1985). The genus Pentremltes Is divided Into two groups based on the vault to pelvis ratio as a measurement of form. Pyriform has a V/P ratio that does not change significantly during ontogeny and growth approximates Isometry. They are pentagonal In cross-section throughout life. Godonlform has a V /P ratio that changes markedly throughout ontogeny and growth Is strongly allometrlc. In cross-section, they are pentagonal as juveniles and pentalobate as adults. Pentremltes tulloaformls has a very low pelvis and a high vault. Pentremltes aodoni has almost no pelvis. Is nearly flat at the base of the cup and has a high vault. It Is also more Inflated than P. tulloaformls. Pentremltes oulchellls has a medium pelvis and a high vault. Most of the specimens are fairly small and because of the ontogentic changes, the species designations are tentative. Class Crinoldea Miller, 1821 Order Monobathrlda Moore & Laudon, 1943 Family DIchocrlnldae S. A. Miller, 1889 Genus Pterotocrlnus Lyon & Casseday, 1859 Range: Upper Mississippian Occurrence: Slaty Fork Quarry, Knobs-Unlon Road, Salt Sulphur Springs Quarry, Greenville; USA Pterotocrlnus serratus Weller, 1920 Figure 72 Remarks - - The genus Pterotocrlnus Is characterized by five radially arranged, large tegmlnal spines. They are located between the arm rays and are referred to as "wing plates." Due to the great variability In wing plate morphology, species classification Is based on these plates (Weller, 1920; Gutschick, 1965; Horowitz, 1965). Pterotocrlnus serratus has wing plates that. In adults, are approximately 12 mm long and 5 mm wide with serrations at the distal end. 276 Phylum Byrozoa Ehrenberg, 1831 Class Stenolaemata Allman, 1856 The bryozoan material In these units was sporadically distributed and commonly poorly preserved. Because of this, Identification below the order level was not attempted in most cases. Specimens were assigned to orders by analysis of external characteristics such as presence of iunaria and vesicular tissue and spacing of zooecia. Exceptions to this are the fenestrates which, providing some zooecia were observable on frond branches, were identified to genus. Identifications were made utilizing Ausich’s (1978) scheme for recognizing fenestrate genera. Order Fenestrate Genus Archimedes Owen, 1838 Range: Mississippian - Permian Occurrence: Sang Run Quarry, Oakland, R & R Quarry, Knobs-Unlon Road, Salt Sulphur Springs Quarry, Alderson, Acme Quarry; North America Archimedes sp. Figure 71 Remarks: Many axes and axes with fronds were collected. Archimedes was identified on the basis of the corkscrew axis. No zooecia were visible on the attached fronds, thus a more complete description of the zooarium was not possible. Varying lengths of axes show some differential spacing of whorls but these were not distinct enough to subdivide them into species. Genus Fenestelia Lonsdale, 1830 Range: Ordovician - Permian 277 Occurrence: Sang Run Quarry, Oakland, R & R Quarry, Knobs-Unlon Road, Salt Sulphur Springs Quarry, Alderson, Acme Quarry Fenestelia sensu lato Figure 71 Remarks: The genus Fenestelia has two rows of zooecia on the branches and none on the dissepiments. A reticulate meshwork Is formed by the branches and dissepiments. The abundance of these fronds In association with Archimedes sp. suggests that some. If not all of the Fenestelia fronds were actually part Archimedes. Genus Lvrooorella Simpson, 1895 Range: Mississippian - Permian Occurrence: Oakland Quarry Lvrooorella sp. Figure 71 Remarks: Qne specimen was collected at Oakland Quarry. It was Identified by the thick boundary from which the fenestrate frond network grows. No other external features were observed for use In Identification. Order Cystoporata Astrova, 1964 Remarks: Specimens consisted of numerous small fragments In a variety of growth forms Including encrusting, cylindrical and ramose. Lunarla are distinct on the external surfaces and the vesicular tissue separates evenly spaced zooecia (Figure 71). Range: middle Ordovician to Triassic Occurrence: Sang Run Quarry, Oakland Quarry Family Rhabdomesldae Vine, 1884 278 Remarks: Rhabdomesonids are small, delicate bryozoans only a few millimeters In diameter. They are cylindrical and ramose In external form and are rare in the Greenbrier rocks studied Range: Upper Silurian - Upper Permian Occurrence: Sang Run Quarry, Oakland Quarry, R & R Quarry, RenIck Valley Order Trepostomata Ulrich, 1882 Remarks - - Specimens consist of abundant, small pieces In a variety of growth forms Including massive, encrusting, cylindrical and branching. Zoolds are closely spaced and no vesslcular tissue was observed on external surfaces (Figure 71). Range: Middle Ordovician to Triassic Occurrence: Sang Run Quarry, Oakland Quarry Phylum Cnidarla Hatschek, 1888 Class Anthozoa Ehrenberg, 1834 Subclass Rugosa Mllne-Edwards & Halme, 1850 Remarks: No attempt was made to Identify these down to any lower taxonomic level. Range: Ordovician - Permian Occurrence: Sang Run Quarry, Oakland Quarry, Montervllle Quarry, Butcher Quarry, Slaty Fork Quarry, R & R Quarry, RenIck Valley, Knobs-Unlon Road, Salt Sulphur Springs Quarry, Alderson, Acme Quarry, Greenville Subclass Tabulate Order Auloporlda Sokolov, 1947 Superfamily Syrlngopirlcae de Fromentel, 1861 Family Syringoporldae de Fromentel, 1861 Remarks: On the outcrop, syringoporid corals exhibit closely spaced vertical tubes. The Intervening spaces are filled with micrite. Observed In thin section, the corallltes are thick 279 walled with tabulae visible In oblique sections. Overall, syrlngoporids are compound and cylidrlcal with moderately thick walled corallltes. They are connected by horizontal tubull or platforms. Generic designation was not possible with the material available (Figure 113). Occurrence: Salt Sulphur Springs Quarry Family Palaeacldae Roemer, 1883 Genus Palaeacis Halme, 1857 In Mllne-Edwards & Halme, 1857c Range: Upper Devonian - Middle Permian; L Carboniferous Occurrence: Sang Run Quarry; North America, Europe (British Isles), Australia (Queensland) Palaeacis sp. Figure 114 Remarks - - This Is a tiny colonial coral with a varying number of corallltes. The surface ornamentation consists of serrated ridges with perforations between the ridges. The basal attachment may have foreign objects Incorporated Into It. Palaeacis sp. Is rare at Sang Run. Preservation was not good enough to allow for a definite species designation. Phylum Arthropoda Class Triloblta Walch, 1771 Order Polymerlda Hupe, 1953 Family Philllpslldae Oehlert, 1886 Genus Paladin Weller, 1936 Paladin chesterensis (Weller, 1936) Figure 72 Remarks - - Identification was based on photographs and descriptions In Chamberlain (1969), BrezlnskI (1988) and Harrington (1959). The glabella is slightly expanded in front, encroaching on the anterior border but not reaching the anterior margin. It is slightly contracted opposite the eyes which are large and posterior In location. The pygydlum has a well defined border. 280 B jüaâüM î Figure 113: Syringoporid coral. A. Outcrop view of reef core, Salt Sulphur Springs Quarry; B. Exposed coral on weathered surface. 281 Figure 114: Palaeacis sp., x 1.4. 282 It is long and multisegmented. A single row of tubercles are present on the axial rings of the pygidlum. Range: Middle MIsslsslpplan - Lower Permian; L lower Carboniferous Occurrence: Sang Run Quarry, Deep Creek Quarry, Oakland Quarry, Butcher Quarry, Knobs- Unlon Road, Acme Quarry; USA, Europe Class Ostracoda Latrellle, 1806 Remarks: Observed only In thin section, these were Identified by comparison to photographs In Horowitz & Potter (1971). Occurrence: Sang Run Quarry, Deep Creek Quarry, Montervllle Quarry, Acme Quarry Phylum Mollusca Class Gastropoda Order Archaeogastropoda Thiele, 1925 Suborder Maclurltlna Cox & Knight, 1960 Superfamily Euomphalacea de Konlnck, 1881 Family Euomphalldae de Konlnck, 1881 Genus Straoarollus Montfort, 1810 Subaenus Euomohalus Sowerby, 1814 Range: Silurian to middle Permian Occurrence: Sang Run Quarry, Deep Creek Quarry; Cosmopolitan Straoarollus fEuomohalusI Sowerby, 1814 Figure 75 Remarks - - Identification was based on descriptions and photographs from Thein and NItecki (1974). The shell Is discoldal to low-splred with a distinct angulation on the outer edge of the upper whorl surface. The base Is slightly flattened. Upper and basal angulations sometimes bear sharp keels. Euomohalus olanodorsatus Meek & Worthen Is known from Chester rocks 283 in Illinois and Missouri. Specimens collected from the Greenbrier are similar in appearance, bear keels and have the same general overall shape. Suborder Neritopsina Cox & Knight, I960 Superfamiiy Neritacea Rafinesque, 1815 Family Neritopsidea Gray, 1847 Subfamily Naticopsinae S. A. Miller, 1886 Genus Naticoosis M’Coy, 1846 Subaenus Naticoosis M’Coy, 1846 Range: middle Devonian to Triassic Occurrence: Deep Creek Quarry; cosmopolitan Naticoosis fNatlcopslsl M’Coy, 1846 Figure 75 Remarks - - identification was based on descriptions and photographs from Thein and NItecki (1974). The shells are moderately high to low spired and relatively broad. The shell of Naticoosis fNatlcooslsl is globular with a slightly protruding spire. The aperture is large and expanded in an oblique direction to the axis. Parietal and coiumeliar lips are moderately thickened and may be crossed by tooth-like markings. Many species undergo great ontogentic changes and it is often difficult to recognize two specimens as the same species if not part of a complex suite (Thein & NItecki, 1974). Kingdom Protista Phylum Sarcodina Schmarda, 1871 Order Foraminiferida Eichwaid, 1830 Class Rhizopodea von Sieboid, 1845 Family Endothyridae Brady, 1884 Range: Devonian - Permian 284 Occurrence: Sang Run Quarry, Deep Creek Quarry, Oakland Quarry, Roaring Creek, U.S. 33, Montervllle Quarry, Kenton-Meadows Quarry, Canaan Quarry, Butcher Quarry, Slaty Fork Quarry, R & R Quarry, Knobs-Unlon Road, Salt Sulphur Springs Quarry, Alderson, Acme Quarry: cosmopolitan Remarks - - Identification was based on descriptions from the Treatise and other published literature. Lower taxonomic designations were not attempted. These foramlnifera are robust and relatively thick walled. They are colled and have many chambers (Figure 74). Kingdom Plantae All algae was described from thin section and identified by comparison to descriptions and photographs In Wray (1977) and Horowitz & Potter (1971). Taxonomic classification Is uncertain (Wray, 1977) and no attempt was made to assign these to any higher (or lower) taxonomic level. Order Dasycladales Family Dasycladaceae Remarks: Single plates with the characteristic round and perforated shape were assigned to Dasycladaceans (Figure 76). Range: Cambrian to recent Occurrence: Roaring Creek, Slaty Fork Quarry, U.S. 64 Sphaerocodlum sp. Remarks: Sohaerocodium sp. was assigned to masses of encrusting laminae and spar filled ovals, which are the test Interiors of the foramlnifera Wetheredella. It encrusted all allochems. Higher power magnification was necessary to properly document its occurrence (Figure 78). Range: Ordovician to Triassic Occurrence: Salt Sulphur Springs Quarry, Acme Quarry 285 GItvanella sp. Remarks: GIrvanella sp. was assigned to all occurrences of tubular knobs and masses of algae (Figure 77). Range: Cambrian to Cretaceous Occurrence: Sang Run Quarry, Deep Creek Quarry, Butcher Quarry, Slaty Fork Quarry, Acme Quarry Calclspheres Remarks: The name calclspheres were assigned to 75 to 200 micron micrlte rings with well defined walls and smooth external surfaces. If highly micrltlzed, they might be confused with brachlopod spines. The small size and absence of any fibrous structure Indicates that they are calclspheres (Figure 80). Range: N /A Occurrence: Sang Run Quarry, Deep Creek Quarry, Oakland Quarry, Montervllle Quarry, Slaty Fork Quarry, R & R Quarry, Acme Quarry APPENDIX A Biostratinomic Utility of Archimedes in Environmental Interpretation 286 PLEASE NOTE Copyrighted materials in this document have not been filmed at the request of the author. They are available for consultation, however, in the author's university library. 287-293, This is also available in Palaios, 1990, Volume 5, pages 160-166 University Microfilms International APPENDIX B Archimedes bedding plane data 294 295 LENGTH 360 .SPECIMEN. (CM)_ QUAD.. nRORRRS DOUBLED. BEDDING PLANE 1 1 2.5 N40W 320 140 2 5.5 N85W 275 95 3 2 N20E 20 200 4 2 N35E 35 215 5 4 N5E 5 185 6 3 N50W 310 130 7 2 N15E 15 195 8 2 N20E 20 200 9 2.5 N35E 35 215 10 1.5 E 90 270 11 3 N60E 60 240 12 4 NlOW 350 170 13 1.5 N 360 180 14 2.5 N60W 300 120 15 3 N65E 65 245 16 3.5 N45E 45 225 17 3 N 360 180 18 7 N45W 325 145 19 5 N20W 340 160 20 2 N85E 85 265 21 5 N40E 40 220 22 2 N55E 55 235 23 1 N55E 55 235 24 1.5 N65E 65 245 25 1.5 N65E 65 245 26 3 E 90 270 27 5 N80E 80 260 28 3.5 N 360 180 29 3.5 N50E 50 230 30 1.5 N50E 50 230 31 1.5 N40E 40 220 32 4 N80E 80 260 33 2 N40W 320 140 34 2.5 N80E 80 260 35 3.5 N50E 50 230 36 8.5 N25W 335 155 37 10 N25E 25 205 38 3.5 N40E 40 220 39 4 N30E 30 210 40 5 N70E 70 250 41 3.5 N 360 180 42 4 N65E 65 245 43 2.5 N30E 30 210 44 2 N45E 45 225 45 2 N85E 85 265 46 3 N30E 30 210 47 3 E 90 270 48 3.5 N15W 345 165 49 3 N15W 345 165 50 4.5 N50W 310 130 51 4 N35E 35 215 52 6.5 N 360 180 53 5 N70E 70 250 54 2.5 N40E 40 220 55 8.5 NlOW 350 170 56 7 N45E 45 225 57 5 N75E 75 255 58 1 N65E 65 245 59 3 N65E 65 245 60 7.5 N35E 35 215 61 2.5 N 360 180 62 13 N35E 35 215 63 5 N65E 65 245 64 3 N 360 180 65 4 N 360 180 296 LENGTH 360 SPF.CTMF.NM c rM i OUAD nRGRF.ES n n tJR I.R D 66 2 N30E 30 210 67 7 NlOW 350 170 68 5 N55E 55 235 69 3.5 N 360 180 70 5 N80E 80 260 71 3 N40E 40 220 72 4 E 90 270 73 2.5 N50E 50 230 74 3.5 N75E 75 255 75 2.5 N70E 70 250 76 5.5 N85E 85 265 77 2.5 N 360 180 78 4 N55E 55 235 79 3.5 N40E 40 220 80 4 N80W 280 100 81 2 N60W 300 120 82 2 N30E 30 210 83 4 N30W 330 150 84 5.5 N35E 35 215 85 5.5 N55E 55 235 86 3.5 N5W 355 170 87 3 N50W 310 130 88 6.5 N15E 15 195 89 4 N35E 35 215 90 4 N45E 45 225 91 6.5 N 360 180 92 2 N15W 345 165 93 3 N15W 345 165 94 3 N 360 180 95 2.5 N30W 330 150 96 6 N65E 65 245 97 5 N15E 15 195 98 3 NlOE 10 190 99 2 N75W 295 115 100 1.5 N15W 345 165 102 8 N40E 40 220 103 4 N20E 20 200 104 4.5 N40E 40 220 105 3.5 N60W 300 120 106 5 N55W 305 125 107 2 N65W 295 115 108 7 N 360 180 109 6 N55E 55 235 110 3 N20W 340 160 111 3.5 N80E 80 260 112 6 NlOE 10 190 113 8 N85W 275 95 114 6.5 N 360 180 115 8.5 E 90 270 116 5 N80W 280 100 117 4 N20E 20 200 118 8.5 NlOE 10 190 119 3.5 N35E 35 215 120 6 N50W 310 130 121 3 N30E 30 210 122 13 N35E 35 215 123 6.5 N5W 355 175 124 6.5 N50E 50 230 125 2 NlOE 10 190 126 3 N40E 40 220 127 7 N35W 325 145 128 2 N15E 15 195 129 9 E 90 270 130 4.5 N30W 330 150 131 3 N65E 65 245 132 3.5 N70E 70 250 133 2.5 E 90 270 134 2 N40W 320 140 297 LENGTH 360 S P P riM F.N fC M l QIIAD DEGREESDOURI. 135 9 E 90 270 136 3.5 N70E 70 250 137 5.5 N20E 20 200 138 5 N35E 35 215 139 1.5 N85E 85 265 140 4.5 N50E 50 230 141 4.5 N20E 20 200 142 5.5 N30E 30 210 143 2 N40E 40 220 144 4.5 NlOE 10 190 145 2.5 N15W 345 165 146 3.5 N60E 60 240 147 4.5 N55W 305 125 148 3 N45E 45 225 149 7 N25E 25 205 150 3 N70W 290 110 151 7.5 N50E 50 230 152 4.5 N45E 45 225 153 3 N20E 20 200 154 6.5 N5E 5 185 155 10.5 N20E 20 200 156 3.5 N40E 40 220 157 4.5 N65W 295 115 158 2.5 N50E 50 230 159 9.5 W 270 90 160 10 N5W 355 175 161 2 N50E 50 230 162 4.5 N20W 340 160 163 2.5 NlOE 10 190 164 1.5 N30E 30 210 165 3.5 N80W 280 100 166 7 N70W 290 110 167 6 N75W 285 105 168 15.5 N5W 355 175 BEDDING PLANE 2 1 2.5 N45E 45 225 2 4 E 90 270 3 4.5 NlOE 10 190 4 2 W 270 90 5 10 N80W 280 100 6 7 N80E 80 260 7 1 NlOW 350 170 8 4 N20E 20 200 9 2.5 N70W 290 110 10 2.5 N30E 30 210 11 3 W 270 90 12 13 N65W 295 115 13 10 N80W 280 100 14 4 N15E 15 195 15 9 N60E 60 240 16 4 NlOE 10 190 17 4 N20E 20 200 18 5 N6E 6 186 19 2.5 E 90 270 20 3.5 N65W 295 115 21 5 N25E 25 205 22 2 N15W 345 165 23 5.5 N15W 345 165 24 3 N25E 25 205 25 5 N25E 25 205 26 7 N40E 40 220 298 LENGTH 360 SPP.riM PN rC M l QUAD DPURPPS n n u R i. 27 2.5 N85W 285 105 28 2.5 W 270 90 29 2 N40W 320 140 30 1 N55W 305 125 31 4.5 W 270 90 32 2 N45W 315 135 33 4.5 N50E 50 230 34 2 N65W 295 115 35 2.75 N30E 30 210 36 2.5 N45E 45 225 37 1.5 N35W 325 145 38 3 N35E 35 215 39 2 N20W 340 160 40 4.5 W 270 90 41 2 N 360 180 42 8 N50E 50 230 43 4.5 N50E 50 230 44 2 N50E 50 230 45 2 N70W 290 110 46 1.5 NlOW 350 170 47 4.5 N 360 180 48 2.5 N85E 85 265 49 10.5 N15W 345 165 50 1.5 N 360 180 51 3 N70W 290 110 52 4 N15E 15 195 53 4 N25W 335 155 54 2.5 N50W 310 130 55 4 N60W 300 120 56 4 NlOW 350 170 57 2.5 N75W 295 115 58 2 N60W 300 120 59 3 N35E 35 215 60 2.5 N70W 290 110 61 4 N25W 335 155 62 5.5 N25W 335 155 63 8 N30W 330 150 64 6 N15W 345 165 65 3 N15W 345 165 66 2 N5W 355 175 67 3.5 W 270 90 68 2 N60W 300 120 69 5 NlOE 10 190 APPENDIX C intraspecific Morphologic Variability in Soirifer pellaensis. Greenbrier Group (Upper Mississippian/Lower Carboniferous), USA 299 300 Brachiopoda through time, MacKirtnon, Lee i Camptaell (eds) C19S0 Balkema, Rotterdam. ISBN 9061911605 Intraspecific morphologic variability in Spirifer pellaensis, Greenbrier Group (Upper Mississippian/Lower Carboniferous), USA Julie LWulff The Ohio State University Columbus, Ohio, USA ABSTRACT: Spirifer pellaensis (Upper Mlsslsslpplan/Lower Carboniferous) has been described from numerous localities In the eastern and mldcontlnental United States. The great morphologic variability exhibited by S. pellaensis raises the question as to whether or not all described specimens are the same species. Differences In deposltlonal environment from the Appalachian Basin westward might have limited faunal distribution. 317 specimens which were previously assigned to S. pellaensis, from 9 localities, were studied. Based on their overall shape, each was assigned to one of four morphotypes. The external characters hinge length, maximum width, length and degree of elation were measured. The data were subjected to a Chi* squared test and Canonical Discriminant Function Analysis. Results Indicate that' the morphotypes are distinct but the overall character of each Is not unique enough to allow Identification as a separate species. Serial sections of each morphotype revealed Identical Internal structures, further supporting the results of the statistical analyses. 1 INTRODUCTION applied to other questions. Including paleoecology of the organism In question, Variation In external morphology among environmental Interpretations or Individuals belonging to the same species distributional patterns. Is common. Brachlopods, for example, may Spirifer pellaensis Is a highly express differences In hinge length, morphologically diverse Upper degree of alatlon, shell length and width MIsslsslpplan (Lower Carboniferous) of fold and sulcus. Explanations for brachlopod. It was first described by these variations Include adaptation for Weller (1914) from the Pella Beds (Late life on different substrata (Alexander Merameclan/Vlsean) of southeastern Iowa. 1975, 1987; Copper 1966b), although random It was described as a "shell below medium genotypic expression cannot be rejected. size, usually wider than long, The method by which a species Is occasslonally with length and breadth Identified can often be problematic. nearly equal, . . . cardinal extremetles Unless populations are studied, the range rounded, rectangular, or more or less of morphologic variability will not be attenuate, . . . (lateral slopes) marked known. If Identification Is then made by from 9*13 simple rounded plications . simply by comparison with published . . mesial sinus originating at or near photographs and written descriptions, the the beak, angular and sharply defined at results could be erroneous. Foster (1974, first, becoming rounded and less sharply 1989) stressed the importance of defined anteriorly . . . rather shallow or recognizing Intraspeclflc morphologic of moderate depth. Near the beak a median variation and Its relationship to plication originates In the sinus . . . geographic distribution. Fossil species becoming gradually stronger (anteriorly) . appear to have more limited distributions . . there may be a single plication (on than m o d e m species, Foster attributed each side) which Is usually, but not this to overspllttlng of morphologically always, weaker than the median one, . . . diverse species. mesial fold sharply defined to the beak, Well defined species concepts are at first scarcely, or not at all, . . . necessary before fossil data can be becoming gradually elevated anteriorly 49 301 last Paleozoic marine Invasions of the MBA continental Interior (DeWltt & McGrew :'CA 1979). In an Interval between two large-scale orogenlc events, MIsslsslpplan rocks of the Appalachian Basin were deposited EIB during relatively mild tectonic conditions which consisted of uplift to the east, northeast and northwest and subsidence In the south (Leonard 1968; Youse 1964). Moderate amounts of clastic material In the northern units (Loyalhanna limestone and silt beds In the Upper Greenbrier) Indicate a provenance to the east and Fig. 1 Map of midconclnencal United northwest (DeWltt & McGrew 1979; States showing extent of Chester Sea In Rlttenhouse 1949; Yelldlng 1984), and the early Chesterlan (Upper MIsslsslpplan; substantial thickening of sediments to the and occurences of Spirifer pellaensis south attest to subsidence there (Arkle (Indicated by filled circle). CA - 1979). Spirifer pellaensis has been Clnclnattl Arch, Afi - Appalachian Basin, described from the Greenbrier Limestone In EIB - Eastern Interior Basin, HRA - south-central Pennsylvania and western Mississippi River Arch. Maryland which Is dominated by grainstones and packstones. Upper Greenbrier units In central West Virginia, from which S. where It Is rounded and of moderate height pellaensis has been described, exhibit a . . . marked by a median furrow" (Weller distinct Increase In fine-grained 1914, p. 340). Clearly, Weller allowed carbonates and are dominated by for a great deal of morphologic wackestones. variability In Sorlfer pellaensis. Since Mild subsidence occurred over broad 1914, Sj. pellaensis has been described areas of the Eastern Interior Basin with from numerous North American localities In the greatest amount of subsidence In the the midcontinent and Appalachian Basin south. However, the consistent thickness (Butts 1917, 1940; Easton 1942; Clrty and lateral persistence of the Upper 1926; Weller 1920; Wulff 1989). Published MIsslsslpplan units Indicates that photographs and descriptions Indicate that overall, subsidence was relatively even Identifications were made simply by (Sable, 1979). The Michigan River Is comparison with the Illustrations and believed to have transported detrltal description In Weller's monograph and sediments Into the basin from source areas other subsequent papers. At the present In the Canadian Shield or the northern time the generic placement of this Appalachian Mountains (Sable 1979). brachlopod Is In question, with several Large-scale fluctuations In the shoreline workers assigning It to the genus resulted In deposition of highly variable Anthracosplrlfer (T. Dutro, pers. comm). sediment packages, and units are This study con»lsts of two objectives. characterized by limestone, sandstones and The first Is to understand the shales. The northern part of the morphological complexities of Spirifer Cincinnati Arch was slightly uplifted as a pellaensis. This Is accomplished through generally emergent shoal area during this quantitative analysis of the external time. Although It contributed little characteristics and examination of sediment to the system, the Cincinnati Internal structures of numerous Arch served as a barrier between the brachlopods assigned to S. pellaensis. Eastern Interior Basin and the Appalachian The second objective Is to identify the Basin. different morphotypes and the llthologles Much of Iowa and Missouri were a stable they are associated with. submerged shelf during this time (Carlson 1979). The Genevlevlan Sea was the last sea to Inundate parts of Iowa during the 2 GEOLOGIC SETTING MIsslsslpplan (Johnson & Vondra 1969), and It transgressed northward creating Late Merameclan and early Chesterlan numerous localized, shoal-separated, sediments were deposited In a large seaway basins. During deposition, environmental that was divided Into two extensions conditions varied continuously, and the northward around the Cincinnati Arch resulting Pella Formation llthologles (Figure 11. These rocks record one of the exhibit great lateral variations. S. 50 302 qualitative subdivision Into 4 morphotypes based on overall characteristics. These are alate, notched, round and intermediate. The Initial assumption was that each morphotype represented a separate species. Alate morphotypes have long hlngellnes relative to the rest of the shell, giving these brachlopods a winged appearance (Figure 2.1). Notched morphotypes exhibit an Indentation of the lateral margin Just prior to development of the hlngellne (Figure 2.2). The notch may be shallow or Fig. 2 Representative examples of the deep. The hlngellne of round morphotypes four morphotypes. 