The Cretaceous-Paleogene Transition in the Northern Mississippi Embayment, S.E

Home , Coryloides, Mississippi embayment, Osmunda, Owl Creek Formation, Porters Creek Formation, Taxodiaceae

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The Cretaceous-Paleogene transition in the northern Mississippi Embayment, S.E. Missouri: palynology, micropaleontology, and evidence of a mega-tsunami deposit

Tambra L. Eifert

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Recommended Citation Eifert, Tambra L., "The Cretaceous-Paleogene transition in the northern Mississippi Embayment, S.E. Missouri: palynology, micropaleontology, and evidence of a mega-tsunami deposit" (2009). Doctoral Dissertations. 2291. https://scholarsmine.mst.edu/doctoral_dissertations/2291

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THE CRETACEOUS-PALEOGENE TRANSITION IN THE

NORTHERN MISSISSIPPI EMBAYMENT, S.E. MISSOURI: PALYNOLOGY,

MICROPALEONTOLOGY, AND EVIDENCE OF A MEGA-TSUNAMI DEPOSIT

TAMBRA L. EIFERT

A DISSERTATION

Presented to the Faculty of the Graduate School of the

MISSOURI UNIVERSITY OF SCIENCE AND TECHNOLOGY

In Partial Fulfillment of the Requirements for the Degree

DOCTOR OF PHILOSOPHY

GEOLOGY AND GEOPHYSICS

2009

Approved by

Francisca E. Oboh-Ikuenobe, Advisor John P. Hogan John M. Holbrook Robert L. Laudon J. David Rogers

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ABSTRACT

Upper Cretaceous to lower Paleogene sedimentary rocks in Southeastern

Missouri record the northwest extension of the Mississippi Embayment, yet very little information exists about them due to lack of exposures. Access to borehole and trench material and well logs provided an opportunity to study the sedimentology, palynology and micropaleontology of the three formations spanning the Cretaceous-

Paleogene (K-Pg) boundary interval: Owl Creek (Cretaceous) and Clayton and

Porters Creek (Paleocene). Lithologic features, palynomorphs (mainly spores, pollen, dinoflagellate cysts), dispersed organic matter, and foraminifera were used to interpret biostratigraphy, paleovegetation, paleoclimatic and depositional conditions, thereby creating a framework upon which further questions involving the K-Pg boundary transition could be addressed.

Three hundred and seventy-nine palynomorph taxa have been identified; most are angiosperms and six taxa (one pollen and five dinoflagellate cysts) are potentially new.

Seventeen of the 18 foraminifera identified are benthic. These microfossil assemblages contain Late Cretaceous and Paleocene taxa, and confirm a Danian age for the Clayton

Formation, which rests unconformably on the Owl Creek. Thus, the K-Pg boundary itself is missing. The characteristics of four distinct graded Clayton units, i.e., basal Coquina

Zone containing rip-up clasts with microtektites, reworked Cretaceous macrofossils, microfossils and palynomorphs, Glauconite Zone, Gray Zone, and upper Hardground

Zone, and driller’s log information suggest that the Clayton Formation was deposited as a single megatsunami following the K-Pg Chicxulub impact event.

ACKNOWLEDGMENTS

First, and foremost, I dedicate my work and talent to the Creator who is my source of life and strength, and the giver of love and all knowledge. I thank all the people who have touched my life in so many different ways. To the spirit of abundance that is in each of you, may you recognize your greatness, discover and follow your path, and make the contribution you came here to make. I give special acknowledgement and gratitude to my loving mother Delores Eifert for her constant encouragement, understanding and unfailing support in this endeavor. To my sister Lori Martin and brother David Eifert, I give my heartfelt thanks for their prayers and love. I offer my loving appreciation to Betty Walker and her son Logan Venohr; this dissertation could not have been completed without their love, support, and encouragement. I am deeply grateful for the love and support of my dear friends Debbie Daws, Janet Thomason and Dewey Millay, whose countless hours of love and encouragement gave me that extra boost of energy to help me complete my research. For the unconditional love of my two little canine friends Tiny and Keyma who spent countless hours by my side, day and night, while writing this dissertation; I am grateful. I am indebted to my Ph.D. advisor Dr. Francisca Oboh-Ikuenobe for her patience, encouragement, support and guidance during my years of study. It has been an honor to work with such a knowledgeable and enthusiastic palynologist such as Dr. Oboh- Ikuenobe. Thanks to my dissertation committee members for their comments and suggestions. Special thanks to Carl Campbell of St. Louis Community College – Meramec for his enthusiastic support and guidance during this journey. Hernan Antolinez and Mohamed Zobaa helped me tremendously with morphological identification of palynomorphs. The Missouri Department of Natural Resources provided access to the U.S. Geological Survey borehole cores at the McCracken Core Repository in Rolla, and USGS provided slides from New Madrid test well 1-X. Thanks to the Nestle-Purina Company for permission to excavate the four trenches in the “kitty litter” quarry Stoddard County. I am gratefult to Tom Lee and Rick Poropat for their financial and physical assistance, and to the American Association of Stratigraphic Palynologists and the Missouri S&T Geology and Geophysics Radcliffe Graduate Scholarship for financial assistance.

TABLE OF CONTENTS Page ABSTRACT……………………………………………………………………….. iii

ACKNOWLEDGEMENTS………………………………………………………...iv

LIST OF ILLUSTRATIONS………………………………………………………. xi

LIST OF TABLES…………………………………………………………………. xv

SECTION

1. INTRODUCTION………………………………………………………….. 1

1.1. BACKGROUND……………………………………………………… 1

1.2. STUDY AREA ……………………………………………………….. 2

1.3. OBJECTIVES………………………………………………………… 4

2. GEOLOGIC SETTING.…………………………………………………… 6

2.1. OVERVIEW………………………………………………………….. 6

2.2. SEDIMENTATION HISTORY………………………………………. 8

2.2.1. Gulfian Series……………………………………………….. 9

2.2.2. Paleocene Series (Midway Group) …………………………. 12

2.2.3. Eocene Series (Wilcox Group)..…………………………….. 12

3. LITERATURE REVIEW…………………………………………………… 13

4. METHODS………………………………………………………………….. 17

4.1. FIELD WORK………………………………………………………… 17

4.1.1. Stoddard County……………………………………………. 17

4.1.2. New Madrid County………………………………………… 18

4.1.3. Scott County………………………………………………… 19

4.2. ANALYTICAL TECHNIQUES……………………………… ……... 22

5. RESULTS…………………………………………………………………… 25

5.1. LITHOLOGIC DESCRIPTIONS……………………………………. 25

5.1.1. Owl Creek Formation……………………………………….. 25

5.1.2. Clayton Formation………………………………………….. 26

5.1.2.1 Coquina Zone……………………………………… 26

5.1.2.2. Glauconite Zone…………………………………… 27

5.1.2.3. Gray Zone…………………………………………. 27

5.1.2.4. Hardground Zone...……………………………….. 28

5.1.3 Porters Creek…...………………………………………….. 32

5.2. PALYNOMORPHS ……………….…………………………………. 33

5.2.1. Overview…………………………………...... 33

5.2.2. Nonmarine Palynomorphs ………………………………….. 34

5.2.3. Marine Palynomorphs ………………………………………. 34

5.3. SYSTEMATIC PALYNOLOGY…………………………………….. 42

5.4. DISPERSED ORGANIC MATTER………………………………….. 65

5.5. FORAMINIFERA…………………………………………………….. 75

6. INTERPRETATIONS………………………………………………………. 77

6.1. PALYNOMORPHS…………………………………………… ……... 77

6.1.1. Palynostratigraphy…………………………………………... 77

6.1.1.1 Test Well I-X (New Madrid County)……………… 77

6.1.1.2 BH-1, BH-9, and BH-10 (Scott County)…………... 81

6.1.1.3 Trenches 1 and 2 (Stoddard County)………...... 82

6.1.2. Species Diversity and Paleoenvironments…………………... 82

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6.1.2.1 Owl Creek Formation……………………………… 83

6.1.2.2 Clayton Formation…………………………...…….. 83

6.1.2.3 Porters Creek Formation…………………………… 83

6.1.3. Paleovegetation……………………………………………… 84

6.1.3.1 Owl Creek Formation……………………………… 84

6.1.3.2 Clayton Formation……………. …………………... 85

6.1.3.3 Porters Creek Formation…………………………… 88

6.2. PALYNOFACIES ASSEMBLAGES………………………………… 103

6.3. FORAMINIFERA……………………………………………………. 105

6.3.1. Biostratigraphy……………………………………………… 105

6.3.2. Assemblages………………………………………………… 105

6.3.2.1 Percent Planktonics………………………………… 106

6.3.2.2 Species Diversity…………………………………... 107

6.3.2.3 Shell-type Ratios…………………………………… 108

7. DISCUSSIONS………………………………………………………………… 110

7.1. FLORISTIC PATTERNS AND PALEOCLIMATIC CONDITIONS.. 110

7.1.1. Latest Cretaceous…………………………………………..... 110

7.1.2. K-Pg Boundary…………………………………………….... 112

7.1.3. Paleocene ……..…………………………………………….. 113

7.2. PALEOENVIRONMENTAL RECONSTRUCTION………………… 114

7.2.1. Introduction……...... …...... …...... …...... 114

7.2.2. Depositional Environments..………………………………… 116

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7.2.2.1 Proximal-distal Trends of Dinoflagellates…………. 116

7.2.2.2 Regional Sequence Stratigraphy………………….... 117

7.3. STRATIGRAPHY AND PLACEMENT OF THE K-PG BOUNDARY…………………………………………………………..121

7.3.1. Introduction…...... …...... …...... …...... 121

7.3.2. Alabama (USA)……………………………………………... 122

7.3.3. Texas (USA)………………………………………………… 123

7.3.4. Cuba………………………………………………………..... 124

7.3.5. Northeastern Mexico...... …...... ……………………….. 125

7.3.5.1 Basal Unit 1: Spherule-rich layer…………………. 125

7.3.5.2 Unit 2: Laminated Sandstone……………………… 126

7.3.5.3 Unit 3: Interlayered Sand-silt Beds………………... 126

7.3.6. Northeastern Mexico, Parras and La Popa Basins……………127

7.3.7. Gulf of Mexico and Caribbean……………………………… 129

7.3.8. Illinois (USA)……………………………………………….. 130

7.4. DETAILED INTERPRETATION OF THE CLAYTON FORMATION………………………………………………………… 131

7.4.1. Well Log Data………………………………………………. 131

7.4.2. Impact-generated Tsunami or Flood Deposit?...... 132

7.4.3. Depositional Model for the Clayton Formation…………….. 132

8. CONCLUSIONS…………………………………………………………..... 136

APPENDICES

A. CORE DESCRIPTIONS FOR BH-1, BH-2, BH-3, BH-9, AND BH-10 IN SCOTT COUNTY, MISSOURI………………………………………. 140

B. QUANTITATIVE PALYNOMORPH DATA FOR BH-1, BH-9, AND BH-10 IN SCOTT COUNTY, MISSOURI: NONMARINE PALYNOMORPHS……….….……………………………………………. 166

C. QUANTITATIVE PALYNOMORPH DATA FOR TRENCH 1 IN STODDARD COUNTY, MISSOURI: NONMARINE PALYNOMORPHS……...... 175

D. QUANTITATIVE PALYNOMORPH DATA FOR CORE CUTTINGS FROM TEST WELL 1-X, NEW MADRID COUNTY, MISSOURI: NONMARINE PALYNOMORPHS...... 179

E. QUANTITATIVE PALYNOMORPH DATA FOR BH-1, BH-9, AND BH-10 IN SCOTT COUNTY, MISSOURI: DINOFLAGELLATES AND OTHER MARINE PALYNOMORPHS...... 184

F. QUANTITATIVE PALYNOMORPH DATA FOR TRENCH 1 IN STODDARD COUNTY, MISSOURI: DINOFLAGELLATES AND OTHER MARINE PALYNOMORPHS ……………………………...... 188

G. QUANTITATIVE PALYNOMORPH DATA FOR CORE CUTTINGS OF NEW MADRID COUNTY, MISSOURI: DINOFLAGELLATES AND OTHER MARINE PALYNOMORPHS …………...... 192

H. NONMARINE PALYNOMORPH TAXA IN THE OWL CREEK: NEW MADRID, SCOTT, AND STODDARD COUNTIES, MISSOURI…...….. 194

I. NONMARINE PALYNOMORPH TAXA IN THE CLAYTON: NEW MADRID, SCOTT, AND STODDARD COUNTIES, MISSOURI……..... 197

J. NONMARINE PALYNOMORPH TAXA IN THE PORTERS CREEK: NEW MADRID, SCOTT, AND STODDARD COUNTIES, MISSOURI... 201

K. GLOSSARY OF PALYNOMORPH TERMS……………………………... 208

L. ILLUSTRATIONS OF SELECTED PALYNOMORPHS: PLATES 1 TO 8….…………………………………………………..……….……….. 217

M. QUANTITATIVE FORAMINIFERA DATA FOR THE OWL CREEK, CLAYTON, AND PORTERS CREEK FORMATION………………….... 234

N. FORAMINIFERA TAXA IN THE OWL CREEK, CLAYTON, AND PORTERS CREEK FORMATIONS……………………………………… 236

O. ILLUSTRATIONS OF FORAMINIFERA: PLATES 1 AND 2….……….. 238

BIBLIOGRAPHY………………………………………………………………….. 243

VITA……………………………………………………………………………….. 266

LIST OF ILLUSTRATIONS Figure Page

1.1. Geologic map of Missouri (taken from Overstreet et al., 2003); expanded southeast portion shows the study areas in New Madrid, Scott, and Stoddard counties……………………………………………………………. 3

2.1. Map of eastern USA showing study area and surrounding geologic features (from Luckey 1985)………………………………………………… 9

2.2. Stratigraphic column of the sediments deposited in Missouri during the Gulfian Series of the Cretaceous and the Paleocene, Eocene, and Pliocene Series of the Tertiary (Adapted from Unklesbay and Vineyard (1992)………...... 11

4.1. Mine view (north) with sump exposure of the Eocene and Paleocene strata at the “kitty litter” site (photograph courtesy of Carl Campbell)…...... 18

5.1. Cross sectional view of trench excavated at the Nestle Purina Plant in Stoddard County, Missouri illustrating the four distinct zones of the Clayton Formation. LS = Limonite.………………………………………….. 29

5.2. A cross sectional view of scour filled structures occurring in the Coquina Zone and trending in a NW to SE direction………………………... 30

5.3. Photograph of trench wall containing complete section of Paleocene Clayton Formation above Cretaceous Owl Creek Formation. Note the deep scour into Owl Creek in lower right corner. Hammer in Lower rright corner is 29 cm long. White rectangle in lower right is a 15 cm scale bar. Modified from Campbell et al. 2008………………………….. 30

5.4. Some common spherical microtektites found within the Coquina Zone of the Clayton Formation in Stoddard County, Missouri (courtesy of Carl Campbell)………………………………………………….. 31

5.5. Some variations in the splashform-type microtektites obtained from the Clayton Formation of Stoddard County, Missouri (courtesy of Carl Campbell)……………………………………………………………. 31

5.6. An example of some very large torpedo shaped, hollow limonite concretions observed between the uppermost Clayton and the lowermost in the Porters Creek…………………………………………………………... 32

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5.7. Percentage distribution of palynomorphs in the Clayton and Owl Creek formations, Stoddard County. Emphasis is placed on Terrestrial vs. Marine,Spores vs. Pollen, Angiosperms vs. Gymnosperms, and the presence/absence of ferns and allied ferns, and Normapolles. Marine palynomorphs are dinoflagellate cysts and acritarchs……………...... 37

5.8. Percentage distribution of palynomorphs in the Porters Creek and Clayton formations, New Madrid County. Emphasis is placed on Terrestrial vs. Marine, Spores vs. Pollen, Angiosperms vs. Gymnosperms, and the presence/absence of ferns and allied ferns. Marine palynomorphs are dinoflagellate cysts and acritarchs……………………………………….. 38

5.9. Percentage distribution of palynomorphs in the Owl Creek and Porters Creek formations in BH-1 core, Scott County. Emphasis is placed on Terrestrial vs. Marine, Spores vs. Pollen, Angiosperms vs. Gymnosperms, and the presence/absence of ferns and allied ferns. Marine palynomorphs are dinoflagellate cysts and acritarchs. Patterned bars represent barren samples……………………………………... 39

5.10. Percentage distribution of palynomorphs in the Porters Creek Formation in BH-9 core, Scott County. Emphasis is placed on Terrestrial vs. Marine, Spores vs. Pollen, Angiosperms vs. Gymnosperms, and the presence/absence of ferns and allied ferns. Marine palynomorphs are dinoflagellate cysts and acritarchs. Patterned bars represent barren samples……………………………………... 40

5.11. Percentage distribution of palynomorphs in the Porters Creek formations in BH-10 core, Scott County. Emphasis is placed on Terrestrial vs. Marine, Spores vs. Pollen, Angiosperms vs.Gymnosperms, and the presence/absence of ferns and allied ferns. Marine palynomorphs are dinoflagellate cysts and acritarchs. Patterned bar represents barren sample…………………………... 41

5.12. Classification scheme used for palynomorphs (adapted from De Villiers, 1997)…………………………………………………………………………. 43

5.13. Photomicrographs of representative samples of the three palynofacies assemblages. A, B) Palynofacies A, sample SC27 (A), sample ST07 (B); C, D) Palynofacies B, sample SC03; E, F) Palynofacies C, sample ST10. Abbreviations for dispersed organic components: BLDEB = black debris; STOM = structured phytoclasts; USTOM = unstructured phytoclasts; P = pollen; FS = fungal spore; A = acritarch; D = dinoflagellate; AMORP = amorphous organic matter……………………..... 67

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5.14. Dendograms for average linkage cluster analysis of palynological samples from BH-1, BH-9, BH-10, Trench 1 and Trench 2 (Q-mode, left-hand) and of dispersed organic matter (R-mode, top), with the data matrix displaced between them………………………………………………. 70

5.15. Percentage distribution of dispersed organic matter in BH-1 core, Scott County. SPORO = sporomorphs, FR = fungal remains, FWA = freshwater algae, MAR = marine, STOM = structured phytoclasts, USTOM = unstructured phytoclasts, BLDEB = black debris, and AMORP = amorphous organic matter……………………………………………...……. 71

5.16. Percentage distribution of dispersed organic matter in BH-9 core, Scott County. SPORO = sporomorphs, FR = fungal remains, FWA = freshwater algae, MAR = marine, STOM = structured phytoclasts, USTOM = unstructured phytoclasts, BLDEB = black debris, and AMORP = amorphous organic matter…………………………………………………….72

5.17. Percentage distribution of dispersed organic matter in BH-10 core, Scott County. SPORO = sporomorphs, FR = fungal remains, FWA = freshwater algae, MAR = marine, STOM = structured phytoclasts, USTOM = unstructured phytoclasts, BLDEB = black debris, and AMORP = amorphous organic matter…………………………………………………….73

5.18. Percentage distribution of dispersed organic matter in Trenches1 and 2, Stoddard County. SPORO = sporomorphs, FR = fungal remains, FWA = freshwater algae, MAR = marine, STOM = structured phytoclasts, USTOM = unstructured phytoclasts, BLDEB = black debris, and AMORP = amorphous organic matter……………………………………….. 74

6.1. Stratigraphic occurrences of palynomorph taxa in the Porters Creek, Clayton, and Owl Creek formations. Numbered are keyed to the list of taxonomic names in Table 6.1. Taxa are divided into major groups: 1, marine dinocysts, undifferentiated; 2-18, bryophyte and pteridophyte spores; 19-41, angiosperm pollen; 42-50, gymnosperm pollen………………………………………………………………………….78

6.2. Ternary diagram used for describing species diversity of palynomorph assemblages (adapted by Duringer and Doubinger, 1985). Formations plotted indicate the following: Owl Creek (nearshore environment; open marine waters); Clayton (nearshore environment; favorable open marine conditions); and Porters Creek (restricted nearshore environment………………………………………………………………….. 84

6.3. Graphical representation of plant groups identified in New Madrid Test Well I-X. Bar scale represents total number of palynomorphs………… 92

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6.4. Graphical representation of plant groups identified in BH-1 core, Scott County. Bar scale represents total number of palynomorphs…………. 94

6.5. Graphical representation of plant groups identified in BH-9 core, Scott County. Bar scale represents total number of palynomorphs…………. 96

6.6. Graphical representation of plant groups identified in BH-10 core, Scott County. Bar scale represents total number of palynomorphs…………. 98

6.7. Graphical representation of plant groups identified in Trench 1, Stoddard County. Bar scale represents total number of palynomorphs……... 100

6.8. Graphical representation of palynomorph species recovered from Scott and Stoddard counties attributable to known plant regions. Bar scale represents the total number of palynomorphs……………………... 102

6.9. Inferred paleovegetation model for the northern Mississippi Embayment during the Paleocene……………………………………………. 102

6.10. Ternary diagram used for describing shell-type ratios versus paleoenvironmental conditions (adapted from Murray (1973). Formations plotted indicate the following: Owl Creek (hypersaline marsh conditions); Clayton (normal marine; hypersaline marsh conditions; and Porters Creek (normal marine; hypersaline marsh conditions)………………………. 109

7.1. Summary characteristics of the three formations studied in the Northern Mississippi Embayment. HST = transgressive systems tract; HST = highstand systems tract.………... …………………………………………… 120

7.2. Generalized map showing the Chicxulub Impact and the movement of a megatsunami wave as it approached the inundated landmasses of Mexico and North America. The study area is in the Northern Mississippi Embayment……………………………………………………… 135

LIST OF TABLES Table Page

4.1. Samples used for palynological analyses…………………………………...... 20

4.2. Samples used for foraminiferal analyses; no depth information is available... 21

5.1. Species diversity for palynomorph assemblages (excluding freshwater algae and fungi) in the Clayton,Porters Creek, and Owl Creek formations.… 35

5.2. Comparison of data for nonmarine palynomorphs (excluding algae and fungi) recovered from the Porters Creek, Clayton, and Owl Creek formations. Note: DS Gym = Different Species of Gymnosperms, DS Ang = Different Species of Angiosperms, DPS = Different Pollen Species, and DSS =Different Spore Species………………………………… 35

5.3. Total numbers of marine palynomorphs recovered from the Porters Creek, Clayton and Owl Creek formations. See section 5.2.1 for statement about foraminiferal linings.………………………………………………….. 36

5.4. Total numbers and percentages of all palynomorphs in the Porters Creek, Clayton, and Owl Creek formations. Emphasis is placed on the terrestrial vs. marine percentages…………………………………….. 36

5.5. Relative abundances (in percent) of dispersed organic matter in BH-1, BH-9, and BH-10, Scott County. SPORO = sporomorphs, FR = fungal remains, FWA = freshwater algae, MAR = marine, STOM = structured phytoclasts, USTOM = unstructured phytoclasts, BLDEB = black debris, AMORP = amorphous, PC = Porters Creek, OC = Owl Creek, PFA = Palynofacies Assemblage………………………… 68

5.6. Relative abundances (in percent) of dispersed organic matter in Trenches 1 and 2, Stoddard County. SPORO = sporomorphs, FR = fungal remains, FWA = fresh water algae, MAR = marine, STOM = structured phytoclasts, USTOM = unstructured phytoclasts, BLDEB = black debris, AMORP = amorphous, CL = Clayton, HG = hardground, Coqu = coquina, OC = Owl Creek, PFA = palynofacies assemblage………………………...... 69

5.7. Principal component loadings for dispersed organic matter. The Asterisk (*) indicates the statistically significant types with absolute values greater than 0.10; eigenvalue (Axis) 1 = 996.463 (69.122%); Axis 2 = 300.480 (20.844%)……………………………………………………………69

5.8. Species diversity for foraminiferal shell types. Porcel. = porcellaneous, Agglut. = agglutinated…………………………...... 76

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5.9. Benthic versus planktonic foraminifera……………………………………… 76

6.1. Selected palynomorphs used for stratigraphic interpretation…………………79

6.2. Tree and shrub taxa in the Porters Creek and Clayton formations…………... 87

6.3. Palynofloral association of the Clayton, Porters Creek, and Owl Creek formations…………………………………………………………….. 89

6.4. Modern plant taxa type in North American regions and zones……………… 90

6.5. Palynomorph counts attributed to different plant groups, New Madrid Test Well I-X………………………………………………………………… 93

6.6. Palynomorph counts attributed to different plant groups, BH-1 core, Scott County. Samples marked “nd” indicate “no data available (barren)”……………………………………………………………………… 95

6.7. Palynomorph counts attributed to different plant groups, BH-9 core, Scott County. Samples marked “nd” indicate “no data available (barren)”……………………………………………………………………… 97

6.8. Palynomorph counts attributed to different plant groups, BH-10 core, Scott County. Samples marked “nd” indicate “no data available (barren)”……………………………………………………………………… 99

6.9. Palynomorph counts attributed to different plant groups, Trench 1, Stoddard County. ……………….…………………………………………… 101

6.10. Foraminifera identified in Trenches 1 and 2, Stoddard County. CL = Clayton, PC = Porters Creek, and OC = Owl Creek…………………………. 106

I. INTRODUCTION

1.1. BACKGROUND

The Cretaceous-Paleogene (K-Pg) boundary interval is considered an important time in Earth’s history because of widespread extinctions that affected life in the marine and terrestrial realms. Ammonoids, rudist bivalves, mosasaurs, ichthyosaurs, and other marine reptiles were wiped out, and about 90% of calcareous nannoplankton and foraminifera became extinct. On land, all dinosaurs and pterosaurs died out, and there were turnovers among some groups of plants. Although there are ongoing debates about the causes of extinctions and the timing (abrupt versus gradual), many scientists now believe that a bolide impact at Chicxulub in the Yucatan Peninsula, Mexico was responsible (Alvarez et al., 1990). The consequences of this extraterrestrial impact changed the landscape and climate, resulting in tsunamis, cooler temperatures, acid rain, regression, and forest fires (Stanley, 2005).

There are several studies documenting the changes in biota and environment during this K-Pg transition in many parts of the world, including North America. In the northern Mississippi Embayment, such studies are very few because of limited availability of rock exposures and very few boreholes. The uppermost Cretaceous and lowermost Paleocene strata in the region record the last geological traces of a marine epeiric influence that inundated the Gulf Coastal Plain Province of North America.

Therefore, detailed geologic history of the area has remained somewhat unresolved. By contrast, numerous studies have focused on the southern portion of the Gulf Coastal region (e.g., Thomas, 1942; Grohskopf, 1955; Cushing et al., 1964; Nuelle and Sumner,

1981; Beard and Meylan, 1987; Williamson et al., 1990; Harrelson et al., 1992) where

there is active prospecting for hydrocarbons. Some pertinent stratigraphic, paleontologic

and palynologic studies of Cretaceous and Paleogene strata in the northern Embayment

include Grohskopf (1955), Stephenson (1955), Stearns (1957), Elsik (1974), Crone and

Russ (1979), Frederiksen et al. (1982), Harrison et al. (1996), Harrison and Litwin

(1997), Campbell (2002), Gallagher et al. (2005), and Campbell et al. (2008). The

limited number of studies has hindered a better resolution of the K-Pg boundary interval

and clearer understanding of the survival of terrestrial biota after the terminal Cretaceous

impact event.

1.2. STUDY AREA

The Cretaceous is the only Mesozoic period represented in Missouri by the uppermost Gulfian Series in the southeastern part of the state (Crowleys Ridge and and

Benton Hills). Together with the overlying Paleogene strata, they were deposited by the northernmost extension of the Mississippi Embayment (Grohskopf and Howe, 1961;

Unklesbay and Vineyard, 1992). These Cretaceous-Paleogene sediments are exposed in the southeastern counties of New Madrid, Scott, and Stoddard (Fig. 1.1). Of the three

Upper Cretaceous beds representing the Gulfian Series, only two, namely the McNairy and Owl Creek formations, are found at the surface. Pre-McNairy Cretaceous beds which are composed of sand, chalk, clay, and limestone are penetrated by boreholes.

Lower Paleogene strata include the Paleocene Series of the Midway Group (Clayton and

Porters Creek formations) and the Eocene Series of the Wilcox Group (Ackerman and

Holly Springs formations) (Koenig, 1961, Unklesbay and Vineyard, 1992, and Campbell,

2002). The Clayton Formation is absent in much of the region. Access to freshly excavated sediments of the Owl Creek, Clayton and Porters Creek at the Nestle Purina

Plant in Bloomsfield, Stoddard County and to several core sediments from U.S.

Geological Survey boreholes provided a wealth of data regarding the K-Pg boundary interval and the terminal Cretaceous impact event.

Figure 1.1. Geologic map of Missouri (taken from Overstreet et al., 2003); expanded southeast portion shows the study areas in New Madrid, Scott, and Stoddard counties.

1.3. OBJECTIVES

This study focuses on the sedimentological, palynological and micropaleontological interpretations of sediments of the upper Maastrichtian Owl Creek

Formation and the Paleocene Clayton and Porters Creek formations in New Madrid,

Scott, and Stoddard counties, in the northernmost extension of the Mississippi

Embayment. The following general questions will be addressed: (1) Which important index fossils (palynomorph and foraminiferal taxa) occur in the sediments? (2) Was the paleovegetation similar across the K-Pg boundary? (3) What were the depositional conditions of the sediments? (4) Is the K-Pg boundary interval seperating the Late

Cretaceous Owl Creek and Early Paleocene Clayton formations?

In order to address these questions, the following major objectives are the targets of this study: (1) Taxonomic identification of organic-walled microfossils or palynomorphs (spores, pollen, dinoflagellate cysts, acritarchs, freshwater algae, fungi), dispersed organic matter (palynofacies), and foraminifera in outcrop and borehole samples; (2) Calibration of spore-pollen, dinoflagellate cyst and foraminiferal biostratigraphy with published biochronological data from the Gulf Coast and other regions for a better resolution of the K-Pg transition in Missouri; (3) Interpretation of paleovegetation, paleoecology and possibly paleoclimatic conditions from the palynomorph and foraminiferal datasets; (4) Reconstruction of depositional environments using lithological, palynofacies and microfossil data; and (5) Determination of the lateral extent and thickness of the Clayton Formation from driller’s logs and electrical logs, and

(6) Develop a depositional model for the Clayton Formation. Thus, this study creates a framework upon which further questions involving the K-Pg boundary transition can be addressed.

2. GEOLOGIC SETTING

2.1. OVERVIEW

The Mississippi Embayment occupies a broad structural trough between the

Appalachian Highlands in the east and the Ozark Plateaus in the west (Thacker and

Satterfield, 1977; Luckey, 1985), which began developing approximately 100 million years ago during the Late Cretaceous. It comprises approximately 160,000 square kilometers of the U.S. Gulf Coastal Plain Province (Grohskopf, 1955; Fig. 2.1), extending southward from its apex in southern Illinois and comprising parts of Alabama, Arkansas,

Illinois, Kentucky, Louisiana, Mississippi, Missouri, Tennessee, and Texas. In Missouri, the lowlands in the extreme southeastern corner of the state, occupy a portion of the northern embayment and cover 6,400 square kilometers (Luckey, 1985).

The basin’s origin lies in the Precambrian during the break up of the supercontinent Rodinia (Cushing et al. 1964). During Rodinia’s break up, there were several rift zones that formed adjacent to the major rift, which split off North America.

As Pangaea began to break up, North America passed over a volcanic “hot spot” in the earth’s mantle (Bemuda hot spot) that was undergoing a period of intense activity (Vogt and Jung, 2007). One of the smaller rift zones existed below the modern Mississippi

Embayment (Van Arsdale and Cox, 2007). Sediment accumulated above the small rift zone to form a proto-Mississippi Embayment (Cushing et al. 1964). The modern embayment is attributed to the rise of sea level in the Cretaceous. With the break up of the supercontinent Pangaea and higher rates of sea floor spreading, the global sea level was considerably higher. The old rift zone was a natural downwarped basin and allowed a natural course for sea level to enter the continental interior as well as exit (Cushing et

7 al. 1964). Reoccurring activity still exists today along the rift’s faults. The 1811-1812

New Madrid Earthquakes were associated with deep faults in this area and are still the largest earthaquakes ever recored in North America (Stewart and Knox, 1993).

During the Late Cretaceous and Early Cenozoic, the entire region underwent subsidence, which allowed the seas to reinvade the area to form the present-day

Mississippi Embayment (Fig. 2.1). With little interruption, the seas deposited sediments from the Late Cretaceous until the latter part of the Paleogene. In southeastern Missouri, these sediments are mostly unconsolidated and nearly flat-lying, and uncomformably overlie consolidated and structurally deformed Paleozoic sedimentary rocks (Pryor,

1962). The Cretaceous-Paleogene sediments range from marine clay and limestone to marginal marine and non-marine sand and gravel. They are exposed along Crowley’s

Ridge in Stoddard County and Benton Hills in Scott County (Unklesbay and Vineyard,

1992) where they dip southward into the embayment. The clastic sediments were transported westward from the southern Appalachians to the embayment by a rather large stream system (ancestral Mississippi River) and entered the marine waters of the youthful embayment to form a deltaic mass (Pryor, 1962). One of the units, the McNairy Sand, is used for commercial purposes and is an important source for groundwater (Luckey,

1985). Nestle Purina Company processes the Porters Creek Clay to make “kitty litter.”

Some rock units found in the surrounding areas of the embayment are absent in southeastern Missouri. Erosion processes have removed a considerable portion from some of the rock units.

Prominent geologic features in the study area, specifically in the central part of the Mississippi Valley, are active fault systems that constitute the New Madrid Seismic

Zone. This zone spans northeastern Arkansas, southeastern Missouri, western Tennessee, western Kentucky, and southern Illinois, and occupies the same area where the Reelfoot

Rift formed more than 500 million years ago (Wright et al., 1965). The Reelfoot Rift and the adjacent platform became a repository for mainly marine Paleozoic carbonate sediments, some of which underwent lead-zinc and barium mineralizations (Leach et al.,

2001).

2.2. SEDIMENTATION HISTORY

The lithostratigraphic sections of the northernmost part of the Mississippi

Embayment were first described by Grohskopf (1955), followed by more detailed descriptions by Grohskopf and Howe (1961) and Koenig (1961). The Cretaceous sediments are restricted to the uppermost part of the Gulfian Series while the Midway and

Wilcox Groups represent the Paleocene and Eocene Series, respectively (Unklesbay and

Vineyard, 1992). A stratigraphic column showing the Cretaceous and Paleogene systems in Missouri are shown in Figure 2.2.

Figure 2.1. Map of eastern USA showing study area and surrounding geologic features (from Luckey, 1985).

2.2.1. Gulfian Series. Harrison et al. (1996) and Harrison and Litwin (1997)

correlated the oldest post-Paleozoic unit (strongly weathered and convoluted clays mixed

with angular to sub-angular gravel and sand) with the pre-Cenomanian Little Bear

Formation in southern Illinois (Mellen, 1937; Pryor and Ross, 1962; Ross, 1963; Kolata

et al., 1981). According to Pryor and Glass (1961), the extensive weathering

10 characteristic of this unit is not found in any other Cretaceous or Paleogene unit in the northern Mississippi Embayment. William and Frye (1975) indicated that the Little Bear

Formation was a pre-Cenomanian soil unit that is probably equivalent to similar paleosols in the same stratigraphic position in the eastern and southern Gulf Coastal Plain.

Harrison et al. (1996) did not recover palynomorphs from this unit but successfully did so from the overlying heterolithic unit of gravels, sand, silt, and clay, which yielded an approximately late Campanian age. They correlated this heterolithic unit with the

Tuscaloosa Formation of Alabama and southwestern Tennessee, even though Christopher

(1980, 1982) dated it as late Cenomanian. They have proposed renaming this unit in the northern Mississippi Embayment as the “Post Creek Formation.”

Above the “Post Creek Formation” is a lignite-rich clay unit with several late

Campanian palynomorph taxa (Harrison et al., 1996 and Harrison and Litwin, 1997) comparable to those in sediments from the southern Mississippi Embayment and Atlantic

Coastal Plain (Tschudy, 1975 and Wolfe, 1976). Based on age determination, stratigraphic position, and lithologic similarities, this unit has been correlated with the

Coffee Sand of Safford (1864) in southwestern Tennessee. The proposed Coffee Sand,

Post Creek Formation, and Little Bear Formation constitute the pre-McNairy sediments of Unkelsbay and Vineyard (1992). The Coffee Sand is overlain by the McNairy Sand, which underlies approximately three-fourths of the lowlands in southeastern Missouri

(Luckey, 1985) and outcrops in the Benton Hills and Crowley’s Ridge areas. Its thickness varies from about 30 meters to more than 80 meters. Within the upper one- third of this unit is a massive, palynomorph-rich clay interval, informally known as the

Zodoc Clay, with a probable early to middle Maastrichtian age. This black clay is often

11 used as a stratigraphic marker in the field. The McNairy is believed to have formed in nonmarine to nearshore marine environments (Frederiksen et al., 1982).

Missouri Column

continued

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Figure 2.2. Stratigraphic column of the sediments deposited in Missouri during the Gulfian Series of the Cretaceous and the Paleocene, Eocene, and Pliocene Series. Adapted from Unklesbay and Vineyard (1992).

overlying the McNairy Sand is the Owl Creek Formation (mostly sand, silt, and clay) from which Farrar (1935) recognized fossil marine invertebrates and plant remains. Palynomorphs indicate a late Maastrichtian age for this marine formation (Harrison et al., 1996).

2.2.2. Paleocene Series (Midway Group). The basal Paleogene (Tertiary) unit in southeastern Missouri consists of the fossiliferous, calcareous and glauconitic sand and clay of the Clayton Formation (Fig. 2.2), which are only three to four meters thick. Little is known of this unit, but its distinctive green color makes it an ideal datum for mapping purposes (Koenig, 1961). Shourd and Winter (1980) interpreted the Clayton Formation as beach deposits. In the Benton Hills and Crowley’s Ridge, much of the Owl Creek is unconformably overlain by the Porters Creek, which exceeds 60 meters in many places in

Crowley’s Ridge. Much of the clay is bentonitic (Unklesbay and Vineyard, 1992), contains relict glass shards and pumice fragments (Grim, 1933; Allen, 1934; Simms,

1972), and is mined for processing “kitty litter.” The Clayton Formation was first studied in the middle 1930s (Farrar, 1935; Farrar and McManamy, 1937). According to Herrick and Tschudy (1967), this unit was deposited in a shallow epeiric sea during the maximum marine transgression (Frederiksen et al., 1982; Harrison et al., 1996).

2.2.3. Eocene Series (Wilcox Group). The Porters Creek Formation is succeeded by the Ackerman Formation, which is a multi-colored, silty clay containing glauconitic sandstone, boulders, and bauxitic clay. It ranges from a few centimeters to as much as 30 meters in several areas (Steward, 1942 and Koenig, 1961). The unit contains small pelecypods and foraminifera, but no palynomorphs have been previously recovered. The overlying Holly Springs Formation consists of well-sorted, very coarse sand and gravel with plant fossils and varies in thickness from a few centimeters to up to

80 meters (Koenig, 1961). This fluvial deposit marked the final retreat of the sea from the northern Mississippi Embayment during the Eocene (Harrison et al., 1996).

3. LITERATURE REVIEW

The Upper Cretaceous-Paleogene (K-Pg) transition has been well studied by geologists and other scientists in several parts of the world because of the terminal

Cretaceous mass extinctions of organisms. Since Alvarez et al. (1980) proposed that a massive bolide impact caused these extinctions and the subsequent discovery of the impact site at Chixculub, Mexico (Hildebrand et al., 1991; Sharpton et al., 1992), sedimentologists, stratigraphers, paleomagnetists, geochemists, and paleontologists have discovered evidence linked to this impact event in several regions of the world. The evidence includes iridium anomaly, siderophile trace elements in chondritic proportions, osmium and chromium isotope anomalies, microdiamonds, nickel-rich spinels, shocked quartz, and altered microtektites. In addition to the deep sea, several K-Pg boundary

sections have been identified in North America, South America, Australia, New Zealand,

eastern Equatorial Atlantic, North Atlantic, Gulf of Mexico, Spain, The Netherlands,

Denmark, Sweden, China, etc. Many of these sections have palynomorph records (Stover

and Patridge, 1973; Benson, 1976; Hultberg and Malmgren, 1986; Askin, 1988; Wang et

al., 1990; Brinkhuis and Schi Øler, 1996; Masure et al., 1998; Oboh-Ikuenobe et al., 1998;

Willumsen, 2000; Brinkhuis et al., 2004; Williams et al., 2004). The global stratotype for the K-Pg boundary is located in a dark gray clay layer at El Kef, Tunisia, where some of these features have been recognized.

Several interdisciplinary special publications have been dedicated to the terminal

Cretaceous extinctions (e.g., Christensen and Birkelund, 1979; Sharpton and Ward, 1990;

Kauffman and Walliser, 1990; Macleod and Keller, 1996; Smit, 1999; Hartman et al.,

2002; Evans et al., 2008). Although many geologists have now accepted the impact

14 theory, the resulting mass wasting (Smit et al., 1996; Bralower et al., 1998; Norris and

Firth, 2002; Alegret and Thomas, 2004), and the fact that several organisms, especially calcareous nannoplankton, dinosaurs, ammonites, rudistid palecypods, and marine reptiles were impacted by mass extinctions, some studies suggest that the K-Pg boundary deposits resulted from changing sea level and regional tectonics (Keller and Stinnesbeck,

1996; Keller et al., 1997). These studies argue that extinctions were more gradual and stepped. The presence of abundant fossil charcoal provides evidence of wildfires below and above the K-Pg boundary in several regions (e.g., Scott et al., 2004), which probably affected terrestrial life. Unlike other groups of microfossils, palynomorphs

(dinoflagellate cysts, acritarchs, chlorophytes, spores, pollen) were less severely affected by the terminal Cretaceous mass extinctions (less than 50% loss) (Firth, 1987; Brinkhuis and Zachariasse, 1988; Brinkhuis and Schi Øler, 1996; Nichols and Johnson, 2002).

In North America the K-Pg interval is present in the Western Interior, Gulf

Coastal Plain, northern Mississippi Embayment, the southeastern region, and the Atlantic

Coastal Plain. The Western Interior sections appear to have recorded continuous

terrestrial sedimentation during this interval, and the boundary itself is exposed in

outcrops (Frederiksen, 1996). Thus, many publications have described the vertebrate,

invertebrate, paleobotanical and palynological records from this region (e.g., Tschudy

and Tschudy, 1986; Wolfe, 1991; Srivastava, 1994; Braman and Sweet, 1999; Sweet et

al., 1999; references in Hartman et al., 2002; Nichols and Fleming, 2002). In general,

nonmarine plants and palynomorphs are dominant elements in these K-Pg interval

sediments. Horton (2002) showed a link between the palynological record of the Hell

Creek Formation in Montana and the terminal Cretaceous extraterrestrial impact, noting

15 that facies changes also affect post-impact species diversity. Nichols (2002) documented an abundance of angiosperms in the Hell Creek Formation in North Dakota; pteridophytes also comprised a fairly significant proportion but gymnosperms and bryophytes (mosses) were few. Another palynological study of the same formation in

South Dakota by Kroeger (2002) showed that lake and marsh deposits were dominated by pteridophytes, bryophytes and microphyllous vascular plants. Evidence of a fern spike in the U.S. Midcontinent and elsewhere (e.g., Wolfe, 1991) suggests that ferns dominated the early successional vegetation during the Early Paleocene. Thus, environmental and depositional factors also affected the palynomorph assemblages, as also confirmed in The

Netherlands (Brinkhuis and Schi Øler, 1996), and Antarctica (Askin and Jacobson, 1996).

An excellent summary of K-Pg spore and pollen biostratigraphy can be found in

Frederiksen (1996), who reviewed the several investigative techniques used by biostratigraphers to subdivide and correlate strata. By using range bases and tops of taxa, and relative abundances, as well as noting the effects of reworking and Lazarus taxa

(pseudoextinctions), palynologists have erected zones (interval, lineage, assemblage), correlated strata by climatic events, and employed graphic correlation. Stover et al.

(1996) reviewed K-Pg boundary dinoflagellates, acritarchs and prasinophytes, noting that few dinoflagellates experienced extinctions. Some palynofacies studies of these boundary sections have been undertaken (e.g., Oboh-Ikuenobe et al., 1997), and they focus on its use as a paleoenvironmental tool.

There is a dearth of K-Pg interval palynological studies in the northern

Mississippi Embayment. Frederiksen et al. (1982) published the first comprehensive biostratigraphic study spanning this interval in this region. They studied the

16 palynomorphs, foraminifera, and calcareous nannoplankton of Maastrichtian-Eocene sediments (Owl Creek, Clayton, Porters Creek) in two U.S. Geological Survey test wells in New Madrid County. Harrison et al. (1996) published another comprehensive biostratigraphical study encompassing all upper Cretaceous strata (pre-McNairy,

McNairy, Owl Creek) and lower Paleocene-Eocene strata (Porters Creek, Ackerman,

Holly Springs). This work was based on a study of cores from three boreholes drilled by the U.S. Geological Survey in the Benton Hills of Scott County. Harrison and Litwin

(1997) later focused more on the palynology of the Campanian strata. However, there are a few older palynological studies on post-Clayton sediments (e.g., Tschudy, 1973, 1975).

4. METHODS

4.1. FIELD WORK

Sediment samples were obtained from borehole cuttings in New Madrid County, cores in Scott County, and outcrops and trenches in Stoddard counties (Tables 4.1 and

4.2). Surface exposures of the Clayton, Owl Creek, and Porters Creek formations in the study area are rare at best due to erosion and land development operations. The Clayton

Formation, which measures approximately 3.01 to 3.62 m (10 to12 ft) in total thickness, can be found in New Madrid and Stoddard counties; however, it is missing in Scott

County.

4.1.1. Stoddard County. The best exposures of the Clayton Formation occur

along Crowley’s Ridge in Stoddard County. This exposure is found at a large “kitty

litter’ strip-mine owned by Nestle-Purina Company and contains approximately 185 cm

of a graded deposit containing layers of microtektites, invertebrate fossils, and abundant

terrestrial and marine palynomorphs (Campbell and Lee, 2001; Campbell, 2002;

Gallagher et al., 2005; and Campbell et al., 2008). The strip mine is located on the east

side of Crowleys Ridge in the W/2, Sec. 21, T27N, R11E (36º58.100’N x 89º52.300’W)

at an elevation of +390 feet (+117 meters). At this locality, the Porters Creek Formation

is mined as one of the ingredients used for manufacturing several brands of “kitty-litter”.

A large sump from the mine face excavations (Fig. 4.1) uncovered the Clayton Formation

and the underlying Owl Creek Formation. In order to measure and sample the freshly

exposed Clayton Formation, four large pits were excavated during the summers of 2003

and 2004. Eleven samples were carefully collected in lateral profiles from both

formations in Trenches 1 and 2. To minimize contamination, targeted horizons for

18 sampling were brushed clean and fresh rock surfaces were exposed after digging deeply into the pits. Samples were obtained for both palynological and micropaleontological

(foraminifera) analyses.

Figure 4.1. Mine view (north) with sump exposure of the Eocene and Paleocene strata at the “kitty litter” site (photograph courtesy of Carl Campbell).

4.1.2. New Madrid County. Sediment samples from New Madrid County come from New Madrid Test well 1-X, which was drilled in 1978 by the U. S. Geological

Survey as part of the Survey’s Earthquake Hazards Reduction Program (Frederiksen et al., 1982). The well is located in SW ¼ SW ¼ SE ¼ sec. 32, T. 21 N., R. 14 E., U.S.G.S.

Test well 1-X was drilled to a total depth of 699.1 m (2,316 ft) and penetrated lower

Paleogene, Upper Cretaceous, and lower Paleozoic rocks. Dr. Norman Frederiksen

(retired USGS Palynologist) provided processed palynological slides from the test well,

19 and six slides spanning the Porters Creek and Clayton formations have been used in this study.

4.1.3. Scott County. The Benton Hills is an upland area, generally regarded as an extension of Crowley’s Ridge, which is at the leading edge of the Mississippi

Embayment in southeastern Missouri. Cores from five boreholes drilled by the USGS in

1993 (BH-1, BH-2, BH-3, BH-9 and BH-10) and in storage at the McCracken Core

Repository in Rolla were studied. The U.S. Geological Survey’s Branch of Geological

Risk Assessment and the Missouri Department of Natural Resources, Division of

Geology and Land Survey coordinated the drilling program. The drilling sites are located on and near an abandoned gravel quarry (SW ¼, SW ¼ NW ¼ sec. 34, T. 29 N., R. 14

E), and extend to a cumulative depth of 71 m. The most productive borehole (BH-1) penetrates Paleocene, uppermost Cretaceous, and uppermost Ordovician strata. Thirty- one samples were obtained from BH-1, BH-9 and BH-10 for palynological analyses.

Table 4.1. Samples used for palynological analyses. ______County/Location Sample No. Slide No. Depth (m) Formation

New Madrid Test well I-X NM01 NM 1417 431.9 Porters Creek Test well I-X NM02 NM 1433 436.8 Porters Creek Test well I-X NM03 NM 1544.2 470.7 Porters Creek Test well I-X NM04 NM 1646 501.7 Porters Creek Test well I-X NM05 NM 1672.5 509.8 Porters Creek Test well I-X NM06 NM 1698.5 517.7 Clayton

Scott BH-1 SC01 TLE-2 7.4 Porters Creek BH-1 SC02 TLE-25 7.62 Porters Creek BH-1 SC03 TLE-3 9.45 Porters Creek BH-1 SC04 TLE-3a 11.9 Porters Creek BH-1 SC05 TLE-4 14.0 Porters Creek BH-1 SC06 TLE-4a 17.2 Porters Creek BH-1 SC07 TLE-4b 18.1 Porters Creek BH-1 SC08 TLE-5a 18.3 Owl Creek BH-1 SC09 TLE-5 18.8 Owl Creek BH-10 SC10 PC10-13.5 13.5 Porters Creek BH-10 SC11 PC10-14.3 14.3 Porters Creek BH-10 SC12 PC10-15.4 15.4 Porters Creek BH-10 SC13 PC10-15.8 15.8 Porters Creek BH-9 SC14 PC9-16.4 16.4 Porters Creek BH-10 SC15 PC10-16.7 16.7 Porters Creek BH-9 SC16 PC9-17.3 17.3 Porters Creek BH-9 SC17 PC9-18.1 18.1 Porters Creek BH-9 SC18 PC9-18.4 18.4 Porters Creek BH-9 SC19 PC9-19.5 19.5 Porters Creek BH-10 SC20 PC10-19.8 19.8 Porters Creek BH-9 SC21 PC9-21.0 21.0 Porters Creek BH-10 SC22 PC10-21.3 21.3 Porters Creek BH-9 SC23 PC9-22.5 22.5 Porters Creek BH-10 SC24 PC10-22.8 22.8 Porters Creek BH-9 SC25 PC9-23.7 23.7 Porters Creek BH-10 SC26 PC10-25.9 25.9 Porters Creek BH-9 SC27 PC9-30.1 30.1 Porters Creek BH-10 SC28 PC10-32.0 32.0 Porters Creek BH-10 SC29 OC10-33.5 33.5 Owl Creek BH-10 SC30 OC10-34.1 34.1 Owl Creek BH-10 SC31 OC10-34.4 34.4 Owl Creek

Table 4.1. Samples used for palynological analyses (continued). ______County/Location Sample No. Slide No. Depth (cm) Formation/Zone

Stoddard Trench 1 ST01 CL-1 180.0 Clayton/Hardground Trench 1 ST02 P1-G-120 160.0 Clayton/Gray Trench 1 ST03 P1-G-100 140.0 Clayton/Gray Trench 1 ST04 P1-G-80 110.0 Clayton/Glacuonite Trench 1 ST05 GL-G 110.0 Clayton/Glauconite Trench 1 ST06 GL-L 75.0 Clayton/Glauconite Trench 1 ST07 P1-LG-60 75.0 Clayton/Glauconite Trench 1 ST08 P1-DG-40 60.0 Clayton/Glauconite Trench 1 ST09 P1-DG-20 50.0 Clayton /Glauconite Trench 1 ST10 CL-2 20.0 Clayton/Coquina Trench 2 ST11 P2-OC 0.0 (base) Owl Creek

Table 4.2. Samples used for foraminiferal analyses; no depth information is available. ______County/Location Sample No. Slide No. Formation/Zone

Stoddard Trench 1 FOC1 CCOC-1 Owl Creek Trench 1 FOC2 CCOC-2 Owl Creek Trench 1 FOC3 CCOC-3 Owl Creek Trench 1 FOC4 CCOC-4 Owl Creek Trench 1 FOC5 CCOC-5 Owl Creek Trench 1 FOC6 CCOC-6 Owl Creek Trench 1 FGLG GL-G Clayton/Glauconite Trench 1 FCL1 CL-1 Clayton/Coquina Trench 1 FGLL GL-L Clayton/Glauconite Mine spoil FKT4 KT-4 Porters Creek

4.2 ANALYTICAL TECHNIQUES

Sample processing for palynology and foramifera was conducted in the

Paleontology Laboratory at the Missouri University of Science and Technology.

Standard palynological procedures of digesting samples in mineral acids were used for processing (Traverse, 2007). Forty-eight samples were used for palynomorph analyses.

Transmitted light microscopy was used for routine identification and description of palynomorphs, and the data was used to determine the diversity and abundance of taxa.

Three slides were prepared for each sample. In unproductive samples with few specimens, the three slides were examined and all species identified were recorded. Only one slide was examined in detail for productive samples, although the other two slides were scanned to make sure that no large discrepancies existed between them. At least

200 specimens per slide were counted in the productive samples.

Palynomorphs were identified using existing literature and reference indices and they include Norris (1986) for nonmarine algae, Stanley (1965), Frederiksen et al. (1982),

Lentin and Williams (1989), and Fensome et al. (2004) for dinoflagellate cysts, Elsik

(1993) for fungi, and Anderson (1960), Stanley (1965), Tschudy (1975), Jansonius and

Hills (1976, and supplements up to 2002), Jameossanaie (1987), Frederisken et al.

(1982), Pocknall and Nichols (1996), and Nichols (2002) for spores and pollen. Age diagnostic and paleoenvironmentally important taxa were photographed using a Nikon

Coolpix™ 9000 digital camera at 40x and 100x. Length and width measurements for palynomorph species identified in the Clayton, Owl Creek, and Porters Creek formations were recorded to the nearest tenth of a micrometer ( µm) using an ocular micrometer.

Both microscope and universal coordinates (Lovins Field Finder) were recorded. Poorly

23 preserved or non-productive samples were not included in the palynomorph counts.

Percentages for general categories of palynomorphs, i.e., spores versus pollen, marine vs. terrestrial, angiosperms vs. gymnosperms, were calculated and recorded.

Forty samples were used for palynofacies analyses. Kerogen slides were not available for the New Madrid Test Well I-X samples and sample SC02 (BH-1), and sample SC14 (BH-9) was barren; therefore, they were excluded from this study.

Transmitted light microscopy was also used for the identification of dispersed organic matter (palynodebris). Three hundred specimens (each with a 5 µm size cutoff) were point counted per kerogen slide, converted to percentages, and subjected to multivariate statistical analyses using programs written by Kovach (2002). Minimum variance cluster analysis (Q-mode and R-mode) was performed on a data matrix generated by Euclidean correlation coefficient. Log transformation (log 2) produced an octave scale that allowed organic components with low percentage values to play a bigger role in grouping samples

(Beck and Strother, 2004). The Euclidean distance is especially designed to work with continuous or ratio scales and the linkage averages all distances between pairs of objects in different clusters to decide how far apart they are (Sokal and Michener, 1958). In addition, data used for cluster analysis were analyzed using principal components analysis for comparison purposes.

The Owl Creek, Clayton and Porters Creek at the Nestle Purina Plant were sampled for foraminifera, and processed using standard techniques (Snyder and Waters,

1984). All but one sample were obtained from fresh surface exposures; the Porters Creek sample was obtained from a mine spoil. For samples that were very coarse and consolidated, NaOH and Na hexametaphosphate, Calgon ™ were added to the water and

24 soaked overnight. Specimens were picked from 74 µm and 150 µm fractions, and affixed to 60-square grid micropaleontological slides with the water-soluble glue Tragacanth™.

They were then identified using a binocular microscope 30X and 40X objectives. With the exception of the New Madirid Test Well 1-X slides provided by U.S. Geological

Survey, palynological and foraminiferal slides are currently in storage at the Paleontogy

Laboratory at the Missouri University of Science and Technology. For detailed resolution, some palynomorphs as well as foraminifera were examined using the

Scanning Electron Microscope (SEM) JEOL T330A housed by the Department of

Metallurgical Engineering at the Missouri University of Science and Technology.

To confirm the thickness and lateral extent of the Clayton Formation, driller’s logs and well logs from water wells and oil test wells maintained by the Missouri

Department of Natural Resources were reviewed. There are about 60 wells with driller’s

logs and 23 wells with electric logs in the study area, all of which were reviewed and tops

picked for Porter’s Creek, Clayton and Owl Creek formations (Campbell et al., 2008).

5. RESULTS

5.1. LITHOLOGIC DESCRIPTIONS

Descriptions of the lithologic units include observations made during field work and detailed visual analysis of core sections at the McCraken Repository. Color, grain size, macrofossils and trace fossils were noted. Detailed lithological descriptions, photographs, and sampling of the Benton Hills cores (BH-1, BH-2, BH-3, BH-9, BH-10) were completed during the summer months of 2002 and 2003 (Appendix A). Harrison et al. (1996) was used as a guide for description. Cores BH-2 and BH-3 were initially described but were later excluded from analysis due to condensed sections of the Porters

Creek and Owl Creek formations. These two cores also cover mostly Cretaceous strata.

The Clayton Formation is missing in all the BH core sections.

5.1.1. Owl Creek Formation. The Maastrichtian Owl Creek Formation comformably overlying the McNairy Formation is exposed along Crowley’s Ridge in

Scott and Stoddard counties, measures 3.32 m to 30.1 m thick, and down dips southeastward into the subsurface of the Mississippi Embayment (Unklesbay and

Vineyard, 1992). The Owl Creek consists of massive, sandy, micaceous clay and commonly is observed with glauconite and small marine invertebrate fossils. In BH-1 core section, the glauconite found has altered to iron oxides. In outcrops, the formation is mostly dominated by molds of thin-shelled bivalves and contains ammonites. The formation is heavily bioturbated in some places and contains many limonite coated burrows. Fresh exposures of the formation are commonly bluish-gray but tend to have more of a yellowish-brown color upon exposure to weathering. Harrison et al. (1996) found fossil marine invertebrates as well as plant remains in outcrops just northeast of the

26 drill holes; however, such fossils were not recovered from the Benton Hills core sections

(Appendix A).

5.1.2. Clayton Formation. The Lower Paleocene Clayton Formation uncomformably overlies the Owl Creek, measures approximately 3 m in thickness, and occurs only in New Madrid and Stoddard counties. In Stoddard County, the formation can be divided into four units based on lithology, color, and fossils (Figures 5.1 and 5.2).

5.1.2.1. Coquina Zone. The basal unit measures approximately 30 cm in thickness and is composed of a limestone coquina containing an abundant assortment of reworked Cretaceous macro- and microfossils. This unsorted unit has a “boudinage” appearance, which typically represents strongly deformed sedimentary rocks. According to Campbell et al., 2008, the unit appears to be that of a scour fill which trends southeast to northwest. The scours are 30 to 50 cm in cross section and 30 cm thick (Figures 5.2 and 5.3). Some are isolated while others are interconnected and the tops are relatively flat and concordant. Within this unit are large oblate to spherical rip-up clasts measuring

3 to 20 cm containing layers of microtektites. The microtektites consist mostly of the spherical forms (Figure 5.4); however, teardrop and dumb-bell shaped forms are also present (Figure 5.5; Campbell et al, 2008). Some appear to have been welded together to form doublets and triplets. The colors vary from dark brown to tan to green. The spherical varieties have a “bubbly” internal appearance. All of the microtektites range in size from 1/2 to +3 mm. Many of the spherical forms have calcite centers; a few appear to have glass centers. Oolites measuring < ¼ mm are found scattered throughout the basal unit and within the rip-up clasts. The oolites have a shiny brown coating which is incased by either clear, sub-angular quartz or fecal pellet centers. Also, scattered

27 randomly through the coquina zone are floating grains of frosted subrounded quartz sand.

The coquina matrix is biomicrite carbonate. Carbonized wood and seeds are also present in this zone.

Most of the macrofossils are mollusks with rare vertebrate specimens such as bony fish, sharks, rays, turtles, and several outstanding Mosasaur fossils (Campbell and

Lee, 2001; Gallagher et al., 2005). Fifty-eight species of invertebrates occur in this zone:

50% bivalves and 30% gastropods. Commonly, bivalve specimens have both valves attached and closed. This zone also contains an assortment of reworked Late Cretaceous benthic foraminifera and palynomorphs (Campbell et al. 2008).

5.1.2.2. Glauconite Zone. This 70 cm-thick zone consists of soft, green glauconitic, sandy clay containing an abundance of Late Cretaceous macrofossil fragments and microfossils, broken and displaced limonitic burrows and internal casts and molds of mollusks and cephalopods. Commonly, hard concretions of calcified fossils are found within small depressions cut into the lower coquina zone. This zone preserves

Late Cretaceous fossils including internal casts and molds and fragments of marine invertebrates, and an assortment of benthic foraminifera. Most of the large fossils have been calcified. It is interesting to note that a majority of the ammonites recovered occur in this zone. The Glauconite Zone appears to contain fossils of animals that were probably pelagic while the lower Coquina Zone contains large benthic fossils, such as

Exogyra costata .

5.1.2.3. Gray Zone. Here the Glauconite Zone uniformly grades into the Gray

Zone, which consists of soft, light-gray clay containing specks of glauconite and occasional manganese oxide pebbles and Thalassinoides burrows (dwelling burrows

28 common in marine shelf environments) in the upper portion. The Gray Zone lacks macrofossils but contain microfossils such as marine and terrestrial palynomorphs and foraminifera.

5.1.2.4. Hardground Zone. This uppermost unit consists of 20 cm of hard clay.

This unit varies slightly from the lower unit by its indurated appearance, which may be

indicative of a hardground. The base of the Porters Creek rests on this upper zone and

includes very large (>100 cm) torpedo shaped, hollow limonitic concretions (Figure 5.6).

Note that the Porters Creek and Owl Creek formations both contain mica but the Clayton

Formation does not.

Gray

Figure 5.1. Cross sectional view of a trench excavated at the Nestle Purina Plant in Stoddard County, Missouri illustrating the four distinct zones of the Clayton Formation. LS = Limonite.

Figure 5.2. A cross sectional view of scour filled structures occurring in the Coquina Zone and trending in a NW to SE direction.

Figure 5.3. Photograph of trench wall containing complete section of Paleocene Clayton Formation above Cretaceous Owl Creek Formation. Note the deep scour into Owl Creek in lower right corner. Hammer in lower right corner is 29 cm long. White rectangle in lower right is a 15 cm scale bar. Modified from Campbell et al. 2008.

Figure 5.4. Some common spherical microtektites found within the Coquina Zone of the Clayton Formation in Stoddard County, Missouri (courtesy of Carl Campbell).

Figure 5.5. Some variations in the splashform-type microtektites obtained from the Clayton Formation of Stoddard County, Missouri (courtesy of Carl Campbell).

Figure 5.6. An example of some very large torpedo shaped, hollow limonite concretions observed between the uppermost Clayton and the lowermost Porters Creek.

5.1.3. Porters Creek. The Porters Creek Formation is remarkably uniform, massive dark gray to almost black gray or brownish-gray, and when exposed and dried, the color changes to a lighter gray. The thickness of the Porters Creek varies, and in some places, exceeds 60.3 m. The clay is characteristically faintly mottled and contains a small amount of sand with fine muscovite flakes. Glauconite, biotite, and glass shards were found within core sections and typically showed brittle behavior breaking with a conchoidal fracture. With the exception of palynomorphs and foraminifera, other fossils are rare to absent in core sections or outcrop samples. This unit is often processed for

“kitty litter” in Missouri and Illinois. The Porters Creek conformably overlies the

Clayton Formation and is unconformably overlain by the Ackerman Formation.

5.2. PALYNOMORPHS

5.2.1. Overview. The following nonmarine palynomorph groups have been identified in this study: spores, pollen, fungal remains, and algae. Marine palynomorphs are dinoflagellates, acritarchs, and foraminiferal linings. Palynomorphs are generally well preserved in many samples, especially those from the Porters Creek Formation.

However, extensive reworking, particularly in the Clayton Formation, resulted in a mixture of Cretaceous and Paleocene palynomorphs in that unit. As a result, many

Clayton palynomorphs are poorly preserved and fragmented.

Three hundred and seventy-nine types of palynomorphs were identified in the

three formations studied, and they represent 282 nonmarine and 97 marine taxa.

Angiosperms dominate the nonmarine assemblage, while marine taxa are mainly

dinoflagellates. In the Owl Creek Formation, one nonmarine alga, four gymnosperm taxa, 16 bryophyte and pteridophyte spores, 2 dinoflagellate cyst types, and 36 angiosperm pollen taxa were identified. Species identified in the Clayton Formation included two nonmarine algae, three gymnosperm pollen, 20 spores, 182 dinoflagellate cysts, and 72 angiosperm pollen. The most diverse spore and pollen assemblage was identified in the Porters Creek Formation, which has four nonmarine algae, 40 dinoflagellate cysts, 23 gymnosperm pollen, 42 spores, and 138 angiosperm pollen.

Foraminiferal linings were surprisingly absent from the palynomorph counts in the Owl

Creek and Porters Creek samples, although foraminifera have been recovered from both formations, albeit very rare in the latter (see section 5.5). Table 5.1 compares the diversity among only spores, pollen and marine microplankton. Appendices B through J

34 contain quantitative data for palynomorphs in the borehole and trench sections as well as lists of taxa identified in the three formations studied.

5.2.2. Nonmarine Palynomorphs. Palynomorphs of lower plants (algae, fungi, bryophytes, lycopods) and vascular plants (pteridophyte ferns, gymnosperms, angiosperms) are represented in the formations studied. Of the 110 taxa identified in the

Clayton Formation (286 spore specimens vs. 1,353 pollen total count), nine are missing from the underlying Owl Creek. As shown in Figure 5.7 there are fluctuations in spores versus pollen for the Clayton samples, with pollen having a higher diversity (Table 5.2).

Pollen, mostly angiosperms, also dominates the Porters Creek and Owl Creek palynoflora

(Figs. 5.8-5.11; see also Table 5.4). In the Owl Creek, Clayton and Porters Creek, pollen constitute approximately 81.5%, 82.6%, and 84.4% of the total nonmarine palynomorph counts (excluding fungal remains and algae), respectively. Angiosperms comprise 78-

85% of the identified pollen in all these formations. Normapolles pollen, a unique Late

Cretaceous and Early Cenozoic oblate and triaperturate angiosperm group found in the middle and high northern latitudes of eastern North America and Europe, occur in all three formations. This extinct pollen group comprises 16.6% of the angiosperm assemblages. Gymnosperms, bryophytes and pteridophytes are fewer.

5.2.3. Marine Palynomorphs. Low to fairly high diversity marine palynomorph assemblages have been identified. The Clayton Formation samples yielded a total of

1007 marine palynomorph specimens, and thus represent the highest percentage among the three formations (Table 5.3). They include 874 dinoflagellates (89 species), 117 acritarchs, and 16 foraminiferal linings (Table 5.2). A total of 226 marine palynomorph specimens representing 180 dinoflagellates and 46 acritarchs were identified in the

Porters Creek Formation samples. The numbers for the Owl Creek Formation are lower

in comparison to the other two formations. Section 5.2.1 earlier noted the absence of

foraminiferal linings in the total counts for the Owl Creek and Porters Creek.