2.1 - alate (x 0.75), Is shorter than the maximum width and the 2.2 - notched (x 0.7), 2.3 - round (x shell Is somewhat longer than the other 1.1), 2.4 - Intermediate (x 1.1). morphotypes (Figure 2.3). Intermediate morphotypes have nearly straight lateral margins, giving this morphotype a square pellaensis is known from that portion of or Intermediate appearance (Figure 2.4). the Pella Formation which Is dominated by These morphotypes do not represent calcareous mudstones. The basin In which ontogenetic change, because each the Pella Formation was deposited was morphotype Is present across the entire separated from the subsiding Eastern size range available. Interior Basin by the Mississippi River A variety of morphometrlc techniques Arch and the,Lincoln Fold (Johnson & were utilized to determine whether or not Vondra 1969). However, the similarity these morphotypes represent separate between the Pella Formation lithologie species. Hinge length, maximum width, characteristics and the transgresslve* length, degree of alatlon, height, height regressive cycles In the Eastern Interior of Interarea, number of lateral costae and Basin suggest that these two areas were, number of fold and sulcus costae ate all at times, connected across the Mississippi characteristics which vary Inter- and River Arch (Johnson & Vondra 1969). This Intraspeclflcally among splrlferld connection would have coincided with the brachlopods. A Chl-squared statistic was overall connection between the Eastern approximated using the Kruskal-Wallls test Interior Basin and the Appalachian Basin (SAS 1985) and the significance of each during the late Merameclan and early variable was calculated for each Chesterlan and would explain the morphotype. The data sec was further widespread faunal distribution from Iowa subjected to Canonical Discriminant to the Appalachian Basin. Analysis (SAS 1985). First, Stepwise Environmental conditions thus ranged Discriminant Analysis determined that all from a shelf lagoon In northern West five variables entered were significant to Virginia and Maryland (Wulff In prep.), to the 85% confidence level for morphologic well circulated, open marine settings In differentiation. These variables were southern West Virginia (Carney & Smosna then used In Canonical Discriminant 1989; Wulff In prep.) and Iowa (McKay et Analysis In order to graphically plot the al 1987). relationships between the morphotypes. Faunal constituents consist of abundant Internal structures of both the pedicle brachlopods followed by bryozoans (of and brachial valves are utilized In which Archimedes Is locally Important), brachlopod species designations. Because echlnoderm columnals and blastolds. much of modern brachlopod taxonomy Is Scattered corals, trllobltes and based on this, serial sections were made gastropods are least abundant. of each morphotype. 3 METHODS 4 RESULTS The specimens utilized In this study are Because many of the specimens were from nine localities (Appendix 1.), 3 were somewhat compressed, neither the height collected during this Investigation and 6 nor the Interarea width could be used with are from museum holdings. External any confidence. The number of costae morphologic diversity exhibited by all varies from 6 • 11 on the flanks and from specimens considered allowed for a 2 - 6 and 1 - 5 on the fold and sulcus, 51 303 üUiMVM wiont HINCIUMCTN mI AUTKM . HINCI/*imM AT WMÆNCTW Fig. 4 External characters used In multivariate analyses. ' JL _Ê_ _î!_ " •™«.Q É1 S E] IS D HIM» Flg. 3 Frequency distribution of costae (rib) number per morphotype. respectively. As expected, Juvenile brachlopods have fewer costae overall. For both the flanks and the fold and sulcus, there Is no relationship between morphotype and number of costae. This Is Illustrated for the lateral costae In Figure 3. Thus, the only external variables that can be used to characterize Fig. 5 Plot of hinge by length, each the morphotypes with any certainty are field delineates distribution of one hinge length, maximum width, length (umbo morphotype. Solid line - round, dashed to anterior margin) and alatlon line - Intermediate, diamonds - notched, (hlnge/wldth at mid-length) (Figure 4). asterisks - alate. These variables, when considered together, simply describe the size and shape of Individuals. function of hinge length, maximum width 4.1 Morphometries and degree of alatlon (Table 2). The second canonical variable explains 16% of A blvarlate plot of hinge by length the variance between morphotypes and Is appears to Indicate that the morphotypes correlated to length, maximum width and are related by allometrlc growth (Figure degree of alatlon (Table 2). The plot of S). These morphotypes do not represent canonical variable 2 by canonical variable this type of ontogenetic change, however, 1 Is shown In Figure 6. because as stated above, each morphotype Is present across the entire size range available. Table 1. Chl-squared approximation 4 The approximated chl-squared statistic degrees of freedom, all values significant Is significant to the 0.0001 level or to 0.0001 or 99.9% level. 99.9% level (Table 1). This Is Interpreted to mean that each morphotype, as defined by the four measured variables, HINGE - 144.86 Is truly distinct. Thus the brachlopod MAXIMUM WIDTH X* - 125.75 population does consist of four separate LENGTH X* - 28.14 morphotypes. HINGE/LENGTH X* - 183.45 Canonical Discriminant Analysis Is MAXWIDTH/ Interpreted differently. The first LENGTH X* - 157.98 canonical variable explains 79% of the ALATION X* - 145.55 variance between morphotypes and Is a 52 304 rmouiNCT It •m I I : IJ t IM Fig. 6 Plot of canonical variable 2 by canonical variable 1, each field Fig. 7 Frequency distribution of delineates distribution of one morphotype. hlnge/length ratio per morphotype. Dark Symbols as In figure S. stippling - round, light stippling - notched, dashed lines - Intermediate, solid lines - alate. Table 2. Total Canonical Structure CAN 1 (79%) CAN2 (16%) along the first lateral costa of the HINGE 0.83 •0.45 pedicle valve. The overall form of the MAXWIDTH 0.76 -0.50 structure In the round morphotype Is LENGTH 0.35 -0.52 unusual, but this may be attributed to WIDTH 0.59 -0.13 extensive recrystalllzatlon or difference ALATION 0.75 -0.51 In growth form. The Important point, however, is that it too, follows along the first lateral costa. The cardinal process (Figure 9) Is a Note that although the morphotype fibrous structure at the posterior of the distributions can be delineated, there Is brachial valve and serves as attachment far too much overlap to suggest that these sites for the dlductor muscles. The morphotypes represent more than one cardinal process for all four morphotypes species. A histogram of the Is U-shaped. hlnge/length ratio approximates a bell The bases of the splrallum are T- or Y- curve and further supports the existence shaped calcareous structures (Figure 10) of one species (Figure 7}. Given that which extend anteriorly and down toward this ratio describes the overall shape of the floor of the brachial valve. In each the Individual, the bell-shaped curve of the four morphotypes, these structures indicates that the population studied has curve gently toward the center and are a normal distribution with respect to the short to moderate In length. possible variations allowed by the The similarity of these structures among hinge/length ratio. With the exception of each morphotype further suggests that all the round morphotypes, each individual morphotypes are members of the same morphotype approximates a normal species, Spirifer pellaensis. distribution as well. Thus based on the results of these morphometrlc tests, the population studied Is considered to be a 5 DISCUSSION single species, Spirifer pellaensis. The apparent discrepancy between the 4.2 Serial Sections results of the Chi-Squared analysis and the Canonical Discriminant Function Serial sections of each morphotype were analyses can be explained by considering ground at 1mm, 2mm and 4mm intervals. the overall variation of each morphotype Figures 8-10 show comparisons of three as defined by the characters measured. Internal structures which are the same for Since each morphotype Is defined by the each morphotype. hinge length, maximum width, length and The dental lamellae (Figure 8) are short alatlon, each Is significant because the and rather stout structures. The most variables only differ within a certain Important feature Is that they all follow range In each morphotype. For example, 53 305 hinge length varies between 11.3 mm and 32.0 mm £or round morphotypes and no other morphotype has hinge length values that £lt that range. However, the morphotypes are de£lned by the overall combination of the variables measured. This was facilitated by calculating the variances of hinge length, maximum width, length and alatlon to create new variables (Canonical AUTV f 2mm Variables 1 and 2). These new variables have been shown to overlap (Figure 6), thus Indicating that the morphotypes, although distinct, do not represent Individual species but morphologic variations of the same species. This paper has shown the wide Intraspeclflc variations In external morphology In Spirifer pellaensis. Careful consideration of distinct features tNTUMuiun: on a sufficiently large population Is necessary to create a composite Fig. 8 Camera lueIda drawing showing characterization of a species. However, position of dental lamellae. familiarity obtained by working with populations may allow Identification of most Individuals without serial sectioning, with the exception of problematic specimens and periodic spot checking. Other Upper MIsslsslpplan brachlopods show similar morphologic variability (le; Spirifer Increbescens), a and It Is possible that this technique may be applied to them as well. An equally powerful use of external features Is In paleoecology where morphologic characteristics can be used to Infer the mode of life of the Individual and Its relationship to the substratum. The occurrence of Spirifer pellaensis In the Appalachian Basin, the Eastern Interior Basin, Iowa and Arkansas Indicates that It was a very widespread Fig. 9 Camera lueIda drawing showing species capable of living in a variety of poslclon o£ cardinal process. environments and under a variety of conditions. Morphotype distribution, however. Is not consistent at all localities and attention should turn to Interpretation of morphotype distributional patterns and the possible causes of these patterns. NvrniKu j j m 6 CONCLUSIONS 1. The 317 Individual brachlopods analyzed In this study all belong to the species Spirifer pellaensis. 2. Multivariate statistical techniques show that although there Is wide variation In external morphology, the morphologic overlap Is too great to warrant creation of separate species. Fig. 10 Camera lueIda drawing showing 3. Internal characteristics of base o£ the splrallum. sectioned morphotypes provide additional 54 306 supporc for the results obtained by study Carney, C. and R. Smosna. 1989. of external characters. Carbonate deposition in a shallow marine 4. Spirifer pellaensis was a very gulf, the Mississippian Greenbrier widespread brachiopod adapted for life in Limestone of the Central Appalachian a variety of environmental conditions. Basin. Southeastern Geology, 30:25-48. Copper, P. 1966b. Ecological distribution ACKNOWLEDGEMENTS of Devonian atrypid brachiopods. Palaeogeography, Palaeoclimatology, I thank Dr. W. I. Ausich for helpful Falaeoecology, 2:245-266. discussions and critiques of this work. S. U. Riddle also participated in DeWitt, W. and L. W. McGrew. 1979. discussions. A. S. Horowitz provided Appalachian Basin Region, p. 13-48. IN locality information. Specimens were Craig, L. C. and C. W. Connor (Coord.) generously loaned by J. Golden, Dept, of Paleotectonic Investigations of the Geology, Univeristy of Iowa; K. Forster, Mississippian System in the United Field Museum of Natural History and A. States. Part I. Introduction and Kollar, Carnegie Museum. H. Sandy Regional Analyses of the Mississippian assisted with serial section preparation. System. USGS Prof. Paper 1010. B . Daye helped with the photography. Funding for this project was provided, in Easton, W. H. 1942. Pitkin limestone of part, by the Appalachian Basin Industrial northern Arkansas. Arkansas Geologic Associates, Friends of Orton Hall and The Survey Bull. 8. Department of Geology & Mineralogy at The Ohio State University. Foster, M. W. 1974. Recent Antarctic and subantarctic brachiopods. Antarctic Research Series, 121, American REFERENCES Geophysical Union. Washington, D.C. Alexander, R. R. 1975. Phenotypic Foster, H. W. 1989. Brachiopods from the lability of the brachiopod Rafinesquina extreme South Pacific and adjacent alternata (Ordovician) and its waters. Journal of Paleontology, 63:268- correlation with the sedimentologic 301. regime. Journal of Paleontology, 49:607-618. Girty, G. 1926. Faunas of the Mississippian and Pennsylvanian periods, Alexander, R. R. 1987. Intraspecific pp. 847-860. IN Reger, D. 1926. Mercer, selective survival within variably Monroe and Summers Counties. West uniplicate lace Devonian brachiopods. Virginia County Report. Lethaia, 20:315-325. Johnson, G. D. & C. F. Vondra. 1969. Arkle, T. Jr. et al. 1979. West Virginia Lithofacles of Pella Formation and Maryland, pp. D1-D35. IN The (Mississippian), southeastern Iowa. Mississippian and Pennsylvanian AAPG Bull., 53:1894-1908. (Carboniferous) Systems in the United States, uses Prof. Paper 1110-A-L. Leonard, A. D. 1968. The petrology and stratigraphy of Upper Mississippian Butts, C. 1917. Mississippian formations Greenbrier Limestones of eastern West of western Kentucky. Kentucky Geologic Virginia. Unpubl. PhD Dissertation. West Survey. Virginia University, Morgantown. Butts, C. 1940. Geology of the Rlttenhouse, G. 1949. Petrology and Appalachian Valley in Virginia. Parts 1 paleogeography of Greenbrier Formation. & 2. Virginia Geologic Survey, Bull. AAPG Bull. 33:1704-1730. 52. Sable, E. G. 1979. Eastern Interior Basin Carlson, M. P. 1979. Nebraska-Iowa Region. p. 59-106 IN Craig, L. C. and Region, p. 107-114. IN Craig, L. C. and C. W. Connor (coordinators). C. W. Connor (coordinators). Paleotectonic Investigations of the Paleotectonic Investigations of the Mississippian System in the United Mississippian System in the United States. Part I. Introduction and States. Part I. Introduction and Regional Analyses of the Mississippian Regional Analyses of the Mississippian System. USGS Prof. Paper 1010. System. USGS Prof. Paper 1010. 55 307 SAS User's Guide. 1985. SCaClsClcs. SAS Roadside Quarry, Greenbrier County, Inscltute; Cary, North Carolina. WV, .4 miles north of Modoc Road on the west side of West Virginia Route Weller, S. 1914. The MIsslsslpplan 219, Droop, W.VA 7.5" quadrangle, brachiopoda of Che Upper Mississippi Alderson Formation, Greenbrier . Valley region. Illinois State Geologic Group, Chesterlan Survey, Monograph 1. Plates and Text. Thompson Quarry, Fayette County, Pennsylvania, National Road (US 40), Weller, S, 1920. The geology of Hardin Wyops Gap Formation, Chesterlan * County. Illinois State Geologic Survey, Bull. 41. limited locality Information obtained from specimen labels In McKay, R. M. et al. 1987. Early museum collections tetrapods, stratigraphy and paleoenvlronments of the Upper St. Louis Formation, western Keokuk County, Iowa. Geological Society of Iowa, Guidebook 46. Wulff, J. I. 1989. Ecophenotyplc variability of Spirifer pellaensis. Abstr. Geological Society of America Annual Meeting, Abstracts with Program. St. Louis. 1989. Yelldlng, C. A. 1984. Stratigraphy and sedimentary tectonics of the Upper MIsslsslpplan Greenbrier Group In eastern West Virginia, Unpubl, MS Thesis. Univ. of North Carollna-Chapel Hill. Youse, A. C. 1964. Gas producing zones of Greenbrier (MIsslsslpplan) limestone, southern West Virginia and eastern Kentucky. AAPG Bull. 48:465-486. Appendix 1 Localities 1 Taylor Quarry, Keokuk County, Iowa. NW, SW, sec. 13, T74N, R13W, Pella Formation, Merameclan 2 Fort Dodge, Iowa; Pella Beds, "Merameclan" * 3 Pella, Iowa; Pella Beds, "Merameclan" * 4 Snyder's Quarry, National Road (US 40), Fayette County, Pennsylvania, Maxvllle Limestone, * 5 Illinois Central Railroad Cut, north of Ft. Dodge, Iowa; Pella Beds, "Merameclan" * 6 Sang Run Quarry, Garrett County, HD, 39*34'0" N, 79'25'6" W, Sang Run, MD-W.VA 7.5" quadrangle, Greenbrier Formation, Chesterlan 7 Oakland Quarry, Garrett County, HD, 39*22'75" N, 79'27'31" W, Oakland, MD-W.VA 7.5" quadrangle, Greenbrier Formation, Chesterlan 56 APPENDIX D Locality Register 308 309 LOCALITY REGISTER Sang Run Quarry: Approximately .5 miles west of Sang Run, Maryland; along the Youghlogheny River. Sang Run, Md - WV 7.5 minute quadrangle. Deep Creek Quarry: Approximately .2 miles north of Thayervllle, MD on U.S. Route 219. McHenry, MD 7.5 minute quadrangle. Oakland Quarry: Approximately 4.1 miles south of the center of Oakland, MD. Cross Youghlogheny River and travel south on side road toward Cherry Bottom Run. Oakland, MD - WV 7.5 minute quadrangle. Canaan Quarry: 10 miles south of Davis, WV on Route 32, quarry on west side of road. Blackwater Falls 7.5 minute quadrangle. Roaring Creek: Exposures along Roaring Creek, approximately 1 mile north of Onego, WV. Onego, WV 7.5 minute quadrangle. Butcher Quarry: Near Bowden, WV on old U.S. 33, 1.4 miles west of the Bowden Fish Hatchery. Bowden 7.5 minute quadrangle. U.S. Route 33: Large road cut on new highway, approximately 6 miles east of Elkins, WV. Large mines In Union Limestone distinctive. Bowden 7.5 minute quadrangle. Montervllle Quarry: Approximately 4 miles west of the Intersection of U.S. Route 219 and Route 15, about .5 miles north of Valley Head, WV. Valley Head 7.5 minute quadrangle. Kenton-Meadows Quarry: Approximately 3.6 miles west of the Intersection of U.S. Route 219 and Route 15, about .5 miles north of Valley Head, WV. Valley Head 7.5 minute quadrangle. Slaty Fork Quarry: 1 mile south of Snowshoe road on U.S. Route 219. Mingo 7.5 minute quadrangle. R & R Quarry: 1.3 miles west of U.S. Route 219 on Savannah School Road. 2.9 miles south of Frankford, WV. Williamsburg, WV 7.5 minute quadrangle. Renick Vaiiey: Approximately .4 miles north of Modoc Road on U.S. Route 219. "Quarry" on east side of road, spoil piles on west side. Droop, WV 7.5 minute quadrangle. Swago Creek: Approximately 1.5 miles northwest of Buckeye, WV on Spruce Flat Road. Hillsdale 7.5 minute quadrangle. U.S. Route 64: 1 mile west of Lewlsburg, WV exit on U.S. 64, south side of highway. Lewlsburg, WV 7.5 minute quadrangle. 310 Acme Quarry: 1.6 miles west of Ft. Spring, WV. Ft. Spring 7.5 minute quadrangle. Alderson: Northeast corner of the intersection of Route 3 and Big Branch Road. 1.7 miles west of Alderson, WV and .3 miles west of the Greenbrler- Summers County line. Alderson 7.5 minute quadrangle. Knobs-Unlon Road: 2.8 miles west of Union, WV on Knobs-Unlon Road. Union, WV 7.5 minute quadrangle. Salt Sulphur Springs Quarry: 1.3 miles northeast of the church in Salt Sulphur Springs on U.S. Route 219. Quarry on south side of road, patch reef on north side of road. Union, WV 7.5 minute quadrangle. Greenville: Approximately .6 miles south of Back Creek Road on Route 122, just south of Greenville, WV; .05 miles north of bridge over Indian Creek to the Greenville Shale - Alderson Formation contact. APPENDIX E Pétrographie Descriptions 311 MICROSCOPIC NON-SKELETAL UNIT ROaCTYFB UmOLOGIC FEAITJRES MACROPAUNA ON OUTXROPFAUNAL COMPONENTS CARBONATE GRAINS NON-CARBONATE WAINS MATRIX/CEMENT DUGSNESB/COMMENTS SANG RUN QUARRY SR-1 [AxeaacBoos F o n ilif- Thtn Itwnjy Btadiiopodi, fiaatntB bcyo- Brachtopod dieUs & spixKS, Nooe Qoaxtz • m d nzed, aogtilat^ M icrita • bioCnrfaaled, alamd- Mkzoipar finnatioD erous] Mmklooc «eatberÎDg, chmlky; F « med. zoazs^nre - tw w nfm aabangolar, aboodast; tA ; m ia o ^M t & poaaifalc dark grey, ihaip cootaa to to rate; ifaeO a live rf, caïd- Irrite ‘ cufaedtil ndividaal paeodoapar Qnaitz tasd derived fiom re- SR-2, — coveted to flo o r çfacxes, feoeit r Hea, fc n m i- grama & doaten; ZIrccD • wcrioed Loyalhanxa bdow o f q a sry ixi& ia, oatncoda - conxmon; ThkkseM « 1.7m gastxopodi, algae - rate; sand SR-2 FaaaSi&roea Thkk bedding. rmcvca"oodnIar R odactid biachiopoda - abend- Mmatoioan debris, hradzîopod Fcloida - coarse sût to aand Quartz-sût, coouoon to M icrite - dense, fine, abosd- Micro^iar focmatioi^ m ktiti- WadBatoDB fur&oe*: W m itrd h n n grey, aat, gastropods, odier fancb- rirella & tp m , Girvanella. abondant; Ir r ite • eahedral micto^MT - cooxnco to zatioD o f grains F s merfiom dadc grey; tfaxa iopods caldspberes > cemrrwn; oatra- mdividaal grains & dosters, abaly paitmga, aharp coittacts coda, fo ra m m ifin a -ta ieto sût, abondant; 2 rc o n * rare Algae > than other biodasts; IMdneaa B 2.9 m comraou ;f meatrafl:a -ia ie ; MoMa>#lldae aand sized, roaoded^nibangdar SR-3 Fcramzni&ra Massive, puckered surfaces, Brachiopods BidotlqrîdfûrarrsnifeTi • M oids - commco Quartz • sand to a3t, rare to M icrite - fine, denae; M icro- Microçar fixmstion, lecry- WadkcstODB W m medbunligb grey abundant; pelxnatozoan debris, common; bemathe & pyrite qrar - scattered > mtcrite; wf pfJTWtnBMW, sharp contacts shell fraynenta, bcyoBotns - sût, eubedral grama - etwwwun ahundsm tb ris , mkritizatwn of bio Thkkneaa s 3.95 m canmm to abundant clasts SR-4 Fosailiferoos M aasht bed, a ll h ighly vea Braduopods, abundart » Eedothyridi - abundara; faracb* btradasts • blodastic, rare; Quartz • sût, Micrite - coarse w/aburaknt Grain trtkritizattan there^WodgreeaAering Orthotetea, Arabraco^iri&r, iopod shells 6 ^ h s s - abund M o ld s -ra re , sand sized Pyrite-sût, rare quartz; Caldte cement-sim Thidoeaa = 1.9 m Cdoaposita ant to common; pelxnatozoan ple mtergrartnlcr, fme-medium debris - common; Bivalves, crystals frfv-tfratf» Otrvmn. e lla, trSobites - rare; caldspberes?; sand sized, rounded to subangular SR-5 Bryozoan Medinrrt-ttun bedding, shell Btadiiopoda, ramose btyozoazB, Btyozoans (non-feneatrate), M o ld s - abundant, fine sand Quartz-aflt,rare;Irrite - Caldte-sparw/sbundantsyo- Recrystilizationofcexmit Gramstooe pavemem on bedding {dsne, Archmrdes - in large blocks, rhell slivers, pelxnatozoan rare taxial rims, heavily lecryttal- th in beds B shell pavement, rame collected debris - abundant; btadiiopod ized, fine to coarse yarned B ig environmental drange- medium beds B bioclaatic bash çînes • comrraai; fbraminifera, kaa stressed, increased buna Thidaaeaa b 2.75 m trUobites - rare; gravd to sand sizc4 subangular DEEP CREEK QUARRY DC-0 Bbturbated T h iid y bedded; F B dark browQ^ Bivalves-described in band None Gsldte grams - sût, Quartz, Irrite - sût, rare to Micrite-dense, massive Wavyextinctioo Mudstme black, W B g r^ lower contact specimen & outcrop molds, un concealed identifiaMc; sliyred grains A Base o f itttddle member, very Hudmeas B 1 ^ m l i ^ patches in is . may bo different from tm its above borrows DC-1 Ostrauxl/Calci- T b inly bedded, nodular weath Perg ftrate bryoxoans, product- Oitracod valres (disarticala- None Irrite? pellets - dusters, hflcrise - dense, bkmbamd, I^iriti 2edpdkts.iecrystal- ^te re Mudstone ering, riu k partings: F « id Sl sp irife rid brachiopods, ted), calcispherei - abundant; scaoered A v o id fillin g very fine UaedriieUa medium dark grey, W w lid # gastrtÿsds-all very rare Poctminifesa - next abundant; g rey;b ioBubated Bivalve fiagments,bradiiopod Big dange in conqrori- CO 1—* ro MICROSCOPIC NON-SKELETAL U N IT ROCaCTYPE UTHOLOGIC FEATURES MACROPAUNA ON OUTCROPFAUNAL COMPONENTS CARBONATE GRAINS NON-CARBONATE GRAINS MATRDOCEMENT DIAŒNESIS/OOMMENrS Thidcneai K m «ptpor, tiflo b itB S • n re ; tie n r ït sized, im ibnded DC-2 Fartsmifen ThW dy bedded; W m dsxk giey; Braduopodi - mcieased diver- Endodxyrids - G ilc i- N cdb Galdte ^>ar - fine to xnediom f^rittzed pellets dkrisBs Giamsttne nodalsrsTctiheriag, co tisent stQr Cram DC-1 iphercs-next abundant; aystals, void fxHinc, syn- iç w trd ; b io d ts tic debris at brschiopod spines, osiiacods, taxial rim s, blocky mosaic Base oCt^per member surface bivsl%s, ednnodeims, pstro- ThidoQBS « 1.65 m pods & tiilo b ite fragments • m e to ccmmoo; Sphaerocodmm- m e ; sand sized, abondant, TOQodcd except focana arhkh have indiftxnct boondaries DC-3 TriloUte/Foram- T hin - medium bedding, beds Brachsopods-6 genera; gastrrx Forammifera, calcispbeies - Mmds - blob like, tiandu- I^te-scattered throughout M ia o y a r - fin e ly csyataUme, Micro^xar fam atian, baodast in ife ia Gramstooe recede npaection; P « brownids pods - rare, trio ln te s - rare abundant; bracbiopod spines, cent, dustered w/Tcrams occurs around pellets f t smaller leoystallizatkQ , dolomite grey to common; pelnalozoan debris b iv a l'^ , btyozoans, Wodasts, fo is tests too; rhombs scattered Thickness = 1 m abundant along haafay layers spines - rare to common; trilo - Blocky spar - void fillin g , bile fragments ôczeaae in mosaic, medium oystals M o id i not as uniform as in abundance fiom DC-2; sand DC-1; biota basically ds sized, abundant & rounded, same but fewer fbrams dreUs f t forams not abraded DC-4 TriloWtc/Fbram- T h in to medium bedded, 2 m inar Brachiopods, crinotds, fene- Trilotnte fragments dominate; M o id s None M icrite - massive, surrounds Syntaxial overgrowths, ly ri- ittife ra PkdkstOQB shale partings, bedding thidc- strate bryozoam weather out foramznifera in abund biodasts; Calote spar- tized peltets, mkritzzed bio ens npaection; F B brown/grey a t surface; 8 bradiiopod ance; bcachiopod v a lic s f t void filin g , Pne to dasts Thickness 8 .7 m speices, 2 gastropod getcra, ^ h r s , frn r Urate btyozoans, crystals 1 trSobite species pelmatoEoan ddxris, trepostome bryozoan-rare to common; giavd to sand sized, abundant, most are unabiaded DC-5 Fmammifrra Masshn f t highly weathered, None AbimdazA biodasts; foraixuni- Abundant unidentxfiaUe grains None KEcrite - d o t^ in place w / RecrystaUizationofall dtdl Wackestooe higM y H oturbated feta increase, deoease m coarser biodastic debris; Thidmcss 8 not measured trBobhes; bracfabpod spines, red (hematite) cement? pcimatozoan debris, trSoUte Color dtangc and con^position fragments, gastropods (rare); indicates begim ing o f change sand sized, abondai! f t to Maucb Cfautdc deposition; unahraded only base o fu n it sampled, top inaccessible O AKLAND QUARRY OQ-1 Fossüî&rous Thick bedded, dxippyweatfaeriag TrüoWte - rare; bryozoans, Foaminifeta-abundant; M le ts • sût sized; ^mte/hematite?, polyoystal- M icrite, possibly mScnapar in Grain overgrowth, pyritized WadcBstODB Thidmeas m 135 m pdmatozoaa debris, bracfak^ bcachiopod spines, bivalves, higUy altered unidentifiable lin e quartz scattered places pellets, reaysbdlization of pods-rare bryozoans, pehnatozoan debris- carbonate grains didls,inkro^ar fonnatioa rare to common, rounded to abraded OQ-2 Shaly liœ s to tB H i^ y weatfaeaed on outcrop, ftoftictid ft s|nrifcrid bracb- (No âên section] frerhrodttcarlyinaocesaiblB iopods, pelmrrtoroan debris. CO I—» CO MICROSCOPIC NON-SKELETAL UNIT ROOCTYPB UniOLOGICFEATURES MACROPAUNA ON OUTCROPFAUNAL COMPONENTS CARBONATE GRAINS NON-CARBONATE (RAINS MATRO^CEMENT DIAŒNBSIS/OOMMENTS Th*dmem = Z^m fisiesttiSB & other faiyoKom*- n re to coDxzDon^ txHobilB-nre OQ-3 Fonzmni£am Thick bedded, b io d iftic None Farazmmfcra, fcoeitnlB biyo- None M le ti > black, pyxitired?. Mkna^iar * manive, biotor- Biodast zeoyatallixatico, PukstODD debfis at tuzfiuB, btoCar^ zoazza, trflcMtea & pehzxalo- acatfcred kmtpH; iotragraiBzlarcaldfiB* znksoflpir fonziatioa bated;, P sdaik grey zoan debni « cozzbdcd; aazxd- YoidnUios Thidmeai s 13 m râ ed , roondcd to vabazzfolaz; b c re a * in forazn S vm iQ f db g rrep t farammifera, many aboodiacB are b r e k n t abraded OQ-4 Paes3i&toas PackatoDB bcda **2czn thick, BradiiDpoda*6ipBcief,zttany Ncn-fimestnte biycBoam, Abondmza, broken, abraded & Biodast RoyitiUizatioo Gzazzxitone (Lag) afaalc intnfaed i are o n fo n flt- jovenflea, nre ngoae corala* pelxnatozoan debris, bradiio- jumbled tmidentifiable grains fizrty cxystillizB, common, fcrooB nzzroae bzyazoani, largo pelma- podapizB s;gnvdtoaaad ireejgiazmlar CUing & syn* No forazzunifin Thickseais 1.2m tnymfp cdozxmals, A fdzinrdea sized taxialrim s CX}*5 Porammifeni Medlitza to thidc bedded, crxn- None Porammilexa dombale, bracb- Abundant unideatiitable gnins Quartz - sût C kldie cem ent-void fUlizxg, M ioritization o f a ll grains Pack itozxe oid dcbrb on weathered n r& c e iopod apnea, rare pcimatozoan & fragments; haradasts • fznely oystaUizB; zniczite - Thtckness35m cdomnals, bryozoans - common; znicrite w/distznct borders. suirouzids grains & badcground Similar Uthology to 0 Q 4 Band sized, abundant overall, rounded OQ-6 FoasQi&rotts Thizdy bedded, essentially a Abundant Sc diverse, poorly Packatoxc shell pavement, zotezbeds prcserwd brKhiopods • 4 gen- (No thin section) above & bdow are dx^>py, olive era; bryozoans « fenestrate dk grey, unfosiflifierous diale lazttcae; trio b ite - rare, Tlûdmesa = .75 m pelznatoBoan debris OQ-7 FossOifisous Thidc bedded, dinçled weather- Br^xiopods * abundant, 8 Dominated by fcrsnxinifera but hxtradifts - abundant Qxeit-sQt sized, rare Micrite-dotty fax places, Qottedfcxtnre, bioclast WadcBstooe ing species; trEoWtes, bivalves, lower in ■twtKiTiee than (X)-5 tzxicrospi f scaoeied; coixxzzxoo, leczystallizaticn Thidmeas = 1.4 m pelzzxatozoan debris, bryoeoazxs, Pcimatozoan debris, edxinoid biotu: bated Archimedes larger here ^ tz e s , bryozoan firagments - Most diverse fauna fax die corxxzxxoxx, sand sized section ROARING CREEK RC-1 FaasOi&rous IiSra- T h id t to massive, w ell cenrrxt- S hdl slivers rV1rTw!r>Tr»n A-km# - ■bmvbnt- D uradasts-irregular ahiçes Ir r ite - spheres db sznall Galdre ^lar, mosaic crystals, Mlorim coatings on biodasts dastGrafaxstooe cd Foramfaxlfera, gastropods - itticrite w/quaxtz, biodasts db dazxq*, sût sized, coznmoo, massive db synta»al rfans, fine Thidm eas» 3 3 m rare; algae, shell slivers, slgae • abuzxdaixt; few coids db w ell rounded to medium crystals: m icrite- H ÿ i energy envfaonngpt trildiitea, bivalves - rare; ecloids "rm rv i A hpfwrr n «nnrhr^TM gravel to sand sized; rounded tosubanpxlar R C 2 faxtradast (Peloidal) T h ick bedded, w ell cemented, Very sparse pcimatozoan debris Pdmstozoan debris, shell hitradasts• loopygzapestoDB Quartz-scatteredthroughout, Csldre yafa*,~10micre:x, Mkzitizatiao o f biodasts Grafaxstone cxditic? slivers, dasydad algae (rare) tocdmg, micritB, soiXB w/algal angular to subangular; microspar fafam-ahuzxdazxt; Thidme#»14m ostracods • pavel to sand coatings, biodasts wA;-lram ,. Irrite? Hematile-ronndet^ zziasahc;caIeilBspar-zzxasaic sized, ahundazfa, rounded to ebundszt; pellets • -Q 3 nan, süt-sized, common crystals, rare, caviqr fiUfaig change subangular pdoids - conxzzxon fizB to medsxm crystals R & 3 faxtradast W adssnme T h ick bedded, lu n y y Outcrop - brachiopods, gastro pelizxalzHoan ifcbris, foranuzxi- faxtradasta - m kritB w/spany None Gsldre spar-massive &^fx*- Micrfaseovdopea Thickness » 1.65 m pods, d ie ll debris fera, shell ûagnmta-romxd- graizB db some algal taxial rfazv, ffas to to I—» MIOIOSOOPIC NON-SKELETAL UNIT ROCKTYPE LTTHOLOQIC FEATURES MACROPAUNA ON OUTCROPFAUNAL COMPONENTS CARBONATE CRAINS NON-CARBONATE GRAINS MATROC/CEMENT DIACæNESB/OOMMENTS ed, m krito coated, aBMl*sized crystals; i ntergranula r cement M o d i (cm r idextifiafcio b io aame aggrading crystal growüi dasta,nn R 0 4 M lc t Wsdœstone Thinly lunutled, limtstane None lUlets-imcritB ^faeres, vexy Q utrtz - acattcred, abondant; C dcile paeado^>ar , between Qotty matrix Dodolei, eonezetkns * 4 on, ibondixa, ^jproxznutely the pyroxene, black non-metallic pellets, abnsdaix, massive HnOe #hmle (no tam - grains, hematite, s3t nzed. Hematite - dustered bands, pies) honzorXallamiiattioia,tasisa- Covered intenral ■ 1.7 m alm afrtx T hkkaesi « j6 m RC-5 Arenaceous PackstooB Medium bedded, croas-bedded, Ncoe Poraminifera - highly m icri- Ooids, intradasts • few; Pdycrystalline quartz, rode Calcite ^ tr , mosaic crystals, MicritizatlooofWocIasts, abondant blade decks, 3 lim e- tized, common, sand sized, p elo idr- fiagments - rare; quartz, z ir Gne to medium, commox^cavit wavy extinction prraoonced stone beds and 2 red calcare foond wArxiciite envelopes con, calcite, coUopbane?, - GUing ous shale mterbedi, r ^ I e sand sized, abimdant, sub- marks Thickness 81.1 m R&6 Arenaceous Giainstcne Nodular Imestone bed, inter- None at base, b ig change at Poraminifera - common, m icri- M o ld s - abundant, ovals & Chert • rare; quartz - abund Calcite • s p a r t grains, Mkritized biodasts beds o f l imestone, concretions, top: bracfaiopodi, fenestrate tized; echinodenns & shell çfaeres, large size range, few ant; pyroxene, hematite, py tn«m. ch ip fy bryozoans, echinodenns, blast- slivers, sand sized, common, ooids, few intradasts rite, caldte, a u ^ (rare), sive, cavity GUing, fin e to T liidaica B 7 m (esL) oid (rare), other bryozoans rounded zircon, black isotropic medium crystals. grains; sand to sût sized, abundant, subangolar-angular CANAAN QUARRY CQ-1 Poraminifera Massive bedding, calcite Nm e Poraminifera - abundant, shell M le ts - hematite, m icrite Hematite - round pdlets, in Caldte tpK • M o td y , dear MtontÎTtîfm wf twngta^ Packstone fille d Gactnres divers, echinoderm debris - dumps, sût sized, common to dense, common; massive, Thidmeas = 4.2m scarce, bracfaiopod spines - void GUing; ^h a n o to Gndy abundxitt, fenestrate btyozoans crystaUine; m icrite is conamai rare; sand sized, abundant, d tirita l hematite GUs some round, forams unabtaded C()-2 Arenaceous (Calcar Very thin bedding, pcody None None None Quartz - & sflt, abundant, Lim e m u d & d ^ m atrix, eous) SUtstone cemented, h ighly weaAered subangular; hematite dkpyrite- digfatly coarse, massive, Thickness 8 J S m common, fuB sand sized bioturbated, abundant CQ-3 FoasUiferousDdo- Medium bedded Echinoderm colnmnals • abuzh Pehirtfvtgrm rotmrma!» . abnnd- PeUctS - Scattered m mstrix Daric,noo-nBtallic, isotropic M icrite (1 ^ ) and (2/3) cotrs- Dolomite fonnatioc, weathered cn tizrd Mudstone Thickncsa a —.15 m am; broken fenestrate bryo blebs-rare er dolomite-commca^ massive & corroded echindderm debris zoans, broken (braminilera, dteU divers - aU sand sized Increase in biodasts fio m cQ-1 common and abraded C(}^ SQ^DolostooB Thinly lanmateck barely gra- (lost specimen) datsomd srith3 Thidaieas 8 .7 m C()-3 [Oditic] boradast Medium-thidc bedded, fossil Hasfay biodasts Pbnminifoa, bradnopodi, Ooids-raretocommo:^maty None Calcite spar - cavity FSlmg Orergrowths, recrystalizatka Fbasiliferous debris deGnes bedding, weU Wvalres, gastropods, biyozo- rings, biodasts as nuclei; f t syiXaxial rims^ kmrgranu- o f dteUs, m icritizatiao, sty- cemezaed, hctease in fbssO ans, corsJs?, edm oderms. . vnWhm «nma la r, Gne to mediam oystals Id ite s CO h-* CJI MICROSœ PIC NON-SKELETAL UNIT ROOCTYPB UmOLOOIC FEATURES MACROPAUNA ON OUTCROPFAUNAL COMPONENTS CARBONATE OUMNS NON-CARBONATE GRAINS MATRWCEMENT D1AŒNESIS/00MMENTS [btse o f ptk o s d tO ilB n fl to v trd top oitracodi • GDOft m e, mkxitD with forami ft biodasti, •equDoe] Tliickaes s 53 m coated, aand, aooB g nvel abed, common a ll together, (CQA*1) Gramnoi» Thicknen s 1.4 m round to fob-tnielar (CQA-2) RedShile Thickaeo a 36 m (CQA-3) GfiittstoiB Base o f paleosal. croa-bed> ded, o o litic , baafay fbaaOa; Tfaickocs & .7 m CQ-6 Hem atitic Gramatone Med. bedded, potaly cemented, Ncoe Edxinodcmi colomnals rare btr^asts - rate; dotty w/ None M icrite, faematite? red grams Tbisispaleoaoll (lU eoaol) PakoBoI daiacteristica, root larger caldte grahm mixed SI w/gtey micrite, casts abondant, fitte d & bric, biotBibated; mdhridaal grains erosioDa] contact to CQ-5 o f pyrite f t peloids in besia- Thtfbiesa s 1.4 m tite cement (CQA-4) Paleosol Thickness = 1 32 m CQ-7 Calcareotts Aren- Very thmly bedded, chippy, None Nooe Nooe M ica - abundant; aligned Hemat ite mad, f ir r , dense; aocoBs/MicaceoQS greyish red parallel to bedding, sOt Tniaifm t w fjwnrTV* SQtstone Thidmeas g 3 5 m sized; quartz* abundant, lû t sized; p y rio - conxmoo (CQA-5) Red Shale Thickness s 3 5 m CQ-8L (Arenaceoos] M o d a l Massive bedding , w ell cemented Nooe Brachi<^)od q iim , foram ini- Ooids - few; pdoids • Hematite? • stmH red graim , Calcite tpar • mtergranalar, Mkritization, calcite owr- PtckstooB horizotXal, light fatownidi fera, echiiwdeim debris, tri abondant, round rare; ^ a rtz • cotrancD, sub- qihano to fine crystals; growths greytopmkidi lob ite Eragstents - a ll m icri- nncrite - rare to common; Thickness s .15 m msergramilar round to angolar (CQA-6) Oolitic Thidm esss J 5 m Gramstooe CQ-8U Arenaceous Adatooe t -am Nooe None - a ll cwkMam grains M lets - micrite, oval, -.1mm Plagiodase, pyroxene, angite, eemwnt^ Grains smaller than in CQ-8L, bedding, pindr f t swell at top hematite? - «««< sixedL «pn™™ iqtanocrystallioe, common; digfatly less abundarX, lam i- surface angular to rounded; quartz - nscntB -conanoD nated, b ig mmeral variety (CQA-7) Pdeosol Thidmeas s .16 m (CAQ-S) Calcareous Thickness s ^ m SStstone Arenaceous Padotone Very thin to thin bedding, Nooe S hdl slivers, carbonate sand, M d d s - oval, few; Intra M yaystalline quartz?, Caldte, bematitB? - inter- *mbbled* caldte grain, Meoaol chqqy, shsly, highly wcaA- sand sized, abundam, angular- dasts - m icrite, dense, few ^ra rtz, plagiodase, hematite, graxmlarcemexgas inCQ-8U, miaritization, wavy extinction ered, poorly cemented , mottled subangular (carbonate san^ pyrtBtene-B ^shano to fiiK ly czyatallnB reddish brown to grayhh yel round to subangular note mineral d iversity low Thidmeas « 1.7 m (CAQ-9) Meosot Thickness» 1.7 m CQ-10 Arenaceous Micaceous Very dtrnly bedded, daqipy to Float from dhecdy above: Nooe None Quartz, metallic hicba - sût M icrite widx very abundant CO I—» CD MICROSOWIC NON-SKELETAL UNIT ROCKTYPE UTH ModttODB CssQe.poody ceyicmnd, H vilw *. pUnti Itencstrial] ûedL aboodciit, romided to qoartz; pyritB • caouaa-raiB itncacgottiinpU cc» ancolar; pyrilB • abnsdint; XhidaKW = -3 .0 m (mosdy ndai dhren - abond- ccocealed) ant U.S.ROinE33 3 3 -lU lU o id a l OoUdc Masshv bedding, w ell censnt* None Pelmstoxoan debris, AeH s li Ooids-common, true & super- Polyoystallme quartz. Caldte* massive & cavity Q - MusitxEStioo o f grabs, wavy 3 3 -lU &aisitosB ed, sbarp contact to 33-2» vers, fbram atikra, bryozoans, Octal coatings; btradasts - quartz, zircon-conanon, sOt Ibg, few syntaxial rims, fbe cxtbctkai, recrystalization o oid i inaeaae npaecdan, cd tinw d spines, algal^m oite micritB w/bodasta, some w / rized; cdlopfaane?, metaUics, to medium crystalline ofooids cton-bedding dasts - sand size4 abundant, algae m tw ng n la r tn m g n lf T h id a m s 5.2m coated, rounded-well rounded; sponge-rare 33-2L Aienaceoos GiatxatoDB Thîdtbed<£xig,lower is green- None Fblmatozoan debris, forammi- Pdoids & btradasts - mot Quartz, caldte, zircon, pyr- Caldtdhematite - btergranu- Mioitizationofsomebio- (pelodal) bh grey: upper is y s y is h red ten, shell slivers - sand tled, irregular shqred-spheies oxeue, attgite - sand sized, lar cement - abundant; dasts, quaztz wavy extinction Lower nn it is more weathered sized, common, rounded w /tnic- common, angular; quartz & cal cavity CUbg, ^A ano to Cne Thidatensl m rite & non casting dte concentrated mbands- crystals, hematite occurs lambated around, between & over grabs 33-2U Aienioeous Moidal As above ForaminiSaa, bryozoans, pel- Pblcnds, —.1mm; btradasts - PolyaystaUbe cpiaxtz, Caldte cement- m aaive, com- M icritization, w avyextbctioa W ide texture range Packstone xnatozoan debris, shell slivers —.2mm average; common quartz, pyronene, pyrite, met- moo, ^ ta n o to B ody crystal- common to rare, sand sized, a ll ica-angular to subangular lin e , mtergranula r; m krite - fnhsngu lT in mngnlmf 33-3 Aienaceoos M oidal Shale litnestiBie - None Forammifera - rare, sand MicriWmkroyar grains - Quartz - abundant; p d y c ry ^ Caldte qpar - ^)tncno to fbe M icritization o f forarxuniJBra Padstone gieemah grey, th in ly bedded sized round to oval, /.I - Smm, ta llb e quartz, plagbdase, crystals, htergrannlar, un Thidmeas = .75 m irregularly shaped patches o f aughe - coarse-line sand evenly distributed, conanon; microspar sized^ subangular to «ng nt» miorite-common 33-4 Kem atitic Micaceoos 1/2 cm thick beds o f lime- None None None Quartz - SÜL Snicidastic w/bematite • None Sütstone stone; Gss3e, led at booom, g/»wnvww»bMtvhnr« MiCS - s3t dense, fine mnd, pods o f ma greeo/grey sbove dtards, abundant; P yrite- trix, abundant Grey slide - bgN y altered Thidmeas w 2 35 m sOt, rare^omtnon unit - o ka and zedire? 33-5 Aienaceoos lU oidal Thidc bedding, slightly grada None Pcimatozoan debris, foram ini- Pddda • finer than m 33-3 Quartz - damdant; plagia Very fb e crystals/grabs o f Micritned biodasts, wavy Grainstone tional contact to dtqipy unit ten, shell slivers - rare, dase, zircon • rare; pyrite • caldte, no q ia r; m aty small cx tb ctkm * strongest yet! above, slightly oolitic on sand sized, rounded, m icri- spheres & dusters, augito? - detrital grabs A bserpanu- weathered surface tized a n d sized, commoo^ angular la r cement; no rim cement; Tw o p a b sizes, la r p quota T h id m e a s .7 m rare mk rospar f t micritB grabs, smaller caldte, bi|dt energy Aienaceoos Wacloe- Thidt bedded, dt^py, medium None Shell slireis - rare to conanon None Quarts - sand^ very abundant; M icrite - conanon, coarse. Noras p«y Mmatozoan debris • highly Ir r ite - abundant, sSt-aand; Thidmeas 23 m altered, sand sized, cooanoD to Hematxte - sût, common No fiesh rock acceaible rare, round to subangular 33-7L Arenaceous M o id a l Medium bedded, w ell cernemed, EVImstozoan d e b ris -tb y Fraambifera, pcimatozoan btradasts • algal bound. Quarts-abundant bikers; Caldte - sparry mosab f t Mioritrzatson around biodasts Padat one cro a bedded d e b is , shell sU veis-all tra o iie , Jm m ; Pdoids - some plagiodase - rare; sarai sized panolar caldte-cmtanon, f t fonunbifen, quartz * wavy Thkknea«64m b g U y weaAered; sponge, tr i- w/bternal stmctuiea angular cavity fiU b g f t few rim a. CO I—» MICROSOOPIC NON-SKELETAL UNTT ROOCTYPB UmOLOGIC PEAlURES MACROPAUNA ON OUTCROPFAUNAL COMPONENTS CARBONATE OW NS NON-CARBONATE GRAINS MATRDC^CEMENT DIAŒNESIS/COMMENTS lob he, fenestrate hiytgoan - giatpmediom crystalline; ImeJ, sand sized - cmnoon. nnerosparÀmodcomnoD large grain size range, ip tr in l^ e n w/hikritB grains, caldte grams w/qoaitz rid t Iqcra 33-7M Aicoaceoiis Wads- As above Mmatosam debrb (Coe) cd PoasMo borrows, elongate, None Qoastz - digfatly less abond rite -m icroaparT, in d ivi- Wavy qoaitz extinctionMic StODB weasheied tvfacB oval, noer grained Ellmg ant; pyroDiene, zircon, a a ^ , doal caldte grains. KVIS tfaas snrtoaodmg naatrix bematitB & pyrite; angolar. microns, hnergranolar, abon& sand-silt sized a rt, massive 33-7U Aienaccouj fidoidal As Abow Nooe P onzsinifen, pelmatozoan Oods-rare; Intradasts- Pdycrystsllm e quartz - raze; Caldte spar, mosaic crystals, M krite envelopes; micririza- Padstone debris, shell d ive ts - cotnmoa 3mm, biodasts w /i micrhe; qnaxtz • abtmdsnt; Plago- qihaixr-faidy cryataQioe, tioo of foramiinfina; wavy ■mdarKad peloids dase-rare; sand sized. grmmnrvTMB, u jte ifn n la r; extinCtlCfl Rctom to higher cm gycnvi- 33-8 Caleaieous Hcmatitic Thinly bedded, grayish ted. None Ncdb None Qoaztz- sût, abondant; sand HwwHtw m nti Altezcd m atrix, fonnatk» o f Sfltstone somewbal fisSe ei'Bnmrm» mica - slivcrs common calcareoos cernent; massive, mica T hidaiesi e 3 3 m to abondant; Pyrite - sût. 33-9 Arenaoeota (Hematitic) Thidy bedded, crass-bedded. None None None Angite, pyroxere, qoartz, dark Fine grains o f (piartz, caldte Pyroxene notably abondant Packstone grayish red to red, weathers isotropic grains, hematite & twwMtite - abondant, lamina- d i^ (translocent. w i^ y dissem- ted; - dxranon; héma Thidmeas w 13 m matedj; sand-silt sized, tite cement db g ra in abondant, angolar 33-10 Oditiclhloidal M assif bedding, hard, large None Pdmaiozoan debris • abundant; Ooids db superficial ooids, Quartz - in cross-beds, scat Calcite qrar-abundant, mas- MîmtiMrinn nf fnmnmifig», Grainstone cross beds, o o litic Csanrinifina. bryozoans, shdl biodasts as nuclei; intra- tered dsewhere, sand sized, rive db c a v i^ CUing; ^ h a r» wavyextsKtkm Thidmeas m 1.7 m divers db trü o b to - rare; dasts-rarc comrrxm, subsngolar-angulsr to medium caystaHioB sand sized, roonded Aphano crystals more corrxnoD cross beds; medium crystal common between ooids A: b i» dasts 33-11 Arenaceous Grxmsttme Thick bedded, weathers roooled None None Nooe Quartz-abondant, sand sized HematiiB cemen^ no ipa n y Wavy extinction, less pro- (Calcareous S an^ sim ilar to Canaan VsUey rounded to angular caldte, csvity fil stone] Thidmeas = 1.65 m ling, Cndy crystalline No fresh sanple aseoesrible Big change, renewed uplift? BUTCHER QUARRY B-1 Arenaceous M assif bedding, well cemented Ncdb Small fonm inifesa, bryozoans, intradasts-mioite; Quartz, plagtodaae, caldte, Fiœ to aphano crystalline Mkritzzstioa 0 f biodasts W adzstooo ThidmcsB«3m crmosds?, Gnvanella? - pdoids - carbonate pyroxene - sobangular, sand ratr;*!» rPifWPir*- tw trjw jM f - rounded, m ia itize d grain-abondarx, angular to sized •b nw d t*» tÎTwe TTT™^ subangolar between grains CO CO MICROSOOPIC NON-SKELETAL UNIT ROCKTYPE UIHOijOOlCFEAlURES MACROPAUNA ON OUTŒOPFAUNAL COMPONENTS CARBONATE O W N S NON-CARBONATE GRAINS MA1R0CAXMENT DUŒNBSIS/COMMENTS B-2 Aieniceod Gieea, moe comdy oysttl- Nooe Fflnminifen-xiiB, stnd sized M w is PoiyoyitsUiDB qoixtt, plag- Carbonate mad, plus rare Wavycatmcdoo Wadcsstooe lin e d an B-1 io d is e , q uxtz, pyimene?, - T hicfaiew g smnd sized, «ngnl» to sebsn- miczospar Basically the same as B-1 w id i golsf more mod B-3 A im irro g t Pmdotpne M t» h « bedded, green ioer- Nooe SmsUfcnmmifeim-nie, fatradasts, micriSB spheres dk PblyaystallinB qoattz, egment, mpkann tn fina MkritZZadoO, WSVy eXtZDCtiaO (ctlcueans Band- beds teddah brown ssnd to sût sized ovals (peloids), abundant qoaitz, pyroxene, benatite?- crystals, mtergranula r, some ftooeT] T h trim rw « 1.05 m coounontoraie, sût sized, nmd possible; mimapar; M icritic grains approximately angular; caldte - s3t aized. hcmstile ocm ot on grain equal abundance as quartz; boundaries (EOaence between l,2 d k 3 is hems the & slightly coarser Arenaceous Gramstooe Cross-bedded, massive, w ell Nooe Fcrammifeia - small, crmoid? M icrite grains, intradasts, M ycrystalline quartz, quartz Caldte cement, Cne-^tano, Mictitzzatioi^ wavy extioctioo [calcareous sand- cencuted few, ssnd sized pdoids, ooids - rare to com plagiodase, irrite ? , zircon?, inter granular, not spar stODe?) Thidmeas s 4 3 m mon; fewer grains than 1-3. sand sized, abundarO, angular- No caldte grains in ts subangular B-S Arenaoeotts Gramstooe/ T hin to medium bedding, Nooe Forammifera, scaOcred echi- Mmds Plagiodase, roicrodine, Calcite spar - common, inter- wavy extinction Calcareous sandstooe weathers to 1 -1 /2 * d iick noderm debris • sand sized, pyrite - rare to common; - paxmlar, fm dy crystalline; beds rare rpiartz - abundant; to abundant süt-sized carbon- Identkal to B-4 with fewer Thidmeas s ^ m subangular ate grains m io ith e d grains B-6 Arenaceous Gramstooe Medium bedding, weathers d i ^ Ncoe Nooe M m ds - ovals & spheres, (Quartz - abundant; rode frag Caldte «*TTiwit. aphano-fine Wavyextinctioa py, lateral dtanges in lith o l- —.Inu n , abundant; Calcite ments, plagiodase, zircon (in crystals, mtergranular cgy. dsmges in oystallinity grains - common to abundant, quartz) - angular-subangular caldte; mud-rare, ^xry fine A esence o fc atbm ategraira Thickness = 3 m angular B-7 [Arenaoeous] Mudstooe Medium bedded, cron- Nooe Girvanella?, forammifera Carbonate grains,» .1mm; Quartz-angular; pyrite, M icrite - caldte? grams bedding fragments, shell divers - pellets-round, stringers; hematite, zircon - sand sized, coarser than the pellets; Thidm en ■ .7 m sand-sit stzed, angular. pdoids angular-subangular, commoo caldte spar- vdd Olmg, fina to medium crystals B-8 Arenaoeous Tbm bedded, flaggy, highly Nooe Poraminifera - Pdoids (Quartz, pyroxene? - abundant, Micro^rar • quartz, caldte, w avy extinction Wackestooe weathered d ie ll slivers - rare, sand pyrite? - common; sand sized n rta llic s - sût sized grains, T hidm en s .7 m sized mngnlw tn BibangnW detrital m atrix, abundazZ; B-9 Arenaceous T hin bedded, less flaggy than Nooe Forammifera - m icritized; Mmds-».15mm PdyaystaUxDc quartz, Pkedominazdy m iaitB w/comm Wavy extmctiop W adxstooB B-8 pdmatQgoan debris, highly (piartz, caldte. pyrite?- microspar-abundant scattered T hidm en g .65 m weathered - « mvmm sand sized p Tfd. abundaitt nwry-flf îivi^«% in p rtm fm rfw 4ehr*« B-10 MoidPiacfcstoQB Medium to ihidc beds, well Ttaoe fossils Mmatazoan debris, fbramxni- Moids, coated grains, c Quartz - kss abundant dian Caldte ^»ar - intergrarmlar. Overgrowth cement, mfcritlza-. oemexaed, ledge farmer, large fera, ecfaxoDidspsBs-sand true ooids older units; hemathe,zircon? syntaxial rans.