Table 5.1. Species diversity for palynomorph assemblages (excluding freshwater algae and fungi) in the Clayton, Porters Creek, and Owl Creek formations.

Formation Total No. No. of Micro- No. of Spores No. of Pollen examined microplankton spores % pollen grains Plankton % grains % Porters 247 38 15.4 42 17.0 167 67.6 Creek Clayton 176 81 46 20 11.4 75 42.6%

Owl Creek 89 30 33.7 16 18.0 43 48.3%

Table 5.2. Comparison of data for nonmarine palynomorphs (excluding algae and fungi) recovered from the Porters Creek, Clayton, and Owl Creek formations. Note: DS Gym = Different species of gymnosperms, DS ang. = Different species of angiosperms, DPS = Different pollen species, and DSS = Different spore species.

Gym. Ang. DS DS Pollen Spore DPS DSS % % Gym. Ang. % % Porters Creek 21.4 78.6 23 138 84.4 15.6 167 42

Clayton 19.2 80.8 3 72 82.6 17.4 75 20 Owl Creek 16.3 83.7 4 36 81.5 18.5 43 16

Table 5.3. Total numbers of marine palynomorphs recovered from the Porters Creek, Clayton, and Owl Creek formations. See section 5.2.1 for statement about foraminiferal linings.

Formation Dinoflagellates Acritarchs Foram linings Total

Porters Creek 180 46 0 226

Clayton 874 117 16 1007

Owl Creek 142 33 0 175

Table 5.4. Total numbers and percentages of all palynomorphs in the Porters Creek, Clayton, and Owl Creek formations. Emphasis is placed on the terrestrial vs. marine percentages.

Formation Sample(s) Terrestrial Terrest. % Marine Marine %

Porters Creek 31 4820 95.5 226 4.47

Clayton 12 1649 62.1 1007 37.9

Owl Creek 7 571 76.5 175 23.5

Clayton

Owl Creek

Figure 5.7. Percentage distribution of palynomorphs in the Clayton and Owl Creek formations, Stoddard County. Emphasis is placed on Terrestrial vs. Marine, Spores vs. Pollen, Angiosperms vs. Gymnosperms, and the presence/absence of ferns and allied ferns and Normapolles. Marine palynomorphs are dinoflagellate cysts, and acritarchs.

Porters Creek

Clayton

Figure 5.8. Percentage distribution of palynomorphs in the Porters Creek and Clayton formations, New Madrid County. Emphasis is placed on Terrestrial vs. Marine, Spores vs. Pollen, Angiosperms vs. Gymnosperms, and the presence/absence of ferns and allied ferns. Marine palynomorphs are dinoflagellate cysts and acritarchs.

SC01 SC02

SC03

SC04 Porters Creek

SC05

SC06

SC07 Owl SC086SC Creek SC09

Figure 5.9. Percentage distribution of palynomorphs in the Owl Creek and Porters Creek formations in BH-1 core, Scott County. Emphasis is placed on Terrestrial vs. Marine, Spores vs. Pollen, Angiosperms vs. Gymnosperms, and the presence/absence of ferns and allied ferns. Marine palynomorphs are dinoflagellate cysts and acritarchs. Patterned bars represent barren samples.

Figure 5.10. Percentage distribution of palynomorphs in the Porters Creek Formation in BH-9 core, Scott County. Emphasis is placed on Terrestrial vs. Marine, Spores vs. Pollen, Angiosperms vs. Gymnosperms, and the presence/absence of ferns and allied ferns. Marine palynomorphs are dinoflagellate cysts and acritarchs. Patterned bars represent barren samples.

Figure 5.11. Percentage distribution of palynomorphs in the Porters Creek formation in BH-10 core, Scott County. Emphasis is placed on Terrestrial vs. Marine, Spores vs. Pollen, Angiosperms vs. Gymnosperms, and the presence/absence of ferns and allied ferns. Marine palynomorphs are dinoflagellate cysts and acritarchs. Patterned bar represents barren sample.

5.3. SYSTEMATIC PALYNOLOGY

Palynomorphs recovered from the Clayton, Owl Creek, and Porters Creek formations are listed according to the following major taxonomic groups: spores, pollen, nonmarine algae, fungi, dinoflagellates and acritarchs. The taxa included herein consist of individual species and undifferentiated genera. Use of undifferentiated genera indicates that their species are difficult to separate consistently because of the state of preservation and/or that their ranges are uncertain; therefore, they are not all used for interpretation.

Spore and pollen classification scheme shown in Figure 5.12 was used in this study. Spores and pollen united into multiple units (dyads, tetrads, polyads, etc.) are treated according to the morphology of a single component grain. Classifications of dinoflagellates follow Fensome et al. (1993) and Fensome and Williams (2004). Age ranges of taxa identified were confirmed using Palynodata (2008), which is a comprehensive Windows bibliographic database.

Appendices B through G list in alphabetical order the palynomorphs identified in

each study site, while Appendices H through J list the nonmarine palynomorph taxa

found in each formation. Appendix K shows the general illustrations and glossary of the

palynomorph terms. Plate and figure numbers (Plates 1 through 8) identify illustrated

palynomorph taxa in Appendix L. In this section, all the taxa identified in this study are

listed; there are remarks for some previously described species, and detailed descriptions

of several palynomorphs that were not assignable to known species. These six potentially

new taxa are designated as lettered species (e.g., Cerodinium sp. A). In the discussion of abundance counted, palynomorphs have been converted to percentages and assigned a

43 relative abundance as follows: <0.1% = rare; <1.0% = infrequent; 1.0-3.9% = common;

4.0-6.9% = abundant; and >7.0% = dominant. Note that the names of authors and dates of publications that follow named species are part of the formal names and are not references to publications listed in the bibliography section.

Figure 5.12. Classification scheme used for palynomorphs (adapted from De Villiers, 1997).

SPORES

Trilete (Cingulate)

Cingulatisporites dakotaensis Stanley 1965 Cingulatisporites radiatus Stanley 1965 Remarks: Trilete spore, outline in polar view ranges from subcircular to subtriangular. Sculpture appears to be verrucate. Spore grain has a distinct cingulum present, which measures approximately 4 µm from spore vesicle. Tetrad mark is generally distinct. Cingulum is psilate with often a yellow-brown color and possesses a radially striated appearance. P/E ratio is 1.0 (subspheroidal). Distribution is “common” for many samples in the Porters Creek Formation of Scott County. Specimens are 20-25 µm long and 20-25 µm wide. Osmunda comaumensis Cookson 1953 Osmundacidites stanleyi Douglas 2002 Osmundacidites sp., Plate 2, Figure A Schizaeoisporites eocaenicus Potonié 1956 Schizaeoisporites sp. Stereisporites sp. Stereisporites antiquasporites (Wilson & Webster 1946) Dettmann 1963 Stereisporites stereoides Potonié and Venitz-Pflug 1953

Trilete (Acingulate)

Anemia tricornitata (Weyland and Greifield) Stanley 1965 Appendicisporites tricornatus (Weyland & Greifeld 1961) Groot et al. 1963, Plate 2, Figure C Baculatisporites sp. Baculatisporites quintus (Thomson & Pflug 1953) Krutzsch 1967 Bullasporis sp. Cardioangulina diaphana Wilson & Webster 1946 Cicatricosisporites dorogensis Potonie and Gelletich, 1933, Plate 1, Figure N

Cicatricosisporites sp., Plate 1, Figures J and K Cyathidites minor Couper 1953, Plate 1, Figure E Remarks: Trilete spore, outline is straight to concave triangular and spore has a thickened or raised trilete mark. Commissure is slightly gaping and the apices are rounded to subrounded. P/E ratio is 1.0 (subspheroidal). Distribution is “common” for samples in the Clayton and Porters Creek formations of Scott and Stoddard counties. Specimens are 35-50 µm long and 32.5-50 µm wide. Cyathidites sp., Plate 1, Figures L and M Deltoidospora sp., Plate 1, Figures L and M Deltoidospora concava Takahashi 1975 Foveosporites sp. Foveosporites triangulus Krutzsch 1959 Gleichenia circinidites (Cookson 1953) Dettmann 1963 Gleichenia sp. Gleichenia triangular Stanley 1965 Remarks: Trilete spore. In polar view, outline exhibits concave triangular shape with rounded apices; trilete mark is very distinct. Commissure is widely gaping. Kyrtome (torus) is present in most specimens. Sculpture is psilate. P/E ratio is 1.13 (subspheroidal). Distribution is “infrequent” for samples in the Clayton, Owl Creek, and Porters Creek formations. Specimens range from 22.5-40 µm long 20-42.5 µm wide. Gleicheniidites senonicus Ross 1949, Plate 1, Figures G and H Gleicheniidites sp. Hamulatisporis hamulatis Krutzsch 1959, Plate 2, Figure E Laricoidites magnus Potonié 1958 Leiotriletes adriennis pseudomaximus (Pflug & Thomson 1953) Krutzsch 1959 Leptolepidites tenuis Stanley 1965 Lycopodium hamulatum (Krutzsch 1959) Frederiksen 1980 Lycopodium heskemensis (Pflanzl 1955) Frederiksen 1980 Lycopodium sp. Lygodiumsporites adriennis (Potonié & Gelletich 1933) Potonié 1956, Plate 1, Figure A Microreticulatisporites sp.

Polypodiaceoisporites sp. Retitriletes sp. Selaginella perinata (Krutzsch et al. 1963) Frederiksen 1980 Sphagnum australe (Cookson 1947) Drozhastchich 1961, Plate 1, Figure F Sphagnum regium Drozhastchich 1961 Sphagnum sp. Sphagnum triangularum (Mamczar 1960) Frederiksen 1980 Stereisporites antiquasporites (Wilson & Webster 1946) Dettmann 1963 Stereisporites minor Zhang 1990 Stereisporites stereoides (Potonié & Venitz 1934) Pflug in Thomson & Pflug 1953 Stereisporites sp. Striatotheca triangulata (Cramer et al. 1974) Eisenack et al. 1976 Todisporites minor Couper 1963, Plate 1, Figure 3 Todisporites sp., Plate 1, Figure 2 Toroisporites major (Pflug and Thomson in Thomson & Pflug 1953) Stanley 1965 Toroisporites sp., Plate 1, Figure I Undulatisporites concavus Kedves 1979

Monolete (Perinous)

Baculatisporites sp. Baculatisporites quintus

Monolete (Aperinous)

Laevigatosporites haardti (Potonié & Venitz 1934) Thomson & Pflug 1953 Laevigatosporites pseudomaximus Pflug and Thomson in Thomson and Pflug 1953 Laevigatosporites sp. Palaeoisoetes subengelmannii Elsik 1968 Reticuloidosporites pseudomurii Elsik 1968

POLLEN

Inaperturate

Cupressacites hiatipites (Wodehouse 1933) Krutzsch 1971, Plate 2, Figure L Inaperturopollenites spp. Types A-D, Plate 1, Figure D Sequoia sempervirens Zalkinskaya 1953 Sequoiapollenites paleocenicus (Thiergart 1938) Stanley 1965 Taxodiaceaepollenites hiatus (Potonié 1931) Kremp 1949

Triprojectate (Normapolles)

Aquilapollenites bertillonites Funkhouser 1961 Aquilapollenites murus Stanley 1961

Polyplicate

Ephedra claricristata Shakhmundes 1965 Ephedra exiguua Frederiksen 1983 Ephedra hungarica (Nagy 1963) Frederiksen 1980 Ephedra sp. Ephedra voluta Stanley 1965 Remarks: Inaperturate ellipsoidal. Sculpture of the thin ektexine consists of approximately three low, wide ridges, which cut across the grain at sharp angles and then loop around backwards giving the appearance of having six muri. Spaces between the ridges are approximately .05 to 1 µm wide. P/E ratio is 3.83 (perprolate). Distribution is “infrequent” for samples in the Porters Creek and Clayton formations in New Madrid and Stoddard counties. Specimens range from 30-57.5 µm long and 12.5-30 µm wide. Ephedripites sp., Plate 2, Figures G and H

Bisaccate

Abies balsamea Leopold 1969 Abies sp. Pinus cembraeformis Frederiksen 1983 Pinus scopulipites (Wodehouse 1933) Krutzsch 1971 Pinus semicircularis Stanley 1965 Pinus strobipites Wodehouse 1933 Pinus sp., Plate 2, Figure I

Monoporate

Aglaoreidia pristine Fowler 1971 Corollina (Classopollis ) sp. Graminidites gramineoides (Meyer 1956) Krutzsch 1970 Graminidites sp., Plate 2, Figure F Milfordia incerta (Pflug & Thomson in Thomson & Pflug 1953) Krutzsch 1961, Plate 2, Figure B Milfordia minima Krutzsch 1970

Diporate

Diporopollenites sp. Type A Diporopollenites sp. Type B Diporopollenites sp. Type C

Triporate

Alsophilidites kerguelensis Cookson 1947 Annutriporites tripollenites (Rouse) Sepúlveda & Norris 1982 Betula infrequens Stanley 1965, Plate 2, Figure N Betulaceoipollenites sp.

Carya paleocenica Stanley 1965 Caryapollenites imparalis Nichols & Ott 1978 Caryapollenites simplex (Potonié 1931) Tschudy & van Loenen 1970, Plate 2, Figures P and Q Caryapollenites veripites (Wilson & Webster 1946) Nichols & Ott 1978 Remarks: Triporate, circular to slightly triangular in equatorial view, oblately flattened. Three round to broadly elliptical shaped pores are present. Exine is smooth to finely granulate. Grains are somewhat thinner in the center causing them to brake or corrode, thus, giving it an irregularly modified area near the center. P/E ratio is 1.0 (subspheroidal). Distribution is “abundant” for samples in the Porters Creek Formation. Specimens range from 27.5-42.5 µm long and 27.5-42.5 µm wide. Celtipollenites gracillis Nagy 1969 Compositoipollenites grandiannulatus Frederiksen 1983 Compositoipollenites sp. Corylus granilabrata Stanley 1965 Corylus sp. Endoinfundibulapollis sp. Engelhardtia microvoveolata Stanley 1965 Engelhardtia sp. Extremipollis caminus Tschudy 1975 Extremipollis versatilis Tschudy 1975 Extremipollis vivus Tschudy 1975 Extremipollis sp., Plate 3, Figure D Insulapollenites rugulatus Leffingwell 1971 Interpollis sp. Kyandopollenites sp. Maceopolipollenites amplus Leffingwell 1971 Momipites coryloides Wodehouse 1933, Plate 3, Figure B Momipites dilatus Fairchild in Stover et al. 1966 Momipites fragilis Christopher 1979 Momipites inaequalis Anderson 1960

Momipites marylandicus Groot & Groot 1962 Momipites microfovelolatus (Stanley 1965) Nichols 1973 Remarks: Triporate. Grains are oblate with triangular outline in polar view. Sides are slightly convex with rounded apexes. A fine punctuation sculpture with lumina is present. P/E ratio is 1.05 (subspheroidal). Distribution is “common” for many samples in the Clayton, Owl Creek, and Porters Creek formations. Specimens are 17.5 µm long and 17.5-22.5 µm wide. Momipites sp. Momipites strictus Frederiksen & Christopher 1978 Momipites tenuipolus Anderson 1960 Myricipites annulites (Martin & Rouse 1966) Norris 1986 Nudopollis endangulatus , (Pflug in Thomson & Thomson & Plug 1953) Pflug 1953 Nudopollis terminalis (Pflug & Thomson in Thomson & Pflug 1953) Elsik 1968 Nudopollis sp. Osculapollis sp. Pistillipollenites sp. Pistillipollenites mcgregorii Rouse 1962 Platycarya sp. Plicapollis retusus Tschudy 1975 Plicapollis sp. Plicapollis usitatus Tschudy 1975 Plicatopollis magniorbicularis Frederiksen 1983 Plicatopollis sp. Proteacidites retusus Anderson 1960 Proteacidites sp. Pseudoculopollis admirabillis Tschudy 1975 Pseudoplicapollis serenus (Krutzsch 1967) Tschudy 1975 Pseudovacuopollis involutus (Krutzsch & Pacltová 1967) Tschudy 1975 Semioculopollis sp., Plate 3, Figure F Subtriporopollenites nanus (Pflug and Thomson in Thomson & Pflug 1953) Fredriksen 1980

Thomsoniopollis sp. Triatriopollenites paradoxus Frederiksen 1980, Plate 2, Figures J and K Triatriopollenites proprius Frederiksen 1980, Plate 2, Figure R Triatriopollenites sp., Plate 2, Figure O Triporopollenites maternus Frederiksen 1980 Triporopollenites sp. Trudopollis plenus Tschudy 1975 Trudopollis variabilis (Pflug 1953) Tschudy 1975 Trudopollis sp. Tschudypollis retusus Anderson 1960 Ulmipollenites sp. Ulmipollenites undulosus Wolfe 1934 Vacuopollis munitus Tschudy 1975

Pantoporate

Chenopodipollis nuktakensis Norris 1986 Chenopodipollis sp., Plate 3, Figure E Juglans nigripites Wodehouse 1933

Zonoporate

Alnipollenites scoticus Simpson 1961 Alnus trina Stanley 1965 Alnus vera (Potonié 1931) Martin & Rouse 1966 Casauarinidites sp. Jarzenipollenites trinus (Stanley 1965) Kedves 1980 Polyatriopollenites stellatus Pflug 1956 Polyvestibulopollenites verus (Potonié 1931) Thomson & Pflug 1953

Monosulcate

Arecipites columellus Leffingwell 1971 Remarks: Monosulcate, sulcus extends close to the entire length of the grain and becomes narrower at the ends. Shape is elongated ellipsoidal. Exine appears thick but becomes thinnest adjacent to the sulcus. Distinct ectosexinous and columella layers are visible. Structure is reticulate. P/E ratio is 1.7 (prolate). Distribution is “infrequent” for samples in the Porters Creek and Clayton formations of Scott and Stoddard counties. Specimens are 30 µm long and 17.5-22.5 µm wide. Arecipites rousei Frederiksen 1973 Arecipites sp. Confertisulcites fusiformis Frederiksen 1973 Confertisulcites sp. Cycadopites giganteus Stanley 1965 Remarks: Monocolpate, pollen has a smooth to finely granular, fusiform shape with psilate thin exine. Furrow extends the entire length of grain and is wider at its ends than in the middle. Sulcus is typically open. P/E ratio is 1.75 (prolate). Specimen sizes range from 50-62.5 µm long and 30 µm wide; 13 specimens measured. Distribution is “abundant”. Cycadopites giganteus occurs in the Owl Creek, and Clayton and Porters Creek formations. Cycadopites scabratus Stanley 1965 Remarks: Cycadopites scrabratus is present in the Owl Creek and Porters Creek. Cycadopites sp. Liliacidites complexus (Stanley 1965) Leffingwell 1971 Liliacidites dividuus Brenner 1963 Liliacidites inaequalis Singh 1971 Liliacidites intermedius Couper 1953 Liliacidites sp. Liliacidites tritus Frederiksen 1980 Liliacidites vittatus Frederiksen 1980 Longapertites sp. Monocolpopollenites sp.

Trichotomosulcate

Triplanosporites sinuosus Pflug 1952

Tricolpate

Acer striatellum (Takahashi 1961) Frederiksen 1980 Bombacadites reticulatus (Couper 1960) Krutzsch 1970 Bombacadites sp. Carpinus subtriangula Stanley 1965 Cupuliferoipollenites sp. Eucommia sp. Faguspollenites sp. Fraxinoipollenites medius Frederiksen 1980 Fraxinoipollenites sp. Fraxinoipollenites variabillis Stanley 1965 Myocolpopollenites reticulatus Elsik in Stover et al. 1966 Myriophyllum sp. Platanus occidentaloides Frederiksen 1980, Plate 3, Figure C Platanus sp. Pseudotricolpites sp. Quercoidites ? genustriatus Stanley 1960 Quercoidites inamoenus , (Takahashi 1961) Frederiksen 1980 Quercoidites microhenricii (Potonié 1931) Potonié 1960 Quercoidites sp. Retibrevitricolpites sp. Rousea linguiflumena Pocknall & Nichols 1996 Rousea monilifera Frederiksen 1980 Salixipollenites parvus Frederiksen 1980 Striopollenites terasmaei Rouse 1962 Tricolpites bathyreticulatus Stanley 1965

Tricolpites erugatus Hedlund 1966 Tricolpites hians Stanley 1965 Tricolpites parvus Stanley 1965 Tricolpites sp. Tricolpites sp. Type A (large pollen) Tricolpites sp. Type B (large pollen) Tricolpites splendens van der Hammen 1954

Pantocolpate

Polycolpites sp.

Tricolporate

Ailanthipites berryi Wodehouse 1933 Ailanthipites marginatus Frederiksen 1983 Ailanthipites speciipites Wodehouse 1933 Araliaceoipollenites profoundus Frederiksen 1980 Aster sp. Basopollis obscurocostatus Tschudy 1975 Remarks: Triporate. In polar view, shape of pollen amb is triangular and often distorted in triplane form. Exine is microverrucate. Ribs or arci are visible in triplane or equatorial view. P/E ratio is 1.38 (prolate) to 1.0 (subspheroidal). Distribution is “common” in several Clayton and Porters Creek samples. Specimen measurements range from 27.5-35 µm long and 20-35 µm wide. Basopollis sp. Boehlensipollis hohlii Krutzsch 1962 Boehlensipollis minimus (Leffingwell 1971) Pocknall & Nichols 1996 Boehlensipollis sp. Caprifoliipites longus Stanley 1965

Choanopollenites sp. Cupanieidites speciosus Stanley 1965 Cyrillaceaepollenites ventosus (Potonié 1964) Frederiksen 1980 Eucommia sp. Faguspollenites sp. Favitricolporites sp. Gothanipollis cockfieldensis Engelhardt 1964 Holkopollenites sp. A Description: Tricolporate, oblate to suboblate shape, equatorial outline is triangular with concave to slightly concave sides and base. Exogerminal aperture and pore canal is u- shaped in appearance when the grains lie in polar view. The endannulus is concave to convex inward. Sculpture is smooth to granulate but often shows wrinkling due to the relatively thick ektexine. P/E ratio is 1.0 (subspheroidal). Distribution is “dominant”. Holkopollenites sp. A occurs from samples in the Clayton, Owl Creek, and Porters Creek formations in all three counties. Size: Specimens are 28-40 µm long and 28-40 µm wide; twelve specimens measured. Remarks: This particular species resembles Holkopollenites chemardensis (Stover et al., 1966); however, it exhibits concave to slightly concave sides and base rather than an outline with straight to very slightly concave sides and flattened base. Also, inner wall layers do not appear incised by channels as H. chemardensis (Stover et al., 1966). Horniella sp. Insulapollenites rugulatus Leffingwell 1970 Interporopollenites turgidus Tschudy 1975 Intratriporopollenites sp. Intratriporopollenites crassipites Norris 1986 Lanagiopollis sp. Lanagiopollis cribellata (Srivastava 1972) Frederiksen 1988 Nyssapollenites albertensis Singh 1971 Nyssapollenites explanata Anderson 1960 Nyssapollenites paleocenicus Frederiksen 1980 Nyssapollenites pulvinus (Potonié 1931) Frederiksen 1980

Porosipollis porosus (Mtchedlishvili in Samoilovitch et al. 1961) Krutzsch 1969 Rhoipites globosus Stanley 1965 Rhoipites latus Frederiksen 1980 Rhoipites pisinnus Stanley 1965 Rhoipites sp. Rhoipites subprolatus Frederiksen 1980 Syncolporites lisamae Potonié 1960 Syncolporites rugulosus Syncolporites sp. Tilia instructa (Potonié 1931) Frederiksen 1980 Tricolporopollenites sp., Plate 3, Figure L Vitis affluens Stanley 1965, Plate 3, Figure M

Hexaporotricopate

Libopollis jarzenii Farabee et al. 1984

Jugate

Ericipites redbluffensis Frederiksen 1980

Freshwater Algae

Botryococcus braunii (Kützing 1849) Batten and Grenfell 1996, Plate 2 Figure A Remarks: Colonial green algae made up of clusters of two or more cells in conical branches. Colonies are roughly spherical and make up several branches that are arranged in a radial manner. P/E ratio is 1.0 (subspheroidal). Distribution is “common” in several samples in the Clayton, Owl Creek, and Porters Creek formations. Length of vesicles ranges from 30-50 µm; width ranges from 30-50 µm. Botryococcus sp.

Catinipollis geiseltalensis Krutzsch 1966 Ovoidites ligneolus (Potonié 1951) Thomson and Pflug 1953 Ovoidites microligneolus Krutszch 1959 Pediastrum boryanum Reinsch 1867 Remarks: Colonial green algae with disc-shaped colonies composed of a variable number of cells. Cells are closely packed or have intervening spaces. Vesicle shape is circular to elliptical; contain large projections. P/E ratio is 1.0 (subspheroidal). Distribution is “rare” in samples in the Porters Creek Formation. Vesicles are 75 µm long and 75 µm wide. Schizosporis cookonii Pocock 1962 Schizosporis laevigatus (Cookson & Dettmann 1959) Stanley 1965 Schizosporis microfoveatus (Cookson & Dettmann 1959) Stanley 1965 Schizosporis parvus Cookson & Dettmann 1959 Spirogyra sp.

Fungi

Diporicellaesporites retipilatus Elsik 1968 Lycoperdon sp. Monoporisporites globusus Clarke 1965 Monoporisporites singularis Sheffy & Dilcher 1971 Monoporisporites sp. Thecaphora sp.

Dinoflagellate cysts

Achomosphaera alcicornu (Eisenack 1954) Davey & Williams 1966, Plate 4, Figure D Achomosphaera andalousiensis (Jan du Chêne 1977) Jan du Chêne & Londeix 1988 Achomosphaera sp. Adnatosphaeridium sp. Alisocysta sp.

Alsiogymnium euclaense (Cookson & Eisenack 1970) Lentrin & Vozzhennikova 1990 Alterbidinium sp. Aptea polymorpha (Eisenack 1958) Sarjeant 1985 Apteodinium sp. Areoligera senoniense (Lejeune-Carpentier 1938) Gocht 1969, Plate 5, Figure F Batiascasphaera baculata Batiascasphaera micropapillata Stover 1977 Batiacasphaera sp. Carpodinium granulatum (Cookson & Eisenack 1962) Leffingwell & Morgan 1977 Cassiculosphaeridia reticulata Davey 1969, Plate 3, Figure G Cerodinium boloniense (Riegel 1974) Lentin & Williams 1989 Cerodinium diebelii (Alberti 1959) Lentin & Williams 1987, Plate 6, Figure C Cerodinium pannuceum (Stanley 1965) Lentin & Williams 1987, Plate 6, Figure B Cerodinium speciosum (Alberti 1959) Lentin & Williams 1987 Cerodinium striatum (Drugg 1967) Lentin & Williams 1987, Plate 6, Figure A Cerodinium sp. A, Plate 6, Figure I Description: Proximate cyst, peridinoid, spherical to subspherical body, two walls relatively thick and smooth, paracingulum delineated by perforate parallel membranes and sulcus indicated by a slight depression on the cyst. Tabulation and processes are absent. Type I archeopyles with only paraplate 2 a; length to width ratio of archeopyle is ~ 1.0 (thetaform). Distribution is “common” in several Clayton, Owl Creek, and Porters Creek samples in all three counties. Size: Overall length and width is 120 µm and 65 µm; height of single apical horn is ~ 35 µm and height of paired antapical horns is ~ 25 µm; five specimens measured. Remarks: This species has the generic characteristics of Cerodinium as given by Lentin and Williams (1987). The specimens studied appear to be close to Cerodinium diebelii (Alberti 1959 and Lentin and Williams 1987) but differ in lacking the highly striated periphragm and narrowed based horns with two antapical horns having different lengths. Cerodinium sp. A can be readily distinguished from other species because of its distinctive two walls that are relatively thick and smooth and paracingulum delineated by perforate parallel membranes and sulcus possessing a slight depresson on the cyst.

Cleistosphaeridium insolitum (Eaton 1976) Stover & Evitt 1978, Plate 3, Figure K Cleistosphaeridium sp. Cordosphaeridium cantharellus (Brosius 1963) Fensome et al. 1993 Cordosphaeridium exilimurum (Davey & Williams 1966) Bujak et al. 1980 Cordosphaeridium fibrospinosum (Davey & Williams 1966) Davey 1969, Plate 6, Figure D Cordosphaeridium funiculatum (Morgenroth 1966) Brinkhuis 1992 Remarks: Chorate, gonyaulacoid cyst, spherical to subspherical with processes being intratabular, tubular, flared at the tips, expanded distally, and fibrous. Processes are of

relatively equal proportion. Archeopyle type P 3” . Distribution is “common” in Clayton samples. Cyst length is 52-56 µm and cyst breadth is 50-51 µm; length of processes measure approximately 25 µm. Specimens may be contamination from younger sediments. Cordosphaeridium minimum (Morgenroth 1966) Benedek 1972 Cordosphaeridium sp. A, Plate 6, Figure E Description: Skolochorate gonyaulacoid cyst, spherical to subspherical body, smooth endophragm and periphragm (processes). Processes are intratabular, tabulate with serrate margins and vary in length. Archeopyle is precingular, Type P 3” , operculum free. Distribution is “infrequent” in Clayton samples from New Madrid County. Size: Cyst length is 50 µm and breadth is 44 µm; average length of processes is 15 µm; three specimens measured. Remarks: Cordosphaeridium sp. A can be readily distinguished from other species because of its smooth endophragm and periphragm and its intratabular processes being tabulate with serrate margins. Cordosophaeridium sp. A closely resembles that of species B which exhibits generic characteristics of C. funiculatum (Morgenroth, 1966, emend. Brinkhuis, 1992). In comparison to species B of Cordosphaeridium , species A has slightly shorter processes that are broader and variable in length. Species A is slightly shorter in size with comparison to species B. In comparison to C. funiculatum , species A appears to lack the fibrous processes. Cribroperidinium sp. Deflagymnium sp.

Deflandrea sp., Plate 6, Figure F Dinogymnium acuminatum (Evitt et al. 1967) Lentin & Vozzhennikova 1990, Plate 3, Figure I Dinogymnium sp. Dinopterygium cladoides (Deflandre 1935) Deflandre 1936 Diphyes colligerum (Deflandre & Cookson 1955) Goodman & Witmer 1985 Diphyes spinula (Drugg 1970) Stover & Evitt 1978 Distatodinium ellipticum (Cookson 1965) Eaton 1976 Distatodinium sp. Fibrocysta lappacea (Drugg 1970) Stover & Evitt 1978, Plate 3, Figure J Fibrocysta sp. Florentinia sp. Gippslandia sp. Glaphyrocysta intricata (Eaton 1971) Stover & Evitt 1978 Glaphyrocysta semitecta (Bujak in Bujak et al. 1980) Lentin & Williams 1981 Glaphyrocysta sp. Gochteodinia sp. Hafniasphaera graciosa (Hansen 1977) Hafniasphaera septatus (Cookson & Eisenack 1967) McLean 1971, Plate 4, Figure F Hafniasphaera sp. Homotryblium sp. Hystrichokolpoma sp. Hystrichosphaeridium tubiferum (Ehrenberg 1838) Davey & Williams 1966 Remarks: Chorate cyst with endophragm forming endocyst and periphragm forming processes. Processes are intratabular, tubular which open distally. Precingular and postcingular series are larger than the antapical or apical series. No paracingular processes are observed. Arecheopyle is difficult to distinguish. Distribution is “rare” to “infrequent” to “common” in Clayton samples. Size: Specimen measures approximately 30 µm long and 30 µm wide. Lanternosphaeridium lanosum Morgenroth 1966 Lejeunecysta hyaline

Lejeunecysta izerzenensis Slimani et al. 2008, Plate 6, Figures G and H Melitasphaeridium sp. Nematosphaeropsis sp. Oligosphaeridium complex (White 1842) Davey & Williams 1966, Plate 7, Figures A and C Remarks: Chorate, gonyaulacoid cyst, spherical to subspherical body cyst, processes are intratabular with tubular structures, which are flared at the tips (multibifurcated) and open distally with digitate distal margins. Paracingulum and parasulcal processes are absent. Paratabulation: 2’, 6”, 0p, 05, 6’”, 1””. Distribution is “common” in many Clayton samples. Cyst length is 35 µm and breadth is 25 µm; length of processes is approximately 20 µm. Oligosphaeridium patulum Riding & Thomas 1988 Oligosphaeridium sp. A, Plate 7, Figure E Description: Chorate, gonyaulacoid cyst, spherical to subspherical cyst body with long tubular structures flared at the tips, processes are intratabular expanding distally with serrate margins. Processes are of equal proportion and terminations appear to be multifurcated. Archeophyle type is 4A. Distribution is “infrequent” in Clayton samples. Size: Cyst length is 50 µm and breadth is 40 µm; processes are approximately 25 µm long; two specimens measured. Remarks: Oligosphaeridium sp. A can be readily distinguished from other species because of its processes expanding distally with serrate margins. Oligosphaeridium complex closely resembles Oligosphaeridium sp. A; however, its processes are open distally with digitate distal margins and the overall body cyst is shorter than that of species A. Operculodinium centrocarpum (Deflandre & Cookson 1955) Wall 1967 Operculodinium echigoense (Matsuoka 1983) Matsuoka et al. 1997, Plate 5, Figure B Operculodinium sp. Palaeocystodinium golzowense Alberti 1961, Plate 4, Figures B and C Palaeocystodinium sp., Plate 4, Figure A Palaeoperidinium pyrophorum (Ehrenberg 1838) Gocht & Netzel 1976, Plate 7, Figures B and D

Paucisphaeridium inversibuccinum (Davey & Williams 1966) Bujak et al. 1980 Pervosphaeridinium sp . Phelodinium magnificum (Stanley 1966) Stover & Evitt 1978 Remarks: Peridinoid, proximate, cornucavate cyst with endophragm and periphragm closely appressed except in the horns area. Cingulum and sulcus are clearly appreciable with thin and folded walls. Archeopyle type is I 2a . Distribution is “infrequent” in the Clayton Formation. Specimens measure 80-83 µm long and 70-72 µm wide. Phelodinium sp. A, Plate 7, Figure F Description: Peridinoid, proximate, cornucavate cyst. Very thin layers, periphragm is slightly folded and striated. Paracingulum is clearly delineated by two parallel ridges. Parasulcus is indicated by interruption of the paracingular ridges. Antapical horns are of equal proportion and widely spaced apart. Archeopyle is type I. Length to width ratio of archeopyle is deltaform with eury- AR<1. Distribution is “infrequent” in Clayton samples. Size: Specimen ranges from 100-110 µm long and 83-85 µm wide; five specimens measured. Remarks: Phelodinium sp. A is characteristically different from most species by having a shorter length, two paired antapical horns instead of one, less prominent striation features, and a parasulcus which is separated down the center due to an interruption of the paracingular ridges. Phelodinium sp. A also differs from Phelodinium magnificum (Stanley 1965; Stover and Evitt 1978) by being wider, having less defined striations running vertically up and down the dinocyst, and its smaller paired antapical horns Phoberocysta neocomica (Gocht 1957) Helby 1987 Phthanoperidinium amoenum Drugg & Loeblich Jr. 1967 Phthanoperidinium sp. Prolixosphaeridium parvispinum (Deflandre 1937) Fauconnier & Masure 2004 Protoellipsodinium spinosum Davey & Verdier 1971 Pterodinium ? spp., Plate 8, Figure G Schematophora speciosa (Deflandre & Cookson 1955) Stover 1975 Senegalinium sp. A, Plate 8, Figure A

Description: Peridinoid, cornucavate elongate cyst with endocysts is displaying pseudo- pentagonal shape with straight sides. Periphragm is slightly striated. Paracingulum and parasulcus are difficult to observe. Length to width ratio for archeopyle is deltaform with steno- (AR>1). Distribution is “rare” to “infrequent” in Clayton samples. Size: Cyst body is 65 µm long and 50 µm wide; apical horn measures approximately 50 µm long and antapical horns measures approximately 40 µm long; two specimens were measured for this slide. Remarks: Senegalinium sp. A is characteristically different from Senegalinium speciosum by its longer length, different archeopyle type, lightly striated periphragm, and lack of densely acuminate wall. Senoniasphaera inornata (Drugg 1970) Stover & Evitt 1978, Plate 4, Figures E and G Remarks: This species disappeared worldwide during the Danian (Gradstein et al., 2004). Senoniasphaera sp. Spiniferites ramosus (Ehrenberg 1838) Davey & Williams 1966, Plate 5, Figures D and E Remarks: Proximochorate cyst with a spherical to subspherical body, circular outline in polar view. Wall structure is laevigate to weakly granulate. Cyst exhibits gonal processes, occasionally intergonal, which are solid, rigid, and slenderly tapering with trifurcate branches carrying bifid tips. Precingular archeopyle type is 3 ”. Distribution is “dominant” in several Clayton samples. Specimens range in size from 22-43 µm long and 17-53 µm wide; processes are 1.2-12 µm long. Spiniferites ? supparus (Drugg 1967) Sarjeant 1970 Spiniferites sp., Plate 3, Figure H, Plate 5, Figures A and C Subtilisphaera sp., Plate 3, Figure N Sumatradinium druggii (Lentin et al. 1994) Systematophora silybum (Davey 1979) Fauconnier & Masure 2004 Tanyosphaeridium regulare (Davey & Williams 1966) Fauconnier & Masure 2004) Tanyosphaeridium sp. Thalassiphora delicata (Williams & Downie 1966) Eaton 1976; Bujak et al. 1980) Thalassiphora inflata Heilmann-Clausen in Thomsen & Heilmann-Clausen 1985 Thalassiphora pelagica (Eisenack 1954) Benedek & Gocht 1981 Thalassiphora sp.