^hano to tfcn, wavy extinction czon-beds on weathered sur- siae4 wmndnd. coated, abuttd- aazid dzed, angolar to au^ medium crystals, sparry mosaic lin e , bioturbated ast angtdar, commoD in places; micritB more aburxi- Biodaits mqr be man abnndan Thidmen g 53 m (soil cover thw i fmpKnt k** fwifJ a t top) dbtafl; jnrrrasn in fosams, cfaangp tonmdrSer lid id o g y at top; moease in biota CO I-* KO MICROSCOPIC NON-SKELETAL UNIT ROCKTYPE LrrHOLOGICFEA*njRES MACROPAUNA ON OUTCROPFAUNAL COMPONENTS CARBONATE (HUUNS NON-CARBONATE GRAINS MATRD^CEMENT DIAGENESIS/OOMMENTS B -II CalcneoasMmbtonB Thin to voytfazn bedding, None None N odb Q osrtt, mica? • r ï t stzed M icrite? assume smce fine Noted change in Ethology we iih e ti d iy p y , ih « ip coo- granted nndatone; calcite tsctto B -1 2 pnay ^ la hematite Thîi-Vw^M«-14™ by photo & meter ftidO B-12L Ajcnaceooi PkckstosB Mediam to thidrbed£ng; None Mmatozoan d eh rif - coated, Few odites • some «ybioclasts MetsBics, zircon?, ()uaitz (as Calcite spar - intergriiBlar, M kritizatian, wavyextinctiao thins iç w tld , hig h ly eroes- weathered; m icritixBd fo n m i- as œ d e i; Intradasts - m ic- in a ll other anils)-G ne aggrading in voids, mediam beddsd, «esÀ en led ntfim, shdl slivcis • nte, clotgr, -1mm, calciie —"d MTgjgrwiiinti «ngnlay csyitals; mnd & mkrospar — B7fCd. en m TTvm tn g ra in s - s n g o ls r B-I2T Aiensoeoos Gnmstone SeeB-l2L Nooe M m atozoan col omnals - few, Caldte grains, pdoids-Gne Rock fiagments, qoartz, {dag- Caldte ^wxr - cavity fillin g , M kritization, wavyextinctioo sand sized, lounded sand sited; Intradasts- iodase, rircon (w /i qoartz & ^ahano to fine crystals, sinrie), metallics • fine sand IncieasB in quartz & cakite, sized, "ng n tT to sabangolar, fU rrff* * *" w iîrfîw» grahte abundant 1-13 Fonüifiteoas Ttmi to mediam bedded, dis- Oatcrop-ragoaecoral,l tri- Girvanella?, fonaxdnifiera hliadasts • tmcrile, rare Pyrite, bemathe, quartz (tnoch M k rite - scattered sût sized M kritizalion Wackcstcne tinct horizontal bedding, well labile, pelmatozoan debris (noted mo ease), pdmaiozoan less than the other units), quartz, abundaitt; spar fillin g cemented; coveted interval (tin y ), Invalves, bradnopods debris Increased, rare trUo- pyrcetcne? - sût sized, round forams, tdvalves, mosaic Substantially diCTerent fiom separates n n ii from B-12 Wte, bradnopod spines, shell e d subangular, scattered, crystals, fine crystals a ll units bdow & Alderscm at Thidmcss s not measoied divers, bryozoans? - sand common rized, angolar, abundant MONTERVnJLE QUARRY M l [PosQi&rous] MS Medium to diick bedded Sparse pelmatozoan debris, Bradnopod shell fragments, ^TOxene, hematite - rare; M icrite - abundant, massive, Ddomitization (Btachiopod]Modstone Thidmeas = 3 jm brachiopods abundant pelmatozoan debris, ostracods Q u a rtz -ih t to fine sand; bioturbated; scattered dolo" [dtsartkolated] - g raw l to subangular to rounded, commo mite rhothbs (<1%) sût sized, common, angolar M2 fPbssili&rousl Mediam be&kd, cross-bedded? Ncne M matozoan debris, rite ll s li- bSradtsts - rare, m iorite dt Rock fragments - rare; pyrite, Mkrite-pa^qfwAnkxospar Mkroipar fiamatkm, m kriti- DdomitizedMudstone Thidmeas»^m w s , forammifera, ostracods? calcite grains; peloids - some isotropic metallics • abund scattered in; dolomite rhombs- zatioo,ddomite formation fine sand to sût sized, rare are rectystallized forans ant; quartz - common, sand abundant; overall massive, sized, rounded to subangular bioturbated M 3 Foasili&roas T hin to th ick bedded None Mmatozoan debris, Intradssts - micrite w/ I ^ t e , hgfM tite - fS t sized, Micrite, now dolomite - rhombs Ddomitization, biodasts Dolonstized Madstotte Covered intervil « 1 m bryozoan fragments, brachiopod calcite grains & biodasts rare to common, rounded masshie^biotarbated, abundant h ig h ly weathered Thidmess = L 6 m riteUs, shell divers, forami- Ttifi-t * - ta riA «>MTvlTir^ routai to subangular; a ll bti>- kem&hashy M4 Possilifisoas Thidcbeddtd, scattered None gnMsnti. Intradasts - m kiite w/ Hematite - red, translucent M krite originally, ddomite Ddomitization o f matrix Ddomitized Mudstone rounded pdlets fiable carbonate grains - sand caldte grains, megdady grains A docs, sû t to sand rhomfaa now - aburafant, massive Thidmeas « 1.45 m to sût sized, cmrunon, round s h ^ d , sand sized sized, small are rounded, Sim ilar to M 3, natch fewer to subangular larger are angular, commcar biodasts M-S Mmdal Fossilif- Thin to tUck bedded, tans Nate Mmatozoan debris * most Intradasts • rare, nncrite. Hematite - rare, s3t sized K & rite - dense, dctQr, M k ritiz a tia n o f tteariy every- W ro o MKROSCWIC NON-SKELETAL UNIT ROCKTYPE LTTHOI jOGIC FEATURES MACROPAUNA ON OUTCRWFAUNALCOMPONENTS CARBONATE CmAlNS NON-CARBONATE CRAINS MATRIX/CEMENT DIACSNBSIS/OOMMENTS awiPidatoPD ts«o2tM -3 ■Wrm<«T»» fng«Tfwnifig«j M . peloidiOce; Moida-abaodaot Thicfaic**.25m 'vilves.biBdtl fianmini&n, tpar,moaaicayatmk,kaa ip n r f, cilci^faeicfT. ib d l abondais than mkritB, cavity SUdsia I/2m ioitB ftl/2 Mhfos • end sized, ihm diat Cning,m6dmmtocoane tpaaycaldlB n nod to labingiiltr, micritB czyatila cnvdcpes M -6 FonilifiaoQf be»* Otss-beddec^ horionC iI ItiZH Bndriopodi • ibozkbot A B ry o m a • fimBStztlB & HemattfiB, sscoQ, pynnene, CridtB - apar, azn^ ciy- M kritizttiaaof paina, « dtsi Gninsttoo ixHdoDf, «tQ cemBzaedtiray dhreao exhcff, pelnatoiotn defcrit, U o d u tt in micriae; Ooid»- pyriSB • tire, roizadBd to fob- atala in voida^ amaU ccya tilf ÜErfcig o f pd n a , wavy faffd^ dikk bed£nf, ookk fattcfaiopod sfaeUs r ih r e if, m e, brokcD ft w b(^, not in aogolar; qoattz • sazai to lin m s Ycada; H em itim fim decietse tow ird top w v l rrnerha »itn: raiets • wA tbs intn- aSt, abondant asfolar cem ent- commote cavity Q - TTikfarai ■ -125 m covdcpet; triloUfet, fcnm i* dist»,notintita ling; fine to medrâm ciyatria; Qoattimare 1ÜBB badcftomid id&rB, tpoogps • R» M icrite • connnoDto rare le tlin n n ftW ii- tv M -7 Fcramini fig» H iid ; to mmivo faeddsf Fonminxfeni • endotfayrifb f t lU o d s • cotzBxuxt; Intndasts- Blade isotropic m etallic bficrilB - dcoae, d oiq r, m ot- M ictoipar fismatiooi? mxDor E WftdcntaDB T h k to fg ■ 4.75 m biferitl • ibondint; trilo> Wodaata in m kritB graina-aQt aized, common, ded, calcilB acaOered «A , pent bite», pdnatoMm dehrif aabangolar to angslar diamicritB Crime - abondant, biycsoin frtcmecCi, calci* m roivB , Motnrbated; Big cnviroomentml dmngo 9{dBta7 - amd rized, mbond- Sparry ayatala wA teata ns, all brdcen except fonzx» KENTON-MEADOWS (yjARRY KM-1 [FbsUiferoaa] Tbidc bedded, ftylditea, I^odactid bcacbkpoda on OBt- (Üriciapfaerea, ahell alxveta, None Q oartz-aUt aized, angolar. M krite • abondant, znizrive, Matrix aliriidy dotqr, ModatCDe d s t^ coocretiaa in lover crep tare forammifera - a ilt aired bioturbated aQdoEtea 4 m ThWrneaa » 4.13 m Similar to DCO KM-2 Aiesaceoua Kbtdftooe Thldcbeddbd Foaail fiagmcsta - tin y , on- Oatracoda (diaarticulated), Ncdb Quartz - a ilt aized, angular, M Icriie - dcoae; mk roapar - M krorpar L r na tion, d o tty Thidmeaa « .55 m MentifwKL, tare fonmlnifera,aiBll rit- abundant; I^ x itB * angular. individual graina mattered matrix vera- lû t aized, common, through matrix; abundant, mazaive, HotsibalBd KM-3 [AzcDMeooa]Modatoœ Medium bedded, notaUy harder None Ncoe Ncdb Q u a rtz -rilt aized, commoo to bEcrito with acme micro^ar, M kto^ar fizrmatioQ thanKM-% vcaihetiamoodr «WiTvtiT*, im Mhw, K etfuihateJ Thtdmeaa « .62 m CblcitB^*arinvci6 Nobiodaata! K M -4L Madatooe Q M om iiized Medium bedded, creea-bedded, Ncdb Ncdb Ncdb Quartz - r ilt aized f t acat D dom itized, p ro b id y waa Ddom ito form atkn IP biodaata at low er part, tered. Cob land aizB commco nJcrilB - abundu^ maaiivB iç p e r haa Nodaata a t aorfacB M iddle o f K& M not acceaaflde, Thidspaa ■ 2.8S m compaiüoncf K & M Lft KM-4 indicatea t h ^ are A s aame K M -4U ItfodatODB (D olcm itized As above Ncdb Biodaatrf Batdyiecognizatie Ncdb Ifc m a tii B ndgrea, duatere- Ddomito ritomba^ coco m krite, Ddomito fdrmatico aand a ire 4 tire , lubangular adt-aizBd, common; Quartz- abondas, maaaWe rare to cctnmoo, lû t aized Sam eaaKM 4L KM-S Moidal AienaceoB» Tbidy bedded, hi^yctoaa- None Fotaminifeta,daaydad algae, Ooida, pdoida - laige aizB Quartz-abundaxZ;zzrcm, CridtBtpar-iotoigmBlar, Veryaiadlartotopcroaa- GtainatooB bedded; top b o l baa rq p le pdmatoaoandebria-aand lange.micritizBd rock fiagmesta • aand aized, medinmtoooaraelycryatallioB bedded anitattK B (^ wide aizB W ro MICROSOOPIC NON-SKELETAL UNIT ROOCTYPB LTTHOLOGIC FEATURES MACROPAUNA ON OUTCROPFAUNAL COMPONENTS CARBONATE GRAINS NON-CARBONATE GRAINS MAIRDC/CEMENT DIAŒNESIS/COMMENTS mmrb nzcd, camDOD «ntwnjn iT tn ■np i! » tittfsoffnios Thicfaice * 2.45 m KM -6 AientcBOQS GrmiiBtooB RoVbrown, chippy, th a ly , th in Ncoe Nooe Micrite grains, altered bio Qoartz • angolar, tw o sizes HezztttitB • infergrazatlar, Large size range o f allodrzns bedded, ifaioIylcmiDttBd dasts - sand sizedL couxnon; [sand A s2 t], hematite - abandam, qibanocrystallme; Thidmem « 1.49 m CklcitB grains, onideatifUble angolar, isotm pk grains A m ioite - mtergranalar, w iy angolar, sand to s3t range. red/orange trandaccml; fzDB angite?, plapodaso - raze KM-7 Oolitic niclatCDe Mediam to diick bedded, cal- Mmatoxam debris- Foraminifen. brtcfaiopod Ooids • biodasts & carbcxi- Rock fiagssmts, pyroxene, py Micrite w ^titzed pains o f Mkzoqnr fixmitian?, wavy cite fille d (xaetuiee A e lli, fayn ffifw , ate grains as nuclei; Pdoids; rite, zircon A nncrodme • quartz - abundant massive; cxtinctiaD Thidm ew b .77 m debris, trSoUtes (maze com Intradasts - dasfcrs of all rare; quartz-2 grain Gridte - single crystals, mon in micrite), ostiacods - ooids A Uoclasts in m icrite sizes, sand A sût, scattered, intergrazsilar, cavity filling. Large grain rfiversily, slide sand sized, akmdant n oolite rounded to sabangolar CzB to mediam isin Z h a lve s, ( h r grained A poitioD, all broken, many w/ o o litic , much fewer calcite micritB coalings, rounded to grams titan previoasdides sabangolar KM-8 Aiesaceoos Peloidil Mediam bedded, oolitic Nooe Bradnopod spines & sliven, Intradasts - few, miohe A Qoartz <• abondant; pciycty- . iutergranular, other M trrktyfinH wf P&ckxtons Thickness B .2dm foram ini&ra, pelmatozoan de biodasts; peloids - some stallzDC quartz, playodase, places fhxely crystallized Quartz - wavy extraction bris, bsynzoans, sponge - all larger and > abondance than aughe - rare, sût dzed; * Mmwnwn- micritized or reoystallxzed, Irrite, hematite • cummon, M k rite - hxtergranular, bare sand rized, common, zoond to sût; all round to sabangolar ly distmguisfaable sabangolar KM-9 Peloidal Odlitic Creu-bedded, somewhat oolitic Nooe intradasts • m icrite w /bio- Quartz - 2 sizes, sand to s3t Gsldte - cavity SUing A M kroqtar A pseudcspar devd- Gminstooe Thidmeas e 6.41 m bcifl, bryozoans (fenestrate A dasts, coarse sand sized; common, round to subangular; rhns, mosaic crystals, over- gpmgnt in ooids, micritized others), ^rooge?, shell a li- Odds - common,biodasts as zircon-raze powths wAtrong lamellae, grains, wavy extinctkn %ers, dasydad algae - a ll nudei, many highly altered, Grm to medium crystalline broken except forams, sand dominate the a ll ochems; Similar to KM-S, rpartz in «{«ed, enfnmfm^ tmr. col oied bands; m krite rite envelopes grains in darioer bands; large grains scattered, small grains pdoids - round, unifcrm size. KM-10 O ditk Grainstone Massive bedding Primatozoan debris, brachio Mmatozoan debris, A ell Odds - abondant, wide size None Sparry calcite m osaic-firm Nibbled edges o f pelmatozoan Thickness = 1.7 m pods (rare) divers, fonunmifera A range (Gne to coarse sand); to coarse crystals debris; biodasts micritiza- gastropods (rare) - a ll cold btradasts-alias cold ticD nudei nudei SLATY FORK QUARRY SF-1 O olitic Fossiliferaas Thidcbeddrag, some sQrldites Nodb Mmatozoan debris, fenestrate Ooids - abundant, biodasts as Nooe Caldte spar-m osaic, MÎCTlÎMtWiftftwnelBW GrazmCooB Thkknce*Z45m bryoBoans; forammifera, dasy iB id e i; intradasts - m icriiB aggrading crystals dad algae - rare; bradnopod A biodasts; Mkritzzed grains dmlls A divers-common SF-2 Fassüiferoaa GridatiaDal cootacttoSF-3, AboniatC foss3 debris a t S hdl feagzocsts - abundant; Nodb Pyrite - common; Hcmathe • M kroqtsr • w/small pods of Mkrospar fonnatioo Wadestooe W B l i ^ olive grey, F b «nrfmrm BnmH tMrtwMpA,*» pelmatozoan debris A trilob ite rare; (Quartz-abundart, s flt lasive CO ro ro MICROSOOPIC NON^KELETAL UNIT ROOCTYPB UTHOLOGIC FEATURES MACROPAUNA ON OUTCROPFAUNAL COMPONENTS CARBONATE GRAINS NON-CARBONATE GRAINS MATRDWEMENT DUGENESIS/OOMMENTS rncdhgn y e y ; medium bed flik k - pdxxuIOBOcos fiip s to S s > n re coed, n g o ltr; Ziicon, pyrox- O u ts pscloed tofBtber ID v e ts d PItCCT Thidm en » L I m 51^3 Fbctflifiaotts T U d i bedding; P ■ olive p e y , Abondant fossil debris (>SP-2) Mmatozoan debris, shell hnradarts - m ioite w/bio- I fcfnattte - #3t, abondant; M io ite dkmi o o q tar scattered, M to o q ta i Caraoation; m ic riti- W tdestooe W s lig b t olivegrey Mmitozoen debris divers « ■tendant^ codothy- * ertmmcn Quartz - sût, abondant, angn- TTMMTMw zstioD offoums A pdiMtozoa Thickoea B 2 ^ m rids • common, sodden appear* la r to sabangolar edges tnce; Dasydads > rare; aU coarre sand-stred, sobsBgolar Apprarmffft n f fgrMnmtfgfa S P 4 PanSifBTOBB T hidi bedding; P ■ dive grey Mmatozoan debris - abondant, Eododiyrtds • ^ P -3 ; braddo* None Ir r ite , faemaSire > rate, Mkrite-scattered mkro^iar, M kmpar lormatian, biodast WadestOQB to p e y , W ■ l i ^ dhre grey regore coral • m e pod spines, sliveis > abondant dlt,sabroooded abnndsnt, massive, tnotnrbated Thidknees m -1 j m (to naxinm m Bryozoans-common to rare; reachable spot) sand-sized, roonded to soban- A ll bot fbtamsnfiera db pelma- golar tozoans are abraded SF-5 Poaafltfieroos F * dive grey, W = li^ Pelrmtozoan debris Bracfaiopod ^SBS, bryozoans- None HeznatitB? - rare M io ite -p a td rc s o f m k ro ^ a r M ioospar form ation, n d c rili- Modstone d iv e grey abondant; endotl^rids, pelma- abondsnt, massive, tuotorbated zatko o f biodasts, peina* Thidmeas B L 2 m tozoan debris, alg a e -common; tozoan debris w Ankritized caldspberes - rare; nnd to edges s ilt sized, sobangular to angular Reached over side o f waU 1er ^Kcnnen; very similar to SP-3dbSP-i SP-6 Fasa&ifioaos Molded weathering; yellow Mmatozoan debris - la rp ; Bryozoans, pelmatozoan debris, httradasts - nucxite, -l/2 n s n Pyrite-commoo to rare, M krite w/dnynncrospar As above WadrestooB borizontml s trie s db sût to y colomnals litte r surface endotfayrids (-«SP-S, ^ P * 3 ) , —.75mm and patches, abundant, masrive, interbeds Girvandla (rare); abundant to bbturfoaled Limited fauna, bryozoais dom- Thickness 8 - 2 m sttbsngular mate like SPS but moease in bryozoans, biodasts larger SF-7 Fossil iferoos Puckered weathering M natozoan debris, smaller Fenestrate bryozoans, Wvalve Ncdb Irrite -abundant to common, KEcrite - dense, massive, None W adxstone Thidmeas b 2.6 m than SP-6 divers & pdmatozoan debris • eubedral crystals, sand to bioturbated ■WmriTtf; farszninifiDa - Doted sût sized dea ease in abondance; cald- ^faetes - rare; abondant on- identifiable biodasts; sand sized, rounded to subangular SF-8 Oolitk Fosriliferaas Nodular, sharp contact to SP-7 Mmatozoan debris - small; Girvanella, pelmatozoan de Ooids - com nco, sand, carboD- Polycrystallioe ip a rtz - rare, Micrite - fine, mtergranular Bwdastmkritizatka Packstone Thidmcss 8—Im small bradtiopods; Pteroto- bris, bryozoaiu (fenestrate & ate grains as nuclei; Q uartz-rare to common, sand db masses, common; Sparry cal- crinos? others), forammifera (rare), Intradasts - larger wAmcrite sized, subangular bradtkpod divers, bivalvniT, db coarse grains, smaller w / cavity Q I ing, qfaaxio to w/ncfa «rare db roonded bfav sand sizet^ abondaxa, roond to papestcDB fa h rk , m krife , fin ely crystallinB d sstt sabangolar rare to commoo SF-9 Fossil ikroosPadc- Bryozoans - fenestrato, bifck M k ts -m k rite spheres, Hematite - rare M krias - mtergraiBtlar, M krite eavdapes stonc/Bryozzxn grey. W 8 l i ^ rdive; silty at surface, larger in low er liste, large, dusters, Bttra- donqw, irxegalar (fistxibation Packstone interbeds part; regore coral,Mastoid- Brachiopods - ponctalB, large; dasts*-1 /2 - 1mm, mkrite G il dte - cement, conanco, Zooecial openings in fene>- Thickneaa 8 3.96 m rare Mmsrezoan colomnals-mkri- w/carbooste grains, common; r,notmosafc. straie bryozoans-identifi* CjO ro w MICROSOOPIC NON-SKELETAL UNIT ROCKTYPE LTIHOLOOICFEATURES MACROPAUNA ON OUTŒOPFAUNAL COMPONENTS CARBONATE GRAINS NON-CARBONATE GRAINS MAIRDC/CEMENT DIAŒNESIS/OOMMENTS tized edges; Gtstrcpod, tr ib O oids • 3 ' A w n ,biodasts [xniczitosbundaDCB in places] able; cosqjea dide w/bodi ute, dasydad - m t; endo as m idet, commoD m krite dk caldte cemeis; tfayrids • common ( SP-10 OolitK GniiBtooc T h iriy bedded, aon-bcddcd, Pelmttozondebris, fartchio- A ll biodasts w /odito coat Odds-abundant, maty w/ Quartz - fjne sand sized, tsie - intorgnmilar cement Ckmea crystal size ioocase ftyldites, F s voy light pods, enausting bcyazoms ings; fortmim&sa, bryozaans, micritB envdopes, biodasts abundattf, most equal g rim causing grain scparstioo, ipey to light g it^ W s ligis pelmatozosn debris, sand sized as nudei size, fine to medium mkritization o f all grains yellow Thidm ev = —2J3 m No grains in contact, a ll s^atatod by cement; ro d a m r this u n it became s ili- ceous looking S F -ll O o litic Gramstooe fie s h surface darker than Crinoid debris - sparse Endothyrids, biyaznsns, shell Ooids-common, biodastnu- Hematite - dark red, mter- Sparry caldte mosaic, abuad- BIodastmicritizatioo,some SF-10, mostly concealed, fiagments, pelmatozosn debris, d e i,l/2 m m ; intradasts- granularmasses, sand sized, ant, cavity filling, fine to flattened ooids singbbed Uvalve fragments, enousting common, d o tty m icrite, 1/2 m common coarsely orystaUiiB T hidm ea a —0.5 m bryozoans (rare), dasydads some U t^a sts inside; Sim ilar to SF-10 w/Iess regu [rare], bradiiopod spines • Mlets-micritespheres. lar cementation A more spar sand rized, common to abundant dustered, mtergranular; those not in ooids have ooids m ^ be onc61ites,bunyy m ia ilB coatings surfaces SF-12 Bbturbated Mudstone F e olive grey, W = light yd- Burrows - filled wAsnd sized Mmatozoan debris, bryozoans, None Hematite - sût, rate M icro^ia r - abundant, masrive. M icroqiar fizm atkm low ; highly Uotuibated in Uodasts,-2mm long; pdmato A d i slivers; unidetuiGed bio turbated low er part, medium bedded zoan debris-rare carbonate graira in matrix; Big cnvirotBnental chango, ito Thickness = 1.52m common, sand to sût sized, body fossils sub" angolar SF-13L Mudstone Lateral dtrqiwarddnngcs to None None Carbonate grains - too small Pyrite - common, fine sand to M krite (dolomite?), randocdy Grain increase m krito to [H ighw all, ic U tiv d y ooids Abash, th ic k bedded to ide rd ify sût sized; quartz - conanon, oriented crystals, some rhombs Hntntnt*»; « f Thidmeas 4.5 m fme sand to sût others interlode, masriTB, matrix abundant, K otur bated finable continuation of facies SF-12 SF-13U Intradast Fbsiilif- Mmatozoan debris - abundant Bryozoans - diverse, large Intradasts - abundant, d o t^ None Caldte - emmim, cavity Q - A ll Moclasa «"W*# w/knicrito croos Gramstooe [—loan], Mmatozoan debris w/biodasts, large size range, lin g A syntaxial rim s, coarse Algal?, high erergy in y lie d *l/2m m - 2mm, some wfinany b io crystals fimn intradasts, notable riaeDs, rare foram s;tril(^ dasts; pellets - süt-sized, increase in biodasts A bryo- bites A dasydads - graw l m icritB spheres, dustored, rized, ahundatg, rounded, m krite envdopes SP-14 OditicGcaîstooB Tbinto medium bedded, Conqaosita?, abnndart small AUWodastsooidcoatod, Ooids • abundant,—iy2znm; Hematke* sand sized, tare GUdte,ddomite?-abundant Pdygooaltexture?,grain 1%^ bedded btvalved shells, bivalves - Mmatozoan debris most abtmd- fifiradasts-1/2-11/2mm, cavity fillin g A intergnuadar czease after cementatkn? ThidaBaB « 6.1 m rare, gastropods • small ant, bryozoans, shell slivcrs, d o tty , m krite w/earbonate ^cry Gne crystals, padced gastropods Abrams-rare; paint A biodasts, canmonto ti^dy Sükeous loddng, ccntiaui- CO ro MICROSCOPIC NON-SKELETAL UNIT ROCKTYPE UIHOLOGIC FEATURES MACROPAUNA ON OUTCROPFAUNAL COMPONENTS CARBONATE (HUONS NON-CARBONATE GRAINS MATROC^CEMENT DIAGENESIS/OOMMENTS and Bzed, aboDdsztt tk s o f SF-13 coviraoaaBot; ODiKMUtkally cotted Uo- d ts s have xmcritB cotlxngB SF-IS Fontli&itnis Oolitic Medimn bedded, nlioeoQS lo c k - ftln a to z a m debris lUm itozacii debrif • tbmidint; M o id s; Ooids - bio* H em itite - to d to t3 ^ com C ddte cemen t t t in SF-14, Reoyttillgation o f cement?, GnilnitooD Fcmnimfeim • eodotfayridi & cUsts mtclet; htxicU sts - mon to abandnt, m tergm ttltr Abtmdini, le ty fine grained, ThicfaicM=2.5m otben trilobitBS. m e , d o tty laeryin oltf bcyccoBif, conis • m e: Cnrrinaed h«^ energy i-nvtmw- •tnd*tized, ■boadiot to com- moQ(«Aookb) SF-16 (Oolitic, Intxidtst) Medium bedded, crot*-bcddo4 M m s to z o o d e b rii Biodtstic btdt, btyozons, Ooids • smaller, fewer rings Hematite - ssnd to sût sized, Caldte - spany mosaic, Micritization o f most caibon- Gmnttone not tflicBoat looking t t o pelmitoKoan debnt, fottm im - than other tmits, biodast ^hexea,rare iitteigiandar, mtedoddng ate grains SF-15 fe ti (decreased abundance), nudei; Intradssts - common, crystals, abondant, massive, Thidmen s 1^ m to top dasydads, trüobitBS, Girvan- gnpestooe-like, dotty, 1/2 frne to coarse ciyKals d la, shell fragments - gravd to ln s n to sand sized, abundant, roond tosnbangnlar R&RQUARRY RRP-I FoasûîGaoos (Intra Massive, hard, darkgt^ both Rugose coral, snail brachio- Brachiopod diells,pelmatozoan btradasts-micritB dbbb- None Micrite, nearing mkrospar in Mioospar fbcmatioo dast) Packstone snr&ces, s tjlo lite s pods, pelmatozoan debris (some debris, coral (2 types), fene clasts, dotty, commoo, 1.25 nun places, common, massive, Wo- large), C on^osita sp. - rare strate bryozoans, endotfayrids to 2mm; MletS & pdoids m turbated (rare), gastr^iods, brachiopod drdtered areas beneath bio ^m es. algally coated grains dasts, larger mioite ovoids (rare) - sand sized, abund ant, rounded, a ll broken RRP-2 O o litic Grainstone L ig h t gtcy * bodi turfaoes, debris Mfnmmn Mmatozosn dcbris, brycEosns O dds-aboi^int,.5-lm m ; Hematite-rare, sût, round Caldte ^ar-commoD, cavity Ncdb stjddites near base, grey craiunun; trUobkes, (brsm ini- M lets - — Jrom, micrite, CD mg, fine to coarse oy- ooids then white odds tqiward, fera - rare; sand sized, w ell dusters, s in ^ , common; stals, aggrading H t ^ energy eixviraoment, massive bedding roonded btradasts • *75 - 2mm, clot- isolated ahoal? ty m ioite w/biodasts; Lunpy ooids - dense p^îerîte radiat ing from center RIW-3U Fossniferous Gradational diange from packed Mmatozoan debris-common, Mmatozoan debris - consnon; Ooids • .5 - 1mm, ermnvm- Hematite • spheres fe mas M k rite pods w/indhndual DdomitB focnatioD Padatone ooids to none; masshre, bard, fewer fossils m o o litic part brycsoans - fenestrates & M k ts - m icrite spheres, s^loiites, sût sized, rare dolomite rhombs scattered; daric pey,styld ifie s others Q i^ y broken), codo- imergrmular; btradasts • A lo t o£ tmidentifiablB debris thyiids, gastropods, trflo - rare, dotQr m krite, indis- -1/2 m ad-1/2 grain supported WlBS, cald^berea? - rare; sand to sût sized, round to mhm gntf , «WîMmt to crmmm RRP-3L M kt-ridx Oolitic SQdolite separates tfus from Mmatozoan debris, bryozoans^ Ooids-.75mm, biodast nudei Hematite ^rtcrcs, dusters* Caldte ^a r - common, fare to Some ooids w /lurspyed^ Gramstooe RRP-3U above dtell fragments, bradnopods, M le ts - very abundant; s m ^ , sût sized, rare to medium crystals^ mosaic, a ll ooid coated-coarse sand m krite ^ - .1 nan, nser^xnd; e«™Tvm aggrading gnüna separated by a lo t o f sized, abundant, well-rounded btradasts • rare, faeavûy cement, ^ p e a r "pushed a pa rf W ro tn MICROSœ PIC NON-SKELETAL UNIT ROCKTYPE UTHOLOGIC FEATURES MACROPAUNA ON OUTCROPFAUNAL COMPONENTS CARBONATE GRAINS NON-CARBONATE (RAINS MATRDOCEMBNT DIACSNESIS/OOMMENTS cold coaled RRP'4 O o litic GruxBtoDD M tssh«, ( ttd ttio n il clun fB Mmatoroen ddaris - commcn Ooids • A - 1mm; connnon to H em atîte-sût, round, red, C sldto spar - common, syntas- Some ^ i t f t smashed g ittn s from d ttk giey to crey w/ bcyoEcans, esdodiynds d t b i abondsm, bioctsstiBidet; rare ral rim s, czviQf C3Iing, fine o o i^ to sU OOtdS aerial (larger) forams, Intradssts - d o tty m icrite to medium crystalline; Tliidcoea s 7.7m (estinated corals - cotTTOCP; gastropod, w/twodasts, j - 2mm; Mod - ccmmoo, imer granular from dide) edÔDoid spines - rare; sand M o id s - alnmdant, Jm m sized, w ell roonded RRP-5 FbaSifiaoos Oolitic SQit otitic , tlte n istin g tre ts Mmatozoan debris-common Fem trate bryozoans, tra d i- Ooids-common, moat w/super Black isotropic grasa-sût CmtMtmrrmfnf.fymiiiiMMi MTTM NonB GninstaoB o f ooids & bbdssts; top » iopods, pcimatozoan debris- Gdal coatings f t biodast sized, rare, round to aubangu- f t mtergranula r, ^ h a n o to faUdc gzey to tdsdc stale t t common; Corals, gastropods, rrndei; Intradasts - dotty, lar medium crystals, H l^ energy biodast breaking top; Hack mst below stale cndodryrids & Inserial forams, m icrite, ^ 2 m n , wide shape environment, noto fewer ooids was tsseaclable ramose bryozoans, algae, range, caldte grams widrm; thm RRP-4 T tiid m e a B 6.lS m (estxmated tsivilves • m e; coarse snd, M o id s - sand sized frtx n d ld e ) rm im no (owexall), roonded RR-1 S ta le Thinly laminate^ wealbert haiticalalB bractoopodi on None Intradssts - elongate, (Quartz f t hem atite-angular, G ay mineralsT some caldte (Joiet inbosjKtaUe einrironmertt [(jio e o y ille s ta le ] platy & ctxÿpy, tdadc dale, —.75mm, m krite , rate; Carbon- mtergranular frile r, sfrt, nmd? ^.75 • 1 m tiiic k ate grams - sût sized, angu- mtmTvknr lar scattered w/qnartz RR-2 Aienaceoos FossOif* C tq p y weslhenng, F » brown- Mmatozoan debris, *at base Mmatozoan debris, ostracods, None QpMtT. enn iiw wi, d ît, m gnlay M io rite /d a ym in e ra b -dense None eiOQS Modstone »hpey,W= li^grey, o f noit, alnmdant loBstia d rd l fragments • connnon; Hematit e - blade, spheres, sw irled appearance, abondaztf, tAldersoD Fonnsimn] highly weattned (mostly mflatos (in sita), cncrostmg bracWopod shells A spnes - single f t dusters - common; massive, tnotnrbated bonedmroad) tsyozoans rtre-coBunon; bivalves, t r ilo Pymxcnc slivers - common Thickness g 15.6 m total bites, bryozoans-rare; ssnd dzed, common o w a ll, subangolar RR-3 ModstoD^Aienaceoos? F « tin e grey, W « mediom None Carbonate grains - «vnnvg* IjnrtT - fine «erwt Caldte p ain s, d ^ minerals, Ncne [vexy bad Am section] olive giey; moetaed weatb- angular; black kotropic abundant, nmssive, Iriotnr- ennfm sy produce ifaaly grains, common batod? Arenaceous Mudstone F g dive pcy, W g light None Mmatozoan debris, abraded f t N ow , calcito rhombs & irxeg- Quartz-common, fim sand. Same as RR-2, d ay minerals. None dive grey,hacizontd part altered, biodasts co nplelsly ulargrsim angular; hematitB - sflt, aonto caldte mod, ings w/coarser m aterial, sandy unidentifiable, in layers f t in ^heres, dusters f t individual grains, bioturbated?, looking voids, sand to sût sized, grains, abundant as replace- atwTvtT*_ mSsngntsr ment and fillin g ; to subangular; I^rroxeneslhers- RR-5 Fenestrate H i^ y weathered, c h y py, Archimedes, encrusting bryo- Fenestrate bryozoans • abund