Trichodinium ciliatum (Gocht 1959) Jan du Chêne et al. 1986

Acritarchs

Micrhystridium piliferum Deflandre 1937, Plate 8, Figure B Pterospermopsis sp., Plate 8, Figure C Sigmopollis callosus Norris 1969 Various acritarchs Veryhachium sp., Plate 8, Figure D

5.4. DISPERSED ORGANIC MATTER

Eight types of dispersed organic matter or palynodebris, namely amorphous organic matter, black debris, unstructured phytoclasts, structured phytoclasts, marine palynomorphs, freshwater algae, fungal remains, and sporomorphs were identified and counted in the samples (Figure 5.13; Tables 5.5 and 5.6). They fall into three broad categories: palynomorphs, phytoclasts, and unstructured (amorphous) organic matter.

The descriptions of these organic components can be found in Oboh-Ikuenobe et al.

(2005).

Three palynofacies assemblages designated A, B and C (Figure 5.13), have been identified from cluster analysis based on three statistically important organic components, namely amorphous organic matter, structured phytoclasts, and sporomorphs. The statistical significance of these components is confirmed by principal components analysis (Table 5.7), which shows that these organic components constitute almost 90% of the total variance in the sample set on the first two axes. On the cluster analyses diagrams in Figure 5.14, the top dendrogram (R-Mode) groups the types of palynodebris, the left-hand dendrogram (Q-Mode) is a grouping of the samples, and the matrix is displayed between them.

Palynofacies assemblage A is represented by samples from all three formations studied. It is characterized by subequal percentages (>20%) of sporomorphs and structured phytoclasts, and overall has high input of terrestrially derived components (see

Tables 5.5 and 5.6; Figure 5.19). Other components vary greatly, but are generally less than 10%; some samples record higher percentages for freshwater algae, black debris, marine palynomorphs, and amorphous organic matter. Samples from the Porters Creek

Formation dominate assemblage B, and are not represented by Owl Creek samples.

Structured phytoclasts predominate, mostly greater than 50% of the total counts.

Sporomorphs are secondarily important in this assemblage, varying between 5-30%.

Other components are less than 10% in a majority of the samples, although a few samples

record higher percentages for black debris, marine palynomorphs, and amorphous organic

matter. Overall, this assemblage has the highest input of terrestrial derived components.

Assemblage C samples, which are from all three formations, generally have more than

60% amorphous organic matter. In some sample sporomorphs, structured phytoclasts,

unstructured phytoclasts and black debris each comprises more than 10%. The Clayton

hardground (ST01) and coquina (ST10) samples belong to this assemblage.

Of the three palynofacies assemblages, only two are represented in BH-1 core

(Figure. 5.15): assemblage A is represented by Owl Creek and Porters Creek samples, and assemblage B is represented by two Porters Creek samples. In the BH-9 core, only

Porters Creek samples are present, and all three palynofacies assemblages are represented

(Figure 5.16). Only two assemblages (A and B) were identified in the BH-10 core (Fig.

5.17), and all three Owl Creek samples and three Porters Creek samples represent assemblage C). In Trenches 1 and 2 (Figure 5.18), the three assemblages are distributed throughout the four Clayton zones, while the only Owl Creek sample analyzed belongs to assemblage B.

~ 40 µm Figure 5.13. Photomicrographs of representative samples of the three palynofacies assemblages. A, B) Palynofacies A, sample SC27 (A), sample ST07 (B); C, D) Palynofacies B, sample SC03; E, F) Palynofacies C, sample ST10. Abbreviations for dispersed organic components: BLDEB = black debris; STOM = structured phytoclasts; USTOM = unstructured phytoclasts; P = pollen; FS = fungal spore; A = acritarch; D = dinoflagellate; AMORP = amorphous organic matter.

Table 5.5. Relative abundances (in percent) of dispersed organic matter in BH-1, BH-9 and BH-10, Scott County. SPORO = sporomorphs, FR = fungal remains, FWA = freshwater algae, MAR = marine, STOM = structured phytoclasts, USTOM = unstructured phytoclasts, BLDEB = black debris, AMORP = amorphous, PC = Porters Creek, OC = Owl Creek, PFA = palynofacies assemblage.

Sample Depth Fm. Loc. SPORO FR FWA MAR STOM USTOM BLDEB AMORP PFA (m) SC01 7.4 PC BH-1 0.00 1.00 0.33 0.00 4.33 0.67 3.33 90.33 C SC03 9.44 PC BH-1 9.67 4.33 2.67 2.33 59.00 7.67 5.00 9.33 B SC04 11.8 PC BH-1 4.00 2.00 0.33 1.33 20.67 3.67 2.67 65.33 C SC05 14.0 PC BH-1 6.33 5.33 3.00 0.33 68.00 5.00 4.33 7.67 B SC06 17.2 PC BH-1 3.00 1.67 1.33 0.33 21.33 2.33 10.00 60.00 C SC07 18.1 PC BH-1 0.33 0.33 0.00 0.67 18.67 11.67 6.33 62.00 C SC08 18.3 OC BH-1 1.00 1.33 0.00 0.00 6.67 0.67 10.67 79.67 C SC09 18.8 OC BH-1 1.00 0.33 0.33 0.00 3.00 1.00 2.67 91.67 C SC16 17.3 PC BH-9 17.67 2.00 0.00 0.00 60.00 2.67 13.67 4.00 B SC17 18.1 PC BH-9 41.67 2.33 0.00 0.67 39.33 5.00 2.67 8.33 A SC18 18.4 PC BH-9 26.67 32.67 0.67 1.33 26.00 7.33 2.67 2.67 A SC19 19.5 PC BH-9 37.67 4.00 1.33 0.67 51.00 3.33 0.67 1.33 A SC21 21.0 PC BH-9 13.33 0.33 0.67 1.33 24.67 13.33 12.67 33.67 C SC23 22.5 PC BH-9 23.67 2.67 1.33 0.00 57.67 6.67 3.33 4.67 B SC25 23.7 PC BH-9 2.33 0.33 3.67 1.33 13.67 22.33 20.67 35.67 C SC27 30.1 PC BH-9 36.67 0.67 0.67 0.00 33.33 11.00 4.00 13.67 A SC10 13.5 PC BH-10 20.00 14.67 0.67 0.67 32.00 12.67 10.33 9.00 A SC11 14.3 PC BH-10 16.33 0.00 1.00 0.00 73.00 1.67 0.00 8.00 B SC12 15.4 PC BH-10 28.33 2.67 0.67 0.67 61.67 2.33 0.67 3.00 B SC13 15.8 PC BH-10 7.33 3.33 0.00 0.00 85.00 2.00 0.00 2.33 B SC15 16.7 PC BH-10 20.00 3.33 1.00 0.00 63.67 4.67 3.33 4.00 B SC20 19.8 PC BH-10 45.00 0.33 0.67 10.67 21.00 4.00 13.67 4.67 A SC22 21.3 PC BH-10 27.67 9.67 0.33 0.00 48.33 11.67 2.33 0.00 A SC24 22.8 PC BH-10 3.00 6.67 2.00 0.67 36.67 5.33 1.33 13.33 B SC26 25.9 PC BH-10 27.00 0.67 0.33 0.33 31.00 10.00 21.67 9.00 A SC28 32.0 PC BH-10 22.33 0.67 2.67 0.67 50.33 4.00 14.00 3.33 B SC29 33.5 OC BH-10 30.00 2.67 0.00 0.67 41.67 5.00 11.67 8.33 A SC30 34.1 OC BH-10 53.33 4.00 0.00 0.00 18.00 4.00 14.00 6.67 A SC31 34.4 OC BH-10 28.33 4.00 5.33 0.00 41.67 3.33 10.00 7.33 A

Table 5.6. Relative abundances (in percent) of dispersed organic matter in Trenches 1 and 2, Stoddard County. SPORO = sporomorphs, FR = fungal remains, FWA = fresh water algae, MAR = marine, STOM = structured phytoclasts, USTOM = unstructured phytoclasts, BLDEB = black debris, AMORP = amorphous, CL = Clayton, HG = hardground, Coqu. = coquina, OC = Owl Creek, PFA = palynofacies assemblage.

Samples Depth CL Location SPORO FR FWA MAR STOM USTOM BLDEB AMORP PFA (cm) Zone ST01 180.0 HG Tr. # 1 2.33 1.00 0.33 7.33 19.30 3.67 5.00 61.00 C ST02 160.0 Gray Tr. # 1 24.70 2.00 0.00 9.00 29.30 7.00 24.00 4.00 A ST03 140.0 Gray Tr. # 1 53.70 1.67 0.00 2.33 25.3 10.0 1.33 5.67 A ST04 110.0 Gray Tr. # 1 30.00 3.33 3.33 6.33 39.00 12.7 1.33 4.00 A ST05 110.0 Gray Tr. # 1 7.00 2.00 0.00 10.70 54.00 7.33 4.33 14.7 B ST06 75.0 Glauc. Tr. # 1 14.30 2.33 0.00 10.00 41.00 4.00 5.67 22.7 B ST07 75.0 Glauc. Tr. # 1 33.30 0.00 0.00 5.78 37.70 12.0 0.00 5.00 A ST08 60.0 Glauc. Tr. # 1 45.30 0.67 0.67 7.33 26.70 10.0 0.67 8.67 A ST09 50.0 Glauc. Tr. # 1 33.00 2.67 0.00 18.30 31.70 8.33 4.67 1.33 A ST10 20.0 Coqu. Tr. # 1 9.67 4.67 0.67 5.33 25.30 7.33 6.00 41.0 C ST11 0.0 OC Tr. # 2 50.00 0.00 0.00 2.67 27.70 4.67 3.33 11.7 A

Table 5.7. Principal component loadings for dispersed orgamic matter. The asterisk (*) indicates the statistically significant types with absolute values greater than 0.10; eigenvalue (Axis) 1 = 996.463 (69.122%); Axis 2 = 300.480 (20.844%).

Organic matter component Axis 1 Axis 2

Sporomorphs -0.319* -0.668* Fungal remains -0.033 -0.012 Freshwater algae -0.005 0.014 Marine palynomorphs -0.013 -0.061 Structured phytoclasts -0.457* 0.720* Unstructured phytoclasts -0.017 -0.072 Black debris 0.020 -0.087 Amorphous organic matter 0.829* 0.139*

S U B A P S S L M O T F M T D O R O F W A O E R O M R A R M B P ST11 + + ST08 + + ST03 + SC30 + + SC20 ST02 + SC26 SC10 + SC18 Absent ST09 + A ST07 + + + <10% ST04 10-20% SC22 + + SC19 20-30% SC31 + Minimum Variance 30-60% SC29 + SC27 + >60% SC17 + ST06 + ST05 + SC24 SC12 SC15 + SC23 + SC28 + B SC16 + + SC13 + + + SC11 + + + SC05 SC03 SC25 ST10 SC21 SC07 + SC06 ST01 C SC04 SC08 + + SC09 + SC01 + + 36000 30000 24000 18000 12000 6000 0 Squared Euclidean

Figure 5.14. Dendrograms for average linkage cluster analysis of palynological samples from BH-1, BH-9, BH-10, Trench 1 and Trench 2 (Q-mode, left-hand) and of dispersed organic matter (R-mode, top), with the data matrix displayed between them.

Porters Creek

Owl Creek

Figure 5.15. Percentage distribution of dispersed organic matter in BH-1 core, Scott County. SPORO = sporomorphs, FR = fungal remains, FWA = fresh water algae, MAR = marine, STOM = structured phytoclasts, USTOM = unstructured phytoclasts, BLDEB = black debris, and AMORP = amorphous organic matter.

SC14

SC16 SC17 SC18

SC19

SC21

SC23

SC25

SC27

Figure 5.16. Percentage distribution of dispersed organic matter in BH-9 core, Scott County. SPORO = sporomorphs, FR = fungal remains, FWA = fresh water algae, MAR = marine, STOM = structured phytoclasts, USTOM = unstructured phytoclasts, BLDEB = black debris, and AMORP = amorphous organic matter.

Porters Creek

Owl Creek

Figure 5.17. Percentage distribution of dispersed organic matter in BH-10 core, Scott County. SPORO = sporomorphs, FR = fungal remains, FWA = fresh water algae, MAR = marine, STOM = structured phytoclasts, USTOM = unstructured phytoclasts, BLDEB = black debris, and AMORP = amorphous organic matter.

Porters Creek

Owl Creek

Figure 5.18. Percentage distribution of dispersed organic matter in Trenches 1 and 2, Stoddard County. SPORO = sporomorphs, FR = fungal remains, FWA = fresh water algae, MAR = marine, STOM = structured phytoclasts, USTOM = unstructured phytoclasts, BLDEB = black debris, and AMORP = amorphous organic matter.

5.5. FORAMINIFERA

Nine horizons in Trench 1 at the Nestle Purina Plant in Stoddard County were sampled from the Owl Creek, Clayton and Porters Creek formations at approximately 20 cm intervals (see Table 4.2). Carl Campbell collected 13 other samples from a sump located at the Plant, but these were not used for determining relative abundances due to the possible mixing of sediments. These sump samples were scanned in order to identifiy foraminiferal taxa only. Using existing literature, in particular Cushman (1951) and

Loeblich and Tappan (1988), as a guide, foraminiferal specimens were identified by the following characteristics: chamber wall, chamber arrangement, chamber shape, aperture shape and position, and special ornamentation. They were assessed for their test composition (porcellaneous, hyaline, agglutinated), relative abundance and diversity

(Tables 5.8 and 5.9). Carl Campbell also supplied some of the photographs used in this study.

A low diversity foraminiferal assemblage was identified in all the formations studied. The Clayton Formation yielded the highest abundance of foraminifera, representing 43.5% of the foraminiferal taxa identified, followed by the Owl Creek

(39.1%) and the Porters Creek (17.4%). A list of the recovered foraminiferal taxa can be found in Appendix M. Benthic foraminifera by far dominate planktonic forms in

abundance and diversity in all three formations, constituting 17 of the 18 taxa identified.

Planktonic specimens comprise 6.2% of the foraminiferal assemblage in the Clayton and

Owl Creek formations; whereas they constitute 14.3% in the Porters Creek Formation

(Table 5.9). With the exception of a few larger foraminifera such as Nodosaria latejugata, Nodosaria affinis, Parrella expansa, Anomalina elementiana, and Vaginulina

76 midwayana , most species recovered were small with rather simple morphologies and little ornamentation (e.g., Gyroidina depressa, Nodogenerina bradyi, Dentalina gardnerae ). The majority of specimens have uniserial and trochospiral chamber arrangements.

Table 5.8. Species diversity for foraminifera shell types. Porcel. = porcelaneous, Agglut. = agglutinated.

Formation No. of Porcel. Porcel. Hyaline Hyaline Agglut. Agglut. Species % % %

Porters 7 2 28.6 3 42.9 2 28.6 Creek

Clayton 16 4 25.0 6 37.5 6 37.5

Owl Creek 16 5 31.3 6 37.5 5 31.3

Table 5.9. Benthic versus planktonic foraminifera.

Formation No. of Benthic Benthic Planktonic Planktonic Species % %

Porters Creek 7 6 85.7 1 14.3

Clayton 16 15 93.8 1 6.2

Owl Creek 16 15 93.8 1 6.2

6. INTERPRETATIONS

6.1. PALYNOMORPHS

6.1.1. Palynostratigraphy . The Owl Creek, Clayton, and Porters Creek

formations yielded some age-diagnostic palynomorphs, although a majority of them are

long ranging. Figure 6.1 shows the stratigraphic occurrences of selected palynomorphs in

all the localities studied. Numbers are assigned to these palynomorphs in Table 6.1;

botanical affinities of nonmarine palynomorphs are indicated where possible. Taxa are

divided into major groups: marine dinocysts, undifferentiated; bryophyte and

pteridophyte spores; angiosperm pollen; and gymnosperm pollen. The palynomorph

assemblages in the three formations are dominated by Maastrichtian-Paleocene taxa

(described below). Several of these palynomorphs are common in the studied samples,

and have also been identified in other studies in the area (Frederiksen et al., 1982) and

elsewhere. These other areas include the southern portion of the Mississippi Embayment

(Tschudy, 1975), the upper Paleocene of the Powder River Basin in Montana and

Wyoming (Pocknall and Nichols, 1996), and the Upper Cretaceous Hell Creek Formation

and Paleocene Fort Union Formation in the northern Great Plains (Stanley, 1965;

Hartman et al. 2002; Nichols, 2002).

6.1.1.1. Test Well I-X (New Madrid County). The Owl Creek was not studied in this section. Palynomorphs in the Clayton strata contain a mixture of Late Cretaceous,

Danian and younger taxa, including several reworked specimens. However, most of the common spores and pollen were present during the Danian (early Paleocene). They include Alsophilidites kerguelensis, Arecipites columellus, Caprifolipites longus, Carya

78 paleocenica, Catinipollis geiseltalensis, Cingulatisporites dakotaensis, Corollina

(Classopollis ) sp.

Figure 6.1. Stratigraphic occurrences of palynomorph taxa in the Porters Creek, Clayton, and Owl Creek formations. Numbers are keyed to the list of taxonomic names in Table 6.1. Taxa are divided into major groups: 1, marine dinocysts, undifferentiated; 2-18, bryophyte and pteridophyte spores; 19-41, angiosperm pollen; 42-50, gymnosperm pollen.

Table 6.1. Selected palynomorphs used for stratigraphic interpretation. ______Scientific-Name Common Name ______

(1) Marine Acritarchs, dinoflagellates, and foraminifera linings. Spores: (2) Cicatricosisporites sp. Gap branch fern (3) Cyathidites minor Tree fern (4) Deltoidospora sp. Fern (5) Gleichenia triangular Fern (6) Laevigatosporites haardti Fern (7) Leptolepidites tenuis (8) Monoporisporites sp. Fungi (9) Osmunda comaumensis King fern (10) Osmundacidites stanleyi Fern (11) Polycolpites sp. Fern (12) Retitriletes sp. (13) Schizaeoisporites sp. Freshwater algae? (14) Selaginella perinata Spike moss (15) Sphagnum australe Moss (16) Stereisporites sp. Moss (17) Triplanosporites sinuosus (18) Undulatisporites sp.

Angiosperm pollen: (19) Ailanthipites berryi (20) Alnus trina Alder tree (21) Alnus vera Alder tree (22) Arecipites spp. Palm (23) Basopollis sp. (24) Betula infrequens Birch tree or shrub (25) Boehlensipollis sp. (26) Bombacadites sp. (27) Caryapollenites sp. Hickory tree (28) Chenopodipollis sp. Herbaceous plant (29) Confertisulcites sp. (30) Cupressacites hiatipites Cedar or cypress tree (31) Eucommia sp. (32) Extremipollis sp. (33) Fraxinoipollenites sp. Ash tree (34) Holkopollenites sp. (35) Liliacidites sp. Blooming flower plant (36) Momipites sp. (37) Nudopollis sp.

Table 6.1. Selected Palynomorphs used for stratigraphic interpretation (continued). ______Scientific-Name Common Name ______

(38) Platacarya spp. (39) Quercoidites sp. Oak tree (40) Rhoipites sp. (41) Salixipollenites parvus Willow tree

Gymnosperm pollen: (42) Bisaccates Various trees (43) Corollina (Classopollis ) sp. (44) Cycadopites sp. Palm (cycad) (45) Ephedra sp. Shrub (46) Ephedripites sp. Herbaceous plant (47) Laricoidites magnus (48) Pinus sp. Pine tree (49) Sequoia sempervirens Redwood tree and Sequoiapollenites paleocenicus (50) Taxodiaceaepollenites hiatus

Corylus granilabrata, Cupanieidites speciosus, Cupressacites hiatipites, Cycadopites scabratus, Fraxinoipollenites variabillis, Gleichenia triangular, Interporopollenites turgidus, Leptolepidites tenuis, Maceopolipollenites amplus, Momipites microfovelolatus,

Osmunda comaumensis, Pachysandra cretacea, Sequoiapollenites paleocenicus and

Tricolpites parvus . The dinoflagellate assemblage that includes Areoligera senonensis,

Cerodinium diebelii, Cerodinium pannuceum, Cerodinium striatum, Hafniasphaera graciosa, Paleocystodinium golzowense, Senoniasphaera inornata, Spiniferites ramosus,

Spiniferites supparus and Thalassiphora inflata also support a Danian age.

The Porters Creek has the highest diversity of spores and pollen. Key palynomorphs suggest middle to late Paleocene. Age-diagnostic nonmarine palynomorphs are Alnus vera, Alsophilidites kerguelensis, Boehlensipollis minimus,

Caryapollenites veripites, Corylus granilabrata, Cupanieidites speciosus, Gleichenia

triangular, Leptolepidites tenuis, Myocolpopollenites reticulatus, Nyssapollenites

explanata, Pistillipollenites mcgregorii, Quercoidites genustriatus and Vitis affluens .

Marine palynomorphs include Cordosphaeridium cantharellum and Spiniferites ramosus .

6.1.1.2. BH-1, BH-9 and BH-10 (Scott County). Few palynomorphs were

recovered from the Owl Creek; however, the occurrence of the following spores and

pollen Cycadopites giganteus, Extremipollis caminus, Gleichenia triangular and

Plicapollis usitatus supports a Maastrichtian age (Harrison et al., 1996). Although three

Owl Creek samples from BH-10 (SC29, SC30, SC31) were studied, no marine

palynomorphs were recovered from the sieved fractions. The kerogen fraction of SC29,

however, yielded less than 1% marine palynomorphs (see Table 5.5). The Clayton

Formation is absent in all the BH borehole sections.

The Porters Creek samples are very rich in spores and pollen, much like the New

Madrid Test Well I-X samples. The presence of Caryapollenites imparalis,

Caryapollenites veripites, Confertisulcites fusiformis, Jarzenipollenites trinus,

Lanagiopollis cribellata, Nudopollis terminalis, Pistillpollenites mcgregorii,

Subtriporopollenites nanus and Triatriopollenites proprius support an age of middle to

late Paleocene . A Paleocene age is also suggested by the co-occurrence of Engelhardtia microvoveolata, Interporopollenites turgidus, Momipites marylandicus, Momipites microfovelolatus, Myocolpopollenites reticulatus and Vitis affluens . Although several marine palynomorphs identified are reworked, the presence of the dinoflagellate taxon

Cordosphaeridium cantharellum supports the assigned Paleocene age.

6.1.1.3. Trenches 1 and 2 (Stoddard County). The Owl Creek contains several non-diagnostic nonmarine palynomorphs and few marine palynomorphs. However,

Maastrichtian taxa such as Extremipollis caminus, Schizosporis cooksonii and

Vacuopollis munitus occur. The Clayton Formation contains a diverse range of marine and nonmarine palynomorphs, including reworked Cretaceous and younger taxa. It is possible that caving of younger sediments was due to the excavation activity by the mining operation for the Porters Creek Clay. The most commonly occurring in-situ

dinoflagellates include Hafniasphaera graciosa, Hafniasphaera septatus, Impagidinium aspinatum, Palaeocystodinium golzowense, Spiniferites ramosus and Thalassiphora inflata , while few specimens of Areoligera senonensis, Cerodinium diebelii, Phelodinium

magnificum, Spiniferites supparus and Senoniasphaera inornata were recovered . These taxa, as well as the spores and pollen Alsophilidites kerguelensis , Arecipites columellus,

Carya paleocenica, Cingulatisporites dakotaensis, Cupanieidites speciosus,

Erdtmanipollis cretaceous, Fraxinoipollenites variabillis, Gleichenia triangular and

Momipites strictus support a Danian age for the formation . There are also several

nonmarine taxa ( Caprifolipites longus, Caryapollenites imparalis, Caryapollenites

veripites, Corylus granilabrata, Cupressacites hiatipites, Cycadopites scabratus,

Interporopollenites turgidus, Maceopolipollenites amplus, Momipites microfovelolatus ) and marine taxa ( Cerodinium pannuceum, Impagidinium aspinatum ) that support a

general Paleocene age.

6.1.2. Species Diversity and Paleoenvironments. One basic approach to paleoecological interpretations is to use species diversity (Duringer and Doubinger,

1985). It is generally recognized today that dinoflagellate species diversity increases

with distance from the shore, and are more abundant on continental slopes and rises. On

the other hand, spores and pollen, although terrestrial in origin, can be easily dispersed by

air and wind into environments other than their natural habitats. They are are usually

abundant in sediments formed in reducing, anaerobic environments such as lakes.

Diagenetic processes such as bioturbation can also affect species abundance. A ternary

species diversity plot with distinct fields for open marine, deltaic, and nearshore

environments (Figure 6.2) can be used to infer the paleoenvironments in which the

spores, pollen and marine microplankton were deposited. It should be noted here that the

dinoflagellates and acritarchs recovered are inner neritic (nearshore) dwellers. Table 5.1

shows the species diversity of these palynomorph groups for the Owl Creek, Clayton, and

Porters Creek formations.

6.1.2.1. Owl Creek Formation. The palynomorph assemblage has 33.7% marine microplankton, 18.0% spores, and 48.3% pollen grains, and plots in a nearshore environment influenced by open marine conditions (Figure 6.3).

6.1.2.2. Clayton Formation. The palynomorphs assemblage has the highest diversity of dinoflagellates. Marine microplankton comprises 46%, spores 11.4%, and pollen grains 42.6%, and plot in a nearshore environment with strong open marine influence (Figure 6.4). The graded nature of this unit, from a basal coquina with microtektites and reworked fossils through glauconitic and gray clay to a hardground, suggests flooding followed by a quiet phase and finally a short period of nondeposition.

6.1.2.3. Porters Creek Formation. These assemblages plotted at the following

percentages: marine microplankton 15.4%; spores 17.0%; and pollen grains 67.6%

(Figure 6.5), showing that the sediments were deposited in a nearshore environment.

Open Marine

Deltaic Nearshore

Figure 6.2. Ternary diagram used for describing species diversity of palynomorph assemblages (adapted by Duringer and Doubinger, 1985). Formations plotted indicate the following: Owl Creek (nearshore environment; open marine waters); Clayton (nearshore environment; favorable open marine conditions), and Porters Creek (restricted nearshore environment).

6.1.3. Paleovegetation. In the following subsections, the paleobotanical affinities of spores, pollen and other nonmarine palynomorphs have been used to infer paleovegetation (refer to Tables 6.1 to 6.9 and Figures 6.6 to 6.12).

6.1.3.1. Owl Creek Formation. The Owl Creek is dominated by angiosperms

and contain a relatively high number of palm trees (Areaceae) and palm plants

(Cycadaceae). Also present within the sample were deciduous trees such as hornbeams

(Betulaceae), hickorys and walnuts (Juglandaceae), ashes (Oleaceae), willows (Fagaceae)

and Tupelo (Nyssaceae). Gymnosperms comprise just over 16% of the recovered pollen

(Table 5.2). The evergreen trees/shrubs consist of a variety of pines/conifers, red cedars

(Cupressaceae), cypresses (Taxodiaceae) and morman tea shrubs (Ephedraceae). Ferns,

vines and mosses include gap branch ferns (Schizaeaceae) and varieties of ferns/vines

(Gleicheniaceae and Polypodiaceae). The few medicinal herbs recovered include

Chenopodipollis, Ephedripites and Ericipites. The highest percentage of spores among

all three formations (18.5%) occurs in the Owl Creek, and similar forms are present in the

Clayton Formation (discussed in the next subsection).

6.1.3.2. Clayton Formation. Angiosperms also dominate the Clayton Formation,

comprising more than 80% of the pollen identified (Table 5.2). The most commonly

occurring angiosperm pollen species belong to Arecipites (palm) , Basopollis,

Chenopodipollis (herb) , Engelhardtia, Favitricolporites, Fraxinoipollenites (tree) ,

Momipites, Nudopollis, Quercoidites (tree) , Rhoipites and Salixipollenites (shrub) .

Arecipites is present in at least 10% of all samples. During the early Paleogene, the

herbal species Chenopodipollis was associated with samples containing dinoflagellates, acritarchs and other marine fossils, suggesting marine or coastal deposition (Nichols and

Traverse, 1971; Boulter and Hubbard, 1982). The tree species Fraxinoipollenites has

been recovered from shores and wetlands.

Gymnosperms tend to be less abundant, comprising 19.2% of pollen recovered

(see Table 5.2). The most common gymnosperm genera are Cupressacites, Ephedra and

Taxodiaceaepollenites . Corollina (Classopollis ) occurs usually as monads but also

occasionally as tetrads and is present in only one Clayton zone in Stoddard County.

Ecologically significant gymnosperms include several types of bisaccates, Cupressacites

hiatipites and Taxodiaceaepollenites hiatus. These gymnosperm pollen grains are

produced in great quantities by trees that are the principal components of swamp-forest

vegetation in many Paleocene depositional environments (Nichols, 1995). It should be

noted that some gymnosperm pollen had a broader ecologic range in the Late Cretaceous

and early Paleogene. For example, Frederiksen (1985) pointed out that during the early

Paleogene, the pollen Ephedra was commonly associated with moist tropical to

subtropical conditions, whereas this type of pollen is mainly observed in dry and alpine

regions today. See Table 6.4 for additional tree species occurring in present day climates

throughout the United States.