None F ytite - abmufant, sjAeres, M tcrifie/day minerals, sOt- None Wackestooe htyr«mM hnriMrtal- W m gw y zoans, pdmatozoan debris, ant, large; Hfdiate f t en dusters in zooecial operdngs, sized quartz f t pyiilB; abund- li^ p ^ to yeDowUt pcy brachiopods - abundant; mgoae crusting bryozoais, bivalves, scattered; Q u a rtz -fit» aand, srZ, massive, bioturbated? Increase in b iodasts, change bracfaiopod spmes f t shells, common, angular to snbangalar, (not "true" m icrite] Ineavtranment pdmatozoan debris - common; scattered a ll Wodasts have bladed crystals on rim s, aand sized, CO ro cn MICROSCOPIC NON-SKELETAL UNIT ROOCTYPB LTIHOLOOICFEATURES MACROPAUNA ON OUTŒ WFAUNAL COMPONENTS CARBONAIBOUUNS NON-CARBONATE GRAINS MATRDC/CEMENT DIAŒNESIS/COMMENTS ftbaodjol ovenU, fabengulâr to tn g o lir RR-6 PeaestnUg tn n iltr to RR-5, mcreije m Wmitozoaa dehrii - Urger, Pene»ttile»,cncni»tingbiyo- Ncne Irrite rilt, ^faetes in zoo* M krite (more mud), plus Ncdb WftdntooB criaoids (ibondinoe & tise) & more abandinttiiin RR-5, small »iwn* - yWrwiT*- e ^ openings f t scattered; quartz-s2t, abundant, mat b n d iio p o d i brachiopod», Aichimeidet f t debris • conunon; shell Quartz * Cne sand, scattered, sive, bktorbaled Same as RR*5, note lade o f others (fewer fepe grates) divers • rsre; gra%tl to smnd coosnon, subangolar bndâoods f t bivalves in thin rized, sobmnfolir section RR*7 reneatiate Shaly limestooe; F " d iv e Archanedes - abondant; en* Fenestrates - large, abundant; Nooe ()aartz-sO t, common, sulx KBcrite - derae, firs , quartz Nooe Wadaestcne grey. W m dusly yellow , chqjpy crusting bcyceoans • common; Mmatozoan debris, bivalves, angular; Hematite - spheres, r ilt ; H enatite - abundant, f t r ia ly M m ataxoan debris *abazMfant; b nd râ p od sbdls f t spines • rilt, less than RR-5 f t RR-6, massive, Inotuibated? Noto true micritB, fewer bio Brachiopods-most tiny, rare sand to s3t*sized, commoo, dasts in thin secriort prob In fla tia subangular ably preservatiooal SWAGOCREEK SC-1 Fdasiltferous T hick bedded, weathers flaggy. Syrsigoporid coral, pehnato- Endothyrids - abundant; Calct- None Quartz - sût, subangular. M krite-l^;m icro ça r-2/3 Mkroapar fermatiao, rare Mttdstooe yeUow/buBcdar; zoan debris q)heres, pdmatozoan debris, Abundant, massive, biotarbated d domits rhombs Thidmeas = 155 m bradnopod shells f t slivers - common to abundant, fme sand Haahy, this loca li^ south o f to sand sized, abundant, iqûift, should have little or rrwiTvWt tn mhmngMtw no sand SC-2 M o id Gramstooe T hick bedded. Nooe Endothyrids, bracfaiopod frag fartradasts - d o tty m krite , Vdlow/brange trmslucent Caldte cem ent-sparry omaak Sorrsemkrite coarings^ m k ri- Thickness » (15 m ments, pelmataeoan debris, rare,—1mm; M o id s grains, sût sized, cotranon coounon, cavity Qlmg f t syn- tizatko o f biodasts echrooid spines - aand sized, taxial rims, fine to abandant, rounded to sub- crystals, aggrading angular SC-3 Ddomitized Mudstooe Medium bedded, ydlow/buff None Ostracods, pelmatozoan debris, btradasts - -l,5nan Plagiodase - rare, sût, sub- M k rite -d o tty , some d d ^ Ddom ito focmatko weathered surface caldspfaeres-sand rized, arrgular rrdte, lodes sw irled m plane Thidaess ■ 25m (estimated) CMTiTnmn, wwwA-,! trt Ud>t, abundant, massive. Note: no fbrarrs bioturbatod SC4 Nothmscctioo T h k k bedded, 1 m SC-5 M oid (Forammifera) Thkk bedded, styldilk, Nodb mkinfkr#- pJm«- btracUsts - consncBi, —5trun, Hematite-rare iM M tnr. iptr,Mkrittred forams arrdgram Grainstone weathered, fresh surface d if- debris - mkri- dotty mkrite w/caldte cavity Q lb g f t s y n tn ia l edges Gculttogetst tized edges, syntaxial rirrs, grams; Moids-corrunoo r im , «ptiMo- to cry ThSdmeasKlm riaell slhcrs f t biodasts. stals, not mosak bcrcasebferams sand sized, abundant, w ell- iDunded to subangular SC-6 (Fossûiferous) Thldcbedded, wdl cementod, Mmatazoon debris - rare Mmatozoan ddiris (largeh Nooe Nooe Ddomisdhikrito-95-97*- DdooBiB form atxB Ddomitized Mudstooe large Utbdcgkvariatko, bryozoans, caldspberes- 5 • 3%: afasndaac, massxre, Thickness « 2 5 m gravd to sand sized, corrunoo, bkturbated subangular SC-7 Ddomitized Mufttosto Weathers ycllow/bufL flaggy, Nooe Nooe Scattered carbooate grains Hematite - rare; Wack iso- Mkrite-ddomito-pey, Ddomltizatkn Ca) ro MICROSOOPIC NON-SKELETAL UNIT ROCKTYPE UmOLOOIC FEATURES MACROPAUNA ON OUTCROPFAUNAL COMPONENTS CARBONATE C3RAINS NON-CARBONATE GRAINS MATRDC/CEMENT DIACENESIS/OOMMENTS Thidknes K 0.6 m tropic cnins, smd stzed. rounded grass scattered w ri, ffw—fuw note ddomite & no biodasts, environmental aigmScaiice? Olct^faere FbsSif* Mediom to tfaidc bedded, r o o ^ fUmatazom debris - rue Traces - oval areas w /^o id s ^ M le ts & pelmds, dustered None M io ite -d o tty , abundant, Qotty mkrite enmsModrtooB db pod ed tor&CB. fo n ils Uodasts, cencuted w/calcxte înpnrïi Aaeaniw ^ nsssive, Uotnrfaated im etse iqnrard, sQrlditic fragment» - ThidcDcn K 13.10 m P rw w m tfif _ pmlpmafMPmTf bris, (xtracods, GirvaxcUa, caldspberes-cocxmoix; sand sized, sabangolar SORT FonSt&rous (Dolo- Ftnmmifera - endothyrids St None Black isotropic grams, M k ri» (r2/3 dolorm »). Note faoease in ideiaifiahle mxtized ) Mudstooe eâhÊnm, hryrvaans fragment# silt, commoi^ rounded abundant, nsssive, Uotuibated biodasts, larger, diveni^ bradnopod shells-common to in creased ahoodam; trilobites, U - valves, edim oid spines - rare; —«d sized, abundant, Toond to snbangulsr SC-9 F o rsm M o id Thideaess s-14S m (3S Nooe Foram im lera-over abundant, Intradasts-dotty micrite Hemathe • mtergranalar Cildte cement-iwtmosak, H i^ energy, note forams in GninstoDB 1.10 m o f coveted s d e rv il) bryozoans, shell slivcrs, w/biodasts, 1 - 23mm, corns» "smears" common, cavity fillin g , fire high energy environraent dasydads, pelmatozoan debris, Mends • gpmmnn; pellctS? crystals, unifcrm crystal size (rare trüobitea) - coarse sût to coarse sand stzed, abundant, rotmded SC-10 FocsiliferottS T hin bedded ftJmstozwn debris • m e, Endothyrids • pelina- Intradasts - micrite w/bio- Nor» M k rite - mk r ospar St some M io o q s f (brmalioa WsdEstooe Thidmcss s 8.2 m Rogose c o rtl on oatoop tozoan debris - abondam, dasts, —3mm - 1mm, ««tuion; nearing paeudo^sr. Pods o f [SO cm cov*d intBival) weathered; bryozoans, shell Oolites - common, -3 m m , both m icrite, dolomite rhombs, fiagments, bradtkpod shells • true ooids St st^eÆdal ooids e«nim 'nr COnfosmg - loolci Ukc common; gastropod, algae, cement too sponge? - rate; sand sized, csasily rounded to subangolar Fanili&roQS O o litic T h idm e s s 2.2m Sptriferid brachiopod, pelma- Dasydads, pcimatozoan debris, Intradasts • dot^, micritB, Hematite - rare, sût sized, Calcite cement- common, Biodasts mkritized GtiinstODB 1 thick bed toKoss debris bryozoan fragments (highly Uodasts, -3 n n n - 2mm; com- subangular mtergrarmlar A sym sjiial rin s [0 5 m co v'd m terval] weathered, bradiiopod shells, moo; Oolites - rare to conanon, fir» crystals appear to be Noted increaae in envrron- common; gastropod, trOobite, most have superficial coalings aeparated by lecrystaHiza- mental energy rare; all tnicritecoakd, tion, nearly polygonal coarse to fine sand, abundant, rounded to subangolar SC-12 O ditic GrÛBtoœ S ^o litic, neditun to thin None Dasydads db Girvanella, k a d i- Intradasts • dotty m krite None Caldte spar - cottiscc, fsae to [23 m cov'd klervsl] bedding topod shells, bryozoan frag w/Uodasts, 3mm - >2nan, [im it ends on h ill Thidmeas 23 m^ ments, frcams-common-rare; rare; Oolites - «tgTvtapv wide topi sand stzed, abundasK overall, size range, biodast nudei; ftiPKbd to i hengntf M lets - conanon, dusters. CO ro 0 0 MICROSOOPIC NON-SKELETAL UNIT ROCKTYPE LrmOUXMCFEATTJRES MACROPAUNA ON OUTCROPFAUNAL COMPONENTS CARBONATE GRAINS NON-CARBONATE QtAINS MATRKAXMENT DIAŒNBSIS/OOMMENTS RENICK VALLEY RV'l MadftoDo Medhan dark giey, Bnrowa? nobby daam ^ M m atoioan debris • rare, M lets? • pyritized Quartz - sût to sand sized, Lim e m nd/^3idastic mud?; Nor wealbeied, chippy ina rtka l ale brachiopod • lir e aand sized angular; I^Tik?be%es, quartz s3t, m krite bleb^ T h ic fa ic * m 13m dusters, stringeis f t mji abondam, massive Quiet, low energy biodasts: all commoa RV-2 [FonOi&rous) Areo* H i^ y «eaihered, harder than Braehiopadi • ibvndtft, Mmatozoan debris * abund- M lets? • p yrils Quartz - sût, subanpdar, Micrite ft fkmrrmdbkbs. None aceoos Mudxtoœ RV*1. lenticalir, psdatioo- Ragaacchcntiea. Anttracoapir* azt. fenestralB biyozoaxa, scattered; Ir r ite - s3t some rilid s s tie in o d ? ; s3t- i l contact above ife r pellaenaia, Ptoductidi, brachiopod shells & spines, spheres, m drridoal scattered aized quartz; abundant. Increase inWodaata T h ic to fw B 0.4 m C ai^>aiha aubqnadrata forammifera & tnvalves • f t dusters; w/i biodasts; m e ; overall common, sand, reond to sobrounded R V 3 Arenaceotts Fdss3if* H ighly weathered, duppy, Brachiopods - few; AnÜstco* Mmatozoan debris » small, M lets?-pyrite Quartz • abundant, s3t, sub- M icrite/caldte - fine grained Ncne eioBS MucfatoDS gradational ccntaa to RV-4; spirifer pellaerais, Cbn^Msita abraded, common: shell angular; I ^ it e as above, bio blebs, quartz s3t; hematite tiu n ly bedded, no Cteah aurf* fubqoadrata & small nnldcnti* d iveti, sand sized, connnm dasts fS ling, spheres, aSt; abundant, massive Decrease in biota, quiet cnvL ace Ced brachiopods stringers, abundant, s3t size T h id a e s s 0.4 m RV-4 FoasSileroos Weathered, dtqrpy, yd lo w to Brachiopods-abundant; Mmatozoan debris - small, Pellets? - pyrite Quartz f t calcite, subangular, M icrite - dense w/areas rtf Mudstooe white grey A . pellaenris, Rngosocfaoastes abraded; B radiiopod shells f t s3t sized; l^ it e - as above, clearer grains (caldte?), Thidaieas B 2.7 m sp., encrusting bryozoans, spines; conunoo, ssnd sized; abundant sSidastics?; abundant, Increase fas tnodasts, abeeoce rare fcoestrate bryozoans Bivalves - rare; subangular massive o f some may be preservational RV-S Fcas3i£eroos H ighly weathered, chqrpy, moat Ardmnedes - abundant; en Fenestrates - abundant, frag- M oids - sand, corrunoo Hematite - QryriteT), much M icrite - dense w/jpods o f None Mudstooe foss3UmQS unit at localiqr crusting f t tiny ramose bryo nrnts f t larger; Mmatozoan less than RV-4; quartz f t dearer crystals (caldte?); Thidmcss b Idl m 2 m(esL) zoans; small brachiopods - debris - common; abundant calcite s3t, subangular, Quartz-s3t,alrnost micro- SfanHartoRV-l-RV-4 shdl debris; calct^faeres?- abundant, massive bivalves - rare; Composita rare; coarse to Cne sand; aubcpiadrata, A . pellaeiuis, subangular InflatU mfT«tu« U .S . ROUTE 64 64-1 Oolitic Grainstooe Mmatozoan debris, bryozoans- Pellets-OJnun, micrite. Black grains, s3t sized. Ckldte - sparry mosaic, cavi Biodasts have nncrite abundant; endotfayrids, gastro dusters, intergranular, com* angular to rounded-rate ty filin g , fine to medium pods, shell fragments, brach- mon; Ooids - many superficial, Liy - mmmfgt io p o ^ Hvalves, corals, tri- dodast rsdei, .1mm, abund- l ite s , dasydads - rare; M#; Intradasts « —1mm, clot sand  ted, abundant overall, ty micrite f t biodasts, rare well rounded calcite grains - 64-2 Foss3i&rous Endotfayrids, trüobhes, pel- faaradasts - —125mm, m icrite Black isotropic grains, on Micrite-dotqr, pdoids ft Increase in bao ticd iren ity, W a d ssto n e matozoand^ri^calcispheres, f t biodasts, doCQr - rare; drells as r^)Iaoemeig - common intergranular mnd; scattered lower energy fimeatrate bryozoans - common; Mdds • .1 - dolomite rirombs; massive f t encrusting bryozoans, dasy dads, coral? - rare; aand sized, abundant overall, sob angular CO ro VD MICROSOOÏTC NON-SKELETAL UNIT ROCKTYPE UTHGLOGICFEAltJRES MACROPAUNA ON OUTCROPFAUNAL COMPONENTS CARBONATE GRMSS NON-CARBONATE GRAINS MATRWCEMENT DUŒNESIS/OOMMENTS ALDERSON. WEST VIRGINIA A-1 Fan3ifiao«i Massive bedding, ebcndsa Mmatozoan debris, Cdnyoiita? Mmatrwwn MeW# BiodasticmicritB intraclasts Qnartz-subangular, conanoB; M icrite-sliÿxîly coarse wkh Padstone fonOi&roas hash, Beshs sp^ Eometria? sm Anthnco- and other biyoaoass-alnmdant common, aflt-stzed carbonate pyrite-rare to common, s ilt- quartz sût, dessB muddy browsid} grey. W'd=ligl% grey s|»rifer peliaosis - rare trüobitBS, (bramimfeia, grams sbted, angular-subangular ocDoite in zooecial openings, Thickness « .7Sm bradxiopod spines & shells* Hematite-rare, sût widen common, massive. rare; sand-sized, rounded to Uodasts subanpdar A 2 BfyozaasEdnaodenn Massive, iotabeds of bio- Ardinnede* - abondant; rogoae Bryozoans - fenestrate and bdraclists - micrite with Pyrite - eubedral, süt-sized. Calcite rpar, ddomite - Dolomite formatkn PadcstoxB dastk had*-10 an tldd:, corals, pelmatozoan debris, others, pelmatozoan debris - biodasts, rare to commco mtergranular and in shdtcred fewer fossil toward top. brachkspodi. encrosting bryo- sbundamt, brachiopod dteUs areas, sût to sand sharp contact to A-1, A spines, rare; gravel - sand sized dolomite crystals. Thickness - J7m rized, roonded to sob-angolar, M ic rite -w ith in zooecia and m icritized edges in sheltered areas, common db massive A-3 Aienaceoos Poasilif- Massive, highly weathered. Fenestrato bryozoans - abund Bryozoans - fenestrate A None Ir r ite - sû t to fme-sand M ioo^ar, quartz sût and Microqrar ftzmatian eroos Modstone Thickness s 1.42m ant, p^twtwyiTn debris - others, pelmatozoan debris A sized, angular, abundant to smaller carbonate grains. algae - rare, snbangular to common; qoartz • r ilt sized, abundail, massive fe b k tu r- Note amount o f quartz ard ■ n g n lf abundant; pyroBcene? - sût bated fjËkermmcrmlm divers, common; angite - rare FbssSiferoos G5 T hick bedded, sharp contact to Pelmatozoan debris • abundant, Bryozoans. bivalve shells, Pdoids • sand-sized, m icrite Pyrite - eubedral to angular Caldte ipar, common, c a v iy None Biyozoaa-Wmatogoan A-3. gradational to A 3; fenestrate bryoBoans - common forams. bradnopod she lls, ovals, common; ooids - sand- pain s, fme sand-sized, rare fHli%%, aggrading crystals GraxDSUne coarsens upward, foasS hmh to abondant; small bradnopods pdmatixtoan debris, tubular sized, rare, weaAcred; Intra- H i^ energy cnrironmeot, big ThicbresswBOm rare, Rogosocbonetes. R etkn- algae - abundant to common, clasts. pavcl-rized. bio- change fio m older units, note laria trSobites A ^dnes - rare; clastte, rate. Pdotdb > bno- lack o f Archrmedes sod-sized dasts A-S Poasûiferotts Massive, fiactures filled with Fenestrate bryozoans (A rd n - Shell slivers, sand-sized. Carbonate grains, sût-sized. Quartz-sût-sized, angular M k rite - dense, fine, quartz Nooe Wackestooe caldte medes). pelmatozoan debris - rare rare, angular to subangular; irrite-sût s flt scattered < A -4 , abundant Thidaess B 1364m abundant, Composita ^ .-ra re , to sand-sized, angular, Two (Efferent types o f samples Amfaracosjfnrifer pellaensis, Uhfosrflifcrocs mudstone plus Di^dsagnzus sp. - abundant highly fbssfliferous wads- KNOBS-UNIONROAD KU-1 Poasflifidous Massho. pods of odds, Isear Nodb BryoMans most abundark-1er»- lotraclasts • m k rite , o vdd . Pyrite - cubic, coarse to Gtb M k rite - massive, dense, Qotty mkrite, dolomite PackstRB ky estratBS.Fistulqwra, others; calcite grains, ciaiuikiii: silt, scattrred A biodast areas w^enestral fe b rk, rhombs scattered in m atrk debris, P « med. dark g r ^ , TWniit* - — 5^mrtmnn; lin in g , common dotty?, abundant; calcite Thkknrss » 3 m Uvahvs, bracUopods, endo- pdlets - mkrite, silt-sized, cement, ^>any m csak, inter- d q rrid forams, tubular algse * dustered near biodasts, rare paxBxlar, fme - metfiura cry rare; sand-sized, round to stals, «MBimifi subangular, m krite en>^opes K U -2 O d itk Fossflifem ts Massive, ooids rnoease then M m atozaan debris^ Bm tre- Fenestrate hryoaoarxs most Ooidsk biodasts as n u d d . Magnetite? - s flt spheres and Caldlc/ddom xteceiiBnt,spar- Gsldte crystal growth across decrease upwards, s flt wisps, mites. rare brsdflopasda •luaiMjaj tfM tayituMM shundsm; hzraclasts-coamteo kregular shipes, rare, scat- ly mosak, individual dolomite allodenrs, dol omite inegnlar teae to K U -I, P ■ «W*;# - ffnmmrmtr> d o tty m k rite w /caldte tered & dustered Bt in ; cavity some preraure sdutioo CO CO o MICROSCOPIC NON^KELETAL UNTT ROOCTYPB LTTHOLOGIC FEATURES MACROPAUNA ON OUTCROPFAUNAL COMPONENTS CARBONATE OW NS NON-CARBONATE CRASSS MAIRD^CEMENT DIAŒNESIS/COMMENTS (fark grey, W « light crey abundaxt, Dasydad algae * grams suing, cuts across allodcm s Thicknen ■ m common, d re ll slivers « rare some aggrading o ystal growth to common, gastropods-rare; sand-sized, rounded, m icrite envelopes KU-3 IroD-RichModsusB Massive, abandaxs d x le til de prfTTMtfWMn Xm. Elm atozoan debris, bryoBoans, E lle ts - m icrite spheres, in Magnetite f t pyrite • sût f t M icrite - fme w / sflt-srzed Calcite in dissolved shell bris OQfoiCacB, toward to p * bris, few mgoae corals. Pier- shell slivers, ostracods, rare voids, geopetal, iotxagranular sand graim , scattered, organ caibonste grams; Ixaradasts voids mkiTiHan# faryoxoana & mût otocrinus plates, fenestrate Sand-sized, sobangular f t burrows - common; Intia- ic material (yeUowAxtange) make up-1/2-1/3 o f matrix, wifpa bryozoans daits - round to oval, doc^ GUs fractures dxsmkrito febric, abundant; Thldbaoa w 2 3 m m icrite, pellets f t biodasts Cridte-m oaric crystals cont- w /in, abundant mon, irxtergxanular,flxre- txredium crystals KU-4 FontUSeroos Massive, Ic n q y weatbern^, Fenestrate bryozoans, pelm t- fenestr ate bryozoans * abund intradasts-rare, micrite w/ Irrite - sût, subrounded M icrite - dotqr, abundant Q o tty - doe to bioturbation, WKckntcDC pods ofbkdastichash,s3( tozoan debris-modemtdy ant, d re ll slivers &■ fragments caxb. grains f t biodasts. carbonate grams, dense txdc- dismicrite4ikB fabric wisps, stxomatactb?, F = med. abondant, mgoae coral, pro* abundant to commoo, pdmato KU-S FaniUferaas Massht, Archhnedes-ridi. Entrem îtes sp., Archimedes fenestrate bryozoans (Archnrre- None Magnetite - in zooecial open Micro^xar-micrite arouixd microspar formation, ddomite WadsstODB F = med grey, W « med gny to sp., assorted brachiopods des), g ra w l to sand, abundant ings, dusters f t stringers, i bnmbf in formation yellow grey pelmatozoan debris, shell common, s ilt sized matrix f t in zooecia, abundark, Thickness = 2.4m divers f t spnes - rare massive Note lack of crinotddsbris KU-6 FonOUcroos Massive, o o litic upsecti oD. E n tremîtes sp, mgoae coral, E rrestrate bryozoans most Ooids - common, biodast Pyrite - s flt, round - sut>- Micro^xar-fhrermcenterof micro^ar formation, ddomite WadxstoDC w ith decrease in fossils, Qeiotfayridina, productid aburrdant, other bryozoans, nuclei; Intradasts - rare to angular, scattered f t dide, coarser axound bio formation sQrlolites, F = dark grey, brachiopods, Archimedes^., pelmatosoan debris - conanon, common, micrite w/wo identi- in small dusters dasts, individual dolomite W smedhimgrey t t g tn efm m m ; foraxzanifera, dasydad algae, CsMeWodasts rbonibs, abundant, massive, Note bczease in biodasts, Thidmeas = 5 3 m debris • abundant, bifoliate btaddopod shells - taxe; sand biotuxbated possible burrow runnrng down bryozoan > rare rized, subrounded, most w ith centeredslide micritB envdopes KU-7 FonQifcitmt Massive, Cunt x-lammations, Entrem îtes sp., ragose coral, Fenestrate facycsoans, F istn li- E llets - sflt, micrite, None M icrite - fine, dense w ith Qotty from pellets f t Wotur- Wackcftooe alternating sparse & fo ssili- Ckiatfayridina, bracWopods* pora, d re ll slhrera f t frag rounded, scattered, abundant; axeas o f dism icrito w ith cal batiot^ Dotonxite replacement kfoaslkho!ogy;at30tn* rare to common; pelmatozoan ments, pelxnatozoan debris • frxtradasts • rare, rxucrite f t d te o r dolomite fillin g chert nodules; a t 32m • bed debris • abundant, small to abordant; brachiopod qdnes f t tnodasts IDb m h 5 (w id i Archimedes) msdtom, 5-fold lumen drells, eduDoid spmes, F w med d irk grey, W « med. frreaaxxnifera, bivalve • rare, li^ g r e y aand-sized, sobangular Thidm esi w 13 m iCU-8 Pbasilifemus Wide variation m lithoIoRf; Mmatozoan debris - snadl, nwiMtn te kym nan# pglmatfw Ellets-m icrite, sflt, form Ncxre M icrite - dotQr, looaely bCcrite envdopes on most bhv Picfcstone massive, o d d gs; sQdolites; rugose coral. E n tre zoan debris - abundant; Erxhv ing d eny m atrix, abundant; pftw# - eat, dasts, ixxicritizatxin oT grain ps, era; F s lig h t gxey, W w mîtes on outerop tlyrid , uni- ft biserial forams Intradasts - —1mm, m icrite w / d te cem ezt-m osaic xyls, edges V . lir it t grey; top very hasfay shell fragments, bivalves, g«nmnn *** common, a v o id s f t w A loorely Thidmeas w 103 m ostracods, bradxiopods, corals packed micrite -1/2-1/2 mod ft grain sup- CO CO MICROSOOPIC NON-SKELETAL UNIT ROOCTYPB UTHGUX3ICFEATURBS MACROPAUNA ON OUTCROPFAUNAL COMPONENTS CARBONATE GRAINS NON-CARBONATE GRAINS MATRDC/CEMENT DIAŒNESIS/COMMENTS Covered IniBTva] B 6 ^ m tdasydad algae-ccmmoo; ported, hcreasB in biodasts gastropod», trilobito, tabular la^er, increased diversity algae • rare; sand^ized, ■tmimtant overall, subaogular KU*9 ArenaeeoafMadrtoDe Eaxndy Ienmated,tinnly bed Nooe Bivalve - 1 , rare, aand s ts d N odb Quartz - d it sized, angular. Mioite-pods, Gne s3t- Bigdtangein ded, w eatien p isty & drippy, Hematite - sand to s ilt a iz ^ sized quartz gramadt bematite KU-8 F «cllbic pcy, W a jeUow scanned, few dusters, [abundant w /i m atrix], matrix pcy, cpiection become# hard rnmviwti - abundant, massive, possibly llmeAooe, massive, lum py, Cdntly laminated. Thidmeas » 4 jm Covered b te rva l s 1S.7S m KU-10 Bryozoan Packstcoe S ilty sxterbeds, debris at Rugose coral, encrusting and Fenestrate btyotoans, Fistu- Intradasts - m icritB w/carb. Nooe M icrite f t caldte g rass, Nooe [Fbssilifinous] surface, F =m ed. dark to dark fenestrate bryoBoars, syringo- lipora f t others, brachiopod g ra im ,-! - 1.5mm, hematite g ra fts into Gne grained y a r, grey, W * d iv e grey; nrassrve porid coral, f t n nemites, riie lls • abundant; Tr3ob ite, [peeudospar?!,conanco to mas-Bryozoans-large fragments, with horizontal s3t lamina- Sfnrifer, Conyosita? Diaphrag pelm atngnu cfebris, bivalve weathered, rare; M n d s • riv e ; B ig change in enviroianem- tioos; tysection - altematmg mas, pelmatozoan debris-rare r id ls - common; forams - rare tmcrite griam,-l/2mm, C rid te cem ent-yarrym osaic increase Wodasts fossSi&nts & unfoss3i&rous Gravel-sandsized,rounded altered bioclasts abundant, cavity GUing, syn beds, uppermost • interbed sis, Pterotocri nus sp. taxial riim , rare aggrading ded tnd foss3i£Broas Is crystals Thickness = 5.25 m KU-11 Mudstooe Thinly laminated, uneven part Nooe Echmoderm fragments, rite ll Nooe Quartz - sand to s3t size^ M icrite-som e dense portions, Ncoe ings; F » olive grey, W « jd - divers - rare, sand-sized, «avnnvm; bematitB - spheres as w/quaitz ft scattered lowish/jgrq^ rounded; Burrows? GDcd w ith dusters, stringeta ft amdc in; abundant, trsssivo Lowerorgy wfebundantyurtz, Thidmeas & 4.S m coarser f t more abundant s3t grains, angular, abund ehmgp in cnvkonxnent, change Covered Interval = 2.2 m quartz, bematitB f t cement ant to commoo in carborsle production with beds ZD KU-9 and KU-11 KU-12 Micaceous #3 ts to o e t Upaection becomes packstone. Mmatozoan debris - rare, Nooe None - though large irXra- Pyrite - ssnd f t s3t-sized M icritB - dense mud, scattered None Arenaceous mudstone massive (>than KU-11), hotiz- Ferrstrate bryozoans-rare dasts in hand specimen d u iry s f t grams; quartz-sand quartz grains, 2 microDs; ootal fractures; F B medium f t s3t sized, «awmmwi m G ib abundant, laminated, biotur- dark p ry , W B light Hue grey m atrix, abundant in quartz bated Top • masrive w/Uricker part rid i layer, subangular; ings, below top b ooe layer w / Mica? - shards o f hid d y bbe- bruhiopds, crinirid debris ft firrngpTrt matertal - efwnmnn plates Thidmess = 9m Covered Interval B 8 tn KU-13L Calcareous s3tstone Laminated, sandy, no fcssBs Nooe Fenestrate bryozoan - rare Nooe Quartz-abundazS, sand, Hematite - Gne, dense, otax- Lanmated, mostly quartz [49.6% quartz] Thidmeas #4jm angular to subangular; ^ rro x - ing OD quartz?, calcite rhombs Covered Interval B S 3 m ens • sandto sBt, cotnmco to he m tfîte egwieTa f Iri** HintrVt » erfnm m - annlT, «fwigiif** yhtM V angite - rare, czystallinD to sBt, individual grass KU-13U PdasBiferoes Debris ddbeates horizontal Pterotocrinus spy Mastoid Padcstzme beds; F B merfium dark grey. {dates, pelmatozoan debris CO to ro M ICRO Sœ PIC NON-SKELETAL UNTT ROOCTYPB UTHOLOGIC FEATURES MACROPAUNA ON OUTŒOPFAUNAL COMPONENTS CARBONATE (RAINS NON-CARBONATE (RAINS MATRDC/CEMENT DIA(RNESIS/œMMENTS W m mediam llg k grey; tbondint; feaestnte f t rsmoR im uled*, x^beddmg midwqf op hryozosns • conancn, Conçoeiie, Top - th ily interbeds, A in m e prodoctid, rugose coral partzQgi, htsliy Isnestooe KU14 FonSt&roas Azdmxsdes donunated, s 3 ^ Cbonetids - abundant; tU m sto* Barrows? * ovals o f darter h tra d is ts - dark tn im te « / Irrite - cubic, süt-sized in M io o ^ ta r • in o . in SÉBB Mkrospar formation WtdxstGoe interbeds, solid limestone, zoan debris - sm all, fenes- m krite , -1m m , common; Fenes carbonate g rtira , l-2m m f t clusters f t indtvidaal scat- toward biodasts, true m ioite F*brow niih gmy to dirk grey tndes, Inflatia mflatos, trates-m ost abundant, some larger; common tered wA bryozoan zooeda; as errvelopes tim n d biodasts, Return to bryozoan envntmmen W «mediumgrey to medium Axafaracospitifer pdlaenns, tn irri^ fWmmtnMwm many mm fenestrates w ith «nhtijnlT.