The most commonly occurring fern spores in the Clayton Formation is

Cicatricosisporites (gap branch) , Cingulatisporites, Cyathidites (tree fern) , Gleichenia

(vine) , Gleicheniidites, Osmunda (king fern) , Stereisporites and Toroisporites . The spore

genus Stereisporites , which occurs with the moss Sphagnum, represents 50% of the sporomorphs. Stereisporites and Sphagnum are often recovered from depositional

environments of cool ponds and bogs or marsh environments (Kroeger, 2002). Species

of Gleicheniidites and Stereisporites are especially common in coal samples (Nichols,

1995). According to Kroeger

Table 6.2. Tree and shrub taxa in the Porters Creek and Clayton formations. ______Scientific Name Common Name Modern Plant ______Abies balsamea balsam firs Abies Acer striatellum maples Acer Alnus trina alders Alnus Alnus vera alders Arecipites spp. palms Arecaceae Betula infrequens birchs Betula Carpinus paleocenica hornbeams Carpinus Carpinus subtriangula hornbeams Carya paleocenica hickorys Carya Caryapollenites imparalis hickorys Caryapollenites simplex hickorys Caryapollenites veripites hickorys Corylus sp. hazelnut or filberts Corylus Cupressacites hiatipites cedar or cypresses Cupressus Faguspollenites sp. beeches Fagus Fraxinoipollenites medius ashes Fraxinus Fraxinoipollenites variabillis ashes Juglans sp. walnuts Juglans Juglans nigripites walnuts Liliacidites sp. yuccas Lily Liliacidites complexus yuccas Liliacidites dividuus yuccas Liliacidites inaequalis yuccas Liliacidites intermedius yuccas Liliacidites tritus yuccas Liliacidites vittatus yuccas Nyssapollenites sp. tupelo Nyssa Nyssapollenites albertensis tupelo Nyssapollenites explanata tupelo Nyssapollenites paleocenicus tupelo Nyssapollenites pulvinus tupelo Pinus cembraeformis pines Pinus Pinus scopulpites pines Pinus semicircularis pines Pinus strobipites pines Platanus sp. sycamores Platanus Platanus occidentaloides sycamores Quercus velutina oaks Quercus Quercoidites sp. oaks

Table 6.2. Tree and shrub taxa in the Porters Creek and Clayton formations (continued). ______Scientific Name Common Name Modern Plant ______Quercoidites genustriatus oaks Quercoidites inamoenus oaks Quercoidites microhenricii oaks Salixipollenites parvus willows Salix Sequoia sempervirens redwoods Sequoia Tilia instructa basswoods Tilia Ulmipollenites sp. elms Ulmus

(2002), Cyathidites appears to be the only fern spore that occurs in greater abundance in

lake deposits than any other known paleoenvironment.

6.1.3.3. Porters Creek Formation. The Porters Creek contains the most

abundant pollen in general and the highest percentage of gymnosperm pollen. Some

palynomorphs are attributable to families of modern day hardwood forests. They include

Pinaceae (pines and firs), Ulmaceae (elms), Cupressaceae (cedars or cypresses), Fagaceae

(oaks and beeches), Betulaceae (hazelnuts, birches, hornbeams and alders), Juglandaceae

(hickorys, walnuts and pecans), Aceraceae (maples), Oleaceae (ashes), Platanaceae

(sycamores), and Tiliaceae (basswoods). Some of the major assemblages representing

the lower layers below the canopy include a variation of the Lily (Liliaceae) as well as

many ferns and mosses, such as Schizaeaceae ( Cicatricosisporites ), Cyatheaceae

(Cyathidites ), Gleicheniaceae ( Gleichenia ), Polypodiaceae ( Laevigatosporites ),

Sphagnaceae ( Sphagnum ) and Selaginellaceae ( Stereisporites ). This assemblage contains

the lowest percentage of spores. Tropical palynomorphs are from the Areaceae (palm

trees and cycads), while medicinal herbs include Chenopodiaceae ( Chenopodipollis ),

Ephedraceae ( Ephedripites ) and Ericaceae ( Ericipites ).

Table 6.3. Palynofloral association of the Clayton, Porters Creek, and Owl Creek formations. ______Air plants (Epiphytes) Aquatic plants Aquilapollenites Aglaoreidia Milfordia Myriophyllum

Blooming flower plants/grasses Ferns: Gothanipollis (belt flower plant) Anemia Graminidites (buffalo grass) Baculatisporites Intratriporopollenites Cicatricosisporites (gap branch) Liliacidites (Lily family) Cyathidites (tree fern) Milfordia Deltoidospora Tricolporopollenites (pasture plant) Gleichenia Gleicheniidites Laevigatosporites Leiotriletes (climbing fern) Lygodium (climbing fern) Lygodiumsporites Osmunda (king fern)

Fungi: Freshwater algae: Diporicellaesporites Botryococcus Thecaphora Ovoidites Pediastrum (green algae) Schizosporis Spirogyra (blue-green algae)

Herbs: Mosses: Chenopodipollis Lycopodium (clubmoss) Ephedripites Selaginella (spike moss) Ericipites Sphagnum Mitella (Miterwort) Pachysandra (perennial) Pistillipollenites Polygala (Seneca Snakeroot)

Palms: Vines: Arecipites Gleichenia Cycadopites (cycads) Lygodium Longapertites Vitis (common grape vine) Proxapertites

Table 6.4. Modern plant taxa type in North American regions and zones (compiled from Harris, 2003). ______Scientific Name Type Zone D/E Plant Region ______Abies T 3 – 9 E 4, 8 Acer T 4 – 10 D 1a, 9 Alnus T 4 – 9 D 9 Betula S 1 – 9 D 1a, 4, 10 Carpinus T 5 – 9 D not available Carya T 4 – 11 D 1a, 8, 9, 10 Corylus S, S (T) 4 – 9 D 1a Cupressus T 7 – 10 E 1a, 2, 4, 10 Ephedra S 6 – 10 E 6 Fagus T 5 – 9 D 1a Fraxinus T 3 – 10 D not available Juglans T 4 – 9 D not available Lily P not available 1a, 2, 6, 8 Nyssa T 3 – 10 D 2 Pinus T 2 – 11 D 1a, 1b, 3, 4, 6, 7, 8 Platanus T 3 – 10 D 2 Quercus T 2 – 10 D 1a, 1b, 7 Salix T, S (T) 2 – 10 D 2, 6, 10 Sequoia T 7 – 10 E 2, 7 Thuja S, T 4 – 10 E 9 Tilia T 2 – 9 D 1a Ulmus T 3 – 10 D 1a Yucca T 4 – 10 E 6 Tupelo T not available D not available ______

Explanation of numbers and abbreviations

Plant Type S stands for shrubs T stands for trees S (T) stands for shrubs that can grow large enough for people to think of them as trees P stands for flowering plants

Deciduous or Evergreen D stands for deciduous plants E stands for evergreen plants

Table 6.4. Modern plant taxa type in North American regions and zones (compiled from Harries, 2003) (continued).

Plant Regions of North America

1 Eastern Forests 7 California 1a Northeastern 1b Southeastern 8 Montane 2 Swamps and Wetlands 9 Pacific Northwest (Tall Trees) 3 Florida 4 Boreal Forest 5 Prairie 6 Desert

Climate Zones: Average Minimum Temperatures Zone ºF ºC 0 no plant life 1 below -50 below -46 2 -50 to -40 -46 to -40 3 -40 to -30 -40 to -34 4 -30 to -20 -34 to -28 5 -20 to -10 -28 to -21 6 -10 to 0 -21 to -16 7 0 to 10 -16 to -12 8 10 to 20 -12 to -7 9 20 to 30 -7 to -1 10 30 to 40 -1 to 4 11 40 to 50 4 to 10 12 50 to 60 10 to 16

Some aquatic medicinal herbs identified include Aglaoreidia (unknown affinity),

Restionaceae ( Milfordia ) and Haloragaceae ( Myriophyllum ). According to Frederiksen

(1985), herbs were significantly fewer during the Paleocene; however, by the end of the

Oligocene, many herbal plants had evolved and began flourishing. Figure 6.12 reconstructs the Maastrichtian to Paleocene paleovegetation in the study area.

Figure 6.3. Graphical representation of plant groups identified in New Madrid Test Well I-X. Bar scale represents the total number of palynomorphs.

Table 6.5. Palynomorph counts attributed to different plant groups, New Madrid Test Well I-X.

Samples Deciduous Evergreen Shrubs Palm Palm Blooming Aquatic Medicinal Ferns/ Mosses Freshwater trees Trees trees Plants flowers plants Herbs vines algae

NM01 43 78 7 31 17 16 0 22 77 7 25

NM02 13 13 16 0 7 0 5 0 21 7 10

NM03 38 10 18 6 0 0 4 0 26 0 3

NM04 3 8 0 18 15 0 5 11 27 0 9

NM05 0 5 3 15 0 0 0 5 23 0 0

NM06 83 35 9 19 27 0 0 12 58 0 0

Figure 6.4. Graphical representation of plant groups identified in BH-1 core, Scott County. Bar scale represents the total number of palynomorphs.

Table 6.6. Palynomorph counts attributed to different plant groups, BH-1 core, Scott County. Samples marked “nd” indicate “no data available (barren).”

Samples Deciduous Evergreen Shrubs Palm Palm Blooming Aquatic Med. Ferns/ Mosses FW Fungi Grasses BH-1 trees Trees Trees plants Flowers Plants herbs vines algae

SC01 nd nd nd nd nd nd nd nd nd nd nd nd nd

SC02 33 53 0 14 0 4 0 24 121 14 24 25 9

SC03 40 20 6 0 19 9 0 19 17 4 4 20 18

SC04 103 63 0 10 2 13 9 1 9 1 5 6 18

SC05 117 15 27 17 12 29 9 7 14 0 2 18 13

SC06 11 21 0 20 13 5 7 11 28 5 3 0 26

SC07 8 13 0 23 2 15 3 27 12 0 3 18 2

SC08, SC09 nd nd nd nd nd nd nd nd nd nd nd nd Nd

Figure 6.5. Graphical representation of plant groups identified in BH-9 core, Scott County. Bar scale represents the total number of palynomorphs.

Table 6.7. Palynomorph counts attributed to different plant groups, BH-9 core, Scott County. Samples marked “nd” indicate “no data available (barren).”

Samples Deciduous Evergreen Palm Palm Blooming Medicinal Ferns Mosses FW BH-9 trees Trees trees plants Flowers Herbs /vines Algae

SC14,SC21, nd nd nd nd nd nd nd nd nd & SC27

SC16 0 4 17 0 0 0 7 0 0

SC17 6 36 14 0 0 8 8 0 0

SC18 13 29 28 16 9 0 13 0 0

SC19 5 22 30 0 0 0 11 0 2

SC23 10 21 0 0 0 0 9 0 0

SC25 0 6 1 0 0 7 2 0 1

Figure 6.6. Graphical representation of plant groups identified in BH-10 core, Scott County. Bar scale represents the total number of palynomorphs.

Table 6.8. Palynomorph counts attributed to different plant groups, BH-10 core, Scott County. Samples marked “nd” indicate “no data available (barren).”

Smpls. BH-10 Deciduous trees Evergreen trees Palm trees Palm plants Med. herbs Ferns/vines Mosses FW algae Fungi Grasses

SC010 10 20 0 0 0 6 0 1 2 14

SC11 0 10 14 0 3 0 1 0 0 4

SC12 10 15 15 0 12 0 0 0 3 17

SC13 nd nd nd nd nd nd nd nd nd nd

SC15 4 11 13 0 4 2 12 1 4 64

SC20 0 29 20 0 0 15 20 4 0 10

SC22 9 10 8 5 0 7 0 8 1 6

SC24 0 7 8 9 0 0 8 0 0 0

SC26 0 18 8 0 0 14 5 0 0 0

100

Figure 6.7. Graphical representation of plant groups identified in Trench 1, Stoddard County. Bar scale represents total number of palynomorphs.

100

101

Table 6.9. Palynomorph counts attributed to different plant groups, Trench 1, Stoddard County.

Samples Decid. Evergr. Shrubs Palm Palm Bloom. Med. Ferns/ Mosses FW Grasses Fungi Trench 1 Trees Trees trees plants flowers herbs vines algae ST01 17 1 0 1 0 0 9 0 0 0 0 0

ST02 2 7 0 5 3 0 3 1 3 0 0 0

ST03 2 12 2 20 0 0 0 18 18 0 23 0

ST04 and 16 22 1 42 0 0 4 15 15 0 0 0 ST05 ST06 and 30 37 0 45 3 9 4 44 4 8 13 0 ST07 ST08 27 36 3 45 9 5 0 50 13 0 0 0

ST09 21 0 0 0 0 0 0 8 0 0 0 0

ST10 57 46 0 30 0 0 6 14 3 9 24 3

ST11 0 5 0 25 0 0 7 3 0 10 6 3

101

102

Figure 6.8. Graphical representation palynomorph species recovered from Scott and Stoddard counties attributable to known plant regions. Bar scale represents the total number of species.

South North

Figure 6.9. Inferred paleovegetation model for the northern Mississippi Embayment during the Maastrichtian to Paleocene. 102

103

6.2. PALYNOFACIES ASSEMBLAGES

Dispersed organic matter components are useful tools for interpreting of depositional environments. Several factors such as climate, tectonics, sea level changes, availability of sediments, accumulation rate, the proximity of the terrestrial vegetation to water, the chemical composition of water and biological activity (Batten, 1996a and

1996b) affect organic matter distribution. In marine and marginal marine environments, such as those in the study area, they are derived from two sources: continent (wood, cuticles, spores, pollen, fungal remains, etc.) and ocean (dinoflagellate cysts, acritarchs, marine amorphous organic matter) (Jaramillo and Oboh-Ikuenobe, 1999). However, terrestrially derived organic matter particles behave as clasts in water and their relative proportions decrease as the distance from the source increases (Oboh, 1992; Oboh-

Ikuenobe et al., 1999). In general, palynofacies can be used as indicators of variations in the distance to the shoreline and can reflect changes in deposition (i.e., relative sea level), although currents and storms may cause organic matter to be re-transported from its original source.

The palynofacies assemblages identified in this study (section 5.4; Figure 5. 14) provide some insight into the depositional conditions during the latest Maastrichtian to early Paleocene. The assemblages appear to be defined by sporomorphs, structured phytoclasts and amorphous organic matter and show no general up-section or down- section trend within each formation. Terrestrially derived components dominate assemblages A and B, indicating proximity to source for these components. Assemblage

A is defined by sporomorphs and structured phytoclasts, and is represented by samples from all three formations. Structured phytoclasts overwhelminghly dominate the Porters

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Creek and Clayton samples that define assemblage B; sporomorphs are secondarily important. Assemblage C is represented by samples from the Owl Creek, Clayton hardgound (ST01) and coquinite (ST10), and Porters Creek, and is characterized by

>60% amorphous organic matter. It has been noted elsewhere that deposition of high levels of amorphous organic matter is caused by increased productivity in surface waters, especially oceans (Powell et al., 1990, 1992; Udeze and Oboh-Ikuenobe, 2005). Among all three formations, the Clayton has the highest percentage of marine palynomorphs

(37.9%) in the total palynomorph counts (see see Tables 5.1, 5.3, and 5.4).

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6.3. FORAMINIFERA

6.3.1. Biostratigraphy. Many Paleocene foraminifera are found also in the

Upper Cretaceous sediments and are known to extend upward into the Eocene Wilcox

Group. However, some species (e.g., Ellipsonodosaria midwayensis , Discorbis midwayensis ) are good index fossils for the Paleocene. Foraminifera recovered from

Stoddard County are used for age interpretations. For a complete list of foraminifera present showing quantitative data, see Appendix N. Cushman (1951) described several foraminifera from the Paleocene of the Gulf Coastal Plain, mainly from Alabama,

Arkansas, Mississippi, Tennessee, and Texas, and many are excellent Paleocene index fossils. Liu et al. (1997) identified similar Paleocene benthic foraminifera taxa from an

Island Beach, New Jersey borehole obtained along the eastern Gulf Coastal Plain.

Foraminifera taxa identified include Dentalina sp., Ellipsonodosaria sp., Globulina sp.,

Nodosaria sp. and Tritaxia midwayensis . The Clayton, Porters Creek, and Owl Creek in

Missouri are stratigraphically equivalent to the sections in the Gulf Coastal Plain. Of the

18 species identified in Trenches 1 and 2, 11 species are also found in the Gulf Coastal

Plain (Table 6.11). These taxa are characteristic of the Paleocene. The palynomorphs present in the Owl Creek contain both Late Cretaceous and Early Paleocene taxa which may have coexisted together during the Late Cretaceous.

6.3.2. Assemblages. Foraminiferal assemblages can be interpreted using four

approaches: percent planktonics, species diversity, shell-type ratios, and taxonomics

(Culver, 1987). They can be used to infer environmental changes and sea-level

fluctuations based on upper depth limits of species, morphologic traits, preservation of

assemblages, and nature of associated biota and sediments (Twenhofel and Shrock, 1935;

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Douglas, 1979; Murray, 1991; Jackson, 1994; Buzas and Culver, 1994; Pardo et al.,

1996; Prothero, 1998). In this study, foraminifera complemented palynology in inferring the paleoenvironmental conditions of the K-Pg boundary and examining faunal turnovers during the terminal Cretaceous extinction event.

Table 6.10. Foraminifera identified in Trenches 1 and 2, Stoddard County. CL = Clayton, PC = Porters Creek, and OC = Owl Creek.

Foraminifera species Stoddard County Cushman (1951) Formation/Counties

Anomalina elementiana CL, PC, OC PC, Kemper County, Mississippi

Dentalina gardnerae CL, PC, OC CL, Sumter County, Alabama and PC, Hardeman County, TN

Discorbis midwayensis CL, OC CL, Butler County, Alabama

Ellipsonodosaria midwayensis CL CL, Barbour County, Alabama

Globigerina compressa CL, PC, OC PC, Wilcox County, Alabama

Globulina rotundata CL, PC, OC PC, Hardeman County, TN

Nodosaria affinis CL, OC CL, Sumter County, Alabama and PC, Wilcox County, Alabama

Nodosaria latejugata CL, OC CL, Noxubee County, Mississippi and PC, Butler County, Alabama

Parrella expansa CL, OC PC, Kemper County, Mississippi

Triloculina laevigata CL Choctaw County, Alabama (formation not reported)

Vaginulina midwayana CL, PC, OC CL, Sumter County, Alabama and PC, Choctaw County, Alabama

6.3.2.1. Percent Planktonics. Planktonic foraminifera are extremely rare in the assemblage recovered from the Owl Creek, Clayton, and Porters Creek formations (see

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Table 5.9); only one species ( Globigerina compressa ) out of the 18 identified is

planktonic. Since planktonics are usually abundant in open shelf and deeper marine

environments (Culver, 1987), the overwhelming dominance of benthic foraminifera in

association with highly diverse sporomorph assemblages in these formations is indicative

of nearshore depositional environments.

6.3.2.2. Species Diversity. The pattern generally recognized today is that

foraminifera become more diverse away from the shorelines with increasing depth

(Culver, 1987). Species diversity is generally low, especially in the Porters Creek.

Majority of benthic taxa contain microstructures, some with very large pores or

perforated walls (i.e., Anomalina elementiana, Discorbis midwayensis, Gyroidina depressa, Dentalina gardnerae, Nodosaria latejugata, Nodosaria affinis ), while others such as Quinquloculina sp., Pyrgo sp., Globulina gibba and Globulina rotundata contain

simple, solid walls or non-perforated. Those with especially large pores may serve to

help provide buoyancy for the organisms. Furthermore, benthic foraminifera found at

extreme depths may use the larger pores to uptake oxygen.

The chamber arrangements also vary, and uniserial and trochospiral forms were

dominant. The uniserial, semi-sessile forms, such as Nodosaria latejugata, Nodosaria

affinis and Dentalina gardnerae usually dwell in the deeper depths of the ocean by

balancing their tests in the water and staying relatively close to the bottom. Vagile

trochospiral forms may be able to move within the water column by means of their

pseudopodia and also use them to pick up food particles and other nutrients. Some thick-

walled forms with striae, ridges, and ribs ( Nodoaria latejugata, Nodosaria affinis,

Vagulinulina midwayana, Parrella expansa ) are able to live within coarser substrates

108 with high energy levels. These special ornamentations provide protection during biotic stresses due to climatic changes. With the exception of few larger foraminifera

(Nodosaria latejugata, Nodosaria affinis, Parrella expansa, Anomalina elementiana,

Vaginulina midwayana ), most species recovered in this study were small (i.e., Gyroidina

depressa, Nodogenerina bradyi, dentalina gardnerae ) with rather simple morphologies

and little ornamentation.

Keller (1996) proposed that the evolution of early Paleogene species began

immediately after the K-Pg boundary with the appearance of very small, unornamented,

trochospiral and/or biserial morphologies. This observation was observed globally across

the latitudes, suggesting that the survivor taxa that dominated benthic foraminiferal

assemblages were able to tolerate wide-ranging temperatures, salinities, oxygen levels,

and nutrient conditions. Also, smaller foraminiferal sizes correlate with reduced

salinities. The amount of CaC0 3 needed for foraminiferal test formation is more than

enough in normal salinity environments; however, it is not enough in freshwater or

brackish water habitats. Thus, foraminifera possessing smaller calcareous tests occur in

reduced salinity environments. Smaller calcareous or agglutinated tests also live

anaerobic conditions. When integrated with lithologic and palynologic descriptions, the

high percentage of smaller foraminifera preserved in the three formations studied,

therefore, is likely due to reduced salinity associated with nearshore deposition.

6.3.2.3. Shell-type Ratios. Agglutinated foraminifera dominate either intertidal marshes or the abyssal plain, while porcellaneous species are common in the shallow shelf (Prothero, 1998 and Lipps, 1993). By plotting the shell-type ratios in the three formations studied (Table 5.8) on ternary diagrams and comparing the results to several

109 modern environments found today (Figure 6.13), we can infer the paleoenvironmental conditions of the foraminiferal assemblages. The six Owl Creek samples plot under normal marine marsh habitats (Figure 6.14), while the Clayton assemblage plots between hyposaline marsh and normal marine marsh habitats (Figure 6.15). These results are indicative of nearshore (littoral) environments, and may explain why some larger foraminifera ( Nodosaria spp., Parrella expansa, Vaginulina midwayana, Anomalina elementiana ) co-occur with the smaller forms characteristic of reduced salinity

(Gyroidina depressa, Nodogenerina bradyi, Dentalina gardnerae ). None of these

foraminifera is a cold-water species. The one Porters Creek sample studied plots close to

normal marine marsh conditions (Figure 6.16). Smaller foraminifera dominate the

assemblage. Thus, foraminiferal data suggest that the northern Mississippi Embayment

experienced warm, shallow marine conditions (normal to hyposaline marsh habitats)

during the late Maastrichtian and Paleocene.

Figure 6.10. Ternary diagram used for describing shell-type ratios versus paleoenvironmental conditions (adapted from Murray, 1973). Formations plotted indicate the following: Owl Creek (hypersaline marsh conditions); Clayton (normal marine; hypersaline marsh conditions; and Porters Creek (normal marine, hypersaline marsh conditions).

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7. DISCUSSIONS

7.1. FLORISTIC PATTERNS AND PALEOCLIMATIC CONDITIONS

Climate affects the abundance, diversity and distribution of organisms. A change in climate results in changes in the geographic ranges of many species. Geographic distribution of ancient life, especially terrestrial floras, has been used extensively to characterize climates of the past. Plants enhance chemical weathering but reduce erosion in areas of dense plant cover (Levetin and McMahon, 1996). Today, the highest sediment yields come from areas of wet-dry seasonality, while the lowest yields come from ever wet and extremely dry areas (Wing, 1988). Depositional environments that are very close to source vegetation, such as river floodplains, levees and ox-bow ponds may accumulate autochthonous or nearly autochthonous concentrations of plant debris (Wing,

1988). In such cases, plants serve as sediment traps. Plant cover can also alter the surface albedo, rate of heat loss from air layers near the surface and rate of evaporation

(Bradley, 1999). Therefore, global climate has varied through time with the areal extent and type of plant cover. The following subsections review detailed paleofloristic patterns elsewhere and discuss the results of this study.

7.1.1. Latest Cretaceous. As the Cretaceous came to a close during the

Maastrichtian (70-65 Ma), an epeiric sea extended from the Gulf of Mexico through the

western interior lowlands to the Arctic Ocean (King, 1977). As a consequene of

widespread transgression and low physiographic topography in and near the ancestral

Gulf Coastal Plain, temperatures were relatively warm and stable with moist conditions

(Benton, 2004). A temperature gradient of only about 0.3º C/1º latitude occurred

111 throughout most of North America during the Late Cretaceous. According to Crowley and North (1991), the Cretaceous through the middle Eocene was subjected to some of the warmest temperatures, perhaps 5-10º C warmer than at present. Therefore, the Late

Cretaceous was a time of some climatic change and gradual vegetational restructuring

(Spicer, 1990). North American data shows that the angiosperms underwent both geographical and ecological diversification (Andrews, 1961; Darrah, 1960; MacLeod and

Keller, 1996).

Vegetational and climatic changes during this time can be divided into two phases: Aptian to early Cenomanian and middle Cenomanian to Maastrichtian

(Upchurch and Wolfe, 1987). The first phase saw the earliest diversification during which most foliage type plants first appeared. Although angiosperms may dominate megafossil assemblages in certain riparian facies, the palynoflora is always dominated (>

60%) by spores and pollen from ferns, sphenophytes and gymnosperms (Upchurch and

Wolfe, 1987). From the middle Cenomanian to the late Maastrichtian, at 30-65º paleolatitudes, angiosperms were one of the most abundant and widespread palynofloras

(Levin, 1999). Forested areas included stands of birch, maple, walnut, beech, sassafras, poplar, and willow trees. According to Upchurch and Wolfe (1987), low-middle northern latitude (30-45º) vegetation was predominantly composed of evergreen trees (as in tropical rain forests).

Two important characteristics used for determining climate conditions are the assemblages of leaf size and drip tips. During the Cretaceous, the leaf assemblages contained noticeably thick-textured, but relatively low leaf size in both fine and coarse- grained facies. Angiosperm leaves also displayed either drip tips or probably fine habit.

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Leaf sizes are related strongly to temperature, humidity/water availability and light levels. Large leaves occur in humid conditions and size decreases with decreasing temperature or precipitation.

Leaves with long tips occur most frequently in evergreen leaves in humid environments and predominate in climates above 15º C (Ricklefs, 2001). Thin leaves are typically deciduous and are most common in climates below 15ºC. These morphological characteristics are most consistent with sub-humid conditions and indicate a forest with open-canopy structure (Tiffney, 1984).

At the end of the Cretaceous, megathermal terrestrial plants (temperatures 20º-25º

C) covered much of the southeast North America (30º - 45º N). In terms of species and specimen abundance, megafossil records show that angiosperms dominated the Gulf

Coastal Plain by the Santonian (Upchurch and Wolfe, 1987). The Owl Creek samples from BH-10 contain a low diversity of palynomorphs produced by both evergreen and deciduous trees. This suggests that conditions in the northern Mississippian Embayment were favorable for clumps of conifers to grow in areas of open dry land (unchanged since

Jurassic times), and for newly evolving angiosperms (i.e., broadleaved trees like today) in denser forests.

7.1.2. K-Pg Boundary. Most upper Maastrichtian to lowermost Paleogene beds

throughout the world are marked by a distinct boundary-clay associated with high iridium

concentrations, shocked quartz grains, and mineral spherules (see Lucas, 1994). One of

the most widely recognized plant-fossil boundary indicators is a sudden and extreme

attenuation in both diversity and abundance of pollen grains preserved within Cretaceous

strata, at or near the boundary clay (Spicer, 1990). This is followed by a sudden increase

113 in abundance of spores within the post boundary clay. Following this, a gradual decline of spores occurs as pollen grains increase once more in diversity and abundance.

Although evidence for high concentrations of iridium and/or shocked quartz is absent in the Danian Clayton Formation, silicate glass spherules (microtektites) are quite abundant in the Clayton coquinite.

Above the boundary clay layer there are a few millimeters of organic-rich rock generally devoid of palynomorphs. This “barren zone” generally preserves rotting vegetation attributed to fairly warm temperatures and dry periods. In the northern

Mississippi Embayment, such a zone was not identified. However, the Clayton hardground preserves little evidence of invertebrate and vertebrate life, but contains some palynomorphs and foraminifera. Just above this layer in the Porters Creek are several centimeters of carbonaceous mudstone containing abundant fern spores and very few pollen grains. This spore-rich horizon likely records a significant vegetational and sea level change.

7.1.3. Paleocene. The latitudinal organization of the Early Paleocene flora was

different from that of the Late Cretaceous (Gastaldo, 1989). During the Danian, an initial

lowering of the MAT (mean average temperature) occurred; however, by mid Paleocene,

the MAT rose steeply and there was an increase in precipitation. These changes are

evident in the widespread formation of peat, which later altered to Paleogene lignites and

coals that now are characteristic of many parts of the mid-continent region (Graham,

1999). With increasing warmth and moisture, the overall diversity of plant life increased,

including the rapid diversification of junglandaceous pollen, and appearance of new

morphotypes appeared (e.g., Carya, Symplocos , thick-walled Alangium , etc., Frederiksen,

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1989a, 1989b). Leaf sizes from Paleocene floras were in most cases larger than those from Late Cretaceous assemblages (Graham, 1999), and half or more of the angiosperm components in the southern United States had drip tips (Upchurch, 1989). Early

Paleocene assemblages from 46º N and South (Gulf Coast) have a high proportion of entire-marginal taxa, thus reflecting megathermal conditions (Graham, 1993). Coastal plain vegetation was likely a tropical rain forest dominated by lianas (vines), cycads, etc.

Graham (1999) reported that microthermal vegetation was restricted to the higher northern latitudes during the Early Paleocene.

There is a general increase in abundance and diversity of angiosperms in the study area. However, gymnosperms appear to increase in numbers but have low diversity in the Porters Creek Formation in comparison to other formations, while spores decrease slightly in abundance in Clayton and Porters Creek samples. With the exception of BH-1

Porters Creek samples SC06 and SC07, the Porters Creek recorded increases in deciduous trees and reductions among evergreens; seven of 10 Clayton samples show a reverse pattern (see Tables 6.6 and 6.9). The overall diversity and abundance of

Paleocene palynomorphs assemblages suggest favorable warm and moist conditions for a diverse plant life. The co-occurrence of evergreens with drip tips and deciduous plants with fine textured leaves indicate sub-humid conditions favorable for forests with open- canopy structures.

7.2. PALEOENVIRONMENTAL RECONSTRUCTION

7.2.1. Introduction. Keller and Stinnesbeck (1996) examined several K-Pg

boundary sections in low to high latitudes, spanning depositional environments from the

115 continental shelf to the shelf-slope and deep sea. They proposed a paleodepth model ranging from approximately 100 to 300 meters for four sections, and a fifth section along the shelf-slope recording an approximate paleodepth of 500 meters. Middle shelf- to inner neritic environments are characterized by generally high sediment accumulation rates, coarse sands, glauconite, breccias, and erosional features related to sea-level fluctuations. Keller et al. (1994a, 1994b) identified this suite of sediments in northeastern and east-central Mexico and the southern United States. These clastic deposits vary in nature and thickness, range from several meters to 10 cm, and sometimes disappear locally.

The four trenches excavated in Stoddard County exposed similar lower Paleocene clastic deposits overlying the Owl Creek Formation; these deposits locally appear and disappear throughout the northern Mississippi Embayment. The Clayton Formation, consisting of only a few tens of meters has been recognized so far in southern Alabama, southwestern Georgia, northeastern Mississippi, southwestern Tennessee, and southeastern Missouri (Wilmarth, 1938). However, within the northernmost portion of the Mississippi Embayment of southeastern Missouri, the preservation of the Clayton

Formation is scarce. The formation has been reported to be that of a deltaic depositional setting (LaMoreaux et al., 1958; Wilamarth, 1938), and research indicates that the

Mississippi and Ohio Rivers ran through the southeastern lowlands of Missouri (Thacker and Satterfield, 1977). Therefore, it is possible that portions of the Clayton may have been eroded away by the action of distributary channels of a river delta, such as the

Mississippi and/or Ohio Rivers. Lithologic, palynomorph, palynofacies and foraminiferal data indicate a nearshore marine environment (littoral to sub-littoral conditions) for the

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Owl Creek, Clayton and Porters Creek (Figure 7.1). The paleodepth of the northern

Mississippi Embayment likely averaged below 200 meters while sea level fluctuated.

7.2.2. Depositional Environments. The controls on the distribution of

palynomorphs and other fossils can be divided into three major groups: stratigraphic,

geographic, and depositional environments. Stratigraphic factors include differences due

to evolution while geographic factors include effects on a limited area of the depositional

environment, such as rainfall variations or local water table variations (Farley, 1988).

The following subsections will discuss environmental reconstruction mainly from

dinoflagellate cyst distribution and regional sequence stratigraphy.

7.2.2.1. Proximal-distal Trends of Dinoflagellates. Marine dinoflagellate cyst

assemblages show a strong proximal-distal signal because of their life strategies

(especially in neritic settings) and their adaptation to specific surface water conditions

(Sluijs et al., 2005). Since Wall et al. (1977) first attributed different dinoflagellate cyst

taxa to specific intervals within modern inner neritic (nearshore) -to oceanic zones,

several other studies have identified similar trends in ancient sequences (Brinkhuis, 1994;

Crouch, 2001; Pross and Schmiedl, 2002). Certain species occur along a proximal-distal

transect. Species of Homotryblium are found in restricted marine lagoonal areas but also co-occurs with Areoligera and Glaphyrocysta , which are restricted to the inner neritic

zone. Some other inner neritic dwellers such as Operculodinium , Spiniferites , and

Cleistosphaeridium also live in the outer neritic zone. These taxa are present, especially

in the Glauconite and Gray zones of the Clayton Formation. Impagidinium appears to be restricted to the deeper oceanic realm.

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Without considering the effects of nutrient availability and water temperature on their diversity, modern dinoflagellate cysts are also strongly dependent on the stresses within ecosystems, which tend to increase in nearshore settings (Patten, 1962; Bradford and Wall 1984; Sluijs et al., 2005). Therefore, lower dinoflagellate cyst diversity and the dominance of inner neritic taxa in the latest Maastrichtian and Paleocene in the northern

Mississippi Embayment are indicative of fair weather wave base and relative shoreline proximities.

7.2.2.2. Regional Sequence Stratigraphy. As with proximal-distal trends,

changes in dinoflagellate cyst assemblage compositions as well as their diversity and

abundance can be used to determine systems tracts related to changes in relative sea level

(Haq et al, 1987; Brinkhuis and Biffi, 1993; Brinkhuis, 1994; Sluijs et al., 2005). An

increase in the outer neritic to oceanic taxa such as Impagidinium, Nematosphaeropsis and Cannosphaeropsis correlates with sea level rise. Likewise, dominance of

dinoflagellate cyst taxa associated with neritic to coastal environments is indicative of

regressive conditions. The evaluation of dinoflagellate species numbers to determine sea-

level change has also been especially useful for establishing a sequence stratigraphic

framework for the K-Pg boundary interval because dinoflagellates did not undergo a

mass extinction as calcareous microfossils. Habib and Miller (1989), Habib et al. (1992),

and Moshkovitz and Habib (1993) noted a relationship between dinoflagellate cyst

diversity and sea level change in upper Cretaceous and lowermost Paleogene sequences

of the southern United States. Minimum species numbers occurred in highstand deposits

and maximum species numbers were observed at the base of transgressive systems tracts.

Uppermost Cretaceous sediments represent a highstand systems tract, followed by basal

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Paleocene sediments deposited in a lowstand systems tract. Sediments of the transgressive and highstand systems tracts succeed these basal Paleocene deposits

(Moshkovitz and Habib, 1993; Sluijs et al., 2005).

Sequence stratigraphic interpretations can be made for the K-Pg boundary interval

sediments in the northern Mississippi Embayment based on dinoflagellate cysts in

addition to other microfossils, macrofossils, and lithologic characteristics. Ternary plots

of palynomorph species diversity and foraminiferal shell-type ratio for all three

formations in the study area indicate a general deposition in an inner neritic (nearshore)

setting (Figure 7.1). However, low diversity and abundance of dinoflagellate cysts in the

Owl Creek supports deposition during a highstand systems tract. The K-Pg boundary

itself is missing and is represented by an unconformity marking the lowstand systems

tract. The basal limestone coquinite of the Clayton Formation occurs as fill within scours

carved into the Owl Creek clay and is characterized by rip-up clasts with microtektites

and reworked vertebrates, invertebrates (including large benthic forms) and

palynomorphs. It marks marine incursion by a megatsunami attributed post-impact

effects due to the Chicxulub impact event (Campbell et al., 2008). This coquinite

represents the early transgressive systems tract. As transgression progressed, the Clayton

graded upward into glauconitic clay (Skolithos ichnofacies) characterized by an increase

in dinoflagellate cyst diversity and abundance as well as increases in larger forminifera

and pelagic macrofossils. A gray clay unit (Cruziana ichnofacies) that lacks macrofossils

but contains abundant and diverse dinoflagellate cysts overlies this unit. The top,

Hardground Zone, of the Clayton Formation lacks macrofossils, contains few

foraminifera and palynomorphs (93% of them dinoflagellates) and may mark a brief

119 period of slow to nondeposition. It probably also represents a condensed section before a sea level highstand marked by the Porters Creek, which has a lower diversity of dinoflagellate cysts than the Porters Creek. As observed by Ekdale and Stinnesbeck

(1998), the different types of ichnofacies (e.g. Skolithos from the Glauconitic Clay and

Cruziana from the Gray clay units) may indicate successive colonizational episodes of the substrate. Due to the difficulty in determining what formation fills the burrows (e.g. Late

Cretaceous or Early Paleocene), we can only speculate that the Clayton Formation represents clastic sediments deposited over a longer period of time. It should be noted here that palynofacies assemblages A (Owl Creek, Gray and Glauconite zones, Porters

Creek) and B (as above except Owl Creek) generally indicate high terrestrial input into the inner neritic environment. Amorphous organic matter dominated by assemblage C

(Owl Creek, coquinite, hardground) may be attributed to increased productivity in surface ocean waters (Powell et al., 1990, 1992; Udeze and Oboh-Ikuenobe, 2005).

120

ee Figure 7.1. Summary characteristics of the three formations studied in the northern Mississippi Embayment. TST = transgressive systems tract; HST = highstand systems tract.

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121

7.3. STRATIGRAPHY AND PLACEMENT OF THE K-PG BOUNDARY

7.3.1. Introduction. It has been known for more than 100 years now that shallow epicontinental seas inundated many of today’s landmasses during the Late Cretaceous.

Toward the end of the period, a maximum transgression divided North America into two continents. As regression began and continued up near the K-Pg boundary, the Atlantic

Gulf Coastal Plain decreased in size and became fragmented bringing with it stream systems that multiplied and lengthened. As the sea levels fell, land connections that were once inundated became reestablished. The placement of the shoreline during maximum transgression, and its subsequent movement during the maximum regression, can be observed during the latest Cretaceous in some areas of the Western Interior Basin

(Waage, 1968; Gill and Cobban, 1973). A short hiatus is commonly present in most of the K-Pg boundary sections worldwide, and represents a short sea-level lowstand

(Canudo et al., 1991; Keller and Benjamini, 1991; Keller et al., 1993; MacLeod and

Keller, 1994; Keller and Stinnesbeck, 1996).

There has been some dispute concerning the age of the K-Pg boundary deposits

on the basin of the Gulf of Mexico shelf and basin (Bralower et al., 2006).

Biostratigraphic interpretations yielding Cretaceous ages for microtektite shelf sequences

in the Gulf region have prompted some authors such as Keller (1996) and Keller et al.

(1996) to question the association of these deposits with the actual Chicxulub event itself.

Notable Gulf of Mexico regional K-Pg studies include, but are not limited to Donovan et

al. (1988), Baum and Vail (1988), Keller (1989), Mancini et al. (1989), Hildebrand and

Boynton (1990), Hildebrand et al. (1991), Pope et al. (1991), Sigurdsson et al. (1991),

Blum and Chamberlain (1992), Jéhanno et al. (1992), Lyons and Officer (1992), Alvarez

122 et al . (1992), Moshkovitz and Habib (1994), Savrda (1993), Stinnesbeck et al . (1993),

Koeberl (1994), and Robin et al. (1994). Some of the best-known clastic deposits

associated with the K-Pg boundary are found in Texas, Alabama, Georgia, Cuba, Haiti,

and Mexico. In order to make comparisons with the Clayton Formation in Missouri,

some of these and other localities will be reviewed.

7.3.2. Alabama (USA). The clastic K-Pg deposits in Alabama are restricted to the Clayton Sands, which are widespread throughout the region. These deposits have been interpreted as transgressive infillings of incised valleys that were cut during a preceding sea-level lowstand (Donovan et al., 1988; Baum and Vail, 1988; Mancini et al.,

1989; Savrda, 1991 and 1993; Moshkovitz and Habib, 1993; Habib et al., 1992), and as high energy impact-generated megatsunami deposits (Hildebrand and Boynton, 1990;

Olsson and Liu, 1993; Habib, 1994; Smit et al., 1994). Several localities in Alabama

(i.e., Braggs, Mussell Creek, Millers Ferry, and Moscow Landing) contain outcrops of gray to olive-gray silty to sandy marls of the Late Maastrichtian Prairie Bluff Chalk. The sections are reported to be intensively burrowed and contain an abundance of Cretaceous body fossils which are mostly bivalves (Mancini et al., 1989; Savrda, 1993; Olsson and

Liu, 1993). A short hiatus was observed in these Clayton Sand sections (Moshkovitz and

Habib, 1993; Olsson and Liu, 1993). On the basis of the irregular geometry of consolidated marlstone and truncation of thick-shelled fossils, Savrda (1993) estimated at least 2-3 meters of erosion occurred.

At the Moscow Landing, the Clayton Sand sections contain an inclined parallel with ripple cross-laminations, rip-up clasts and reworked Cretaceous fossils. Few

Ophiomorpha burrows are present within the lower beds while Thalassinoides and

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Planolites burrows are present in the middle and upper beds of the Clayton Sand sections

(Savrda, 1993). According to Savrda (1993) and Moshkovitz and Habib (1994), these sediments and fossils indicate that deposition occurred in a marginal marine tidally influenced environment. The Clayton Sands are now considered to be of early Danian age, which is near equivalent to the Clayton Formation in southeastern Missouri.

Likewise, the underlying Prairie Bluff Chalk may be equivalent to the Owl Creek

Formation. At all four Alabama localities, truncated, basal limestone beds of the Clayton

Formation overlie the Clayton Sands and/or Prairie Bluff Chalk. Mancini et al. (1989) and Savrda (1993) reported that this sharp contact is clearly an erosional feature at

Mussell Creek, Braggs, and Moscow Landing, and the abrupt lithological change at

Millers Ferry may also indicate discontinuous sedimentation. According to Keller

(1996), the presence of Danian microfossils (mostly foraminifera) in the Clayton Sand sections argue against deposition caused by a K-Pg boundary bolide impact. She also reported that shocked quartz, tektite glass, or other impact indicators were absent in the

Clayton Sands.

7.3.3. Texas (USA). Outcrops along the Brazos River in central-eastern Texas

contain a nearly continuous record across the K-Pg boundary (Jiang and Gartner, 1996;

Keller, 1989; Hansen and Upshaw, 1990; MacLeod and Keller, 1991; Hansen et al. 1993;

and Beeson, 1992). Here, the K-Pg transition contains calcareous claystones of the

Kinkaid Formation. At its base, resting unconformably upon a scoured surface of the

Maastrichtian Corsciana Formation, it consists of coarse sand containing shell hash and

shale intraclasts covered by a thin limestone layer. Bourgeois et al. (1988) and

Hildebrand and Boynton (1990) interpreted this clast deposit as an impact-generated

124 tsunami deposit, which correlates with the proposed Chicxulub impact structure (Smit et al., 1992, 1994). Keller (1989, 1992) attributed these sections to a catastrophic deposit related to the latest Maastrichtian sea-level lowstand and subsequent transgression.

Keller (1996) reported that there were no documentations of shocked quartz, Ni-rich spinels, or microtektites found within the clastic unit.

Keller (1996) questioned the validity of Danian foraminifera at this interval by suggesting that the microfossils were poorly preserved and beyond accurate identification. As with the Clayton foraminifera in Missouri, the marly sediments contained well-preserved Late Maastrichtian, shallow-water benthic assemblages; however, several planktonic foraminifera was also observed within this section. Unlike the Texas section, Missouri unit contains only one Planktonic species ( Globigerina compressa ). A lithological change to a glauconite-rich unit occurs with a sudden truncation of species ranges (MacLeod and Keller, 1991). Also, a short hiatus or condensed section was found in the Clayton Sands. Keller (1996) argued against an impact-generated tsunami because of the absence of microtektites, shocked quartz, foraminifera dwarfing and/or size sorting at the proposed K-Pg boundary.

7.3.4. Cuba. A large boulder bed discovered in the uppermost Cretaceous sediments of Cuba has been proposed to be a proximal ejecta blanket corresponding to the nearby K-Pg boundary bolide impact (Bohor and Seitz, 1990). However,

Brönnimann and Rigassi (1963); Dietz and McHone (1990); and Iturralde-Vincent (1992) argued that this particular boulder was not the result of a proximal ejecta blanket but rather exfoliation weathering of a coarse, calcarenaceous part of a megaturbidite. This unique weathered bed forms a sheet-like unit that is widely recognized in Cuba as the

125

Cacarajicara, Amaro, and Peñaver formations (Pszolkowski, 1986; Iturralde-Vincent,

1992). From foraminiferal data, Keller (1996) determined that this unique bed was early to middle Maastrichtian in age.

7.3.5. Northeastern Mexico. Over a dozen K-Pg boundary sections containing sliciclastic deposits at or near the boundary are found in northeastern Mexico. Although the lithology and thickness vary, the depositional sequences show comparable data.

These sections cover over 500 km in a north-northwest-south-southeast-trending area

(Keller et al., 1994a and 1994b). The clastic deposits have been attributed to impact- generated K-Pg boundary megatsunami (Smit et al., 1992, 1994) as well as a series of normal, high-energy turbidity currents triggered by an impact (Bohor and Betterton,

1993). These deposits have also been interpreted as gravity flows or turbidity currents related to the Late Maastrichtian sea-level lowstand and tectonic activity (Stinnesbeck et al., 1993; Keller et al. 1994a; and Adatte et al. 1994). Based on lithology, mineralogy, petrology and stratigraphy, these clastic deposits have been determined to cover a distance over 300 km in northeastern Mexico. Stinnesbeck et al. (1996) subdivided these sections into the three units discussed below.

7.3.5.1. Basal Unit 1: Spherule-rich layer. These clastic deposits disconformably overlie the Mendez Formation and consist of soft-weathered sediments with abundant spherules. Foraminiferal tests, clasts of the underlying Mendez Formation, and mud clasts containing Turonian age foraminifera are also present. This unit is generally massive or crudely stratified and contains large-scale trough cross-stratification.

The spherules range from 1 to 5 mm in diameter and contain blocky calcite or a variety of green, microcrystalline phyllosilicates which include smectite and glauconite. Some of

126 the spherules are quite large and have several small spherules inside of them. The types of spherule include those formed around foraminifera or sediment grains and rutile crystals; a thin organic wall, suggesting infilled algal resting cysts, encloses some spherules. Glassy spherules are absent, although rare glass fragments occur (Stinnesbeck et al., 1993, 1996; Keller et al., 1994a). The spherule layer contains a 20-25 cm thick well-cemented sandy limestone layer at the top of unit 1 and can be found throughout the area. This layer contains a few graded spherules at the base and top. Convolute bedding is present at the top of the unit and is draped by the overlying spherule-rich sediments.

7.3.5.2. Unit 2: Laminated Sandstone. This unit contains horizontally, weakly laminated sandstones with mud clasts at its base. At El Mimbral in the study area, discrete layers of plant debris are reported. Rare charcoaled plant debris is generally present in this unit. Sand beds are defined as grading upward to slightly finer sands often containing mica and a clay-rich matrix. This unit disconformably overlies unit 1.

Burrows infilled with spherule-rich sediments are found near the base of unit 2 (Ekdale and Stinnesbeck, 1994), suggesting that existence of invertebrates after unit 1 was deposited was followed by erosion prior to deposition of the sandstone unit 2.

7.3.5.3. Unit 3: Interlayered Sand-Silt Beds. This unit consists of interlayered

sand, shale, and silt beds with a variety of sedimentological features such as ripple marks,

horizontal laminations, small-scale crossbedding, flaser bedding and convolute

lamination. The fine-grained layers typically have faunas of Maastrichtian age indicating

normal hemipelagic sedimentation and also have distinct layers of zeolites. Very small,

charcoaled plant fragments are sometimes present, and mud clasts are commonly found

near the base of the Mendez Formation at the El Peñon, La Lajilla, and La Sierrita

127 localities. The unit is often heavily burrowed by Chondrites, Zoophycos, and

Thalassinoides often heavily burrow the top of the unit (Stinnesbeck et al., 1993; Keller et al., 1994a; Ekdale and Stinnesbeck, 1994). The heavily burrowed horizon indicates repeated recolonization by invertebrates; thus the unit appears to have undergone slow deposition over an extended time interval. All of the outcrops contain clastic deposits, although the La Parida clastic section thins out and locally disappears. Therefore, the thinning out reveals a transition between the Mendez and Velasco formations with no lithological changes in the unit present, and when the outcrops cover one hundred or several hundreds of meters, unit 2 first disappears laterally and then unit 1 follows. Unit

3 has been appears to be the most laterally continuous. The disappearance of unit 2 followed by unit 1 represents individual channel fills or fan deposits. Channelized fills are recognized for having the thickest deposits within the center while thinning toward the edges.

7.3.6. Northeastern Mexico, Parras and La Popa Basins. The Parras and La

Popa basins of Coahuila and Nuevo Leon, Mexico contain the Late Cretaceous to

Paleocene Parras Formation and Fiunta Group which has a composite thickness of about

5.4 km of paralic sedimentary rock (McBride et al. 1974). McBride et al. (1974) reported

that this clastic basin-fill was deformed during a post-Paleocene (Laramide) event that

formed the main folds of the Sierra Madre Oriental. Ejecta-rich stata located at or near

the K/Pg boundary in La Popa basin is interpreted by Shipley et al. (2003) as deposits

from tsunami waves and tsunami-induced subaqueous debris flows as the result of the

Chicxulub impact. According to Shipley et al. (2003), an ejecta-bearing event deposit

occupies a stratigraphic position within the upper 5-15 m of the Late Cretaceous Delgado

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Sandstone Tongue on a sharp contact above a delta front and lower shoreface deposits; the event deposit is continuous but varies laterally and stratigraphically in thickness.

Occurring at the lower base of the strata, a conglomerate matrix with sandstone contains a distinctive assemblage of grains that include bubbly calcite spherules, micrite-coated silicate and sparry carbonate grains (Shipley et al. (2003). The bubbly calcite spherules, glass tektites, and coated grains are interpreted as impact ejecta. Shipley et al. (2003), propose that the ejecta were deposited at the site prior to reworking by wave and debris flow processes. In the southeast part of the La Popa basin, as much as 4.6 m of locally thick ejecta-rich conglomerate strata occupy the valley-like features (Lawton et al.,

2005). The southeastern portion containing clast supported textures, graded- plana, conglomerate sandstone couplets, upcurrent-dipping low-angle cross-laminae, and transported fossils indicate deposition by a south- to southeast-directed turbulent, supercritical flow (Lawton et al. 2005). In the northwestern part of the basin, ejecta grains are present but less common in correlative deposits. According to Lawton et al.

(2005), sediment, ejecta, and organisms were eroded from shoreward environments and transported basinward by backflow of run-off surge(s) emplaced against the continent by one or several tsunami(s). Ekdale and Stinnesbeck (1998) used trace fossils to determine whether or not the proposed impact strata were deposited in a matter of hours and/or days or even years. Their portion of the research covered the Cretaceous-Paleogene sequences in Nuevo Leon and Tamaulipas, Northeastern Mexico. Ekdale and Stinnesbeck (1998) identified three distinct sedimentary units which represent distinctly different depositional events. Unit I is an unbioturbated, laminated deposit of alternating smectite grains and calcite spherules. Unit II is a sandstone section that is mostly unbioturbated,

129 but a few spherule-fill burrows occur near the base of the unit. Several burrows were truncated by overlying sand layers within Unit II indicating that they were excavated following deposition of the first sand layers and then filled with spherules, scoured, and overlain by more of Unit II sand. Unit II consists of alternating sandstone, siltstone, and shale that contain abundant trace fossils, including Chondrites, Ophiomorpha, Planolites, and Zoophycos. According to Ekdale and Stinnesbeck (1998), the nature of the trace fossil occurrences attest to at least three successive colonizational episodes of the acreting substrate. The burrows were filled with Late Cretaceous sediments. Trace fossil evidence reported by Ekdale and Stinnesbeck (1998) indicates that the entire K-Pg clastic sequence must have been deposited over a long periof of time.

7.3.7. Gulf of Mexico and Caribbean. A mixture of reworked microfossils,

impact-derived materials and lithic fragments occur near the K-Pg boundary of the

basinal Gulf of Mexico and Caribbean (Bralower et al., 1998). This mixture or “cocktail”

assemblage is interpreted as a gravity flow triggered by the Chicxulub impact. Although

the high percentage of reworked microfossils may cause inaccuracy in dating the clastic

sections, biostratigraphy has been used to determine the maximum age of the K-Pg

boundary strata. The lowest occurrence of Paleocene microfossils and the presence of

spherules, shocked quartz, and Ir anomalies were used to identify the boundary. Ocean

Drilling Program Sites 536, 540 and 1001 and Beloc contain older reworked microfossils

mixed with late Maastrichtian species. Most of the taxa are long ranging and extend

through the Late Cretaceous. Species restricted to the Late Maastrichtian are rare,

indicating that most, if not all microfossils, are reworked. Interestingly, the lowermost 5

cm of the Paleocene contains reduced reworked assemblages.

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Sites 536 and 540 of the basinal Gulf of Mexico have generated many debates regarding the origin of sediments near the K-Pg boundary. Based on the distribution of spherules, shocked quartz, glass fragments and an Ir peak that corresponds to the K-Pg boundary, Alvarez et al. (1992) proposed that these clastic sediments were redeposited following the Chicxulub impact. However, Keller et al. (1993) argued that these sediments were early or early late Mastrichtian in age based on the absence or rarity of the Late Maastrichtian foraminifera. Both planktonic and benthic foraminifera occur in both sites. Sandy and pebbly chalk “cocktail” deposits at Sites 537 and 538 contain quartz and sanidine grains, granule-sized fragments of schist, gneiss, granite; and shallow-water limestone is present, as are smectite spherules at Site 537. Smectite spherules are commonly formed by the alteration of impact-derived glass tektites (Izett,

1990). Sites 536 and 540 have similar assemblages. Bralower et al. (1998) recognized these clastic deposits as gravity flows (turbidites), whereas Alvarez et al. (1992) interpreted considered them to be reworked by waves and currents triggered by the

Chicxulub impact.

7.3.8. Illinois (USA). Cope et al. (2005) described the Early Paleocene Clayton

Formation in the Golden Cat Company’s clay pit near Olmsted in Pulaski County,

southern Illinois. The formation consists of up to 6 m of bioturbated, dark green,

glauconitic, micaceous, fine- to medium sand alternating with dark gray clay. Fossils

collected from a spoil pile included bryozoans, mollusk, decapods, and vertebrates, and

most of them consisted of phosphatic internal molds. The Clayton Formation was dated

at 60.6 ± 1.4 Ma using potassium-argon method; the youngest (top) unit dated at 60.6 ±

1.3 Ma (Cope et al., 2005). Using also the potassium-argon method, the underlying Late

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Cretaceous Owl Creek yielded a 65.7 ± 1.4 Ma date. When compared to the eastern Gulf

Coast, the lower diversity of the fauna and few benthic species found in the Clayton

Formation here suggests that the head of the Mississippi Embayment during the Danian consisted of brackish to near normal marine conditions.

7.4. DETAILED INTERPRETATION OF THE CLAYTON FORMATION

7.4.1. Well Log Data. Examination of driller’s logs and electrical logs covering

9,000 square kilometers reveals that the Clayton Formation dips uniformly 700 meters to

the southeast over 100 kilometers or about 12 meters per kilometer (Campbell et al.,

2008). This is a typical dip for all the Cretaceous and Paleogene units in this area. The

Owl Creek Formation thins from 21 meters in the southeast to 5 meters in the northwest,

and overlying Porters Creek thins from 190 meters to 40 meters over the same distance.

Whereas these overlying and underlying units thin from southeast to northwest, the

Clayton Formation appears to have a uniform thickness of 3 to 5 meters throughout the

Missouri’s bootheel. The Clayton interval cored in New Madrid Test Well 1-X is 4

meters thick (507-511m interval). Frederiksen et al. (1982) described this unit as

“glauconitic shelly marl, grading upward into glauconitic shelly sand, which grades,

rather abruptly into glauconitic silty clay of the Porters Creek.” The New Madrid test

well is located approximately 100 km southeast of Nestle-Purina Plant in Stoddard

County. Across the Mississippi River in Olmstead, Illinois, Cope et al. (2005) did not

provide data on the units comprising the Clayton Formation, although they identified the

same groups of fossils.

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7.4.2. Impact-generated Tsunami or Flood Deposit? This is a logical question to ponder considering that tsunami and flood deposits have some common characteristics.

Several studies of ancient and modern tsunami deposits have documented the features that are unique to tsunami deposits (e.g., Foster et al., 1991; Bondevik et al., 1997;

Dawson and Smith, 2000; Fujiwara et al., 2000; Goff et al., 2000, 2004; Smoot et al.,

2000; Sawai, 2002; Nichol et al., 2003; Vandenberghe et al., 2003; Morales et al., 2008;

Scheffers et al., 2008). These characteristics include: (1) erosional contact to the underlying unit; (2) sediments which are coarser than the underlying and overlying facies, sometimes begining with shell accumulation or mixed facies that can include muddy clasts and reworked plant fragments, and ending with muddy sand or sandy gravel with muddy matrix; (3) the presence of exotic sediments derived from outer coastal or continental shelf environments that may be rich in heavy metals (Pb, Cu, Ni, Fe, and Cr); and (4) abundant allocthonous sediment that may include micro- and macro-fauna, including mixed assemblages of foraminifera, diatoms, ostracods and marine molluscs derived from open and protected environments in a sandy or muddy matrix. Shell-rich deposits typically include a mixture of articulated and broken valves . Descriptions and interpretation of the Clayton Formation in sections 5.1.2 and 7.2.2.2 show that these characteristics are present.

7.4.3. Depositional Model for the Clayton Formation. The Chicxulub bolide impact event probably generated a large-scale tsunami, both directly from the Gulf of

Mexico rushing into the crater (Matsui et al., 2000) and indirectly from shelf collapse into the Gulf of Mexico (Bourgeois et al., 1988; Bourgeois, 1994). Cretaceous-Paleogene boundary interval sequences in several regions in the Western Hemisphere contain

133 tsunami deposits that have been related to post-impact effects (Bourgeois et al., 1988;

Maurrasse and Sen, 1991; Alvarez et al., 1992; Iturralde-Vincent, 1992; Montanari et al.,

1994; Habib et al., 1996; Olsson et al., 2000; O’Campo et al., 1996; Sharpton et al.,

1996).

Campbell et al. (2008) proposed that the Clayton Formation in the northern

Mississippi Embayment was deposited by the same mechanism. They envisaged that seismic shaking and concomitant shelf collapse into the Gulf of Mexico basin created a megatsunami merging with large waves from the direct impact. A ramp-like narrow

Mississippi Embayment probably focused the tsunami into a bore moving from southwest to northeast, picked up material from the shallow seafloor, and generated a suspension cloud. Wave heights greater than 200 meters engulfed the headland area in southeast

Missouri and created a backwash. The suspension cloud settled out as one graded unit

(185 cm thick at the Purina Plant). The heaviest material (including reworked invertebrate/vertebrate fossils and wood debris) filled the scours in the Owl Creek seafloor, depositing the coquinite layer. Organic-rich and lighter elements formed the overlying glauconitic unit, while the finest material devoid of macroorganisms settled out as the upper clay unit. Worms always seem to survive and burrowed into the resultant deposit at will. A possible period of nondeposition likely developed a hardground on the upper clay. Figure 7.2 reconstructs this depositional scenario.

The rarity of mica in the Clayton Formation (as opposed to the Owl Creek and

Porters Creek) may be related to the source areas for the strata in the study area. Pryor and Glass (1961) noted that the drainage basin of the southern Appalachian Mountains, which extended into the northeast portion of the embayment, was the source area for both

134 the mica-rich Owl Creek and Porters Creek clays. The southeast to northwest trend of the coquina scour-fills suggests a different source (from the southeast) for the Clayton sediments.

135

Figure 7.2. Generalized map showing the Chicxulub Impact and the movement of a megatsunami wave as it approached the inundated landmasses of Mexico and North America. The study area is in the Northern Mississippi Embayment.

136

8. CONCLUSIONS

This study has documented a detailed description of the K-Pg boundary interval sedimentary sequence in the northern Mississippi Embayment using sedimentology, palynology, micropaleontology (foraminifera) and well logs. Outcrops are sparse and weathered in the study area in southeastern Missouri, and they do not expose the Danian

Clayton Formation which sits atop an unconformity above the upper Maastrichtian Owl

Creek Formation and is overlain by the Porters Creek Formation. The K-Pg boundary itself is missing. As part of the study published by Campbell et al. (2008), this work contributed important information for interpreting a 185 cm interval of the Clayton

Formation exposed in four trenches at the Nestle Purina Plant in Bloomfield, Stoddard

County. Borehole sediments from Scott and New Madrid counties were also analyzed for this study. Multi proxy data have been used for biostratigraphy, paleovegetation and paleoclimatic reconstruction, and inferring paleoenvironmental conditions for all three formations and for proposing a depositional model for the Clayton Formation. The major findings of this study are briefly highlighted below.

(1) Three hundred and seventy-nine palynomorph taxa were identified.

Angiosperm pollen grains dominate the palynomorph assemblages in the three formations. The Owl Creek yielded the poorest assemblage, whereas the highest diversity and abundance of marine palynomorphs (chiefly dinoflagellates) occurred in the

Clayton Formation. The Porters Creek appears to have the most diverse angiosperm pollen. However, a small percentage of gymnosperm pollen and spores of bryophytes, lycophytes and pteridophytes (ferns) were present. Pollen and spores included long- ranging taxa as well as Masstrichtian and early Paleogene forms. Although dinoflagellate

137 cysts were also mostly Maastrichtian and early Paleogene in age, the presence of

Senoniasphaera inornata in the Clayton confirms a Danian age for this formation.

Cordosphaeridium cantharellum, Cerodinium pannuceum and Impagidinium aspinatum support a Paleocene age for the Porters Creek Formation. Six potentially new species, one pollen and five dinoflagellate cysts, were described.

(2) A low diversity foraminiferal assemblage dominated by benthic species (17 of

18) was identified in this study. These foraminifera were more diverse and abundant in the Owl Creek and Clayton and included Late Cretaceous and early Paleogene taxa commonly found in the Gulf Coast, including the Danian species Ellipsonodosaria midwayensis . About 99% of foraminifera in the Porters Creek were reworked.

(3) Paleovegetation and paleoclimatic conditions were reconstructed from pollen

and spore data. Evergreen and deciduous trees were important elements in the

Maastrichtian assemblage, suggesting that conifers grew in open dry land as the newly

evolving angiosperms grew in denser forests. Although bryophytes, ferns and their allies

were minor components, they were more abundant in the Owl Creek. The Paleocene was

likely submitted to warm and moist conditions and the co-occurrence of evergreens with

drip tips and deciduous plants with fine textured leaves indicate sub-humid conditions

favorable for forests with open-canopy structures.

(4) Using ternary plots of palynomorph and foraminiferal species diversity,

foraminiferal shell-type ratios, and proximal-distal trends of dinoflagellate cysts, inner

neritic (nearshore) paleoevironmental conditions with hyposaline marsh influence were

inferred for all three formations. Typical outer neritic to oceanic dinoflagellate cysts are

absent (e.g., Impagidinium, Nematosphaeropsis ), while the assemblages contain mostly

138 inner neritic forms such as Homotryblium . However, the presence of Operculodinium

and Spiniferites especially in the Clayton Glauconite and Gray zones (which contain

pelagic macrofossils) suggest possible middle neritic conditions. Palynofacies

assemblages provided additional information, in particular with respect to amorphous

organic matter abundance in assemblage C, which includes the Clayton coquinite and

hardground. The Porters Creek appears to have undergone slightly less open marine

influence.

(5) Sequence stratigraphic interpretation was based mostly on changes in

dinoflagellate cyst assemblage compositions as well as their diversity and abundance. An

increase in the outer neritic to oceanic taxa generally correlates with sea level rise,

whereas of neritic to coastal taxa is indicative of regressive conditions. Also, minimum

species numbers occurred in lowstand deposits and maximum species numbers were

observed at the base of transgressive systems tracts. Using the regional sequence

stratigraphic model for Upper Cretaceous and Lower Paleocene strata of the southern

United States as a guide, and integrating dinoflagellate assemblages with other

microfossils, macrofossils, and lithologic characteristics, the following interpretation was

made: (a) the Owl Creek represented deposition during a highstand systems tract; (b) a

lowstand systems tract marking the K-Pg boundary was eroded; (c) the Clayton coquinite

marked the onset of transgression followed by deeper sedimentation of glauconitic and

gray clay and a short period of nondeposition (hardground, possibly a condensed

section); and (d) the Porters Creek was deposited during a highstand systems tract.

(6) The Clayton was deposited as a graded megatsunami deposit due to the after-

effects of the Chicxulub bolide impact. Its basal limestone coquinite has a lumpy,

139 boudinage appearance and appears to be an infill within scours carved into the Owl Creek

Formation. Large macrofossils, foraminifera, palynomorphs, carbonized wood and seeds, and rip-up clasts of the Owl Creek containing layers of microtektites that are morphologically identical to those found at other locations around the Gulf of Mexico characterize this unit. Organic-rich and lighter elements were deposited in the overlying glauconitic shale unit, which in turn is overlain by a macrofossil-poor gray clay unit. A hardground marking a short period of nondeposition or condensed section caps the

Clayton Formation. Well log data indicated a uniform thickness of 3 to 5 meters through the bootheel region. The suggested southeast source area supports deposition by a ramp- like narrow Mississippi Embayment that probably focused the post-impact tsunami into a bore moving from southeast to northwest.

140

APPENDIX A.

CORE DESCRIPTIONS FOR BH-1, BH-2, BH-3, BH-9, AND BH-10

IN SCOTT COUNTY, MISSOURI

141

DRILL-HOLE LOG BH-1

Location: Abandoned gravel quarry on Leonard Weber Farm, SW ¼, SW ¼, NW ¼ sec. 34, T. 29 N., R. 14 E., Scott County, Missouri.

Collar elevation: 139.9 m Inclination at collar: ~90º; length: 71.0 m

Drilled: 9/16/1993-9/22/1993

Unit Depth

Mounds Gravel

Coarse Cobble Gravel 0.0-.213 m

Section A: Cobble to fine grained pebbly sand, poorly sorted, subrounded to subangular, reddish-brown in color. Clasts consist of recycled quartz (orthoquartzite), sandstone, and brown and gray chert, large clasts occur (diameter: 4-7 cm).

Holly Springs Formation

Medium Pebble Gravel 0.213-1.52 m

Section B: Very coarse to fine pebbles, poorly sorted, rounded to subrounded, reddish- brown in color, clasts consists of cherts (black, brown, grey, and reddish-brown), small pebbles to grain size recycled quartz which are clear, black, reddish-brown, and gray.

Note : There appears to be a fining upward in this section. The first 85 cm contain chert and sand grains ranging from 1-22 mm in grain size, and directly below this is a fine matrix interbedded with large grains of chert and recycled quartz ranging from 20-45 mm. The lower portion of this section contains red stain from iron oxidation.

Pebble Gravel 1.52-1.98 m

Section C: Very coarse pebble gravel to medium grained sand, poorly sorted, fining upward, lighter in color than in section B. Clasts include grey, black, brown, yellow- brown, and dark-red brown chert, contains red, white, and clear recycled quartz (rounded to subangular.

At approximately 6 (83 m), a few black chert pebbles occur.

Medium Pebble Gravel 1.98-2.13 m

Section D: Similar to Section B, but red stain is more prominent.

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Sand 2.13-2.62 m

Section E: Fine to coarse-grained sand, poorly sorted, rounded to subrounded, coarse grains are subrounded, red staining from iron oxidation. Clasts are clear, white, and brown-red quartz and black and gray chert.