«ngp!T abundaiU, rmasNe l i ^ grey; midway > d iÿ p y w / Etunetria, Martxma, Rbyncaoel- debris - enmnmn; ihcU divezs m io ite coating encrusting bryozotns f t Archt* lid ? • ennwwfln to m e ; Gastrth Other bryozoans common; gas medes; n od o lir, b o n ^ pod - m e , fc n tiemites tropod - m e ; sand-sized, Thickness « 5.4 m common overall; round to sul^ Total 119.4 m. angular ACME QUARRY AQ-1 Aienaceoos Foasüif- Thick bedding; F «dark grey; Abundant pelmatozoan debris Mmatozoan debris-corrunon, btradasts - rare, irregular Quartz - abundant, coarse to Mkrite • brown, fbe pdoid -1/2-1/2 grain-mud erous Modstone W « medium g r ^ highly weathered; Algae • sand faloba o f matrix rratterial only Gne sand,angular;pyrite- duyed masses, Imer granula r supported Thickness « 1 .6 m sizert tubular, gJv»pMin; Sub- darker; carbonate grains- fine to coarse sand, irregular may be s ilk k , mnd too; angular to sobrounded dr^s,Uod^,blades,common Quartz-coarsesÜtgrains; I^Toxene? - sût, common, sub- abundant, massive, bioturbated angular AQ-2 Mudstooe Thidc bedded, chert stringeri; Scattered brachiopods Orbonate graim , coarse sand Quartz - aand, « n g n lf to sub- M c rite - brown, Gxte dumps, None P « brewnish bUck, W « medium to sût sized, higU y angular, abundant in coarse w/quaitz sût f t dark grans, p e y , contact to AQ-3 very weathered layers, rare to common in Gne AbundarZ, massive Horizontal layering in dide sharp, laminated layers; I^ rito - masses f t alternate Cne mudstooe f t Thidmeas « 1.25 m mdividaal grains, 31 - 3m m , coarser mudstooe w/goartz comnxm; I^roxene - divers, AQ-3 htradast Foasflif- Thidc bedded, h i^ y fract Pelrmtozoan debris - snadl, Pdmatozoan debris - abundant, Intradasts - m krite , bk>- Q uartz-s û t to Gne sard, M krite - brown, slightly S ilica m echmoid pâalete erous Wackestorg ured; P « brown/blade, W « efwrimm tn weathered, coarse aand to gra dasts, -Im tn ; carbonate graitte «ng n lf^ rwfwwun- hématite » grainy, quart z sût mxxed in ; dolomite formation tT»tînm lt£ bt g w y pods on outcrop vel sized; Btyozoans - a ll sons m icritized sût, dusters f t stringprs. abondant, masshre, biot'd? fossü debris on surface types, brachiopods, bivalves - bioturbated, jumhled grains. Thkkness « .55 m conm on; da^dads, Sphaeroco- dium , echmcnd spines, gastro pods - tare, sand sized AQ-4 Foasüikrous Thidc bedded; P «brown/black, Mmatozoan debris - small, (Htracods - abundazS, disarti- None Quartz-Coe sand; Hem atite- M k rite - dense, grey brown, SQddites Mudstooe W «m edium grey rare; Rugose coral, rare colated, sand sized; Pdmato sand, izslividaal graira f t hx (Ostracod Mudstooe] Tfaidoaes « 139 m bradnopods on outcrop zoan debris - common; E n d od ^ fractures, subrounded to sub Sim ilar to DC-1 but not as tids, i pia ea - rare; angular d n k caldspberes-comrrroo AQ-5 FdasOifiaous T h ick bedded, lateral change Mmatozoan debris - smaB, M m atozoan debais- weathered None Quartz - sût to sand, suban- M k rite - Gne to somewhat A tw rvtT * Wackestooe to more fosaüs; P « brown/ common; tare braddopods f t tooat abundaiU; bryoBoazB, golar, common to abundant; coarser; quartz sflt scattered little dae; note abundant black, W «medium grey bryozoans on outoop shell slivera-common; Dasy Hematite - sût, spheres, A hundartt, massive, bioturbated quartz Thidmeas « 135 m dads, teüobitea, gastropods- dusters f t single grans - tare, sand sized; ■bpnrtafit ovenD; a ll bndsn CO to CO MICROSCOPIC NON-SKELETAL UNIT ROOCTYPB LTTHOLOGIC FEATURES MACROPAUNA ON OUTCROPFAUNAL COMPONENTS CARBONATE GRAINS NON-CARBONATE CHAINS MATRDC/CEMENT DIAŒNESIS/COMMENTS AQ -6L PdnSifiaoBs T bick bedded, frftctsred fio m Mnmtozasn debris - small, Endothyrids, shdl aliveis, Intradasts-grey/blackmic- Quartz-mit & sand, common; Micrim-grahy.optolO Mkritiatiottof forama W td n to o e hüating; t caOciod chert common; btyozoans, mgoae pelmatozoan debris, Girvanella, rile, 1 /2-2 mm; carbonate Hemat ite - sHt, mdnddual & m icions; quaitz sût scattered Dodoles; F « btowo/bUdc, W a coral on ooiCTop bryozoans-common ; T rflo - hash* grains - abundant stringers - common; subround - w /i, duiXTy texture due to Mmatozoan debris weathered, medhnn duk srey [thick unit Htes, brachiopod spines, subangular, less rpm tz than HodtStictM ah- mkmd#Y* moderste energy, bjoturbatkn bat no re tl obvious break, it ostracods - common to rare; d d e r units :, WotuAaled? cans ing juitdding if just tfiidcl] Gdcispberes - common; round - Pomns, caldiptees A ostra Thkknew = 4.9 m sabangnlar cods > bryozoans, btadis, etc. AQ-6U [Fbraminifiaal e 6L b 6L Endothyrids (m icritized), Oir» btradasts - rare, Sphaero- Quartz-nit, angular to su^ MicrxlB - grtmy sritb quartz Micritized fbrammi6ra. Wackestooe vsnella, caldspberes - codium encrusting bryozoans angular, common; black isotrtx sût, abundant, massive, dlicaiefdacement bechkuh pelmatettnari dsbris - tlze tO pic grains, angular to suban derm pûtes common; trilobitea, bryozoans, gular, rare to common ostracods - rare; sard sized, Fewer forams A other biodasts round - subangular than 6L; combmed A noted *de crease in biota upward” AQ-7 [Arenaceous] Mediam A Ihm bedded; weathers None Girvanella, d x d l divers - None (Quartz - angular to su!^ M icrite (as m Q , grainy w ith PîftflM ta w M tW ty tmrmprifte Mudnooe cWppy, continuous bed used to enmmnw- d^bris - angular, common; I^ rrit - sand s3t A sand quartz; abundant, tazz change firom ^ to 7 w trace around quarry; F « dark rare; burrow? verticd; all ■mall dusters, rare to massire, bioturbated? grey. W s dive grey sand size^ subangular subrounded to subangular Thickness g .84 m AQ-8 FbssOikrous Thick bedded, F = hrowi^grcy, Fenestrates, pelm atozoan S hdl slivers - abundant; btradasts - common, 1/2to Quartz- sOttosand, angular M icrite - less graix^y than Silica le^acesBitt o f pelmato- Wadaestoce W = yd lo w grey A b ris (some large), shell bryozoans - fergsttate, others 2 mm, m icrite plus carbonate common; p y rite - s ilt to sand, AQ-6 A A (y 7 ; quartz sût zoanznaterid Thidmeas s 233 m divers - abundant; Trilobite, grams indtvidud grians, few abundant, masshe, bbturbated Rirtfiftmitea^pmtfactMfa» A b ris - rare to common; sand dusters Note boease m bryozoans A sized, rounded to subangular; dteUslhters mkiTxtmf» «wi«4pntiftaH e hkw dasts A(2-9L Foasili&rotts Thidc bedding, grades tyw ard Rugose cord - rare; pelmato Pdmatozoan A b ris , bryozoans btradasts - irregular d i^ , Hematite - trearly cubic, sût M icrite - Cne, dense; quartz- silica ti^ a d n g edtmoid Padatone into o d h ic fossûiferous zoan debris - abundant [a ll types] - abundant; ecfai- m icrite blobs, denser than to sand sized, rare; Limomte? sût, coarser A dearer than spmes rode; F s farown/bladc, W s med Doid spiztes - rare m common; futronndmg m atrix common, coarse to fb e sand m atrix, common, massive li^pcy. endothyrids, trilolxtes, -1 /2 -1 /2 mnd-gram support Thickness s 2 3 m (measured) braddqpod shells, gastropods- ed; increase b biodast size, B 4 3 m estimated rare; gravel to sand sized, tOtd A'fkTM# round to subangular debris AQ-9U Mmatozoan Abris - common Bryozoans - fenestrate most M m A --1/2 can, micritized M icrite-C n e, dense, less appears reworked, higher common, pelmatozoan A b iis - grams, common than cemeitt; calcite cemcitt energy camnxm; foram iniferi - rare to mtergranular, qAano to fbe rfirfi divcTS - abund crystalline ant, sand sized, a ll micrite coated A (^1 0 Fosailiferoos Medium beddbg Mmatozosn A bris-abundant; Bryozoans - large fiagments, O oA-consnat, highly wea- Polycrystallme quartz? - veb M icrite -dense, brown, fit» , Micritiaation o f grams [O o litic ] Packstene T hidm css* 3 0 m gastropoA (tmy) - tare; braddopoA shells - rare to m icrite centers, most Q lm g; quartz sand A sût, rare quartz sût bradiiopoA - tmy, cotranon commotx; pdmatozoan d d x is - are superCcid costings; common, scattered; pyrite - 0mA-washed in, not repre- CO CJ -fs* MICROSœ PIC NON-SKELETAL UNIT ROOCTYPB UmOLOOICPEATURES MACROPAUNA ON OUTCROPFAUNAL COMPONENTS CARBONATE OUUNS NON-CARBONATE GRAINS MATRDOCEMENT DIAGENESIS/œMMENTS nre; grtvd to sod sized, A nsn Cne s o d , inS vidoal gnins, ■B'if t iw nf tmtt rrwv4ttw« « btign lf tn «ngnlf ergwmnn^ m brfmnd tO AQ-11 MudRoDB B ictm td , indeL None Nodb Nodb Q uiitZs3t, ' axnm on* m e ; M k rite - deise dk individoal None bedding; F « medhua dâik Pyrite-sût, ssnd dusters, gnins w /i miarte range; pty.W sdivegtey common; m ics - s3t divers, mkindanr, nwaaivB, biatnrbsted Quiet etrvsODQient, DO Ismms- rsre to e tions; bioturbated AQ-12 lAttsteeoos] Modstooo M m ive (Aeer Ikee), sim iltr None Ncdb CsrboostB gnins - ssnd to Qusrtz-s!lt,sngulsr,mbnnd- M ic rite -b ra w n , dense patches None IfloatstxDple] to AQ-11,tnayfaBWDOimit; sflt sized, subogul sf, cerimrm sot; Pyrite - sflt, ssnd «parts A: carbonate grains; W « olive grey/yellow grey dusters, sbundmnt; M ics • larger grains nearing mrcrxK low energy, heavier dasts T h id a e n B estimated divers, sQt, n re to common; apai; abnTwtmn# nssslvo wsshed in, bioturbated? lubognlsr to sngulsr AQ-13 MttdstODe/Micaeeosf Mra4mm kHHmg, lam twterf?, Outcrop = crinoid debris, Nooe None Q uartz- fine s flt, subangular Micrite - brown, fine gnroed. None {1 3 J, 13.Madstone wctthciY Dodultr, cberty; Nastoid, rugose cccil common; Hematte - s flt, less Quartz sflt, leasers upward; F s mediam d u k grey ifao AQ-12, common; Mica- abundant, trsssive, do bioCnr- Faint itm ina tio is,m ica is Tbicknen = 2.84 m more th o AQ-12, common, faation atignwi aligned AQ-14 Modstooe Qtmiiated) Thixdy lamintted, no thup None Ncdb Cirbonste g nin s, s3t sized, Quartz sflt • conceutnted in MicTO^MT-brown w/scattered Mîcroçar fomstion bedding faicaJcs; W E yellow / highly weathered, subangular, coarser layers, scattered quartz, coarse laye n have common-rare throughout; Pyrite - indivi mme quartz Slroo^y lamhated; no Ctuna Thlcknen = —2 m dual grass & dusters concen- bated in layers, scattered s flt grass; m ics-noted de crease in abundance; rare, smaller divers AQ-IS Oolitic gmsstax Massive to thick bedded; do Pelnstozoan debris - abundant Mmatozoan «kbris, drell Ocntis - Tn<4t«tîngr nuclei; Hematite - Gne to cotise Caldte tptr, mtergranular; Extemive recrystalization o f sedimentary structures; chert diven, fcnestnte faryozoars- — 1 mrr^ abundant; In tn - sand, rare to common; round to aggrading crystal size, Cne sanqite, coarser crystals and/or s flt stringers at top gnwMTinn; gU lugU y reoystsl- dasB « brown m icrite, irte - subangular what compacsed Thidmeas = 1 8 m + ized gular boundaries w /biodasts, and/or carbonate grahs, -1mm, Rig wmlimBiiaiital ebm|p SALT SULPHUR SPRINGS QUARRY S3-1 Fbasfliferons Massive, base o f what we can None Bryozoans (fenestrate t e n - Oolites - A n m avg., «xxnmon, I ^ t e - dusters & mdividual M icrite - grey w idtdism icrite D issduticn A spar d lin g W adxstone see, very small exposure, crusting), pelmatozoan debris, weathered; Intradasts - w ith grains, lining Iriodasta, sflt texture, m ottled, abundant, W=rrxd. grey, F^ned. dL grey sytmgoporids, d id l slivers - in ooids, dark micrite with sized, common massive, Hoturbated Quiet environment, note corals Thickness = 1.85 m common, Brachiopod diells, algae A carbonate g raiia cm a l-ra re ; sand-sized, rounded in ooids, angular otherwise S3-2 O olitic Fossfliferaus T h id t bedded, s flt stringers, Rogoae corals, pelmatozoan Algal balls with ooid coatings Ooids-abundant, biodasts as Pyrite-s ilt, rounded to M k rite • «fense, grey, intra- Flattened ooids, outer r ings PackstoQB Wwdark grey. Furred lid itfu y debris, brachiopods (Anthraco- -1.2-1 j nan avg., pdmstozo- nudei; Intradasts - bio- angular, coiraiion pamlar, massive, comrrxm tanixnoff Thkknessw^m sprifierpellaeosis) - rare an «iebris, fenestrate biyo- dastic w ith algae, common Caldte • song w ^ntBtloddng zoans, coral, trilobites, for- crystals, common, Gne to H igh energy W cn MICROSCOPIC NON-SKELETAL UNIT ROCKTYPE UTHOLOGIC FEATURES MACROPAUNA ON OUTCROPPAUNAL COMPONENTS CARBONATE GRAINS NON-CARBONATE (H um s MATRDC/CEMENT DIAC3ENESIS/C0MMENTS •m iz iiib a , (u tro po d s • nrdinmciyAml# er«nmnw bfichiopod ffacUt-nre S3-3 P oaS iiiam s Is ti* - Very thick beddinf. vcriea R s to u c o n l. p d m ta o a RencftntB, U fclta ts & other Ooida - connnm to m e, wuhe Ecrite • mdtvidoal aad aggnx Mkrite-dense, gt^,masiive dotty firombonowing, distWickBstooe from higMy o o litic to fo v 3 *b ris . brechiopodi tty a e o n s , algae (coating & in; pdletx-common, micrite, gates, tilM aed, concexxn- neomoiplnc spar in voids h u h , s3t itilo gm to v tfd tofara #itW n m atrix) - abundant; dosdy packed, dotQr qjpear- ted along Cnctoxes, rounded d o l^ peOeted m icritB (£ s - top, ity lo lifc s . Padcrk jr« y . Syt in goporid coral, pelmato- ance; lotradaats-biodastic toeuheikal-conanon xm oite textme), baotnrfaaied, moderate coeqy, a lo t o f W *M ed I t grey trmn dcfafii, tra ctio p od abellfl algal balls, many are coated musxve, aixxndint tian^Hs ted grains Thidcncw ■ 1.01 m Cfanmnry bcyoBoans, common CUdte • m terioddngay- trilobitea, eduooid ipioes - stals in voids m e ; aatd-abed, totmded to S3-4 BryozoaiVEchgaxtena Masshe, erosioml sax&ce to Coonpositasp., Anthracospiri- Ebyozaans (fenestrate dt fotradasts - —1mm, mtcrhe w / - (me s3t, lin in g BÆcrâe • deme, massive, in - Rare caldte overgrowths, S3*3.discoatinaoosooidbtr. &r pdlacmis, encmsting otbeis), brtdrn, jumbled, caldte grains - common s^olites- m rg ra n o la rt larger areas w / s3ica replacement along sty- Psdark grey, Wsaned. grey; few faryozoans - rare; pdmatozoan ndcrite coated, pelmatosoan biodasts - efTMrmn; fTtlgitw Id te s fossils on sorface debris, abundant rkb fis (< bcyos) • abundant; tptr, ^ntaxlal rims (few), Thidmcss = 2B m gastropods, bivalves, forams- intergranular, f™ - med czy- Moderate errrgy though high rtre , sand-sized, rounded to stals emugh to break iRodasts, subangular, nucrite cttvdopes breakage also due to borrowing S3-5 FouSiferous Pindy crystalline in outcrop, Mmatozoan debris - abundant, lUmatozaan debris, fenestrate tntradasts • dense m icrite, P yrite -sand-sized aggregates Mkzite-dense, gr^w/cal- None Padotone P « dark g%^, W = med. l i ^ t PmtzemitBs, S p iriierid - rase tnfoliate St encrusting bryo- some d otty rilt-riz e d grains; - cite grasB, abundant, m anive y c y , covered by dfqwtone zoans - abundant; Dasydad sût grains around pyrite mas- Thidmess = .63 m algae, ostracodA bradxiopods, s u & u cem ett in fractures, Wvalves, gastrop)ds, trilo - ■tmrwtant tr> enrrmm Wtcs, coral, foram ini& ra- m e to common, sand-sized Bryozoan Wackestone Massive, gradational contac t Encrusting bryozoans - abund tfelmatozoan debris, fenestrate M lets, micrite in drell Hematite - sQt-stzed^ scat M icrite - coarser w/carbcnate None to S3-7, tight ooids then bed ant, peotzemitBS,pelmatozoan & other bryozoans - common, voids - rare; ooids • rare; tered, in (factures, common to grains,lightor in color than ded crirmid/bfastoid hash, debris, Ardmnedes, braduo- corals, algae, tr3odtes, Intradasts - abundant to rare, subrounded to angular mfwrtaW# TWMiWB Intradasts very abundattf, sih stringers, o d d l enses, pods - common to rare forandnifera, bivalves, algal common, most have large bio- make up a good poitioD o f die P s med. dark grey, W s lig h t encrustations, calctspfaetes - dasts, dense dark mxcrite slide grey m e , sand-sized Thidmess B 2.0 m S3-7 Bryozoan WackestozB Massive, (d ty fenestrate Archinrdes • abundant, blast- Fenestrate bryozoans, pehna- Pellets - rare to common, Hematite - ted A massive, Stylolites Large bryozoans, little re- bryozoan fabric, F % dark grey oids, bryozoans, rugose coral, tozoan debris, shell divers - lim onîte?; Intradasts - dense scattered grains A workixjg, no ooids m lateral to d iv e grey, W = ^eUow - pelmalozotn deWs, spirifer- corals, foiam m i- m ioite w/biodasts, large ("MilST algae n . Areas dnges as to S3-5 A S3-6, med. dark g r ^ id - common to rare fera, spi nes, tubular algae - w/ coarser browner micrite Thidmess B 133 m m e , sand-sized, subrounded - near fractures, abundant, arate frem natrec subangular massive S3-8 Bryozoan(oolidc) H i^ y foasiliferous, sût FUmatozoan debris - abunrP Fenestrate bryozoans - large. O oids-c Lbiodaattmdei Lim onite? - few individual K ficrite - dense, dark w/carb- smashed ooids Wackestone ati ingéra, gradual change to arg, Ardmnedes, blastoid, >2nan, other bryozoans-common btradasts • dark grey mic- grains, grain coatfep A frac CBate grains, massive, coarser ooSitic limestone at top, RctkalsriaT sp., rugose cor Mmatozoan ddns-next rite w/bkxdasts A/dr carbtx ture £31, sand-sized, e«Tim m browner m icrite, dism icihe- ooida srasbed bo, litd e tm s - P Blight olive grqr,W « med als, braduopoda, encrusting m icrite edges; afadl nate grains, c u iiiw n , sand- A h ric in denser areas, abnnd- p ort otfstewisD, sinular to ium grey. A fenest rate bryozoans-tare divers A Sphsetocodium en- rized axs, biotnibated? u n it 28 o f reef^ note diange Thidaiess B ^1 5 m crustations, tubular algae - in matrix color, scattered CO CO MICROSCOPIC NON-SKELETAL UNTT ROCKTYPE UTHOLOGIC FEATURES MACROFAUNA ON OUTCRWFAUNAL COMPONENTS CARBONATE GRAINS NON-CARBONATE GRAINS MATRDC^CEMENT DIAŒNESIS/OOMMENTS ceEnxsoi^ gtstrapod, trilobites, ooids b tn tromid IxytBom ostxicodi - m e ; C r * ^ to sxsdow m id liz e t^ e b o siltzl o ven ll S3-9 Oolitic pellet-ridi Med. bedded, «resthentoond- Now FeoestralD bcyoxoSDS - large, Omds-abundant, biodasts as Hematite, ihom bi^cubic grains Caldte « m o n ic spar, caviQr O dds-pressure sdutiotv GniQstODe ed (not bumpy Itke S3-8 & abundtrtf, Mmatoioan debris nudei; M lets - abundant, sand-sized, common cuing ft ^ntazial rims. S3-10), F « duk grey. W s & Sphaerocodiam - commco; m icrite, dusters, intragrann< 1 1 ^ grey gasôopods, coca], faradiiopod lar; Intradasts - large size Like unit 2C o f roadside rect T h kkzcsi ■ A3 m drells, dasydad A tubular range, m icrite w/caib. grams high energy dreal algae - rare, gravel to sand A/or biodasts, w/algal size common (2nd to ooids) enorustaticos 53-10 Fossflifetoos WS Massive, irregolar tan striog- None Fenestrate bcycBoans, targe Odds, common, weathered, broNcDB M icrite - deisB, grey, areas SQ idites Btyozocn-Ridi c n , some la tra l variation, ken, micrite centers; Intra- l îmnnîte stahed, somBwhat Wsckestooe F as light olive pey, W « algae (in bryozoan zooeda), dasts • grey micrite, bio coarser w/carbonare grans; low energy, letum to bryozoan dusly )e llo w . med. lig h t grey, Sphaerocoditun encrustations, dasts w/Sphaeiocodinm ft/or Sphaerocodium-boand areas; cnvirtmment, same as u n it 5 in scattered pclmatozoen hadi & pelmalocBoan debris, encrust carbonate grabs abundartt, ixassive, dotnrbared roadside reef ooidpods ing bryozoans - consnon; focant- Thickness B 139 m inifera, shell slivers - rare, gnare! to sand sized, subangu la r GREENVILLE. WEST VIRGINIA G-1 T h in to very th in bedded; None None Hematite . sUt, jodjvidoal Mud? sfliddastic mud; quartz None WgWy weadned, dipping grabs - « vnmnn; (JuastZ - sUt sût, organics f t ban-rich south at 35 degrees; to fsB sand sized; subangular grabs A true shale Thidmess = 42.7 m to round - abundant; Organks- abundant, throughout specimen like cement G-2L Oolitic grabstaoe Thicfcbedded, basal Alderaon Anthracospgifcr pdlaensis; Mmatozoan debris-common, f V*M« . cnmmcn tn HenstitB - sUt, m dividnal G ddte ^)s r, comnxm; bder^ Recrystallization o f aH Thidmess « 3.65 m * pdmalozoan debris - to tmcritizer^ coated; bryzoaia- no radial fabric; carbonate/ grabs f t dusters, round, granular Qling; aggrading grains ft cement; coarser, . abundant; blastoid dasyclads - rare; sand sized, micrite grabs-abundant crystal size, fme to medium similar to AQ-15 plates - abundant; Rugose rounded coral; PterotocritBU-abtmd- G-2U FbssUt&tous Mmatozoan debris - ptmïI, Mmatozoen debris - common; Ooids - common None C aldte tptr, bttergrannlar. Recrystallizatioa as above G rrirutone abundant; gastropods • srm ll, d re ll slhrers, bryozoans- Cue to medbun crystals rare; Composita sp., Eumettia common to rare; dasyclads- Odds reworked Erom below; sp., fimestrate bryozoans, tare; sand sized^ rounded to fewer ooids f t mare bindasts rugose coral • rare; unusual subangular pclmatozoan plates S ALT SULPHUR SPRINGS REEF 219-1 Foasiliferous Unbedded, massive, not as AbundazS fossil has on Fenestrafe bryozoans f t pelnB- Dense pods o f (me grained (Quartz- sQt sized, angular, M krife-abundant, massive, Volume reduction o f pelmatx^ WadrestODB fe l^ as other A rdiim e dc» 'rid i surface; Rugose corals abund tmn»w A wnin Jrt; caldte, darker dtan matrix subangular, common no structure, rery Gne zoan debris beds; W ^ t grey, g r ^ to ant, Aichbnedes f t pelmatozoan valves, trflobbes, fcrammi- grained, quarts scatfered. CO W MICROSœ PIC NON-SKELETAL UNIT ROCKTYPB UTHOLOOICFBAIURES MACROFAUNA ON OUTCROPPAUNAL COMPONENTS CARBONATE GRAINS NON-CARBONATE CHUUNS MATRDQCEMENT DIAŒNESB/DOMMENTS rn .d k. debris Earn, ilgae - xtre; ssnd faseneef fades 3.10 m long sized, sbtmdml ovcrsU 219-2 Syrisgapand Reef core; W&med. grey. Famed. Sctnered Rugose corals plus Sytmgoporid coral - abundant N odb Quartz - sût, rare, angular Micrite-abundant,massive. None Wadkestcne It grey to iL dive grey; sytmgoporid coral & doQiina&t; Sphaexocodiom- Quartz scatteied; caldte massive, mostly reef mftom abundant; fimestrate bryozoans GUs corailitc centers, com- Reef Core fades Ardiimedea wackestone interca cate, also encrusted lated 219-2a PbssUiferocs Massive, small exposure, below Rugose coral, hasfay pelmato Fenestrate bryozoans, pehnato- Intradasts - few, dense, Blade, isotropic, non-metallic M icrite - dense, fme w/coars- None Wadcestone core zoan debris zoan debris, trUobites. darker micrite, oreg. shqte sût sized, rare er calcite grains, abundant. algae; sand sized, abrâdant, Siqxra-reef fades angular.allbroken 219-2b Algal Gradational contact to reef None Sphsetocodium-abundant; Intraclasts - algal coated, I^Toxenes?, p yrite; sand to M icrite - massive & encrusted; None Wadaestone core; massive, scattered fba- pelmatozoan debris, bryozoan carbooate grains-coral de sût sizted, rare to common sOs; F q ncd. grey, W=med. iL fiagments, trûobite Bag- bris from below, abundant Super-reef fades grey m ents-all encrusted 219-2C O d itk As in 219-4 - t i^ t ly packed None A ll p o litic a lly coated; bryo Ooids - abundant; pellets - None . fpar, common, mas None Grainstooe ooids, abraded fossil debris zoans, ediiiK xkrm s; sand sized abnndaitf, round, .05 mm; sive, mtergraxnxlar fOtmg, abundant btradasts - m krite. few med to coarse crystals Oolite rixoal fades 219-3 Foasiliferous btercalaled w/core; Ardmne- Mmatozoen debris, Ardiimedcs Bryozoans - fenestrate & en- Golds - few; pellets - irrcg. (Quartz-sût, common-rare. Mioo^xar & micrite - very M te a n ^ if f f matirm, peîm rtfv Wackestone des rich; F ^ ned dk d i ^ W s at snrfrce, ntgosB corals & crustmg, larger than m other d i^ d , no mtemal structures, angular fme, both abundaitf, massive zoan debris reduced, more (A rchimedes) med grey - med It grey; bradxiopods rare facies, abundant; brachiopod porous dxells, pelmatozoan debris - trûobite fragmexzs- btetreef fades rare; sand sized, subangular to angular 219-4 Oditic Massive w/some fa in t >*-A4mg« Rugoaans, braduopods, pelma- Fenestrate bryozoans, pelmato Ooids - highly weathered; Hematite - sand, rare, angular Calcite ^xar-common, mtei^ M ioitization o f bioclasts, GrainstoxB Fadk to ncd dk grey; W s It tozoan debris zoan debris, encrusting bryo btradasts - biodastic, granular, med to coarse crys flattened ooids ercy: zoans; sand sized, abundant, irregular s h ^ , large tals a ll p o litica lly coated Oolite shoal fades 219-5 Fenestrate Massive, foasÛiferous, hashy Archimedes and pdm itozoan Encrusting & fenestrate bryo btradasts - rare to common. None MicriteAnioo^ar, abundant; None WadzstoDB debris, some syrmgoporid coral zoans, pelmatozoan debris- caldte grains scattered; abundant; gravel to sand sized Brown r compare to grey m io it Background fades - lithology abundant, round to angular mother fades; abundant, sîmûarto ArchmsdesBeddmg massive Plane across road at Salt Solidatr Springs Quarry CO CO 0 0 APPENDIX F Occurrence of facies In all localities 339 340 FACIES # GENERAL FACIES SUBFACIES UNITS INCLUDED REGION 1 OSTOACOD/CALaSPHERE MS OSTRACOD/CALCISPHERE MS DC-1 FOSSILIFEROUS (AREN) MUDSTONE SR I BIOTURBATED MUDSTONE BIOTURBATED MUDSTONE DC-0 FOSSILIFEROUS WACKESTONE FOSSILIFEROUS WACKESTONE OQ-l.SR-2 FORAMINIFERA WACKESTONE OQ-7.DC-5.SR-3 FORAMINIFERA PACKSTONE FORAMINIFERA PACKSTONE OQ-3 TRILOBITE/FORAM PACKSTONE DC-4 FOSSILIFEROUS PACKSTONES SR-4 FORAMINIFERA GRAINSTONE FORAMINIFERA GRAINSTONE DC-2, OQ-5 TRILOBITE/FORAM GRAINSTONE DC-3 BRYOZOAN RICH GRAINSTONE BRYOZOAN RICH GRAINSTONE SR-5 FOSSILIFEROUS GRAINSTONE FOSSILIFEROUS GRAINSTONE (LAG) OQ-4, OQ-6 (LAG) REGION 2 8 AREN. FOSS. MUDSTONE AREN FOSS MUDSTONE KM-1, KM-2, KM-3, KM-4L, KM-4U.B-7.B-I1 BRACHIOPOD MUDSTONE M l 9 FOSS. DOLO. MUDSTONE FOSS. DOLO. MUDSTONE CQ-3,M-2,M-3,M-4 10 AREN. MICACEOUS MUDSTONE AREN. MICACEOUS MUDSTONE CQ-10 11 FOSSILIFEROUS WACKESTONE FOSSIUFEROUS WACKESTONE B-13 FORAMINIFERA WACKESTONE M-7 INTRACLAST WACKESTONE RC-3 12 ARENACEOUS WACKESTONE ARENACEOUS WACKESTONE B-1, B-2, B-8, B-9,33-7M, 33-6 PELLET-RICH WACKESTONE RC-4 13 ARENACEOUS (FOSS) PACKSTONE ARENACEOUS PACKSTONE RC-5, B-3, B-12L.CQ-8U PELOID-RICH PACKSTONE B-10 AREN. PELOIDAL PACKSTONE 33-2U, 33-3,33-7L, 33-7U, CQ-8L, KM-8 14 FOSSILIFEROUS PACKSTONE PELOIDAL FOSS. PACKSTONE M-5 FORAMINIFERA PACKSTONE CQ-1 15 OOLITIC PACKSTONE OOLinC PACKSTONE KM-7 16 ARENACEOUS HEMA PACKSTONE ARENACEOUS HEMA PACKSTONE 33-9 17 PALEOSOL PALEOSOL CQ-6,CQ-9 18 ARENACEOUS GS/PELOK) GS ARENACEOUS GRAINSTONE RC-6, B-4, B-5, B-6, B-12T, 33-2L, 33-11, KM-6 PELOIDAL OOLITIC GRAINSTONE 33-IL, 33-lU, KM-9,33-10 FOSSILIFEROUS INTRACLAST GS RC-1, CQ-5, M-6 PELOIDAL ARENACEOUS GS KM-5,33-5 INTRACLAST PELOID GRAINSTONE RC-2 19 OOLITIC GRAINSTONE OOLITIC GRAINSTONE KM-10 20 SILTSTONE AREN. (CALC) SILTSTONE CQ-2 CALC. AREN. MICACEOUS SILTST. CQ-7 HEMATmC MICACEOUS SILTSTONE 33-4 CALC. HEMAirnC SILTSTONE 33-8 REGION 3 21 FOSSILIFEROUS MUDSTONE FOSSIUFEROUS MUDSTONE SF-5, SC-1, SC-6, SC-8, SC-8T, RV-4,RV-5 FAQES # GENERAL FACIES SUBFACIES UNITS INCLUDED 341 22 AREN/AREN FOSS/OSTRACOD ARENACEOUS MUDSTONE RR-3, RR-4, KU-9, KU-12, AQ-7, MUDSTONE AQ-12.RR-2 AREN FOSS MUDSTONE RV-2.RV-3.AQ-1.A3 OSniACOD MUDSTONE AQ-4 23 MICACEOUS MUDSTONE MICACEOUS MUDSTONE AQ-13.2 24 MUDSTONE/DOLOMmZEDMS MUDSTONE/DOLOMmZED MS SF-13L, RV-1, KU-3, SC-3, SC-7, AQ-11 25 LAMINATED MUDSTONE LAMINATED MUDSTONE KU-11, AQ-2, AQ-13.1, AQ-14 26 FOSSILIFEROUS WACKESTONE FOSSILIFEROUS WACKESTONE SF-2, SF-3, SF-4, SF-6, SF-7, SC-10. 