Gravel 2.62-2.74 m

Section F: Similar to Section A.

Missing 2.74-3.04 m

Ackerman Formation

Clay 3.04-4.66 m

Section G: Fine sand to very fine silt, mottled light-grey, yellow-brown, and dark pink, coarse to fine sand grains are deposited along outer perimeter of core sample deposits, sand grains are absent within internal core, plastic.

Clay-Silt 4.66-6.09 m

Section H: Very fine sand (outer perimeter) to very fine clay-silt, light grey with some yellow-brown staining, plastic.

Porters Creek Formation

Clay 6.09-6.40 m

Section I: Very fine silt, light grey and yellow-brown, shrinkage, similar to Section H, contains some angular grains on outer perimeter.

Clay 6.40-16.7 m

Section J: Clay varies from light to dark when wet, silt present with some mica flakes throughout entire section, slightly plastic, pyrite is found at 30’8” and 32’5, lignite is present throughout section. At approximately 55’7” small amounts of glauconite grains are present, therefore, suggesting very slow sedimentation.

Owl Creek Formation

Silt and Clay 16.7-18.1 m

Section K: Thinly bedded silt and clay, dark and light gray in color, some mica present, possible bioturbation, very fine quartz crystals, muscovite at ~55’6”, lignite present throughout section, very friable. 143

Silt 18.1-18.5 m

Section L: Silt with some clay, grey, light gray, and brown with dark yellow (limonite) throughout section, fine-grained quartz throughout section, some muscovite, small amounts of lignite throughout, very friable with strong bioturbation.

Note: Limonite represents weathering (oxidation); may also represent precipitation in bogs and lakes.

Silt 18.5-19.2 m

Section M: Orange-yellow, dark grey, and grey silt, 60% limonite, friable, fine-grained, subrounded to subangular quartz grains throughout, also muscovite, limonite dominates at base of section cut.

Silt 19.2-19.8 m

Section N: Similar to Section M but has sand content with limonite, some dark gray, light pink color throughout, some muscovite present.

Silt-Sand 19.8-20.2 m

Section O: Fine-grained sand, dark yellow-brown, well-sorted, some dark grey from 19.8 to 19.9 m, quartz grains. Dark, opaque grains and minor amounts of mica are present.

Note: Can see gradation of silt going into sand.

McNairy Sand Formation

Sand 20.2-20.4 m

Section P: Fine-grained sand, rounded to subrounded, moderately to well-sorted, clear quartz grains, dark opaque minerals, light to medium orange-brown in color, similar to Section O.

Sand 20.4-21.6 m

Section Q: White to light tan sand, fine-grained, well-sorted subangular clear quartz, rounded dark minerals and mica, very friable.

Sand 21.6-22.7 m

Section R: Light orange sand, fine-grained, moderately sorted, subangular quartz, dark minerals and some larger flakes of mica, friable.

144

Silt 22.7-22.9 m

Section S: Yellow-brown, pink, white, grey, and dark gray, highly compacted, mica (muscovite) distributed throughout, mica flakes are fairly large, quartz grains are subangular, well-sorted sediment, friable, strong bioturbation.

Silt 22.9-23.2 m

Section T: Yellow, white, pink, grey, tan, finely layered, large mica flakes of muscovite throughout, quartz grains are subangular, fine grains well-sorted, no signs of bioturbation, similar to previous section (T).

Silt and Clay 23.2-25.4 m

Section U: Dark and light grey silt and clay, finely laminated, contains large amounts of muscovite, fairly large flakes of mica, fine-grained quartz, well-sorted, small amounts of lignite throughout section, in some places more lignite.

Clay 25.4-25.8 m

Section V: Mostly all dark clay, highly consolidated, massive in places, quartz grains are subrounded to subangular, fine-grained, some mica flakes, but not as prominent as in previous section (U), limonite is absent.

Silt and Clay 25.8-26.3 m

Section W: Similar to previous section but more silt present, more friable than in previous section.

Clay and Silt 26.3-28.7 m

Section X: Clay with large amounts of silt, fine-grained, well-sorted, combination of quartz and mica, small quantities of lignite distributed throughout.

Zodoc Clay of the McNairy Sand Formation

Clay 28.7-31.4 m

Section Y: Dark grey, massive clay, low quantity of silt, coarser (rough texture), few micas and quartz grains, light gray is silty, low amount of lignite present.

Note: Good place to sample for palynomorphs.

145

Clay-Sand 31.4-31.5 m

Section Z: Dark yellow, dark grey, medium-tan, and white-tan when wet, fine-grained, well-sorted, rounded quartz, some lignite, outer perimeter contains mica (muscovite), possible bioturbation.

Note: Possible transition zone.

Sand-Silt 31.5-31.5 m

Section AA: Light pink, yellow, white-tan, fine to medium grained, well-sorted, rounded to subrounded quartz, some Fe oxidation, some lignite, wavy texture in grain matrix.

Clay-Sand-Silt 31.5-32.0 m

Section BB: Light brown, tan, dark yellow, dark grey, white-tan, fine to medium grained, mostly well-sorted, Fe oxidation.

Silt-Sand 32.0-32.9 m

Section CC: Light brown, tan, white-tan, dark yellow, and dark orange in spots, grey, fine-grained, well-sorted, rounded to subrounded, Fe oxidation in spots. Some lignite, quartz grains are white, yellow, and clear, few dark opaque minerals are distributed throughout, wavy texture in quartz grains. Dark opaque minerals are more abundant at 32.3 m and heavy concentrations of Fe oxide (dark orange-yellow) are present from 32.6 to 32.7 m.

Sand-Silt 32.9-33.2 m

Section DD: White, tan dark-orange-yellow in spots, pink, finer grained compare to section CC, well-sorted, rounded quartz grains, low amounts of lignite present, an abundance of muscovite at 33.0 m, Fe oxidation.

Silt 33.2-33.8 m

Section EE: White, tan, light yellow, pink, brown-orange, very fine grained, fine laminations present (example: 33.3 m), porous from 33.8-33.87 m. Heavy concentrations of muscovite at 33.2 m, muscovite is distributed throughout, rare dark opaque minerals distributed throughout.

Silt 33.8-35.0 m

Section FF: Very fine silt, white-tan, pink, yellow, orange, and light grey, muscovite present, patches of pink, yellow, and orange at 34.1 m, patch of pink at 34.3 m and a patch of yellow at 34.8 m, dominantly white-tan in color.

146

Clay-Silt 35.0-36.1 m

Section GG: Mauve-pink, white-tan, light grey, and grey, possibly light yellow, very fine-grained, more consolidated and massive than Section FF, well-sorted dark opaque minerals sparsely distributed, some muscovite, some FE oxidation present in spots.

Clay-Silt-Sand 36.1-36.12 m

Section HH: Goes from massive (consolidated) to loosely packed, clay-silt. Very fine- grained silt to medium sand, moderately sorted, dark pink-red, orange, yellow, and grey, specks of muscovite distributed throughout, specks of lignite (rare), quartz grains are medium sized and rounded to subrounded, rare dark opaque minerals present, Fe oxidation.

Note: Changes in color go upward from dark orange-yellow to dark pink-red. Also, becomes less consolidated toward end of section.

Sand-Silt 36.12-38.1 m

Section II: Dominantly yellow, some pink in places, light grey, fine-grained, well to moderately sorted, rounded to subrounded, muscovite distributed throughout, dark opaque minerals sparsely distributed, porous in areas, friable.

Sand-Silt 38.1-41.1 m

Section JJ: Sand and silt interbedded with clay, dominantly dark yellow, mauve-pink, light grey, grey, some shrinkage at 38.1 m, fine silt to fine sand, moderately sorted, quartz grains are rounded to subangular, moderately sorted, minor amounts of dark opaque minerals, muscovite present throughout, orange patches throughout, porous, Fe oxidation present, streaks of white distributed throughout, porous, shrinkage near 41.1 m.

Sand-Silt-Fine layers of Clay 41.1-42.6 m

Section KK: Mostly light yellow-brown, grey with white clay layers, finely interbedded, fine-grained, moderately sorted, quartz grains are rounded to subrounded, muscovite distributed throughout, fairly massive (consolidated), light pink to dark pink in places, quartz grains are clear, white yellow, and brown-orange, porous in places.

Sand-Clay-Silt 42.6-43.2 m

Section LL: Light grey, grey, yellow, orange, and tan, fine-grained, well-sorted, dominantly quartz with minor dark opaque minerals, porous, fairly massive (consolidated) shrinkage from 42.6-42.7 m.

147

Sand-Clay-Silt 43.2-49.9 m

Section MM: Light grey, yellow-grey, orange, red, yellow, fine-grained, moderately sorted, rounded to subrounded, clay partings of white, red, liesegang banding present from 43.2 to 43.7 m, some shrinkage at 43.5 m, muscovite distributed throughout, quartz grains dominant, heavy Fe oxidation present at 43.8 m, brown, liesegang banding at 46.9 m.

Note : Liesegang bands represent secondary bands which are caused by rhythmic precipitation within a fluid-saturated rock.

Sand-Conglomerate 49.9-52.4 m

Section NN: Light tan, yellow, orange with pebble to cobble stones of chert, shrinkage at 50.2 m, poorly sorted, chert pebbles and cobbles are white, yellow, and grey, pockets of lignite present, quartz grains are fine-grained to coarse-grained, fine mud matrix throughout, some Fe oxidation present.

Note : Chert fines upward.

Chert 52.4-53.3 m

Section OO: Chert pebbles and cobbles with dark clay. Chert color is white, light grey, grey, banded, orange, and brown, covered with clay.

Coffee Sand

Sand-Clay 53.3-54.8 m

Section PP: Dark and light grey clay with high abundance of lignite, fine-grained with patches of muscovite and finely distributed muscovite, spots of white chert and silt distributed throughout, fine-grained quartz, massive.

Sand-Clay 54.8-59.4 m

Section QQ: Dark and light grey clay, at 56.5 m the core rock is very light in weight from ~ 57.6 to 59.4 m, gypsum blooms are present, finely laminated, quartz grains are rounded and fine-grained, well-sorted, sandy texture, moderately sorted, some muscovite.

Clay 59.4-60.5 m

Section RR: Silty, light grey to medium grey clay with white clay distributed throughout, large quantity of white clay at 60.3 m, some lignite, similar to Section QQ but lighter in color, pyrite and gypsum blooms are present at ~ 60.3 m.

148

Clasts 60.5-62.4 m

Section SS: Gravel to cobble size, poorly-sorted, sub-rounded to subangular, chert clasts range from light white-gray to dark gray, 2-5 cm in diameter.

Sand-Gravel 62.4-64.6 m

Section TT: Light to dark grey, poorly sorted, fine-grained sand to gravel size clasts. Clasts are light grey to dark grey, subrounded to angular. Some gypsum blooms and small quantities of pyrite. Quartz grains are dark grey.

Clay-Silt-Gravel 64.6-67.6 m

Section UU: Similar to Section TT but finer matrix, clay present, clasts are smaller at the top of 64.6 m. Clasts coarsen to cobble size at ~ 65.7 m and become finer with depth, light grayish white to dark grey, some muscovite, grains of quartz are fine and rounded to subrounded, section is poorly sorted.

Little Bear Formation

Clay with Gravel 67.6-69.1 m

Section VV: Light to dark grey, dark yellow, tan, dark brown-orange, gravel, matrix is very fine, clasts range from light grey to dark grey and are subrounded to angular. Specks of muscovite present, Fe oxidation present, clasts appear to be mostly located at perimeter of core section. Clasts are 1.2-3 cm diameter.

Joachim Dolomite

Limestone 69.1-71.0 m

Brown-red, gray, fine crystalline, finely laminated, angular clasts appear from 70.2 to 70.4 m.

149

DRILL-HOLE LOG BH-2

Location: Approximately 91.4 m north of Route E and English Hill Road intersection on Leonard Weber Farm, center W ½, Sec. 34, T. 29 N., R. 14 E., Scott County, Missouri.

Collar elevation: 113.0 m

Inclination at collar: ~90º, length: 59.4 m

Drilled: 9/23/1993-9/28/1993

Unit Depth

Alluvium

Silt 0.0-.914 m

Section A: Medium brown to medium tan when wet, majority silt, sparse grains of very fine quartz sand and specks of dark opaque minerals distributed throughout core section, (locally) quartz grains vary from very fine, subrouned to coarse, subangular, twigs and other organic debris found throughout section particularly top of section 0.0-.426 m.

Note: Upper portion (0.0-.0914 m) is more of a medium brown. Remainder of section is medium tan to light brown in color.

Sand 0.914-1.22 m

Section B: Medium tan to light brown, very fine silt to fine grain quartz, rounded to subrounded, moderately-sorted, fines upward.

Sand-Gravel 1.22-1.64 m

Section C: Medium brown and tan, fine-grained to coarse pebbles which consist of white, light brown, yellow, dark-red, and black chert with recycled quartz (orthoquartzite), clasts range from (diameter: .396 to .914 m), some dark staining (manganese) throughout, fines upward.

Silt 1.64-3.96 m

Section D: Tan, white to light brown, fine silt, specks of muscovite and dark, opaque minerals sparsely distributed throughout, fine quartz grains found locally along perimeter of core section, cherts vary in color (dark red, yellow, black, brown, yellow-white), some Fe oxidation present (red-staining), twigs common, fines upward.

150

Sand-Gravel-Silt 3.96-4.57 m

Section E: Dark yellow-brown, pooly sorted, some silt, clear, white, and black, fine to coarse-grained, subrounded to subangular quartz, clasts are poorly sorted and consist of fine pebble gravel to coarse pebble gravel, rounded to subangular (chert) and varies in color (as in Section D), specks of muscovite and dark, opaque minerals present throughout core section.

Note: Section is coarser grained from (4.11-4.41 m).

Clay-Sand-Gravel 4.57-4.63 m

Section F: Light tan, light grey, grey, and dark yellow, similar to Section E but with silty clay present.

McNairy Formation

Clay-Silt 4.63-4.72 m

Section G: Light grey and dark yellow, finely laminated, moderate specks of muscovite, very silty.

Silt 4.72-5.09 m

Section H: White-grey, very fine silt with muscovite distributed throughout, some patches of higher muscovite concentrations, approximately 5.09 m and Fe nodule with a diameter of 1 cm is present with higher concentration of muscovite.

Clay-Silt 5.09-5.79 m

Section I: Light grey and light yellow-brown, fine silt interbedded with clay, muscovite present throughout. In some places, patches occur with heavy concentrations of muscovite. Finely laminated, some patches of orange-yellow color, some lignite present.

Silt-Clay 5.79-7.62 m

Section J: Medium grey and light grey, very fine silt, heavy concentrations (layers of muscovite) breakage occurring from 5.79-6.18 m, partings can break as small as 5 mm, some lignite present, more consolidated from 6.18-6.94 m, thicker partings occur with muscovite from 6.94-7.19 m, parting size averages in width of 2.5 cm, partings of muscovite show an angle of ~ 25º from its horizontal position in core.

Note: Partings reverse angles.

151

Clay-Silt-Gravel 6.72-7.98 m

Section K: Light to medium grey, heavy concentrations of muscovite, clasts are rounded to subangular, poorly sorted with fine silt to medium pebble gravel that consist of yellow, orange brown, grey, and red chert with white quartz, some muscovite, no muscovite partings present, glauconite found (locally) on outer perimeter of core section.

Note: Compared to Section J, this section appears to have less mica present.

Silt-Clay 7.98-8.26 m

Section L: Light to medium grey, white and brown-yellow, (locally) some sand along outer perimeter and chert fine pebble gravel, muscovite partings at ~ 15º angle.

Silt-Clay-Sand 8.26-10.6 m

Section M: Dark yellow-red, heavy concentrations of muscovite, lignite sparsely distributed, heavy Fe concentration throughout.

Sand-Silt 10.6-11.2 m

Section N: White, fine silt to very fine sand, relatively well-sorted, specks and concentrations of lignite present, friable, some Fe oxidation present, grains are rounded to subrounded.

Sand 11.2-14.0 m

Section O: Yellow, orange, pink, light grey, fine-grained quartz, well-sorted with muscovite distributed throughout, sparse amounts of dark opaque minerals, some manganese present (locally), more consolidated than in Section N.

Zodoc Clay

Sand-Clay 14.0-14.1 m

Section P: Similar to section O but with more clay present and color is medium tan to light gray.

Clay-Silt 14.1-16.5 m

Section Q: Medium to dark grey, massive, low angle partings in places, muscovite distributed throughout, specks of lignite.

Clay-Sand 16.5-16.8 m

Section R: Dark to medium grey and yellow-brown, similar to Q but more sand present. 152

Sand 16.8-17.5 m

Section S: Yellow-brown and orange, fine grained, well-sorted, subrounded to subangular, clear quartz, dark opaque minerals and muscovite rare, at base of section, darker Fe oxidation present.

Sand 17.5-17.6 m

Section T: Fe oxide concentration, quartz grains are clear, fine-grained, well-sorted, rare muscovite, patches of dark fine-grained minerals (possibly squartz), especially where Fe oxide in greatest.

Sand 17.6-18.1 m

Section U: White with some yellow-brown, silty texture, very fine-grained, clear quartz with dark opaque minerals distributed throughout, muscovite present, quartz grains are subrounded to subangular and well-sorted. Fe oxidation present in patches and small spots.

Silt 18.1-19.6 m

Section V: White with some yellow-orange where concentrations of Fe oxide are present, well-sorted, very silty, abundant muscovite, few dark opaque minerals present, friable.

Silt-Sand 19.6-23.4 m

Section W: White, yellow-orange, yellow-brown, pink, and light grey, slightly sandy texture, dark opaque minerals distributed throughout, quartz grains are subrounded to subangular, well-sorted, abundant muscovite, spots of heavy Fe oxide concentrations.

Sand 23.4-25.9 m

Section X: Similar to Section W but more sand present.

Sand-Clay 25.9-27.4 m

Section Y: Brown and tan-brown, some orange in places, mostly sand with variable clay content, fine-grained, well-sorted, muscovite present throughout, subrounded to subangular, dark opaque minerals present throughout.

Sand-Clay 27.4-30.1 m

Section Z: Yellow, yellow-brown, red-orange, light gray, pink and white-tan, similar to Section Y but more sand content and larger mica flakes present throughout, clay content variable. 153

Sand 30.1-31.6 m

Section AA: Yellow-brown and tan, porous, fine to very fine clear and dark quartz, moderately sorted, subrounded to subangular, some muscovite, rare opaque minerals present.

Sand-Clay 31.6-32.1 m

Section BB: Yellow-brown, orange, pink, and light grey, very fine-grained quartz grains which are subrounded to subangular, moderately sorted, porous, muscovite present (some places abundant), thin layers of clay present throughout.

Silt-Clay 32.1-32.3 m

Section CC: Yellow-brown and pink-brown, more clay content than in Section BB, porous, fine to very fine silt, some muscovite present throughout, no dark opaque minerals, clayey in spots.

Sand 32.3-33.1 m

Section DD: Yellow and orange-brown, fine to medium-grained, rounded to subrounded quartz, rare muscovite, dark opaque minerals absent, slightly clayey.

Sand 33.1-33.5 m

Section EE: Yellow-brown and yellow-orange, fine to medium-grained, poorly sorted, subrounded quartz, rare muscovite, near base of section there is fine pebbles of white- gray chert present.

Clay-Sand 33.5-34.5 m

Section FF: Dark to medium gray, sandy, massive, muscovite, very fine-grained, rounded, quartz, circular grains present in clay, possibly oolites, see red marking on core box.

Sand 34.5-35.1 m

Section GG: Tan and yellow-tan, moderately sorted, rounded to subrounded, fine- grained, no muscovite, small, fine pebbles of chert, at 35.0 m pebble has oolites, from 35.0-35.1 m muscovite is present.

Clay-Silt-Sand 35.1-35.2 m

Section HH: Yellow-brown, medium and light gray, finely laminated, silty and sandy, muscovite present, quartz grains are very fine-grained, Fe oxides present in places.

154

Clay-Silt 35.2-35.6 m

Section II: Medium and dark grey, oolites present locally around perimeter of core section, massive, somewhat silty, low angle partings contain more muscovite.

Conglomerate (Sand and Gravel) 35.6-35.9 m

Section JJ: Yellow-brown, orange-brown, and dark pink, fine to coarse-grained quartz, rounded to subrounded, well-sorted quartz sand, pebbles to gravel appear throughout with depth, pebbles and gravel are chert with various colors and are subrounded to subangular, dark opaque minerals present, no muscovite, Fe oxide present.

Gravel 35.9-38.1 m

Section KK: White, light gray, and yellow, coarse pebbles to cobbles, diameters range from 16 mm to 5 cm, coated with fine light clay.

Clay-Gravel 38.1-38.2 m

Section LL: Dark grey clay with very fine to medium pebble chert, some muscovite, quartz grains are clear, fine-grained and rounded, lignite abundantly distributed.

Coffee Sand Formation

Clay-Silt-Sand 38.2-39.0 m

Section MM: Dark and medium grey, golden-brown specks, silt forms wavy texture, muscovite present, lignite abundantly distributed, golden-brown and clear quartz sparsely distributed, quartz grains are rounded.

Clay-Silt 39.0-43.1 m

Section NN: Light grey, silty texture, few quartz grains, no muscovite, lignite rich at 39.4 m, gypsum blooms present at 39.5 m and 41.4 m, lignite distributed throughout, possible pyrite at ~ 42.9 m.

Clay-Sand 43.1-43.5 m

Section OO: Light grey, white (clay), and yellow-brown, very fine-grained, well-sorted, rounded to subrounded quartz, pyrite specks and gypsum bloom at 43.2 m, no muscovite, no dark opaque minerals, small portion of lignite at top of section marking transition zone.

Note: White clay layers present throughout.

155

Sand-Clay 43.5-44.1 m

Section PP: Dark yellow and red-brown with white clay layers, fine to very fine-grained, subangular to subrounded, well-sorted, clear and white quartz, grey and dark grey chert, more silt present at base, Fe oxide present throughout.

Post Creek Formation

Gravel-Clay 44.1-51.2 m

Section QQ: Clasts of white-gray, medium grey and dark grey, orange-red, and yellow brown ranging from large cobbles (3 cm to 7 cm) to small pebble gravel, pebbles and gravel are subrounded to subangular, gypsum bloom found with pyrite at ~ 45,7 m, gravel is more angular (breccia) from 50.2 m to 51.1 m, pebbles are more rounded, pebbles and cobbles vary in size from 44.1 to 50.2 m, base has more clay content, fines toward transition zone.

Clay-Silt 51.2-53.1 m

Section RR: Brown-grey, yellow-brown, dark orange, and white, massive, silty texture, iron oxide present at 51.2 m and 52.7 m, fine-grained pyrite at 52.4 m, lignite-rich at ~ 53.0 m to 53.1 m, coarse pebbles and cobbles distributed.

Little Bear Formation

Clay-Claystone 53.1-53.3 m

Section SS: Light yellow-brown and yellow-grey, massive clay matrix, some fine liesgang bands, angular fragments of claystone throughout clay.

Clay-Sand 53.3-53.9 m

Section TT: Light to medium grey, yellow-brown, red-brown, white, gypsum bloom (white) occurs at 53.3 m, pyrite present at 53.3 m, angular claystone, large cobbles are rounded, angular pebble-gravel.

Silt-Clay 53.9-56.0 m

Section UU: Yellow-tan, pink, orange, white, gray silt with clay matrix, orange liesgang banding occurs at ~ 54.2 to 54.5 m, angular fragments of claystone.

Clasts 56.0-56.7 m

Section VV: Light to dark grey-black, coarse pebble gravel to cobble size chert clasts, rounded to subrounded ranging from 1 to 3 cm, fragments of claystone. 156

Clay 56.7-58.5 m

Section XX: Yellow-tan with black streaks throughout, medium to coarse pebbles scattered throughout (sparse), pebbles are chert which are rounded to subrounded, orange spots isolated of Fe oxide, dark streaks are most likely lignite.

Silt-Clay 58.5-59.16 m

Section YY: White, powdery (like talcum powder).

Clay-Silt 59.16-59.2 m

Section ZZ: Very similar to Section XX but no black steaks present.

Joachim Dolomite

Dolomite 59.2-59.4 m

Section AB: Light to medium grey, finely crystalline, Fe oxide present.

157

DRILL-HOLE LOG BH-3

Location: Field on Leonard Weber Farm, approximately 241.5 m southeast of Route E and English Hill Road, SW ¼, NE ¼, SW ¼, Section 34, T. 29 N, R. 14 E, Scott County, Missouri.

Collar elevation: 101.1 m.

Inclination at collar: - 90º; length: 35.9 m.

Drilled: 11/3/93 – 11/8/93.

Unit Depth

Alluvium/Colluvium

Clay 0.0 - .362 m

Section A: Yellow-brown to brown-grey, silty, some sand, porous, moderately sorted with plant debris, subrounded to subangular, fine-grained quartz sand.

Alluvium

Sand .362 – 3.62 m

Section B: Dark brown, brown to yellow-brown, fine to very fine-grained, rounded to subrounded, fines upward, quartz grains are yellow, white, clear, and pink-red, at ~ 3.32 to 39.9 m, there is a section of pink-red chert which is approximately 1 cm in diameter, moderately sorted with exception of pink-red chert, some dark opaque minerals distributed throughout.

Sand 3.62 – 5.85 m

Section C: Brown, light brown, tan, fine to very coarse grained, moderately sorted with cobble size chert distributed throughout, rounded to sub-rounded, similar to Section B, specks of muscovite distributed, some recycled quartz of various sizes (1-2 cm in diameter), dark and red opaques distributed throughout.

Sand 5.85 – 8.15 m

Section D: Medium brown to tan-brown, very fine to very course-grained, rounded to subrounded, poorly sorted, quartz grains are clear, dark and red opaques, similar to Section C, no muscovite present, larger pebbles occur at 5.85 and 6.33 m which are rounded to subrounded, somewhat silty.

158

Sand-Gravel 8.15 – 11.3 m

Section E: Light brown to brown, tan, very poorly sorted, very fine sand to coarse cobble gravel, some silt, no muscovite, dark and red opaques, various colors of chert gravel and recycled quartz, gravel measures from 2 mm to 2.5 cm in diameter, similar to Section D, loosely compacted, gravel is rounded to sub-angular.

Sand 11.3 – 11.6 m

Section F: Light brown to brown, tan, very fine to coarse-grained sand, very poorly sorted, some silt and fine to medium pebbles, some organic material from 11.4 – 11.5 m, no muscovite, similar to Section E.

Sand-Gravel 11.6 – 15.3 m

Section G: Brown-tan, fine to coarse pebble gravel, poorly sorted, sand (quartz) is fine to coarse-grained, gravel is scattered throughout and includes chert and recycled quartz, various colored gravel, large clast at ~ 12.0 m) (diameter: ~ 3 cm), gravel consists of various colors (pink, purple-red, white, tan, yellow, grey, and dark grey, no muscovite, dark opaque minerals present, loosely compacted.

Sand-Clay-Gravel 15.3 – 20.8 m

Section H: Green-grey to green-tan, white-green, very poorly sorted, clay matrix with granule to coarse pebble gravel, pebbles are subrounded to subangular, various colors of chert and recycled quartz, at ~ 17.5 m green clay with iron oxidation of purple-red color (17.5 – 17.8 m), clasts are various colors (white, green-white, yellow-brown), fragment of lignite at ~ 17.8 m, clay mostly absent from 17.8 to 20.5 m, at 20.6 to 20.8 m there is a dark coating on gravel.

Note: Appears to be a transition zone.

Absent (no recovery) 20.8 – 22.3 m

Post Creek Formation?

Clay-Gravel 22.3 – 23.8 m

Section I: Medium to light green-grey, pale green, very silty, some very fine sand scattered, color patterns have a swirling appearance, matrix supported with fine to coarse cobble gravel, no muscovite, gravels consist of chert and recycled quartz ranging from 1.5 – 4.5 cm in diameter, subrounded to subangular, rare organic material present throughout.

159

Sand-Clay-Gravel 23.8 – 23.9 m

Section J: Gray to pale green-grey and dark brown-black, poorly sorted, rounded to subrounded, fine to coarse-grained sand, some chert, siltstone present ~ 23.9 to 24.0 m, possible pyrite present in one small confined area, possible lignite present.

Clay 23.9 – 24.7 m

Section K: Light grey to dark-grey, dark purple-red, brown-black, and pale green, some swirl color patterns, more massive than Section J, small quantities of sand, organic material surrounding pale green clay, possibly lignite (dark material), iron oxidation occurs at 24.1 m, 24.3 m, and 24.6 to 24.7 m.

Little Bear Formation

Gravel-Clay 24.7 – 27.1 m

Section L: White, light grey, yellow-brown, and pale green, sandy-clay matrix, dominantly white, poorly sorted, weathered chert ranging from < 1 cm to > 5.5 cm in diameter, sand matrix is fine to medium-grained and dominantly pale green, possibly siltstone present.

Clay 27.1 – 27.2 m

Section M: Light grey-green, purple-red, and brown, green, very fine to fine sand grains, rounded, some siltstone.

Gravel-Clay-Sand 27.2 – 29.8 m

Section N: Light grey, brown-grey, purple-red, very fine to fine sand with clear quartz and red-brown quartz, poorly sorted, subrounded to subangular pebble gravel with various colors, matrix supported at top of section and clast supported at base (29.8 m), iron oxidation.

Missing (no recovery) 29.8 – 30.7 m

Clasts 30.7 – 32.3 m

Section O: White-grey, yellow-brown, red-black, subangular to angular clasts, very coarse pebble gravel to cobble measured as large as 3.5 cm in diameter.

Note: Logs record that matrix washed away during drilling.

160

DRILL-HOLE LOG BH-9

Location: 7.5’ quadrangle plotted on USGS map 1-2744, SW ¼, SE ¼, Section 33, T. 29 N, R. 14 E., Scott County, Missouri. Quadrangle is approximately 15-20 mi N. of NMS Zone. Collar elevation: 113.1 m Drilled: 1996

Unit Depth

Clay 0.0-2.59 m

Section A: Fine sand to very silty clay, yellow-brown to dark pink (mauve). Contains dark nodules. Sand grains are clear to white. Plant material is present. Sands become progressively coarser. Progression goes from fine, medium, and coarse sand grains. Red staining due to oxidation. Medium sorting with rounded grains.

Clay-silt 2.59-4.57 m

Section B: Very fine sand to silt. Red staining is present from oxidation, orange-brown in color. Course grains that are composed of clear quarts and orange and dark opaque minerals are dispersed sparingly throughout core. Medium-sorted, subrounded to rounded grains. Shrinkage present.

Clay-silt to medium sand 4.57-5.02 m

Section C: Poorly sorted, medium sand to very fine silt, light gray to light brown. Dark opaque minerals are composed of clear quartz. Subangular to subrounded and poorly sorted. Outer perimeter of core section has coarser grains. Becomes progressively finer grained and well-sorted. Grains are somewhat subangular.

Clay-silt 5.02-7.62 m

Section D: Same color as in section C described. Finer grains and more sorted. Dark opaque minerals are present. Some shrinkage. Yellow staining occurs from 6.64 -7.92 m.

Very fine silt 7.62-8.83 m

Section E: Light grey, very fine silt, well-sorted, rounded to subangular lacks dark opaque minerals.

Fine silt 8.83-10.4 m

Section F: Light grey, fine silt, subangular to angular, well-sorted. Some grains are dark and range from medium to large sand. Some yellow staining is present. 161

Fine sand-silt 10.4-11.9 m

Section G: Light grey to white color, well-sorted, subrounded, porous. Quartz grains are clear to white. Very few dark opaque minerals are present.

Medium sand-silt to coarse sand 11.9-14.9 m

Section H: Light grey to white, poorly sorted (silt to medium sand), round to subangular. Some yellow and dark staining is present. Becomes progressively coarser in grain size.

Coarse sand-silt 14.9-15.4 m

Section I: Light gray to light yellow. Coarse quartz grains, poorly sorted, subrounded to rounded. Dark black and orange opaque minerals are present. Quartz grains are clear, somewhat porous.

Sand 15.4-16.5 m

Section J: Orange to brown, very poorly sorted, rounded to subangular. Orange staining present, quartz grains are clear to white. Some dark opaque minerals are present throughout core.

Porters Creek Clay

Clay-silt 16.5-17.4 m

Section K: Light o medium grey with yellow-brown staining, very fine silt. Contain fine laminations with mica partings throughout section. Pyrite and ooids present on outer perimeter.

Gravel to Clay 17.4-18.0 m

Section L: Light to medium grey with yellow staining, fine clay to gravel, poorly sorted. White, gray, and dark gray chert clasts range from (.30-.60 m). Grains are rounded to angular. No mica present.

Pebble-gravel to clay 18.0-18.2 m

Section M: Light to medium grey with yellow-brown staining. Lignite present with some lamination. Pebbles are lighter in color and angular to subrounded.

Clay 18.2-19.5 m

Section N: Clay varies from light to dark when wet, silt present with some mica flakes throughout entire section. Pyrite and lignite are also present. Mica partings are present, especially from 18.89-19.50 m. Friable in places. 162

Clay 19.5-21.3 m

Section O: Similar to Section N, but contains glauconite.

Clay, silt, and sand 21.3-22.6 m

Section P: Similar to Sections N and O but contains medium sand (quartz) grains.

Clay, silt with gravel 22.6-22.9 m

Section Q: Dark grey with white to light grey gravel. Gravel is angular to subangular and poorly sorted.

Clay, silt, and medium sand 22.9-23.8 m

Section R: Dark to light grey clay with silt and medium sand. Grains are clear, rounded to subrounded. Overall: poorly sorted fairly sorted. Lignite present.