64-2, KU-4, KU-6, KU-7, KU-14, S3-1, S3-3, AQ-5, AQ-6L, AQ-8, A-5 FENESTRATE WACKESTONE RR-5, RR-6. RR-7, KU-5, S3-6, S3-7, S3-8.S3-10 FOSS INTRACLAST WACKESTONE AQ-3 FORAMINIFERA WACKESTONE AQ-6U 27 FOSSILIFEROUS PACKSTONE FOSSILIFEROUS PACKSTONE RRP-3, KU-1, KU-8, KU-13U, S3-5, AQ-9L.A-1 BRYOZOAN PACKSTONE SF-9.KU-10 BRYOZOAN ECHINODERM PS A-2.S3-4 FOSSILIFEROUS INTRA PACKSTONE RRP-1 28 OOLITIC FOSSnJF PACKSTONE OOLITIC FOSSIUFEROUS PACKST SF-8, AQ-10, S3-2 29 OOLITIC FOSSnJF GRAINSTONE OOLITIC FOSS GRAINSTONE SF-1, SF-15, SC-11. KU-2, RRP-5 OOLITIC GRAINSTONE SF-10, SF-11, SF-14, SC-12, RRP-2, RRP-4,64-1, AQ-15, G-2L OOLITIC PELLET GRAINSTONE RRP-3+.S3-9 GRAINSTONE (OOLITIC, INTRA) SF-16 30 FORAMINIFERA PELOID GRAINST FORAMINIFERA PELOID GS SC-2, SC-5, SC-9 31 FOSS GS/INTRA FOSS GS FOSS GS/INTRA FOSS GS G-2U,A-4,SF-13U 32 BLACKSHALE BLACK SHALE RR-1,G-1 33 MICACEOUS SILTSTONE MICACEOUS SILTSTONE KU-12.1 34 CALCAREOUS SILTSTONE CALCAREOUS SILTSTONE KU-13L APPENDIX G Point Count Data 342 lOCALITY MC CE DO MS HC QZ MT PY HE LI 2R PX AU PQ FS MI PE IN CG RF oo CT OR PT PD SF CS AL FO HR OS EV BY TR CO SP GA BU TOTAL SR-1 209 34 0 0 0 15 0 12 0 0 0 0 0 0 0 0 4 0 0 0 0 0 0 0 6 20 0 00000000000 300 SR-2 191 17 0 0 0 15 0 19 0 0 0 0 0 0 0 0 21 0 0 0 0 0 0 0 17 18 1 1 0 0 0 0 0 0 0 0 0 0 300 SR-3 134 79 0 0 0 3 7 0 0 0 0 0 0 0 0 0 17 1 0 0 0 0 0 0 11 39 0 1 8 0 0 0 0 0 0 0 0 0 300 SR-4 48 155 0 0 0 9 2 0 0 0 0 0 0 0 0 0 24 7 0 0 0 0 0 0 13 38 0 0 4 0 0 0 0 0 0 0 0 0 300 SR-5 20 167 0 0 0 0 0 5 0 0 0 0 0 0 0 0 24 1 0 0 0 0 0 0 11 7200000000000 0 300 DEEP CREEK QUARRY DC-0 191 0 0 0 0 65 34 1 0 0 3 0 1 0 0 0 0 0 4 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 299 DC-1 240 0 0 0 0 5 16 0 0 0 0 0 0 0 0 0 0 0 8 0 0 0 4 0 0 0 5 2 1 4 15 0 0 0 0 0 0 0 300 DC-2 1 179 0 0 0 0 2 0 0 0 0 0 0 0 0 0 19 11 2 0 0 0 0 0 19 3 0 31941 0 0 1 0 0 0 0 0 300 DC-3 7 158 0 0 0 0 8 0 0 0 0 0 0 0 0 0 35 2 1 0 0 0 0 0 16 0 0 21141 0 0 0 0 0 0 0 0 281 DC-4 65 109 0 0 0 0 1 0 0 0 0 0 0 0 0 0 24 1 6 0 0 0 0 0 24 0 0 0 8 26 0 11 21 1 0 0 0 0 297 DC-5 168 70 0 0 0 0 16 0 0 0 0 0 0 0 0 0 3 1 10 0 0 0 10 0 17 17 0 3 12 1 1 1 2 2 0 0 0 0 334 QAKIAND QUARRY OQ-1 98 60 0 0 0 0 25 0 0 0 0 0 0 0 0 0 3 0 15 0 0 0 0 0 29 65 0 0 6 2 0 7 10 2 0 0 0 0 322 00-3 132 68 0 0 0 0 9 0 0 0 0 0 0 0 0 0 8 0 6 0 0 0 0 0 12 25 0 0 20 11 0 0 5 3 1 0 0 0 300 OQ-4 36 125 0 0 0 0 2 0 0 0 0 0 0 0 0 0 2 0 4 0 0 0 3 0 38 47 0 0 0 17 0 7 30 0 0 0 0 0 311 00-5 104 66 0 0 0 4 1 0 0 0 0 0 0 0 0 0 48 22 16 0 0 0 0 0 19 18 0 0 24 2 0 1 0 1 0 0 0 0 326 00-7 133 31 0 0 0 0 11 0 0 0 0 0 0 0 0 0 31 32 31 0 0 0 0 0 18 20 0 0 3201000000 313 BUTCHER QUARRY B-1 0 35 10 84 0 84 7 0 0 0 0 0 2 0 0 0 54 2 9 0 0 0 0 0 5 4 0 0 2 0 0 0 0 0 0 0 0 0 298 B-2 105 17 5 33 0 103 2 0 1 0 1 1 0 0 0 0 21 1 13 0 0 0 0 0 0 5 0 0 0 0 0 0 0 0 0 0 0 0 308 B-3 8 114 0 0 0 70 0 0 39 0 0 0 0 1 0 0 41 0 20 1 0 0 0 0 3 5 0 0 3 0 0 0 0 0 0 0 0 0 305 B-4 29 117 0 0 0 68 2 0 0 0 0 0 0 2 0 0 53 4 9 1 0 0 0 0 15 4 0 0 2 0 0 0 0 0 0 0 0 0 306 B-5 21 126 0 0 0 104 2 0 0 0 0 0 0 3 0 0 28 0 17 0 0 0 0 0 3 1 0 0 0 0 0 0 0 0 0 0 0 0 305 B-6 24 0 0 0 0 94 0 0 0 0 3 0 0 12 0 0 16 0 19 0 0 0 0 0 3 00010000000 0 0 .172 B-7 229 17 0 0 0 24 0 0 0 0 0 0 0 0 0 0 9 0 7 0 0 0 0 0 5 11 0 0 0 2 0 0 0 0 0 0 0 0 304 B-8 173 18 0 0 0 65 0 0 8 0 0 0 0 3 0 0 16 0 9 0 0 0 0 0 0 8 0 0 0000000000 300 B-9 184 15 0 0 0 62 0 0 6 0 2 0 0 0 0 0 17 0 10 0 0 0 0 0 2 6 0 00000000000 304 B-10 31 53 0 3 0 28 0 0 2 0 0 0 0 0 0 0 124 5 4 0 0 0 0 0 41 19 0 0 0000000000 310 B-12L 30 41 4 23 0 56 1 0 0 0 0 0 1 0 0 0 108 11 1 0 12 0 0 0 22 8 0 0 1 0 0 0 0 0 0 0 0 0 319 B-12T 15 96 0 11 0 101 1 0 0 0 1 0 0 0 1 0 52 0 9 0 1 0 0 0 5 9 0 0 0 0 0 0 0 0 0 0 0 0 302 B-13 202 19 0 0 0 36 7 0 0 0 2 0 0 0 0 0 5 0 3 0 0 0 0 0 11 17 0 0 0000000000 302 U .S. ROUTE 33 RT.33-1L 26 90 0 0 0 4 0 0 0 0 0 0 0 0 0 0 95 14 9 0 25 15 0 0 28 5 0 0 3000000200 316 RT.33-1U (SAME AS ID RT.33-2L 0 99 0 0 0 78 3 0 48 0 0 ., 0 0 1 0 0 49 0 17 0 0 0 0 0 9 2 0 0 0000000000 306 RT.33-2U 26 151 0 0 0 62 1 0 1 0 0 0 0 0 0 0 38 0 17 0 0 0 0 0 6 3000000000000 305 RT.33-3 32 115 0 0 0 109 0 0 0 0 1 0 0 2 0 0 34 0 8 0 0 0 0 0 5 2 0 0 0 0 0 0 0 0 0 0 0 0 308 RT.33-5 29 173 0 0 0 50 7 0 0 0 0 0 0 0 0 0 42 0 12 0 0 0 0 0 230020000000 0 0 320 RT.33-7L 19 80 0 13 0 64 1 0 1 0 1 0 0 0 0 0 83 2 7 0 1 0 0 0 19 12 0 0 0 0 0 0 0 0 0 0 0 0 303 RT.33-7M 157 99 0 0 0 36 1 0 0 0 0 0 0 0 0 0 1 0 5 0 0 0 0 0 0 0 0 0 1 0 0 0 0 0 0 0 0 0 300 RT.33-7U 39 98 0 0 0 65 0 0 0 0 1 0 0 0 0 0 75 0 3 0 0 0 0 0 16 7 0 0 1 0 0 0 0 0 0 0 0 0 305 RT.33-9 59 9 0 0 0 137 10 0 41 0 0 5 0 0 0 0 0 0 40 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 301 RT.33-10 10 93 0 0 0 20 0 0 0 0 0 0 0 0 0 0 80 20 5 0 27 0 0 0 25 2100200000000 0 303 RT.33-11 2 45 0 0 80 103 0 0 0 0 0 0 0 0 0 0 42 2 18 0 0 0 0 0 290000000000 0 0 303 KENTON-HEAD OHS QUARRY KM-1 227 18 2 30 0 11 2 0 0 0 0 0 0 0 0 0 0 0 2 0 0 0 0 0 0 10 0 0 0 Q 0 0 0 0 0 0 0 0 302 KM-2 171 12 34 6 0 57 2 0 0 0 0 0 0 0 0 0 8 0 7 0 0 0 0 0 0 3 0 1 0 0 0 0 0 0 0 0 0 0 301 KM-3 81 37 129 0 0 47 6 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 300 KM-4L 3 8 281 0 0 11 1 0 0 0 0 0 0 0 0 0 0 0 1 0 0 0 0 0 0 0 0 00000000000 305 KM-4U 47 5 230 0 0 2 2 0 0 0 0 0 0 0 0 0 10 0 0 0 0 0 0 0 0 4 0 00000000000 300 KM-5 25 61 0 0 0 60 0 0 0 0 0 0 0 0 0 0 128 2 1 0 0 0 0 0 21 4 0 01000000000 303 KM-6 4 25 0 0 0 110 13 0 105 0 0 0 0 0 0 0 13 0 20 0 0 0 0 0 3 8 0 0 0 000000000 301 w -P» w LOCALITY HC CE 00 MS HC QZ MT PY HE LI 2R PX AU PQ FS HI PE IN CG RF 00 CT OR PT PD SF CS AL FO BR OS BV BY TR CO SP GA BU TOTAL KM-7 186 28 0 8 0 19 0 0 0 0 0 0 0 0 0 0 25 0 2 0 0 0 0 0 7 25 0 0 0 0 0 0 0 0 0 0 0 0 300 KM-8 45 70 0 11 0 53 1 0 0 0 0 0 0 0 0 0 81 5 5 0 • 0 0 0 0 13 21 0 0 0000000000 305 KM-9 3 64 7 0 0 21 0 0 0 0 0 0 0 0 0 0 167 10 2 0 13 0 0 0 20 10 0 0 0000000000 317 KM-10 6 114 1 0 0 1 0 0 0 0 0 0 0 0 0 0 10 14 0 0 146 0 0 0 8 1 0 0 0 0 0 0 0 0 0 0 0 0 301 HanSRVILIZ QUARRY H-1 242 16 4 0 0 18 10 0 0 0 0 0 0 0 0 0 0 0 5 0 0 0 0 0 0 6 1 0 0 0 0 0 0 0 0 0 0 0 302 M-2 72 10 160 0 0 42 5 0 0 0 0 0 0 0 0 0 0 0 5 0 0 0 0 0 0 6 0 0 0 0 0 0 0 0 0 0 0 0 300 H-3 55 8 196 0 0 0 0 0 0 0 0 0 0 0 0 0 15 0 2 0 0 0 0 0 10 15 0 0 0000000000 301 H-4 28 1 232 0 0 0 1 0 0 0 0 0 0 0 0 0 25 0 0 0 0 0 0 0 7 10 0 0 0 0 0 0 0 0 0 0 0 0 304 M-5 69 101 0 0 0 1 2 0 0 0 0 0 0 0 0 0 88 0 0 0 0 0 0 8 26 5 1 0 1000000000 302 M-6 27 38 3 0 0 55 0 0 0 0 0 0 0 0 0 0 30 120 0 0 8 0 0 0 12 14 0 0 0 000000000 307 M-7 214 31 0 0 0 3 1 0 0 0 0 0 0 0 0 0 4 1 0 0 0 0 0 0 0 26 0 0 21 0 0 0 0 0 0 0 0 0 301 ROARING CREEK RC-1 25 103 0 0 0 14 5000000000 28 66 00300 31 26 301 RC-2 21 129 00003000000000 41 100 0 0 0 0 0 10 18 322 RC-3 176 27 0005 14 000000000 16 44 00000 5 14 301 SEE ORIG SH 210 56 0 0 0 24 50000070000010000 0 2 307 RC-5 11 86 0 0 0 98 000000010064782200 11 14 304 RC-6 0 146 0 0 0 60 3 0 19 0 1 1 0 2 0 0 52 1 10 0 1 0 0 3 7 306 CANAAN QUARRY CQ-1 112 71 0 0 0 1 7 0 30 0 0 0 0 0 0 0 4 0 1 0 0 0 0 0 9 29 0 0 34 0 0 0 0 0 0 0 0 0 298 CQ-2 0 9 228 0 0 0 4 0 0 0 1 0 0 0 0 0 0 0 0 0 0 0 0 0 0 3 0 0 0 0 0 0 0 0 0 0 0 0 245 CQ-3 44 15 176 0 0 1 1 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 15 48 0 0 0 0 0 0 0 0 0 0 0 0 300 CQ-5 28 104 0 0 0 1 0 0 22 14 0 0 0 0 0 0 8 90 0 0 10 0 0 0 21 25 0 0 1 9 0 0 1 1 0 0 11 0 346 CQ-6 87 18 0 0 152 36 0 0 0 0 0 0 0 0 0 0 2 0 3 0 0 0 0 0 0 2 0 0 0 0 0 0 0 0 0 0 0 0 300 CQ-8L 14 103 0 0 0 30 1 0 11 0 0 0 0 2 0 0 86 1 9 1 1 0 0 0 17 29 0 0 0 0 0 0 0 0 0 0 0 0 305 CQ-8U 75 83 0 0 0 93 0 0 14 0 0 0 0 0 0 0 19 1 0 0 0 0 0 0 1 3 0 0 0 0 0 0 0 0 0 0 0 0 289 CQ-9 96 50 0 0 0 100 0 0 19 0 1 0 0 3 0 0 28 0 0 2 0 0 0 0 2 3 0 0 0 2 0 0 0 0 0 0 0 0 306 CQ-10 141 0 0 0 0 26 26 0 0 0 0 0 0 0 0 7 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 200 SZATY FORK QUARRY SF-1 0 96 0 0 0 0 0 0 0 0 0 0 0 0 0 0 30 24 0 0 72 0 0 0 50 27 0 0 0 0 0 0 0 0 0 0 0 0 299 SF-2 98 35 97 0 0 22 2 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 23 24 0 0 0 0 0 0 0 0 0 0 0 0 301 SF-3 193 3 0 0 0 35 13 0 0 0 0 0 0 0 0 0 1 1 1 0 0 0 0 0 13 37 0 0 4 000000000 301 SF-4 224 0 0 0 0 15 3 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 16 41 0 0 1000000000 300 SF-5 262 7 0 0 0 4 4 0 0 0 0 0 0 0 0 0 0 00000001200 0 2 0 0 0 0 0 0 0 0 0 300 SF-6 221 0 0 0 0 31 3 0 0 0 0 0 0 0 0 0 7 0 0 0 0 0 0 0 10 25 0 0 3 0 0 0 0 0 0 0 0 0 300 SF-7 220 13 0 0 0 8 5 0 0 0 0 0 0 0 0 0 2 0 0 0 0 0 0 0 9 42 0 0 4 0 0 0 0 0 0 0 0 0 303 SF-8 70 70 0 0 0 14 8 0 0 0 0 0 0 0 0 0 56 9 0 0 25 0 0 0 16 32 0 0 0 0 0 0 0 0 0 0 0 0 300 SF-9 61 82 0 0 0 3 0 0 0 0 0 0 0 0 0 0 22 50 0 0 30 0 0 7 15 31 0 0 0 0 0 0 0 0 0 0 0 0 301 SF-10 5 91 0 0 0 0 3 0 0 0 0 0 0 0 0 0 47 52 0 0 85 0 0 0 13 4 0 0 0 0 0 0 0 0 0 0 0 0 300 SF-11 0 105 0 0 0 0 0 0 2 0 0 0 0 0 0 0 24 0 0 0 102 0 0 0 8 12 0 0 0 0 0 0 0 0 0 0 0 0 253 SF-12 140 1 140 0 0 1 2 0 0 0 0 0 0 0 0 0 1 0 0 0 0 0 0 0 0 25 0 0 0 0 0 0 0 0 0 0 0 12 322 SF-13L 0 4 0 278 0 4 15 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 301 SF-13U 29 57 0 0 0 0 0 0 0 0 0 0 0 0 0 0 11 77 0 0 0 0 0 1 79 13 0 0 1 0 0 0 32 0 0 0 0 0 300 SF-14 0 111 0 0 0 0 0 0 0 0 0 0 0 0 0 0 37 10 0 0 124 17 0 0 4 0 0 0 0 0 0 0 0 0 0 0 0 0 303 SF-15 4 74 0 0 0 0 6 0 0 0 0 0 0 0 0 0 32 33 0 0 107 14 0 0 13. 23 0 0 0 0 0 0 0 0 0 0 0 0 306 SF-16 1 105 0 0 0 0 1 0 0 0 0 0 0 0 0 0 45 44 0 0 58 26 0 0 7 13 0 0 0 0 0 0 0 0 0 0 0 0 300 SHAGO CREEK SC-1 225 21 0 0 0 5 3 0 0 0 0 0 0 0 0 0 3 0 0 0 0 0 0 0 3 36 0 0 4 0 0 0 0 0 0 0 0 0 300 SC-2 12 46 0 0 0 0 0 0 0 0 0 0 0 0 0 0 60 38 0 0 8 6 0 0 9 19 0 0 8 0 0 0 0 0 0 0 0 0 206 SC-3 179 0 104 0 0 5 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 16 0 0 0 0 0 0 0 0 0 0 0 0 304 SC-5 3 116 0 0 0 0 3 0 0 0 0 0 0 0 0 0 66 47 9 0 4 0 0 0 15 24 0 0 21 0 0 0 0 0 0 0 0 0 308 SC-6 25 0 244 0 0 0 1 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 01020 0 0 0 000000000 300 SC-7 20 8 268 0 0 1 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 5 0 0 0 0 0 0 0 0 0 0 0 0 302 SC-8 243 11 0 0 0 1 2 0 0 0 0 0 0 0 0 0 6 0 0 0 0 0 0 0 2 24 0 0 11 0 0 0 0 0 0 0 0 0 300 SC-8T 72 1 183 0 0 0 1 0 0 0 0 0 0 0 0 0 1 2 0 0 0 0 0 0 21 25 0 0 1 0 0 0 0 0 0 0 0 0 307 SC-9 48 95 0 0 0 0 19 0 0 0 0 0 0 0 0 0 88 19 1 0 0 0 0 11 3 16 0 0 16 0 0 0 0 0 0 0 0 0 316 SC-10 30 8 149 0 0 1 0 0 0 0 0 0 0 0 0 0 9 35 0 0 6 0 0 0 45 23 0 0 0 0 0 0 0 0 0 0 0 0 306 SC-11 30 63 0 0 0 0 0 0 0 0 0 0 0 0 0 0 23 53 0 0 40 20 0 0 34 37 0 0 0 0 0 0 0 0 0 0 0 0 300 SC-12 15 73 0 0 0 0 0 0 0 0 0 0 0 0 0 0 25 20 0 0 152 6 0 0 6 3 0 0 0 0 0 0 0 0 0 0 0 0 300 R ( R CCAL COMPANY QUARRY RRP-1 84 64 0 0 0 7 0 0 0 0 0 0 0 0 0 29 52 0 0 0 6 0 0 25 31 0 0 0 0 0 0 0 0 0 0 0 0 300 RRP-2 0 95 0 0 0 0 0 0 0 0 0 0 0 0 0 12 12 0 0 173 7 0 1 0 2 0 0 0 0 0 0 0 0 0 0 0 0 302 RRP-3 101 32 70 0 0 0 0 0 0 0 0 0 0 0 0 9 8 0 0 25 0 0 0 12 40 0 0 0 0 0 0 0 0 0 0 0 0 300 RRP-4(1) 49 45 0 0 0 5 0 0 0 0 0 0 0 0 0 12 27 0 0 75 12 0 24 29250 0000 00 00 0 0 0 305 RRP-4(2) 3 112 0 0 0 0 0 0 0 0 0 0 0 0 0 19 15 0 0 101 39 0 0 9 500000000000 0 303 RRP-5 0 125 0 0 0 0 0 0 0 0 0 0 0 0 0 54 17 0 0 60 23 0 0 13 8 0 0 0 0 00000000 300 RR-1 109 0 0 0 0 0 0 65 0 0 0 0 0 0 23 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 300 RR-2 240 2 0 0 0 31 0 0 0 0 0 0 0 0 5 0 0 0 0 0 0 0 0 2 4 0 0 0 0 0 0 0 0 0 0 0 0 300 SLIDE TOO T HICK: RR-3 RR-4 200 13 9 0 0 32 17 0 0 0 0 0 0 0 0 2 3 0 0 0 0 0 0 0 0 27 0 0 0 0 0 0 0 0 0 0 0 0 303 RR-5 216 8 5 0 0 IS 0 12 0 0 0 0 0 0 0 0 2 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 42 0 0 0 0 0 300 RR-6 211 0 1 0 0 23 0 23 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 42 0 0 0 0 0 300 RR-7 244 1 0 0 0 18 0 7 0 0 0 0 0 0 0 2 0 0 0 0 0 0 0 0 1 27 0 0 0 0 00000000 300 U. S . HIGHWAY 64 RT.64-1 3 89 0 6 28 0 115 25 13 23 303 RT.64-2 165 10 12 23 23 0 0 0 24 43 311 RSHICK VALLEY RV-1 264 2 0 0 0 23 0 9 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 2 0 0 0 0 0 0 0 0 0 0 0 0 300 RV-2 220 3 0 0 0 29 0 18 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 4 26 0 0 0 0 0 0 0 0 0 0 0 0 300 RV-3 237 0 0 0 0 31 0 0 17 0 0 0 0 0 0 0 1 0 0 0 O' 0 0 0 0 14 0 0 0 0 0 0 0 0 0 0 0 0 300 RV-4 251 1 0 0 0 11 0 17 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 1 19 0 0 0 0 0 0 0 0 0 0 0 0 300 RV-5 232 1 0 0 0 8 0 2 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 3 54 0 0 0 0 00000000 300 KNœS-UNIW ROAD KU-1 143 39 0 0 0 11 0 0 0 0 0 0 0 0 0 0 17 21 0 0 10 12 0 8 11 8 0 0 0 0 0 0 30 0 0 0 0 0 310 KU-2 2 58 0 0 0 0 0 0 0 0 0 0 0 0 0 0 13 52 0 0 12931 0 0 6 9 0 0 0 0 0 0 0 0 0 0 0 0 300 KU-3 260 13 0 0 0 7 0 0 0 20 0 0 0 0 0 0 10 6 0 0 0 0 0 5 0 5 0 0 0 0 0 0 0 0 0 0 0 0 326 KU-4 225 20 0 0 0 3 0 0 0 4 0 0 0 0 0 0 7 3 0 0 0 1 0 7 331000000000 0 0 0 304 KU-5 173 0 77 0 0 12 4 0 0 0 0 0 0 0 0 0 3 13 0 0 0 0 0 0414000000000 0 0 0 300 KU-6 21 2 199 0 0 0 7 0 0 0 0 0 0 0 0 0 3 15 0 0 0 0 0 0 1 38 0 00000000000 286 KU-7 189 14 1 0 0 1 0 0 0 0 0 0 0 0 0 0 5 9 0 0 0 0 0 17 17 0 0 0 0 0 0 0 50 0 0 0 0 0 303 KU-8 77 43 0 0 0 0 0 0 0 0 0 0 0 0 0 0 14 49 0 0 5 11 0 14 52 40 0 00000000000 305 KU-9 244 16 0 0 0 31 7 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 1 0 0 0 0 0 0 0 0 0 0 0 0 299 KU-10 27 40 67 0 0 0 0 0 0 0 0 0 0 0 0 0 17 28 0 0 0 21 0 0 29 71 0 0 0 0 0 0 0 0 0 0 0 0 300 KU-11 266 0 0 0 0 31 0 6 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 1 0 0 0 0 0 0 0 0 0 0 0 0 304 KU-12.1 0 0 0 0 0 167 0 0 60 0 0 0 0 0 0 73 1 0 0 0 0 0 0 0 0 0 0 0 0 0 00000000 301 KU-12.2 230 0 0 0 0 62 8 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 300 KU-13L 123 0 0 0 0 149 3 0 0 0 0 0 0 0 0 24 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 299 KU-14 244 2 0 0 0 4 9 0 0 0 0 0 0 0 0 0 1 30 0 0 0 0 0 0 3 7 0 0 0 0 00000000 300 SALT SUlf HU R SPRINGS QUARRY S3-1 223 4 31 0 0 3 15 0 0 0 0 0 0 0 0 0 2 5 0 0 2 0 0 0 3 13 0 0 0 0 0 0 0 0 0 0 0 301 S3-2 106 13 0 0 0 0 4 0 0 0 0 0 0 0 0 0 8 24 0 0 102 22 0 0 11 11 0 0 0 0 0 0 0 0 0 0 0 301 S3-3 188 6 0 0 0 0 5 0 0 0 0 0 0 0 0 0 9 36 0 0 15 10 0 0 12 10 0 13 0 0 0 0 0 0 0 0 0 304 S3-4 89 56 0 0 0 0 5 0 0 0 0 0 0 0 0 0 7 25 0 0 1 9 0 0 7242 0 0 00 0 0 0 0 0 0 0 306 S3-5 171 16 0 0 0 0 0 9 0 0 0 0 0 0 0 0 3 2 0 0 0 9 0 0 48 38 0 4 0 0 0 0 0 0 0 0 0 300 S3-6 157 0 0 0 0 0 6 0 0 0 0 0 0 0 0 0 6 104 0 0 0 1 0 0 15 16 0 0 0 0 0 0 0 0 0 0 0 305 OJ cn MC CE DO MS HC QZ KT PY HE LI ZR PX AU PQ FS MI PE IN CG RF 00 CT OR PT PD SF CS AL FO BR OS BV BY TR CO SP GA BU TOTAL S3-7 207 7 0 0 0 0 2 0 0 0 0 0 0 0 0 0 9 27 0 0 0 8 0 0 15 40 0 0 2000000000 317 S3-8 153 12 0 0 0 0 0 0 0 0 0 0 0 0 0 0 6 27 0 0 42 20 0 0 9 31 0 0 0 0 0 0 0 0 0 0 0 0 300 S3-9 6 47 0 0 0 0 0 0 0 0 0 0 0 0 0 0 8 46 0 0 139 27 0 21 4 2 0 0 0 0 0 0 0 0 0 0 0 0 300 S3-10 166 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 2 27 0 0 51 9 0 0 9 35 0 0 0 0 0 0 0 0 0 0 0 0 299 ACHE LIKEST ONE QUARRY AO-1 177 1 0 64 7 0 0 0 0 0 0 0 0 0 1 1 0 0 0 0 0 0 28 21 0 0 0 0 0 0 0 0 0 0 0 0 300 AQ-2 252 8 0 27 3 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 10 0 0 0 0 0 0 0 0 0 0 0 0 300 AQ-3 154 4 0 29 7 0 0 0 0 0 0 0 0 0 16 37 0 0 0 3 0 0 19 31 0 0 0 0 0 0 0 0 0 0 0 0 300 AQ-4 245 14 0 10 6 0 0 0 0 0 0 0 0 0 1 0 0 0 0 0 0 0 8 16 0 0 0 0 0 0 0 0 0 0 0 0 300 AQ-S 134 20 0 40 11 0 0 0 0 0 0 0 0 0 3 17 0 0 0 3 0 0 34 38 0 0 0 0 0 0 0 0 0 0 0 0 300 AQ-6L,AQ-6U 226 11 0 10 19 0 0 0 0 0 0 0 0 0 7 9 0 0 0 1 0 0 5 11 0 0 1 0 0 0 0 0 0 0 0 0 300 AQ-7 253 0 0 30 3 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 14 0 0 0 0 0 0 0 0 0 0 0 0 300 AQ-8 215 0 13 11 3 0 0 0 0 0 0 0 0 0 5 0 0 0 0 0 0 0 5 48 0 0 0 0 0 0 0 0 0 0 0 0 300 AQ-9 129 7 0 0 0 0 0 0 0 0 0 0 0 0 11 11 0 0 0 3 0 0 43 9? 0 0 0 0 0 0 0 0 0 0 0 0 301 AQ-9U 129 32 0 0 0 0 0 0 0 0 0 0 0 0 28 10 0 0 0 41 0 0 19 41 0 0 0 0 0 0 0 0 0 0 0 0 300 AQ-10 130 1 0 14 2 0 0 0 0 0 0 0 0 0 3 10 0 0 36 37 0 0 11 56 0 0 0 0 0 0 0 0 0 0 0 0 300 AQ-11 253 0 15 9 13 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 10 0 0 0 0 0 0 0 0 0 0 0 0 300 AQ-12 217 28 16 29 10 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 300 AQ-13.1 269 0 6 14 6 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 5 0 0 0 0 0 0 0 0 0 0 0 0 300 AQ-13.2 245 0 0 10 8 0 0 0 0 0 0 0 0 38 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 301 AQ-14 241 0 12 10 0 25 0 0 0 0 0 0 0 12 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 300 AQ-15 1 94 0 0 0 0 0 0 0 0 0 0 0 0 18 24 0 0 139 20 0 0 2 2 0 0 0 0 0 0 0 0 0 0 0 0 300 G-1 261 0 31 6 0 0 0 0 0 0 0 0 2 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 300 G-2L 0 119 0 0 0 0 0 0 0 0 0 0 0 12 13 0 0 108 34 0 0 3 2 0 0 0 0 0 0 0 0 0 0 0 0 291 G-2Ü 0 99 1 0 0 0 0 0 0 0 0 0 0 10 7 0 0 21 27 0 0 4 31 0 0 0 0 0 0 0 0 0 0 0 0 200 A-1 149 7 2 20 0 0 0 0 0 0 0 0 0 0 2 22 0 0 0 5 0 0 78 15 0 0 0 0 0 0 0 0 0 0 0 0 300 A-2 48 37 13 2 0 0 0 0 0 0 0 0 0 0 0 17 0 0 0 2 0 0 112 69 0 0 0 0 0 0 0 0 0 0 0 0 300 A-3 250 6 30 3 0 0 0 0 0 0 0 0 4 0 0 0 0 0 0 0 0 0 2 0 0 0 0 0 0 0 0 0 0 0 0 304 A-4 0 0 2 0 0 0 0 0 0 0 0 0 0 41 32 0 0 11 25 0 0 38 60 0 0 0 0 0 0 0 0 0 0 0 0 301 A-5 270 0 16 9 0 0 0 0 0 0 0 0 1 0 0 0 0 0 0 0 0 0 4 0 0 0 000000000 300 KEY MS - MICRIT E PY - PYRITE FS - FEIQSPAR CT - COATED GRAINS FO - FORAMINIFERA CE - CALCIT E CEMENT HE - HEMATITE MI - MICA OR - ORGANICS BR - BRACHiœODS DO - DOLQHI TE U - LIMONITE PE - PELOIDS PT - PELLETS OS - OSTRACODS MS - MICROS PAR ZR - ZIRCON IN - INTRAOASTS PD - PEIMA DEBRIS BV - BIVALVES HC - HEMATX TE CEMENT PX - PYROXENE CG - CARBONATE GRAINS SF - SHELL FRAGMENTS BY - BRYOZOANS QZ - QUARTZ AU - AUGITE RF - ROCK ÎRAGMENTS CS - CALCISPHERES TR - TRILOaiTES MT - HETALL ICS PQ - POLYXLY QUARTZ 00 - OOIDS AL - ALGAE CO - CORAL Ca > -P* APPENDIX H Fauna! List 347 REGION 1 - WESIERN MARYLAND Çystoporates Treprâtome 348 SANG RUN QUARRY SR-1: Ostracods - common Comulitellid Calcispheres - common Foraminifera - common DEEP CREEK QUARRY Algae - rare DC-0: Bivalves (few) Fenestrate bryozoans - rare, molds trace fossils Diaphragmas? sp. - juvenile, rare DC-1: Brachiopods: Comtwsita sp.-rare SR-2: Ostracods - rare to common Diaphragmas sp.-common Foraminifera - rare to common Martinia? sp.-rare Calcispheres - common Ovatia sp.-rare Girvanella? - common Protoniella cf. P. parvus-common to rare Brachiopods - abundant to rare Ostracods-abundant Anthracospirifer oellaensis Calcispheres-abundant Composita subouadrata Foraminifera-abundant Diaphragmas cestriensis endothyrids Eumetria sp. Gastropod-rare Ovatia sp. Fenestrate bryozoans-hashy on outcrop Gastropods - rare DC-2: Brachiopods: all rare, flattened Anthracospirifer pcilaensis SR-3: Foraminifera - Endothyrids - abundant Composita subouadrata Calcispheres? - common Diaphragmas cf. £ . cestriensis Orthotetes kaskaskiensis Brachiopods Ovatia sp. Anthracospirifer pellaensis Protoniella? sp. Composita sp. Martinia sp. Ostracods-common Calcispheres-abundant Bryozoans - common Foraminifera-abundant Trepostomes endothyrids Çystoporates Algae - rare Girvanella Pelmatozoan debris - rare to common Sphaerocodiam Bivalves - rare DC-3; Brachiopods: common to abundant Rugose Coral - rare Anthracospirifer pellaensis Palaeacis sp. - rare Composita subouadrata Paladin chesterensis - rare Diaphragmas cestriensis Martinia contracta Gastropods - rare Orthotetes kaskaskiensis Straoarollus fEuomohalusl Protoniella parvus turreted Gastropods: rare to common SR-4: Foraminifera - Endothyrids - abundant Naticopsis fNaticopsisl Girvanella? sp. - rare Paladin chesterensis Calcispheres? - common Caicispheres-common to abundant Trepostomes - common Foraminifera-abundant endothyrids Brachiopods - abundant Trace fossils Anthracospirifer trellaensis Pelmatozoan debris-common on outcrop Composita subouadrata Diaphragmas cestriensis DC-4: Brachiopods: abundant Martinia sp. Anthracospirifer breckinridgensis Orthotetes kaskaskiensis Anthracospirifer pellaensis Composita subouadrata Diaphragmas cestriensis SR-5: Foraminifera - Endothyrids - rare Eumetria nsp. Eumetria vemeuliana Bryozoans - abundant Girtyella? sp. Archimedes sp. Ovatia sp. ramose Gastropods: common (float specimens collected in 1987, 1988) Naticopsis fNaticopsisl Straparollus fEuomphalusl Archimedes sp. Fenestella sensu lato Paladin chesterensis-common Protoniella sp. Foraminifera-abundant 349 endothyrids Paladin chesterensis - rare Biyozoans-rare Pelmatozoan debris-rare Bryozoans: common Archimedes sp. DO-5: Foraminifera-abundant Fenestella sensu lato endothyrids Trepostome sp. Rhabdomesonids Çystoporates OAKLAND QUARRY Foraminifera: common OQ-1: Paladin chesterensis-rare endothyrids Pelmatozoan debris - abundant Foraminifera-abundant Echinoid plate - rare endothyrids Bivalves (two morphotypes): rare to common others Bryozoans } Echinoderm columnals} rare REGION 2 - NORIH-CENTRAL WEST VIRGINIA Brachiopods } ROARING CREEK OQ-2: Brachiopods: rare Composita sp. indct. RC-1: Girvanella - rare Ovatia sp. RC-2: Pelmatozoan debris - rare Paladin chesterensis-rare Dasydad algae - rare Bryozoans } RC-5: Foraminifera - Endothyrids - common fenestrate } rare, in hand specimen RC-6 (top): non-fenestrate } Pelmatozoan debris (pentagonal lumen) Pelmatozoan debris Foraminifera - Endothyrids - common OQ-3: Foraminifera-common CANAAN QUARRY endothyrids Calcispheres?-common CQ-1: Foraminifera - Endothyrids - abundant OQ-4: Brachiopods: common to abundant CQ-3: Pelmatozoan debris - abundant Anthracospirifer rxllaensis Composita subouadrata CQ-8L: Foraminifera - Endothyrids - common Orthotetes kaskaskiensis Juvenile brachiopods CQ-10: Bivalves - pectens, some elongate (top) plants Bryozoans: rare to common on outcrop, storm shell lag UÜ. ROUTE 33 Archimedes so. Fenestella sensu lato 33-lL: Foraminifera - Endothyrids - common Lvropora sp. Rhabdomesonids 33-2L: Foraminifera - Endothyrids - rare Trepostome -2U: Foraminifera - Endothyrids - rare Cystoporate Pelmatozoan debris - some large 33-5: Foraminifera - Endothyrids - rare Rugose coral - rare 33-7L: Foraminifera - Endothyrids - common OQ-5: Foraminifera: Endothyrids - abundant Pelmatozoan debris - common, small -7M: Pelmatozoan debris - common, small OQ-6: Brachiopods: abundant -7U: Foraminifera - Endothyrids - common Anthracospirifer pellaensis Composita sp. BUTCHER QUARRY Orthotetes kaskaskiensis Protoniella? sp. B-l-B-5: Foraminifera - Endothyrids (small) - rare Paladin chesterensis - rare B-7: Girvanella - common Bryozoans: common fenestrate B-8-B-9: Foraminifera - Endothyrids (small) - rare rhabdomesonids trepostomes B-10: trace fossils Pelmatozoan debris - abundant Foraminifera - Endothyrids - rare OQ-7: Brachiopods: common to abundant B-13: Anthracospirifer pellaensis Anthracospirifer pellaensis "Composita’-like - small Composita subouadrata Orthotetes kaskaskiensis Paladin chesterensis - rare SF-2: Pelmatozoan debris Foraminifera - Endothyrids - rare to Brachiopods - small 350 common Pelmatozoan debris - abundant, small SF-3: Pelmatozoan debris Bivalves Foraminifera - Endothyrids - common Echinoid spines - few Dasydad algae - rare Rugose coral - rare Girvanella? sp. - rare to common SF-4: Pelmatozoan debris (pentameral lumen) Rugose Coral MOmERVnXE QUARRY Foraminifera - Endothyrids - common M-1: Brachiopods - abundant SF-5: Pelmatozoan debris - tiny Anthracospirifer pellaensis (rare) Foraminifera - Endothyrids - common Echinochoncus sp. Girvanella - common Inflatia inflatus Calcispheres - rare Ovatia sp. Productid brachiopod (with distinct SF-6: Pelmatozoan debris - small, some large spine bosses - Antiouatonia?') Foraminifera - Endothyrids - common Girvanella - rare Pelmatozoan debris - rare Ostracods? - common to rare SF-7: Pelmatozoan debris - small Foraminifera - Endothyrids - common to rare M-S: Foraminifera - Biserial - abundant Calcispheres - rare Calcispheres? - abundant SF-8: Composita? sp. M-6: Brachiopods - abundant Anthracospirifer trellaensis Pelmatozoan columnals - small Composita sp. Pterotocrinus? sp. Diaphragmas so. Foraminifera - Endothyrids - rare Eumetria? sp. Girvanella? sp. - rare Inflatia inflatus Martinia? sp. SF-9: Pelmatozoan debris - abundant, small, some Orthotetes sp. larger Blastoid - Pentremites sp. - rare Rugose coral Dasydad algae - rare Foraminifera - Endothyrids - rare Rugose coral - rare M-7: Foraminifera - abundant Endothyrids SF-10: Pelmatozoan debris - Biserial Encrusting bryozoans Brachiopods - unident. KENTON MEADOWS QUARRY SF-11: Pelmatozoan debris - rare KM-1: Productid Brachiopods Foraminifera - Endothyrids Calcispheres? - rare Dasydad algae - rare KM-2: Productid brachiopod SF-12: Pelmatozoan debris - rare Ostracods - rare Burrows Foraminifera - common SF-13: Pelmatozoan debris - abundant KM-4L: Burrows Foraminifera - Endothyrids - rare -4U: Pelmatozoan debris - common, small Dasyciad algae - rare KM-5: Foraminifera - Endothyrids - common SF-14: Composita? sp. Dasydad algae - common Bivalves - rare KM-7: Pelmatozoan debris - rare Gastropods - small Abundant small bivalved shells KM-9: Foraminifera - Endothyrids - common Dasydad algae - rare SF-15: Pelmatozoan debris - common Foraminifera - Endothyrids - rare KM-10: Pelmatozoan debris - abundant Diaphragmas? sp. - rare SF-16: Pelmatozoan debris - common Algae - abundant REGION 3 - SOUTHEASmRN WEST Girvanella VIRGINIA Dasydad SLATY FORK QUARRY R & R COAL COMPANY QUARRY SF-1: Foraminifera - endothyrids - rare RRP-1: Composita? sp. - rare Dasydad algae - rare Pelmatozoan debris - abundant, some encrusting very large, Gastropods - turreted & planar 351 many small Blastoids - rare Rugose coral - rare Ostracods? - rare Foraminifera - Endothyrids - rare Echinoid spines bosses - rare Cephalopod - rare RRP-2: Pelmatozoan debris - common Foraminifera - Endothyrids - rare SWAGO CREEK RRP-3: Pelmatozoan debris - common SC-1: Ovatia? sp. Foraminifera - Endothyrids - rare Anthracospirifer pellaensis - abundant molds RRP-4: Pelmatozoan debris - common Pelmatozoan debris - common Foraminifera - common Syringoporid coral Endothyrids Biserial Foraminifera - Endothyrids - abundant Calcispheres? - RRP-5: Pelmatozoan debris - common Foraminifera - rare SC-2: Foraminifera - Endothyrids - abundant Endothyrids Biserial SC-3: Ostracods Calcispheres RR-1: Inarticulate brachiopods - outcrop SC-5: Foraminifera - Endothyrids - abundant RR-2: Inflatia inflatus - abundant SC-6: Pelmatozoan debris - rare Trepostome bryozoans SC-8: Pelmatozoan debris - rare Pelmatozoan debris - common Foraminifera - Endothyrids - common Ostracods? - common Ostracods - common Calcispheres - common RR-5; Brachiopods - abundant, small Girvanella? sp. - common Composita? sp. Anthracospirifer sp. SC-9: Foraminifera - Endothyrids - very abundant Girtyella? sp. Dasyciad algae - common Pelmatozoan debris - abundant SC-10: Pelmatozoan debris - rare, small Bryozoans - Archimedes sp. - abundant Foraminifera - Endothyrids - common Trepostomes Rugose coral - rare Rugose coral SC-11: Spiriferid brachiopod RR-6: Brachiopods - small Pelmatozoan debris Comrx>sita?-like Dasyciad algae - common Bryozoans - SC-12: Algae - common Rhabdomesonids - few Girvanella Trepostomes Dasyciad Archimedes sp. Pelmatozoan debris - abundant RENICK VALLEY RR-7: Brachiopods - small Composita?-like RV-1: Burrows - abundant, nobby clusters Eumetria sp. - rare Inflatia inflatus Inarticulate brachiopods - rare Pelmatozoan debris - abundant, some RV-2: Brachiopods large Com ^ita sp. Blastoids - rare, Pentremites sp. Rueosochonetes sp. Spiriferids Bryozoans - abundant Productids Archimedes sp. encrusting - button-shaped, flat RV-3: Brachiopods Composita sp. RR-float: White oolitic zone from pit Composita-like. small Spiriferid Diaphraemus sp. - common, brachial valves exterior up RV-4: Anthracospirifer pellaensis - abundant Composita? sp./Martinia? Rueosochonetes sp. - abundant sp. - abundant Pelmatozoan debris - common Bryozoans - encrusting (common) Bivalves - small, some large fenestrate - rare flat specimens Bryozoans - fenestrates RV-5: Brachiopods Comoosita-like - abundant, tiny KU-2: Pelmatozoan debris - small, rare Comooslta sp. Pentremites tulirraformis 3 5 2 Inflatia inflatus Brachiopods - unident. - rare Orthotetes sp. Dasyciad algae - common Productid Rueosochonetes sp. KU-3: Pelmatozoan debris - common Pterotocrinus sp. - rare to common Pelmatozoan debris - rare Blastoid - tare Blastoids - common Pentremites pulchellis Bryozoans Pentremites tulioaformis Archimedes sp. - abundant Rugose coral - rare encrusting rhabdomesid • tiny Bryozoans - Fenestrates - rare Rugose coral - rare Bivalves - rare KU-4: Brachiopods Composita? sp. US. ROUTE 64 Productid spiriferid 64-1,2: Dasyciad algae - rare Pelmatozoan debris - common, small ALDERSON Pentremites sp. - rare to common A-1: Brachiopods - rare Foraminifera - Endothyrids - rare Anthracospirifer pellaensis Bryozoans - fenestrates Composita-like - small Rugose coral - rare Eumetria? - small Girvanella - rare Pelmatozoan debris - small KU-5: Pentremites tulipaformis - rare Foraminifera - Endothyrids - rare Archimedes sp. - common A-2: Pelmatozoan debris - common Rugose corals - rare Brachiopods - unident. - rare Brachiopods - unident. KU-6: Brachiopods - rare Bryozoans Cleiothvridina? sp. Archimedes sp. - abundant productids encrusting - abundant Foraminifera - Endothyrids - rare A-3: Pelmatozoan debris - common Pelmatozoan debris - abundant, small Pentremites tulipaformis - rare to common Bryozoans fenestrate - abundant Bryozoans Archimedes sp. - rare to common A-4: Brachiopods - rare bifoliate? Reticularia sp. Rugose Coral - rare Rugosochonetes sp. Dasyciad algae - rare Pelmatozoan debris - abundant KU-7: Brachiopods - rare Foraminifera - Endothyrids - common Cleiothvridina? sp. Bryozoans unidentified genus fenestrates - common to abundant Foraminifera - Endothyrids - rare Girvanella - abundant Pelmatozoan debris - abundant, small to medium, A-5: Brachiopods 5-fold lumen Anthracospirifer trellaensis - rare Pentremites tulipaformis - rare Composita sp. - rare Rugose coral - rate Diaphragmas sp. - abundant, small KU-8: Pelmatozoan debris - small, 5-fold lumen Pelmatozoan debris - abundant Pentremites sp. - rare to common Foraminifera - common Bryozoans Endothyrids fenestrates - abundant Biserial Archimedes sp. Uniserial Rugose coral - rare KNOBS-UNION ROAD Algae - Girvanella - rare KU-1: Pentremites sp. Dasyciad - common Foraminifera - Endothyrids - rare Algae - rare KU-10: Brachiopods Girvanella Composita? sp. Dasyciad Diaphragmus? sp. spiriferid AQ-S: Pelmatozoan debris - rare to common, Foraminifera - Endothyrids - rare small 353 Pclmatozoan debris • rare lo common Brachiopods - rare Pentremites sp. Dasyciad algae - rare Pterotocrinus serratus AQ-6L: Pelmatozoan debris - common, small Bryozoans Foraminifera - endothyrids - common fenestrates Girvanella sp. - common Flstulipora sp. Ostracods - common to rare Calcispheres - common Paladin chesterensis Bryozoans - rare Rugose coral - rare Corals Rugose AQ-6U: Pelmatozoan debris - common, small Syringoporid Girvanella - common KU-12: Pelmatozoan debris - rare AQ-7: Girvanella - common Bryozoans - fenestrate - rare AQ-8: Pelmatozoan debris - abundant, some large KU-13: Brachiopods Biyozoans - fenestrate, abundant Composita sp. Paladin chesterensis - rare productid Pentremites sp. - common Productid brachiopods - common Pelmatozoan debris - abundant Pterotocrinus sp. AQ-9: Pelmatozoan debris - abundant Blastoids - rare to common rugose coral - rare Biyozoans - common Foraminifera - Endothyrids - rare to common fenestrates ramose AQ-9U: Pelmatozoan debris - abundant to common Rugose coral - rare AQ-10: Brachiopods - tiny, unidentified, common KU-14: Brachiopods - rare to abundant Pelmatozoan debris - abundant Anthracospirifer pellaensis Eumetria sp. Gastropod - rare Inflatia inflatus Martinia sp. AQ-15: Pelmatozoan debris - abundant Rueosochonetes sp. rhynchonellid? SALT SULPHUR SPRINGS QUARRY Pelmatozoan debris - small Pentremites sp. S^-2: Anthracospirifer pellaensis - rare Rugose coral - rare Bryozoans - fenestrates Foraminifera - Endothyrids - rare Gastropods - rare S®-3: Pelmatozoan debris - abundant Rugose coral - rare ACME QUARRY Foraminifera - Endothyrids - rare Girvanella - abundant AQ-1: Anthracospirifer pellaensis - rare S®-4: Brachiopods Pelmatozoan debris - abundant, small Anthracospirifer pellaensis Girvanella sp. - common Comtmsita sp. AQ-2: Pelmatozoan debris - rare, small Pelmatozoan debris - abundant, small Brachiopods - rare Encrusting bryozoans - rare AQ-3: Pelmatozoan debris - common to abundant, small S-’-S: Brachiopods - Spiriferid, rare Brachiopods - rare Algae - rare Pelmatozoan debris - abundant Dasyciad Blastoid - Pentremites sp. Sphaerocodlum Foraminifera - rare Dasyciad algae - rare AQ4: Pelmatozoan debris - rare, small Ostracods - abundant S^-6: Brachiopods Foraminifera - Endothyrids - rare Protoniella? sp. - rare Rugose coral - rare Brachiopods - rare Pelmatozoan debris - common Pentremites sp. - common Bryozoans common to abundant Archimedes sp. Composita? sp. encrusting Blastoid 354 Foraminifera - rare Girvanella - rare G R EBN VnXE S®-7: Brachiopods - Spiriferid, rare G-2L: Brachiopods Anthracospirifer trellaensis Pelmatozoan debris - abundant Pentremites sp. - common Pelmatozoan debris - abundant, small to medium Bryozoans Pentremites sp. - abundant plates Archimedes sp. - abundant Pterotocrinus serratus- wing plates Rugose coral - common to rare Rugose coral Foraminifera - rare Dasyciad algae • rare Girvanella - rare G-2U: Brachiopods - rare Brachiopods Ctomposita sp. Reticularia? sp. - rare Eumetria sp. - juvenile (1) Pelmatozoan debris - abundant, small (unusual plates) Pelmatozoan debris - abundant Rugose coral - rare Blastoid - Pentremites sp. - rare Gastropods • rare, small Dasyciad algae • rare Bryozoans - rare Archimedes sp. Fenestella sensu lato encrusting Rugose coral - rare Algae - common Girvanella Sphaerocodlum S^-9: Algae - rare Girvanella Sphaerocodlum - common Dasyciad S -10:Algae - common Girvanella Sphaerocodlum S^-Float from top bench (approximately unit S^- 10) Anthracospirifer sp. Composita sp. Girtyella? sp. Martinia sp. Reticularia sp. Rhynchonellid unidentified brachiopods Rugose coral Pelmatozoan debris - abundant Blastoids - Pentremites sp. - abundant Pterotocrinus serraius - wing plates Archimedes sp. S^-Midwaii Float - Wackestone Composita sp. Diaphraemus? sp. Orthotetes sp. Reticularia sp. spiriferid small unidentified brachiopods Archimedes so. Bivalve S^-Midwall Float - Oolitic Grainstone Rugose Coral fenestrate bryozoans APPENDIX I Cluster Analysis Data 355 LOCALITY SR DC OQ RC US MQ KM CQ BQ SF RR RV us KU sss AL AQ GV TAXON 33 64 Anthracospirifer breddnridsensis X Anthracospirifer pellaensis XXXX X XXXX XX X C le io th v r id in a sp . X Composita subouadrata XXXX X XX XXXXX Diaphraem us cestriensis X X XXX X X XXX E c h in o c o n c h u s sp . X Eumetria vemeuliana XXXX XXX Eum etria n. sp. X GirtveUasp. XX X Inflatia inflatus XX X X M artinia contracta XXX XX Orthotetes kaskaskiensis X X XXX X O v a tia s p . X X X Protoniella parvus XX X Reticularia sp. X XX Rueosochonetes sp. XXX Paladin chesterensis X X XXX X Archimedes SP. X X XXXX X Trepostomes X X Çystoporates X X Rhabdomesonids X X X X P e n tre m ite s sp p . X X X XX X Pterotocrinus X XX X CO C J l cn LOCALITY SR DC OQ RC US MQ KM CQ BQ SF RR RV US KU SSS AL AQ GV TAXON 33 64 Pelmatozoan debris XX XXXXX XXX XXX X XXX Rugose corals X XX XX XXX XX XX SvringODoracea X NaiicoDsis (Naticovsis) X Straoarollus (Euormhalus) X X Endothyraceans X XX XX X XXXX X X XX X Biserial foraminifera X X X Uniserial foraminifera X Aviculopecten X Bivalves XX XXXXX Calcispheres X XXX X XX Ostracods XXX X G ir v a n e lla XX XXX Dasvclads X X X SDhaerocodium sd. X X P a la e a c is SD. X Lyroporellasp. X W en APPENDIX J Anthracospirifer pellaensis measurements 358 CORRBCIBD MORPH ACCORDING TO DISCRIKNANT FUNCTION ANALYSIS ALRATIO OBS LOCALITY MORPH HINGE MAXHIDTH LENGTH WIDTH RIBS HLRATIO HLRATIO ALATION A 36.5 36.5 22.4 31.6 9 1.62946 1.62946 1.15506 0.0515653 1 1.11888 0.0490737 2 N 32.0 32.0 22.8 28.6 10 1.40351 1.40351 3 H 31.0 31.0 23.7 26.6 9 1.30802 1.30802 1.16541 0.0491736 4 A 33.0 33.0 22.4 27.3 11 1.47321 1.47321 1.20879 0.0539639 5 R 25.7 27.4 21.4 26.5 8 1.20093 1.28037 0.96981 0.0453183 6 N 25.6 25.6 23.9 27.0 9 1.07113 1.07113 0.94815 0.0396715 7 I 25.0 25.6 19.3 25.9 8 1.29534 1.32642 0.96525 0.0500130 8 N 24.8 24.8 21.4 23.7 8 1.15888 1.15888 1.04641 0.0488978 9 A 28.8 28.8 18.0 24.8 11 1.60000 1.60000 1.16129 0.0645161 10 N 23.0 23.0 18.0 21.2 8 1.27778 1.27778 1.08491 0.0602725 11 R 15.0 17.0 14.0 16.7 8 1.07143 1.21429 0.89820 0.0641574 12 R 14.6 17.2 13.2 17.0 7 1.10606 1.30303 0.85882 0.0650624 13 R 9.0 12.4 9.0 12.4 8 1.00000 1.37778 0.72581 0.0806452 R 6.3 10.5 7.3 10.5 7 0.86301 1.43836 0.60000 0.0821918 14 0.0395854 15 A 31.7 31.7 26.0 30.8 9 1.21923 1.21923 1.02922 16 A 39.0 39.0 24.8 29.3 10 1.57258 1.57258 1.33106 0.0536717 17 A 34.6 37.7 24.6 35.0 9 1.40650 1.53252 0.98857 0.0401858 18 I 34.0 34.0 23.5 27.4 8 1.44681 1.44681 1.24088 0.0528032 19 R 21.3 27.3 21.0 26.3 8 1.01429 1.30000 0.80989 0.0385660 20 I 28.0 29.0 20.8 27.6 9 1.34615 1.39423 1.01449 0.0487737 21 I 31.0 32.0 20.2 29.0 8 1.53465 1.58416 1.06897 0.0529191 22 I 26.4 26.4 18.8 23.3 8 1.40426 1.40426 1.13305 0.0602685 23 A 27.2 27.2 17.2 22.0 10 1.58140 1.58140 1.23636 0.0718816 24 N 30.6 30.6 17.0 23.8 9 1.80000 1.80000 1.28571 0.0756303 25 I 26.5 27.0 19.0 24.0 8 1.39474 1.42105 1.10417 0.0581140 26 N 25.3 25.3 19.2 21.7 8 . 1.31771 1.31771 1.16590 0.0607239 27 I 26.0 25.6 18.5 24.2 9 1.40541 1.38378 1.07438 0.0580746 28 I 22.3 24.8 16.3 23.5 8 1.36810 1.52147 0.94894 0.0582169 29 N 30.0 30.0 20.4 22.0 8 1.47059 1.47059 1.36364 0.0668449 30 I 26.0 27.3 18.8 25.0 8 1.38298 1.45213 1.04000 0.0553191 31 I 20.8 22.3 15.0 20.6 7 1.38667 1.48667 1.00971 0.0673139 32 I 19.4 22.3 15.4 21.9 7 1.25974 1.44805 0.88584 0.0575224 33 R 19.0 19.4 15.6 18.6 8 1.21795 1.24359 1.02151 0.0654811 34 I 18.4 20.0 13.8 17.6 8 1.33333 1.44928 1.04545 0.0757576 35 N 34.5 34.5 22.3 33.0 11 1.54709 1.54709 1.04545 0.0468814 36 N 38.3 38.3 24.1 30.0 9 1.58921 1.58921 1.27667 0.0529737 37 N 33.5 33.5 22.4 30.5 7 1.49554 1.49554 1.09836 0.0490340 38 A 40.0 40.0 23.2 27.2 8 1.72414 1.72414 1.47059 0.0633874 39 N 32.6 32.6 22.0 28.8 11 1.48182 1.48182 1.13194 0.0514520 40 A 38.0 38.0 24.2 ■ 28.3 9 1.57025 1.57025 1.34276 0.0554858 41 N 34.0 34.0 28.8 30.8 9 1.18056 1.18056 1.10390 0.0383297 42 A 34.0 34.0 23.0 30.0 10 1.47826 1.47826 1.13333 0.0492754 43 I 31.0 31.0 20.0 28.7 11 1.55000 1.55000 1.08014 0.0540070 44 I 29.4 29.4 20.0 26.6 10 1.47000 1.47000 1.10526 0.0552632 45 I 27.0 27.0 18.5 25.5 7 1.45946 1.45946 1.05882 0.0572337 46 I 32.0 32.0 24.4 30.0 8 1.31148 1.31148 1.06667 0.0437158 47 R 23.7 25.7 19.8 24.8 9 1.19697 1.29798 0.95565 0.0482649 48 N 26.2 26.2 18.8 24.0 8 1.39362 1.39362 1.09167 0.0580674 49 A 31.8 31.8 21.7 27.2 9 1.46544 1.46544 1.16912 0.0538764 50 I 21.7 24.0 16.8 21.3 8 1.29167 1.42857 1.01878 0.0606416 51 R 24.0 27.4 22.4 26.6 7 1.07143 1.22321 0.90226 0.0402793 52 R 22.6 22.6 22.3 22.0 1.01345 1.01345 1.02727 0.0460660 53 R 14.6 19.0 17.8 18.5 9 0.82022 1.06742 0.78919 0.0443365 CO 54 R 17.7 19.5 19.3 18.7 8 0.91710 1.01036 0.94652 0.0490427 cn 55 R 21.6 23.4 19.6 22.7 8 1.10204 1.19388 0.95154 0.0485481 UD CORRECTED MORPH RCCORDIHQ TO DISCRIKHAMT FUNCTION M U LTSIS ALATION ALRATIO OBS LOCALITY MORPH HINGE MAXWIDIH LENGTH WIDTH RIBS HLRATIO HLRATIO 1.18919 0.0720721 56 |] 22.0 22.0 16.5 18.5 9 1.33333 1.33333 I 30.0 30.0 23.6 26.0 8 1.27119 1.27119 1.15385 0.0488918 57 1.00000 0.0515464 58 I 24.0 26.0 19.4 24.0 7 1.23711 1.34021 23.0 26.5 16.0 25.4 8 1.43750 1.65625 0.90551 0.0565945 59 0.95238 0.0517598 60 p 20.0 22.0 18.4 21.0 8 1.08696 1.19565 p 14.6 16.0 13.0 15.9 8 1.12308 1.23077 0.91824 0.0706338 61 0.82278 0.0685654 62 I 13.0 16.8 12.0 15.8 8 1.08333 1.40000 I 16.0 16.0 13.2 16.3 8 1.21212 1.21212 0.98160 0.0743633 63 1.06034 0.0623732 64 I 24.6 24.6 17.0 23.2 8 1.44706 1.44706 p 27.6 27.6 17.3 23.0 9 1.59538 1.59538 1.20000 0.0693642 65 1.18227 0.0729794 66 I 24.0 24.0 16.2 20.3 10 1.48148 1.48148 p 25.6 25.6 17.4 22.4 7 1.47126 1.47126 1.14286 0.0656814 67 1.09453 0.0521204 68 R 22.0 22.0 21.0 20.1 10 1.04762 1.04762 p 25.3 19.3 23.1 9 1.31088 1.31088 1.09524 0.0567481 69 25.3 0.0663669 70 P 24.8 24.8 17.3 21.6 9 1.43353 1.43353 1.14815 I 19.4 21.0 16.3 20.5 10 1.19018 1.28834 0.94634 0.0580578 71 0.0533428 72 p 22.5 22.5 19.0 22.2 7 1.18421 1.18421 1.01351 P 26.0 26.0 15.0 21.7 7 1.73333 1.73333 1.19816 0.0798771 73 0.0664267 74 I 20.3 21.1 16.0 19.1 7 1.26875 1.31875 1.06283 P 25.0 25.0 15.3 21.7 9 1.63399 1.63399 1.15207 0.0752989 75 0.0626012 76 N 23.2 23.2 17.0 21.8 10 1.36471 1.36471 1.06422 77 A 41.0 41.0 25.2 29.0 10 1.62698 1.62698 1.41379 0.0561029 78 A 48.0 48.0 24.0 30.8 12 2.00000 2.00000 1.55844 0.0649351 79 A 43.0 43.0 23.6 29.8 11 1.82203 1.82203 1.44295 0.0611421 80 A 33.6 33.6 17.2 25.0 10 1.95349 1.95349 1.34400 0.0781395 81 p 40.0 40.0 24.2 29.8 9 1.65289 1.65289 1.34228 0.0554662 82 A 32.5 32.5 24.0 25.4 10 1.35417 1.35417 1.27953 0.0533136 83 P 34.7 34.7 20.3 27.0 8 1.70936 1.70936 1.28519 0.0633096 84 p 33.0 33.0 22.4 27.3 7 1.47321 1.47321 1.20879 0.0539639 85 p 36.0 36.0 24.2 27.2 9 1.48760 1.48760 1.32353 0.0546913 86 p 32.0 32.0 22.8 26.3 8 1.40351 1.40351 1.21673 0.0533654 87 p 27.5 27.5 19.2 23.0 8 1.43229 1.43229 1.19565 0.0622736 88 p 23.6 25.0 20.4 23.5 8 1.15686 1.22549 1.00426 0.0492282 89 P 23.0 23.0 17.6 29.5 9 1.30682 1.30682 0.77966 0.0442989 90 R 16.5 21.2 18.2 20.5 8 0.90659 1.16484 0.80488 0.0442241 91 P 21.0 21.0 19.6 20.3 8 1.07143 1.07143 1.03448 0.0527797 92 R 18.0 20.2 19.0 19.7 7 0.94737 1.06316 0.91371 0.0480898 93 R 19.2 21.0 16.9 20.7 8 1.13609 1.24260 0.92754 0.0548838 94 R 15.4 19.0 17.7 18.5 8 0.87006 1.07345 0.83243 0.0470301 95 P 13.2 19.4 17.0 19.2 7 0.77647 1.14118 0.68750 0.0404412 96 P 15.3 17.9 17.0 17.4 9 0.90000 1.05294 0.87931 0.0517241 97 P 28.0 28.0 20.8 25.7 9 1.34615 1.34615 1.08949 0.0523795 98 P 31.5 31.5 18.2 25.0 10 1.73077 1.73077 1.26000 0.0692308 99 N 25.6 25.6 19.7 23.0 9 1.29949 1.29949 1.11304 0.0564997 100 I 23.0 23.0 19.5 21.0 9 . 1.17949 1.17949 1.09524 0.0561661 101 p 20.0 21.0 19.0 20.4 9 . 1.05263 1.10526 0.98039 0.0515996 102 N 17.2 17.2 19.7 23.3 7 0.87310 0.87310 0.73820 0.0374720 103 A 31.6 31.6 21.0 23.0 11 1.50476 1.50476 1.37391 0.0654244 104 P 24.7 24.7 20.0 23.5 8 1.23500 1.23500 1.05106 0.0525532 105 N 22.6 22.6 19.8 22.3 9 1.14141 1.14141 1.01345 0.0511845 106 I 25.0 25.0 12.8 21.3 9 1.95313 1.95313 1.17371 0.0916960 107 A 13.8 13.8 16.0 22.7 10 0.86250 0.86250 0.60793 0.0379956 108 N 26.8 26.8 15.4 . 19.3 9 1.74026 1.74026 1.38860 0.0901689 109 R 19.1 23.0 21.3 22.0 7 0.89671 1.07981 0.86818 0.0407597 110 I 17.6 19.8 16.2 \ 19.0 8 1.08642 1.22222 0.92632 0.0571800 CORRECTED MORPH ACCORDING TO DISCRIHHANT FUNCTION ANALYSIS DBS LOCALITY MORPH HINGE MAXHIDIH LENGTH WIDTH RIBS HLRATIO MLRATIO ALATION ALRATIO 1.16972 0.064985 111 5 N 25.5 25.5 13.0 21.8 9 1.41667 1.41667 112 5 I 25.5 25.5 19.4 24.1 7 1.31443 1.31443 1.05809 0.054541 113 5 I 24.1 24.1 18.7 22.8 1.28877 1.28877 1.05702 0.056525 114 5 I 20.0 20.0 14.4 19.0 9 1.38889 1.38889 1.05263 0.073099 115 5 R 19.0 19.0 18.8 19.5 8 1.01064 1.01064 0.97436 0.051828 116 5 R 20.2 20.2 19.0 19.2 9 1.06316 1.06316 1.05208 0.055373 117 5 R 20.0 21.5 17.4 21.0 9 1.14943 1.23563 0.95238 0.054735 118 5 R 13.6 IB.O 14.2 17.5 9 0.95775 1.26761 0.77714 0.054728 119 5 R 23.2 23.2 19.5 20.8 8 1.18974 1.18974 1.11538 0.057199 25.7 25.7 19.6 23.0 8 1.31122 1.31122 1.11739 0.057010 120 5 N 0.061901 121 5 N 27.0 27.0 19.3 22.6 8 1.39896 1.39896 1.19469 122 5 I 26.5 26.5 18.0 24.6 9 1.47222 1.47222 1.07724 0.059846 123 5 N 22.1 22.1 16.4 21.8 9 1.34756 1.34756 1.01376 0.061815 124 5 I 20.2 20.2 14.4 19.0 8 1.40278 1.40278 1.06316 0.073830 125 5 R 19.4 22.0 18.7 21.7 8 1.03743 1.17647 0.89401 0.047808 126 5 I 21.4 21.4 16.1 19.0 9 1.32919 1.32919 1.12632 0.069958 127 5 I 20.0 20.0 14.0 17.8 7 1.42857 1.42857 1.12360 0.080257 128 5 R 17.5 21.0 16.5 20.3 8 1.06061 1.27273 0.86207 0.052247 129 5 I 20.3 21.3 14.1 19.6 9 1.43972 1.51064 1.03571 0.073455 130 5 I 20.2 20.2 14.0 19.4 8 1.44286 1.44286 1.04124 0.074374 131 5 I 18.6 2 0 .0 14.1 18.7 8 1.31915 1.41844 0.99465 0.070543 132 5 A 26.6 26.6 13.0 19.8 8 2.04615 2.04615 1.34343 0.103341 133 6 I 19.1 22.7 16.6 21.1 8 1.15060 1.36747 0.90521 0.054531 134 6 I 20.2 22.0 18.6 20.8 7 1.08602 1.18280 0.97115 0.052213 135 6 I 18.5 23.0 15.8 22.8 7 1.17089 1.45570 0.81140 0.051355 136 6 I 21.0 21.0 18.0 21.5 7 1.16667 1.16667 0.97674 0.054264 137 6 I 15.7 21.0 17.0 22.6 0.92353 1.23529 0.69469 0.040864 138 6 A 22.6 22.6 17.0 19.0 7 1.32941 1.32941 1.18947 0.069969 139 6 R 18.0 24.4 19.0 20.0 6 0.94737 1.28421 0.90000 0.047368 140 6 R 16.3 2 0 .0 18.0 0.90556 1.11111 141 7 A 25.0 25.0 17.0 18l0 1.47059 1.47059 ll38889 0l081699 142 7 I 25.0 25.0 17.0 23.0 8 1.47059 1.47059 1.08696 0.063939 143 7 I 20.0 27.0 19.0 26.8 7 1.05263 1.42105 0.74627 0.039277 144 7 N 26.0 26.0 19.5 24.6 8 1.33333 1.33333 1.05691 0.054201 145 7 I 24.4 24.4 2 0.2 25.3 8 1.20792 1.20792 0.96443 0.047744 146 8 N 25.0 25.0 24.8 27.3 7 1.00806 1.00806 0.91575 0.036925 147 8 A 22.0 22.0 13.0 6 1.69231 1.69231 148 8 I 22.0 22.0 18.6 22'.3 10 1.18280 1.18280 ol98655 0.053040 149 8 R 24.0 24.0 24.0 24.7 6 1.00000 1.00000 0.97166 0.040486 150 8 A 24.6 24.6 15.4 19.5 6 1.59740 1.59740 1.26154 0.081918 151 8 N 29.3 29.3 23.1 27.0 1.26840 1.26840 1.08519 0.046978 152 8 A 30.0 30.0 16.6 23.0 7 1.80723 1.80723 1.30435 0.078575 153 8 N 26.0 26.0 20.0 24.8 9 1.30000 1.30000 1.04839 0.052419 154 8 I 21.0 21.0 17.5 20.6 1.20000 1.20000 1.01942 0.058252 155 8 I 18.0 18.0 16.5 18.4 1.09091 1.09091 0.97826 0.059289 156 1 N 34.8 34.8 23.0 29.4 8 1.51304 1.51304 1.18367 0.051464 157 1 A 35.0 35.0 22.0 26.0 9 1.59091 1.59091 1.34615 0.061189 158 1 N 30.5 30.5 22.3 28.0 8 1.36771 1.36771 1.08929 0.048847 159 1 N 34.8 34.8 21.5 28.5 8 1.61860 1.61860 1.22105 0.056793 160 1 N 34.8 34.8 23.2 28.8 8 1.50000 1.50000 1.20833 0.052083 161 1 A 26.7 26.7 16.8 24.3 10 1.58929 1.58929 1.09877 0.065403 162 1 I 25.6 25.6 17.8 22.8 9 1.43820 1.43820 1.12281 0.063079 W 163 1 I 22.4 24.8 16.5 22.3 9 1.35758 1.50303 1.00448 0.060878 CT> 164 1 I 18.0 20.8 14.6 20.2 9 1.23288 1.42466 0.89109 0.061034 165 1 A 47.2 47.2 24.2 28.0 13 1.95041 1.95041 1.68571 0.069658 CORRECTED MORPH ACCORDING'TO DISCRIHHANT FUNCTION ANALYSIS ALRATIO OBS LOCALITY MORPH HINGE MAXWIDTH LENGTH WIDTH RIBS HLRATIO HLRATIO ALATION 0.061799 166 1 A 44.0 44.0 24.3 29.3 11 1.81070 1.81070 1.50171 A 48.0 48.0 24.1 19.7 11 1.99170 1.99170 2.43655 0.101102 167 1 1.38415 0.051647 168 1 A 45.4 45.4 26.8 32.8 10 1.69403 1.69403 169 1 I 36.3 36.3 24.3 32.6 9 1.49383 1 .4 9 3 8 3 1.11350 0 .0 4 5 8 2 3 35.5 35.5 21.4 16.0 9 1.65888 1.65888 2.21875 0.103680 170 1 A 0.061340 171 1 A 38.0 38.0 2 1 .0 29.5 9 1.80952 1.80952 1.28814 42.0 2 1 .0 2 7 . 7 9 2 .0 0 0 0 0 2 .0 0 0 0 0 1.51625 0.072202 172 1 A 42.0 ■ 0.050151 173 1 N 34.6 34.6 22.4 30.8 11 1.54464 1.54464 1.12338 39.2 39.2 23.0 30.9 9 1.70435 1.70435 1.26861 0.055157 174 N 0.121429 175 1 A 40.8 40.8 21.0 16.0 9 1.94286 1.94286 2.55000 39.4 39.4 23.6 27.9 1 0 1.66949 1.66949 1.41219 0.059838 176 A 0.061080 177 1 I 31.4 31.4 20.4 25.2 9 1.53922 1.53922 1.24603 28.2 29.4 22.4 29.4 8 1.25893 1.31250 0.95918 0.042821 178 1 I 0.058015 179 1 I 34.6 34.6 21.0 28.4 9 1.64762 1.64762 1.21831 180 1 I 32.0 32.0 22.4 31.2 9 1.42857 1.42857 1.02564 0.045788 181 1 N 34.0 34.0 21.7 24.0 9 1.56682 1.56682 1.41667 0.065284 182 1 I 30.0 30.0 19.0 2 4 . 0 9 1.57895 1.57895 1.25000 0.065789 183 I 26.8 29.5 21.0 29.2 9 1.27619 1.40476 0.91781 0.043705 184 I 30.0 27.6 20.6 26.7 8 1.45631 1.33981 1.12360 0.054543 185 I 24.5 25.2 18.0 22.8 9 1.36111 1.40000 1.07456 0.059698 R 24.0 24.3 21.5 23.0 7 1.11628 1.13023 1.04348 0.048534 186 1 0.033729 187 1 R 15.5 22.3 20.7 22.2 9 0.74879 1.07729 0.69820 A 28.8 28.8 19.0 25.0 8 1.51579 1.51579 1.15200 0.060632 188 1 0.068437 189 1 N 26.6 26.6 16.4 23.7 8 1.62195 1.62195 1.12236 190 1 I 20.2 24.0 12.6 23.0 8 1.60317 1.90476 0.87826 0.069703 191 1 A 25.4 26.0 16.3 24.6 8 1.55828 1.59509 1.03252 0.063345 192 1 A 25.0 26.8 16.1 23.0 1 0 1.55280 1.66460 1.08696 0.067513 193 1 I 21.3 23.0 15.3 21.2 9 1.39216 1.50327 1.00472 0.065668 194 1 A 24.0 24.0 15.0 19.8 9 1.60000 1.60000 1.21212 0.080808 195 1 R 18.4 2 0 .0 17.6 2 0 .0 8 1.04545 1.13636 0.92000 0.052273 196 1 R 17.8 2 0 .0 15.0 18.7 7 1.18667 1.33333 0.95187 0.063458 197 1 I 18.4 20.7 15.0 20.1 8 1.22667 1.38000 0.91542 0.061028 198 1 R 15.3 19.7 16.6 18.4 7 0.92169 1.18675 0.83152 0.050092 199 1 R 15.1 18.3 15.0 17.5 8 1.00667 1.22000 0.86286 0.057524 200 1 I 17.7 19.4 13.3 18.5 6 1.33083 1.45865 0.95676 0.071937 201 1 R 13.3 16.3 13.3 16.3 8 1 .0 0 0 0 0 1.22556 0.81595 0.061350 202 1 I 17.2 17.2 13.5 18.0 8 1.27407 1.27407 0.95556 0.070782 203 1 R 17.0 17.0 15.2 15.7 8 1.11842 1.11842 1.08280 0.071237 204 R 8.0 12.0 12.0 11.4 6 0.66667 1.00000 0.70175 0.058480 205 1 R 9.3 12.6 10.1 12.6 6 0.92079 1.24752 0.73810 0.073079 206 R 8.0 11.5 8.8 11.0 7 0.90909 1.30682 0.72727 0.082645 207 5 N 34.7 34.7 22.3 25.8 8 1.55605 1.55605 1.34496 0.060312 208 5 N 31.5 31.5 19.1 24.2 8 1.64921 1.64921 1.30165 0.068149 209 5 N 29.8 29.8 18.7 22.4 1.59358 1.59358 1.33036 0.071142 210 5 N 28.7 28.6 21.0 25.0 9 1.36667 1.36190 1.14800 0.054667 211 5 N 28.0 28.0 18.5 23.0 9 1.51351 1.51351 1.21739 0.065805 212 5 R 23.7 24.0 20.3 21.8 1.16749 1.18227 1.08716 0.053554 213 5 I 25.5 25.5 18.8 22.5 9 1.35638 1.35638 1.13333 0.060284 214 5 I 22.5 22.5 18.6 23.0 9 1.20968 1.20968 0.97826 0.052595 215 5 N 22.2 22.8 18.3 22.2 1.21311 1.24590 1.00000 0.054645 216 5 N 24.2 24.2 18.2 22.3 1 0 1.32967 1.32967 1.08520 0.059626 217 5 N 24.1 24.1 19.0 21.9 1.26842 1.26842 1.10046 0.057919 218 5 R 21.0 21.0 17.2 19.5 8 1.22093 1.22093 1.07692 0.062612 CO 219 5 A 27.7 27.7 16.0 21.6 1 1 1.73125 1.73125 1.28241 0.080150 W oi REFERENCES Alexander, R. 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