163

DRILL-HOLE LOG BH-10

Location: 7.5’ quadrangle plotted on USGS map 1-2744, NE ¼, NE ¼, Section 5, T. 28 N., R. 14 E., Scott County, Missouri. Quadrangle is approximately 15-20 mi N. of NMS Zone. Collar elevation: 113.4 m Drilled: 1996

Unit Depth

Mounds Gravel

Coarse Cobble Gravel 6.67-9.44 m

Section A: Cobble to fine grained pebbly sand, poorly sorted, subrounded to subangular, reddish brown in color. Clasts consist of recycled quartz (orthoquartzite) sandstones, and brown and gray chert, large clasts occur (diameter: 4-7 cm), fining upward in section.

Holly Springs

Medium Pebble Gravel 9.44-10.1 m

Section B: Very coarse to fine pebbles, poorly sorted, rounded to subrounded, reddish- brown in color. Clasts consist of cherts (black, brown, grey, and reddish-brown). Small pebbles to grain size recycled quartz which are clear, black, reddish-brown, and grey are found in section, coarsens upward.

Ackerman

Clay-silt 10.1-12.5 m

Section C: Very fine clay-silt, light-grey, yellow brown, and dark pink, coarse to fine grains are deposited along outer perimeter of core section, sand grains are absent within internal part of core, plastic in nature.

Porters Creek

Silt-clay 12.5-15.5 m

Section D: Very fine silt-clay, light grey and yellow-brown, contains some subangular grains on outer perimeter. Also contains some lignite and shows shrinkage. Pyrite gives the yellow color in places.

164

Silt-clay to clay 15.5-16.4 m

Section E: Very fine silt-clay, yellow brown to light grey, no lignite present. Some small staining patches occur from iron oxidation, possible pyrite present.

Sand-silt 16.4-19.2 m

Section F: The silt in this section has a much coarser texture than in Section E and there appears to be less clay. Color is greyish-white. No lignite present, some grain sizes are clear quartz and are rounded to subrounded, orange-brown staining is present in some places.

Clay-silt and sand 19.2-19.8 m

Section G: Light, medium, and dark grey color, sand grains are mostly clear except where heavy concentrations of lignite are present. Grains are highly concentrated on outer perimeter of core section, some shrinkage present.

Clay-silt 19.8-21.3 m

Section H: Very fine-silt and clay, medium grey, ooids present and no shrinkage. Very fine lignite veins present as well as pyrite and mica in some places.

Clay-silt-sand 21.3-23.4 m

Section I: Dark grey to black, poorly sorted, lignite and pyrite present, especially on outer perimeter of section, shrinkage present.

Silt-clay 23.4-25.9 m

Section J: Light to medium grey to white-black, silt-clay. Lignite is present in some very small areas of section. Pyrite is absent.

Silt, sand, and small pebbles 25.9-28.7 m

Section K: Light to medium grey, black, and white patches present, poorly sorted. Pebbles are angular to subrounded and sand grains are mostly clear, rounded to subrounded.

Clay-silt 28.7-29.0 m

Section L: Light to medium grey silt with clay, yellow staining in center and outer portions of section.

165

Owl Creek

Clay-silt 29.0-30.3 m

Section M: Light grey to white clay with silt. Lignite and/or pyrite absent, some shrinkage.

Silt 30.3-32.0 m

Section N: Grey, light grey, and light green silt with clay, yellow staining in patches. From 30.26-31.08 m material is friable. Shrinkage appears from 31.39-31.69 m.

Silt 32.0-32.9 m

Section O: Section is similar to Section N, however, material is more solid and color is light grey to white.

Silt-clay 32.9-34.5 m

Section P: Medium grey to light-medium pink silt-clay, some muscovite present.

166

APPENDIX B.

QUANTITATIVE PALYNOMORPH DATA FOR BH-1, BH-9, AND BH-10 IN

SCOTT COUNTY, MISSOURI: NONMARINE PALYNOMORPHS

167

Quantitative Data: BH-1.

Depth (m) 7.31 m 7.62 m 9.45 m 11.9 m 14.0 m 17.2 m 18.1 m 18.3 m 18.8 m

Core Section (interval) R- R- R-1393- R-1470- R-1393- R-1470 - R-1470- R-1470- R-1393- 1393- 1393- 2/COR 1/COR 3/COR 3/COR 2/COR 4/COR 4/COR 1/COR 14/COR

Sample # SC01 SC02 SC03 SC04 SC05 SC06 SC07 SC08 SC09 Abies balsamea 0 0 2 0 0 0 0 0 0 Aglaoreidia pristine 0 0 0 0 0 0 2 0 0 Ailanthipites berryi 0 0 0 0 0 4 0 0 0 Ailanthipites marginatus 0 0 0 3 0 13 0 0 0 Ailanthipites speciipites 0 0 0 10 2 0 0 0 0 Alnipollenites scoticus 0 0 0 0 2 0 0 0 0 Alnus vera 0 12 0 15 7 0 0 0 0 Aquilapollenites bertillonites 0 0 0 0 2 0 0 0 0 Aquilapollenites murus 0 4 0 0 0 0 0 0 0 Araliaceoipollenites profound. 0 0 2 0 0 0 0 0 0 Arecipites sp. 0 14 16 3 14 0 0 0 0 Arecipites columellus 0 0 2 5 0 3 3 0 0 Arecipites rousei 0 0 0 0 3 20 17 0 0 Baculatisporites sp. 0 2 0 0 0 0 0 0 0 Baculatisporites quintus 0 0 0 0 3 0 0 0 0 Basopollis obscurocostatus 0 26 1 0 0 0 5 0 0 Bisaccates 0 39 13 55 74 2 0 0 0 Boehlensipollis minimus 0 0 6 0 0 0 0 0 0 Botryococcus sp. 0 24 0 0 0 0 0 0 0 Botryococcus braunii 0 0 0 5 0 3 0 0 0 Bullasporis sp. 0 0 0 0 3 2 4 0 0 Caryapollenites simplex 0 5 0 2 4 0 3 0 0 Caryapollenites imparalis 0 0 0 2 0 0 0 0 0 Caryapollenites veripites 0 2 21 33 32 0 0 0 0 Celtipollenites gracillis 0 0 0 0 0 7 0 0 0 Chenopodipollis sp. 0 7 4 0 0 27 2 0 0 Chenopodipollis nuktakensis 0 6 4 0 2 0 0 0 0 Choanopollenites sp. 0 0 0 0 0 0 7 0 0 Cicatricosisporites sp. 0 2 0 0 1 0 6 0 0 Corollina (Classopollis ) sp. 0 12 0 4 0 0 0 0 0 Compositoipollenites granil. 0 0 0 0 0 0 3 0 0 Confertisulcites fusiformis 0 0 1 4 2 0 0 0 0 Cupressacites hiatipites 0 14 0 3 0 0 13 0 0 Cupuliferipollenites sp. 0 10 2 9 0 0 0 0 0 Cyathidites minor 0 6 2 0 0 0 9 0 0 Cycadopites giganteus 0 8 1 0 0 0 13 0 0 Cycadopites scabratus 0 0 0 2 2 0 0 0 0 Cyrillaceaepollenites ventosus 0 0 0 4 0 0 0 0 0 Deltoidospora sp. 0 11 0 0 0 0 0 0 0 Deltoidospora concave 0 2 0 0 0 0 0 0 0 Diporopollenites sp. Type B 0 5 0 0 0 0 0 0 0 168

Diporopollenites sp. Type C 0 5 0 0 0 0 0 0 0 Diporicellaesporites sp. 0 0 1 0 0 0 0 0 0 Endoinfundibulapollis sp. 0 3 0 0 0 0 0 0 0 Ephedra sp. 0 0 0 0 5 0 0 0 0 Ephedra claricristata 0 0 3 0 18 0 0 0 0 Ephedra exiguua 0 0 3 0 2 0 0 0 0 Ephedripites sp. 0 0 1 0 0 0 7 0 0 Erdmanipollis cretaceous 0 0 1 0 0 0 0 0 0 Ericipites redbluffensis 0 0 1 0 5 0 0 0 0 Eucommia sp. 0 0 0 0 0 0 3 0 0 Extemipollis sp. 0 45 0 0 0 0 0 0 0 Extremipollis caminus 0 60 0 0 0 0 0 0 0 Extremipollis sp. 0 x 0 0 0 0 0 0 0 Extremipollis versatilis 0 70 0 0 0 0 0 0 0 Extremipollis vivus 0 5 0 0 0 0 0 0 0 Faguspollenites sp. 0 1 0 0 0 0 0 0 0 Favitricolporites sp. 0 3 0 5 3 8 2 0 0 Foveosporites triangulus 0 3 0 0 0 0 0 0 0 Foveosporites sp. 0 0 3 0 0 0 0 0 0 Fraxinoipollenites sp. 0 0 10 0 0 0 0 0 0 Fraxinoipollenites medius 0 0 0 0 4 0 0 0 0 fungal spore 0 11 2 0 0 0 0 0 0 Gleicheniidites sp. 0 2 5 4 0 0 0 0 0 Gleichenia sp. 0 0 0 1 0 0 0 0 0 Gleichenia triangular 0 29 0 2 0 0 0 0 0 Graminidites sp. 0 9 2 18 9 2 13 0 0 Graminidites gramineoides 0 0 0 0 4 0 13 0 0 Holkopollenites sp. A 0 47 0 0 0 0 0 0 0 Horniella sp. 4 1 0 13 0 0 0 0 0 Inaperturopollenites sp. 0 3 3 0 0 0 0 0 0 Type B Insulapollenites rugulatus 0 0 0 0 0 0 3 0 0 Intratriporopollenites crass. 0 0 0 0 2 0 0 0 0 Jarzenipollenites trinus 0 0 0 2 4 0 0 0 0 Juglans sp. 0 3 0 0 0 0 0 0 0 Juglans nigripites 0 0 1 0 0 0 0 0 0 Kyandopollenites sp. 0 0 6 0 0 0 0 0 0 Laevigatosporites sp. 0 59 7 2 4 7 0 0 0 Laevigatosporites haardti 0 0 0 0 0 5 0 0 0 Lanagiopollis cribellata 0 0 3 3 0 0 0 0 0 Leiotriletes pseudomaximus 0 0 1 0 0 0 0 0 0 Libopollis jarzenii 0 0 0 0 3 0 3 0 0 Liliacidites sp. 0 0 4 0 0 0 0 0 0 Liliacidites complexus 0 0 0 6 0 0 0 0 0 Liliacidites inaequalis 0 0 0 0 0 2 0 0 0 Liliacidites intermedius 0 0 3 0 0 0 0 0 0 Liliacidites tritus 0 0 0 0 0 10 0 0 0 Liliacidites vittatus 0 0 2 0 18 0 0 0 0 Longapertites sp. 0 0 0 0 10 0 0 0 0 Lycoperdon sp. 0 0 2 0 0 0 0 0 0 169

Lycopodium sp. 0 0 0 2 0 0 0 0 0 Lygodiumsporites adriennis 0 0 0 0 0 0 3 0 0 Milfordia incerta 0 0 0 2 0 3 5 0 0 Milfordia minima 0 0 0 0 5 0 0 0 0 Momipites sp. 0 7 5 4 14 0 0 0 0 Momipites coryloides 0 2 0 0 0 0 8 0 0 Momipites dilates 0 1 0 0 0 0 0 0 0 Momipites fragilis 0 4 0 0 0 0 0 0 0 Momipites inaequalis 0 0 3 0 3 0 0 0 0 Momipites marylandicus 0 0 0 0 3 0 0 0 0 Momipites microfovelolatus 0 6 3 0 0 0 6 0 0 Momipites strictus 0 0 0 0 5 0 0 0 0 Momipites tenuipolus 0 4 0 0 0 0 0 0 0 Monocolpopollenites sp . 0 0 9 0 0 0 0 0 0 Monoporisporites singularis 0 0 3 5 0 0 0 0 0 Myocolpopollenites reticulates 0 1 2 0 0 0 4 0 0 Myricipites annulites 0 13 0 0 0 0 0 0 0 Myriophyllum sp. 0 0 0 7 2 0 0 0 0 Nudopollis sp. 0 3 0 0 0 0 0 0 0 Nudopollis terminalis 0 0 0 0 9 0 0 0 0 Nyssapollenites explanata 0 1 0 0 2 8 0 0 0 Nyssapollenites paleocenicus 0 3 0 0 0 0 0 0 0 Nyssapollenites pulvinus 0 0 0 0 0 0 4 0 0 Osculapollis sp. 0 0 1 0 0 0 7 0 0 Osmundacidites stanleyi 0 0 0 0 3 0 4 0 0 Palaeoisoetes subengelmannii 1 0 0 3 0 0 4 0 0 Pediastrum boryanum 0 0 0 0 2 0 0 0 0 Pinus sp. 0 0 3 0 4 0 0 0 0 Pinus semicircularis 0 0 X 0 0 0 0 0 0 Pinus strobipites 0 0 X 0 0 0 0 0 0 Pistillipollenites mcgregorii 0 11 8 0 0 0 2 0 0 Platacarya sp. 2 1 0 39 29 0 4 0 0 Platanus sp. 0 0 0 1 0 0 0 0 0 Platanus occidentaloides 0 0 0 0 3 0 0 0 0 Plicapollis retusus 0 2 0 0 0 0 0 0 0 Plicapollis usitatus 0 3 0 0 0 0 0 0 0 Plicatopollis sp. 0 7 0 0 2 3 1 0 0 Plicatopollis magniorbicularis 0 0 0 0 3 0 0 0 0 Polyatriopollenites stellatus 0 0 0 0 3 0 0 0 0 Polygala sp . 0 0 0 1 0 0 0 0 0 Polypodiaceoisporites sp . 0 0 0 0 0 0 0 0 0 Polyvestibulopollenites verus 0 0 2 0 0 0 0 0 0 Porosipollis porosus 0 0 2 0 0 0 0 0 0 Proteacidites sp. 0 1 0 0 0 0 0 0 0 Proteacidites retusus 0 0 0 0 0 0 0 0 0 Pseudoculopollis admirabillis 0 11 0 0 0 0 6 0 0 Pseudoplicapollis sp. 0 2 0 0 0 0 0 0 0 Pseudolplicapollis serenus 0 0 2 0 0 0 0 0 0 Pseudovacuopollis involutus 0 6 0 0 0 0 0 0 0 170

Quercoidites sp. 0 1 2 0 4 0 0 0 0 Quercoidites inamoenus 0 0 0 0 4 0 0 0 0 Quercoidites microhenricii 0 0 2 0 0 0 0 0 0 Retibrevitricolpites sp. 0 0 0 0 2 0 0 0 0 Reticuloidosporites pseudo. 0 0 0 0 3 0 0 0 0 Retitricolpites virgins 0 7 0 0 0 0 0 0 0 Retitriletes sp. 0 0 3 5 5 20 5 0 0 Rhoipites sp. 9 2 0 22 0 0 0 0 0 Rhoipites latus 7 0 0 0 0 0 4 0 0 Rhoipites pisinnus 0 4 3 0 5 0 0 0 0 Rhopites subprolatus 0 0 0 2 0 0 0 0 0 Rousea linguiflumena 0 0 0 0 5 0 0 0 0 Rousea monilifera 0 0 0 2 0 0 0 0 0 Salixipollenites parvus 0 4 0 12 0 0 0 0 0 Schizosporis cookonii 0 0 4 0 0 0 0 0 0 Semioculopollis sp. 0 14 0 0 0 0 3 0 0 Sequoia sempervirens 0 0 0 0 0 11 2 0 0 Sphagnum sp. 0 1 2 1 0 0 0 0 0 Spirogyra sp. 0 0 0 0 0 0 3 0 0 Stereisporites antiquasporites 0 2 0 0 0 0 0 0 0 Stereisporites sp. 0 0 0 0 0 0 0 0 0 Stereisporites stereoides 0 0 2 0 3 0 5 0 0 Striatotheca triangulate 0 0 0 2 2 0 2 0 0 Subtriporopollenites nanus 0 0 0 0 2 9 3 0 0 Syncolporites sp. 0 0 0 0 5 0 0 0 0 Syncolporites rugulosus 0 0 1 0 2 0 0 0 0 Taxodiaceaepollenites hiatus 0 9 0 3 13 0 6 0 0 Thecaphora sp. 0 0 0 0 0 18 0 0 0 Thomsoniopollis sp. 0 2 2 0 0 0 0 0 0 Tilia instructa 0 0 0 0 10 0 0 0 0 Todisporites minor 0 11 0 0 0 0 0 0 0 Toroisporites major 0 0 0 0 0 0 4 0 0 Toroisporites sp. 0 0 0 0 0 0 x 0 0 Triatriopollenites paradoxus 0 0 2 0 13 0 0 0 0 Tricolpites sp. 0 1 0 0 3 0 0 0 0 Tricolpites hians 0 0 0 2 0 0 0 0 0 Tricolpopollenites sp. 0 0 16 0 4 0 0 0 0 Triplanosporites sp. 0 0 0 7 0 0 0 0 0 Triplanosporites sinuosus 0 35 0 3 0 0 0 0 0 Triporopollenites sp. 0 0 0 0 4 0 0 0 0 Triporopollenites maternus 0 0 3 0 0 0 0 0 0 Trudopollis sp. 0 1 0 0 0 0 0 0 0 Trudopollis plenus 0 3 0 0 0 0 0 0 0 Trudopollis variabilis 0 7 0 0 0 0 0 0 0 Tschudypollis retusus 0 0 0 0 0 0 3 0 0 Ulmipollenites undulosus 0 0 0 0 3 0 0 0 0 Vacuopollis munitus 0 7 0 0 0 0 0 0 0 Total 23 770 226 340 428 187 229 0 0

171

Quantitative Data: BH-9.

Depth (m) 16.4 m 17.3 m 18.1 m 18.4 m 19.5 m 21.0 m 22.5 m 23.7 m 30.1 m Core-Section (interval) B-9563 B-9564 B-9565 B-9570 B-9562 B-9570 B-9566 B-9571 B-9560 Sample # SC14 SC16 SC17 SC18 SC19 SC21 SC23 SC25 SC27 Acer Striatellum 0 0 0 0 0 0 10 0 0 Ailanthipites marginatus 0 0 5 0 0 0 0 0 0 Arecipites sp. 0 17 14 28 25 0 0 1 0 Arecipites rousei 0 0 0 0 6 0 0 0 0 Basopollis 0 3 0 17 10 0 4 0 0 obscurocostatus Bisaccates 0 0 4 4 0 0 0 0 0 Botryococcus sp . 0 0 0 0 0 0 0 1 0 Catinipollis geiseltalensis 0 0 0 x 0 0 0 0 0 Chenopodipollis 0 0 0 0 0 0 0 7 0 nuktakensis Compositoipollenites 0 0 0 0 13 0 0 0 0 grandiannulatus Confertisulcites fusiformis 0 0 0 0 0 0 2 0 0 Cupressacites hiatipites 0 0 23 15 19 0 15 5 0 Cupuliferoipollenites sp. 0 0 0 0 0 0 3 0 0 Deltoidospora sp. 0 0 4 0 0 0 2 0 0 Engelhardtia 0 4 0 0 0 0 0 0 0 microvoveolata Extremipollis caminus 0 0 15 0 0 0 0 0 0 Extremipollis versatilis 0 2 0 0 0 0 0 0 0 Extremipollis vivus 0 0 0 0 3 0 13 0 0 Favitricolporites sp. 0 0 4 0 0 0 0 0 0 Fraxinoipollenites sp. 0 0 6 0 5 0 9 0 0 Fungi 0 0 0 0 0 1 0 0 0 Gleicheniidites sp. 0 0 0 0 0 1 0 1 0 Gleicheniidites senonicus 0 0 0 4 0 0 0 0 0 Gleichenia sp. 0 1 0 0 0 0 0 0 0 Gleichenia triangular 0 0 4 9 7 0 5 0 0 Graminidites sp. 0 0 0 0 0 0 0 1 0 Inaperturopollenites sp. 0 0 0 0 0 0 0 0 2 Type A Interporopollenites 0 0 0 0 0 0 3 0 0 turgidus Laevigatosporites haardti 0 0 0 0 4 0 0 0 0 Laevigatosporites 0 1 0 0 0 0 0 0 0 pseudomaximus Lanagiopollis cribellata 0 2 0 0 0 0 0 0 0 Liliacidites sp. 0 0 0 9 0 0 0 0 0 Lycopodium hamulatum 0 0 0 0 0 0 0 0 1 Momipites sp. 0 0 0 0 0 0 4 0 0 Momipites coryloides 0 0 0 11 5 0 10 0 2 Momipites dilatus 0 0 0 0 12 0 0 0 0 Momipites 0 1 20 0 10 0 0 0 0 microfovelolatus Monocolpopollenites sp. 0 3 0 0 0 0 0 0 0 Nudopollis sp. 0 0 0 19 0 0 0 0 0 Nudopollis endangulatus 0 0 7 0 1. 0 0 12 2 0 Nudopollis terminalis 0 0 3 0 19 0 3 0 0 172

Platacarya sp. 0 0 0 13 0 0 0 0 0 Platanus occidentaloides 0 0 2 0 0 0 0 0 0 Plicapollis retusus 0 0 0 8 0 0 0 0 0 Proteacidites retusus 0 0 0 7 0 0 0 0 0 Pseudoculopollis 0 0 0 0 0 3 0 10 0 admirabillis Pseudoplicapollis serenus 0 0 0 0 0 0 8 0 0 Rhoipites sp. 0 0 8 0 5 0 0 0 0 Schizosporis parvus 0 0 0 2 0 0 0 0 0 Semioculopollis sp. 0 5 0 0 0 0 0 7 0 Sphagnum sp. 0 0 0 0 0 3 0 0 0 Sphagnum australe 0 0 0 0 11 0 0 0 0 Taxodiaceaepollenites 0 4 9 10 3 0 4 1 0 hiatus Thomsoniopollis sp. 0 0 0 0 0 0 12 0 0 Toroisporites major 0 0 0 0 0 0 2 0 0 Triporopollenites sp. 0 0 12 5 0 0 0 0 0 Trudopollis sp. 0 2 0 0 0 0 0 0 0 Total 0 45 140 161 157 8 121 36 5

173

Quantitative Data: BH-10.

Depth (m) 13.5 14.3 15.4 15.8 16.7 19.8 21.3 22.8 25.9 32.0 33.5 34.1 34.4 B- B- B- B- B- B- B- B- B- B- B- B- B- Core-Section (Interval) 9572 9573 9574 9575 9567 9576 9577 9561 9578 9579 9597 9598 9599 SC22 Sample # SC10 SC11 SC12 SC13 SC15 SC20 SC24 SC26 SC28 SC29 SC30 SC31

Alnus trina 0 0 0 0 0 0 0 0 0 0 0 0 2 Arecipites sp. 0 14 15 0 13 20 8 8 8 0 0 0 2 Basopollis obscuroco. 0 0 0 0 0 0 2 0 8 0 0 0 0 Betula infrequens 0 0 0 0 0 0 5 0 0 0 0 0 0 Bisaccates 14 5 6 0 0 11 0 0 9 0 0 0 0 Bombacadites sp. 0 0 0 0 0 0 0 0 5 0 0 0 0 Botryococcus sp. 0 1 0 0 1 4 0 0 0 0 0 0 0 Catinipollis geiseltalensis 0 0 0 0 0 0 0 0 5 0 0 0 0 Chenopodipollis sp. 0 3 12 0 4 0 0 0 0 0 0 0 0 Cingulatisporites 0 0 0 0 0 0 4 0 0 0 0 0 0 dakotaensis Cingulatisporites 0 0 0 0 4 3 0 0 0 0 0 0 0 radiates Corollina 0 0 0 0 0 10 0 0 0 0 0 0 0 (Classopollis ) sp. Cupressacites hiatipites 6 5 9 0 0 12 10 7 9 0 0 0 2 Cycadopites giganteus 0 0 0 0 0 0 5 0 0 0 0 0 2 Cycadopites scabratus 0 0 0 0 0 0 0 9 0 0 0 0 0 Diporopollenites sp. 0 0 0 0 3 0 0 0 0 0 0 0 0 Type A Engelhardtia sp. 0 0 4 0 0 0 0 0 0 0 0 0 0 Extemipollis sp. 0 0 0 0 0 3 0 0 37 0 0 0 0 Extremipollis caminus 0 0 0 0 0 0 0 0 0 0 0 0 3 Foveosporites triangulus 0 0 0 0 0 0 3 0 0 0 0 0 0 Fraxinoipollenites sp. 0 0 0 0 0 0 4 0 0 0 0 0 0 fungal spore 2 0 0 0 0 0 0 0 0 0 0 0 0 Fungi 0 0 3 0 4 0 1 0 0 0 0 0 0 Gleicheniidites sp. 0 0 0 0 0 6 0 0 6 0 0 0 0 Gleichenia triangular 0 0 0 0 0 9 0 0 1 0 0 0 2 Graminidites sp. 14 4 17 0 64 10 6 0 0 0 0 0 0 Horniella sp. 0 0 0 0 0 0 0 0 0 0 0 0 4 Lanagiopollis sp. 0 0 0 0 0 0 3 0 0 0 0 0 0 Leiotriletes pseudomax. 0 0 0 0 0 0 0 0 0 0 0 0 0 Leptolepidites tenuis 0 0 6 0 0 3 0 0 0 0 0 0 0 Momipites sp. 0 0 0 0 0 0 14 0 0 0 0 0 0 Momipites coryloides 0 0 0 0 0 9 6 0 0 0 0 0 0 Momipites 0 0 0 0 0 0 6 0 4 0 0 0 0 microfovelolatus Nudopollis terminalis 0 0 0 0 0 9 0 0 5 0 0 0 0 Palaeoisoetes 0 0 0 0 4 0 0 0 0 0 0 0 0 subengelmannii Pinus cembraeformis 0 0 0 0 0 0 x 0 0 0 0 0 0 Pinus semicircularis 0 0 0 0 0 0 x 0 0 0 0 0 0 Plicapollis usitatus 0 0 0 0 0 0 0 0 0 0 0 0 3 Polypodiaceoisporites 0 0 0 0 3 0 0 0 0 0 0 0 0 sp. 174

Proteacidites retusus 0 0 0 0 0 0 10 0 0 0 0 0 0 Quercoidites sp. 10 0 10 0 0 0 0 0 0 0 0 0 0 Rhoipites sp . 0 0 0 0 0 0 12 1 0 0 0 0 0 Schizosporis cookonii 0 0 0 0 0 0 8 0 0 0 0 0 0 Selaginella perinata 0 1 0 0 0 0 0 0 0 0 0 0 0 Sphagnum sp. 0 0 0 0 0 0 0 0 2 0 0 0 0 Sphagnum regium 0 0 0 0 0 7 0 8 3 0 0 0 0 Stereisporites stereoides 0 0 0 0 0 10 0 0 0 0 0 0 0 Taxodiaceaepollenites 0 0 0 0 11 6 0 0 0 0 0 0 0 hiatus Thomsoniopollis sp. 0 0 0 0 0 0 0 0 9 0 0 0 0 Toroisporites major 0 0 0 0 0 0 0 0 7 0 0 0 0 Tricolpites sp. 0 0 0 0 0 4 2 0 0 0 0 0 0 Tricolpites 0 0 0 0 0 5 0 0 0 0 0 0 0 bathyreticulatus Undulatisporites 6 0 0 0 0 0 0 0 0 0 0 0 0 concavus Vitis affluens 0 0 0 0 0 0 3 0 0 0 0 0 0 Total 52 33 82 0 111 141 112 33 118 0 0 0 20

175

APPENDIX C.

QUANTITATIVE PALYNOMORPH DATA FOR TRENCH 1 IN STODDARD

COUNTY, MISSOURI: NONMARINE PALYNOMORPHS

176

Quantitative Data: Trench 1.

Depth (cm) 180 160 140 110 110 75 75 60 50 20 0

R-1393- B- B- B- R-1393- R-1393- B- B- B- R-1393- B- Core-Section, Interval 22/COR 9568 9583 9580 25/COR 24/COR 9600 9582 9581 23/COR 9584

Sample # ST01 ST02 ST03 ST04 ST05 ST06 ST07 ST08 ST09 ST10 ST11

Ailanthipites marginatus 0 0 0 0 0 0 0 0 0 4 0 Alnus trina 0 0 0 0 0 2 0 0 0 0 0 Annutriporites tripollenites 0 0 0 0 0 4 0 0 0 0 0 Aquilapollenites murus 0 0 0 0 0 0 0 0 0 1 0 Araliaceoipollenites 0 0 0 0 0 0 0 0 0 1 0 profoundus Arecipites sp . 1 5 20 17 25 27 0 41 0 30 12 Arecipites columellus 0 0 0 0 0 18 0 4 0 0 0 Arecipites rousei 0 0 0 0 0 0 0 0 0 0 13 Aster sp. 0 0 0 0 0 0 0 0 0 6 0 Baculatisporites sp . 0 0 0 0 0 13 0 0 0 0 0 Basopollis sp . 0 0 0 0 0 0 0 0 0 2 0 Basopollis 0 0 0 0 0 0 0 3 0 0 0 obscurocostatus Betula infrequens 0 0 0 0 0 0 0 0 3 0 0 Bisaccates 0 0 0 0 0 9 3 0 0 6 5 Bombacadites reticulatus 0 0 0 0 0 0 0 0 0 2 0 Botryococcus sp. 0 0 0 0 0 8 0 0 0 0 6 Caprifoliipites longus 0 0 0 0 0 0 0 0 0 1 0 Cardioangulina diaphana 0 0 3 0 0 0 0 0 0 0 0 Carya paleocenica 0 0 0 3 0 0 0 0 6 1 0 Casauarinidites sp. 0 0 0 0 0 0 0 0 0 2 8 Catinipollis geiseltalensis 0 0 0 0 0 0 0 4 0 0 0 Chenopodipollis sp. 0 3 0 0 0 0 0 0 0 0 3 Chenopodipollis 1 0 0 0 0 0 0 0 0 3 0 nuktakensis Cicatricosisporites sp. 0 0 0 0 0 2 3 4 0 0 0 Cingulatisporites 0 0 12 0 0 0 0 0 8 0 0 dakotaensis Corollina 0 0 0 0 0 0 0 0 6 0 0 (Classopollis) sp. Compostioipollenites sp . 0 0 6 0 0 7 0 0 0 0 6 Corylus sp. 0 0 0 0 0 0 0 9 6 0 0 Corylus granilabrata 0 0 0 0 0 0 0 0 6 0 0 Cupanieidites speciosus 0 0 0 0 0 0 0 0 0 11 0 Cupressacites hiatipites 0 7 12 0 20 11 10 36 0 12 0 Cyathidites minor 0 0 0 0 0 7 0 0 0 0 0 Cycadopites sp. 0 0 0 0 0 3 0 0 0 0 0 Cycadopites scabratus 0 3 0 0 0 0 0 0 0 0 0 Deltoidospora sp. 0 0 0 0 0 1 0 0 0 0 0 Ephredra volute 0 0 2 0 1 0 0 3 0 0 0 Ephedripites sp. 0 0 0 0 4 0 0 0 0 3 4 Ericipites redbluffensis 8 0 0 0 0 4 0 0 0 0 0 177

Extremipollis caminus 0 0 0 0 0 0 0 0 0 0 4 Extremipollis versatilis 0 0 0 0 0 0 0 0 0 4 0 Favitricolporites sp. 0 0 0 0 0 7 0 0 0 11 0 Foveosporites triangulus 0 0 0 0 0 0 0 8 0 0 0 Fraxinoipollenites sp. 5 0 2 0 0 9 4 14 0 0 0 Fraxinoipollenites 4 2 0 0 0 0 0 0 0 0 0 variabillis Fungal spore 0 0 0 0 0 0 0 0 0 3 0 Gleicheniidites senonicus 0 0 0 0 0 0 0 0 0 0 7 Gleichenia sp. 0 0 0 0 5 3 0 0 0 0 0 Gleichenia circinidites 0 0 0 0 0 0 0 5 0 0 0 Gleichenia triangular 0 1 6 0 0 10 4 21 0 14 0 Graminidites sp . 0 0 23 0 0 13 0 0 0 24 6 Hamulatisporis hamulatis 0 0 0 0 0 x 0 0 0 0 0 Holkopollenites sp . A 0 0 0 0 0 4 0 0 0 0 1 Horniella sp. 0 0 0 0 0 0 0 0 0 9 5 Inaperturopollenites sp . 0 1 0 0 0 5 0 5 0 5 0 Type A Inaperturopollenites sp . 0 0 0 0 0 21 0 0 0 0 10 Type C Interporopollenites 0 0 0 0 0 0 0 0 0 5 0 turgidus Intratriporopollenites 0 0 0 0 0 0 0 5 0 0 0 crassipites Kyandopollenites sp. 0 0 0 0 28 0 0 0 0 0 0 Laevigatosporites haardti 0 0 0 0 0 0 0 4 0 0 0 Leptolepidites tenuis 0 0 0 0 0 0 0 10 0 0 0 Liliacidites dividuus 0 0 0 0 0 9 0 0 0 0 0 Lycopodium heskemensis 0 0 0 0 0 0 0 0 0 0 6 Maceopolipollenites 0 0 0 0 0 0 0 0 0 0 3 amplus Microreticulatisporites sp . 0 0 0 0 3 0 0 0 0 0 0 Momipites sp . 0 0 5 0 2 5 0 0 0 11 0 Momipites coryloides 0 0 0 0 2 17 0 0 0 3 0 Momipites 0 0 8 0 0 0 8 8 0 0 0 microfovelolatus Monoporisporites 1 0 0 0 0 0 0 0 0 9 0 singularis Monoporisporites 0 0 0 0 0 0 0 5 0 0 0 globusus Myricipites annulites 0 0 0 0 0 0 10 0 0 0 0 Nudopollis terminalis 0 0 0 0 0 4 0 3 0 0 11 Nyssapollenites 0 0 0 0 0 0 4 0 0 0 0 albertensis Nyssapollenites pulvinus 0 0 0 0 0 0 0 0 0 3 0 Osmunda comaumensis 0 0 10 0 0 0 0 0 0 0 0 Platacarya sp. 8 0 0 0 13 0 6 0 0 53 0 Plicapollis sp. 0 0 0 0 0 0 0 0 0 4 0 Nudopollis terminalis 0 0 0 0 1 0 0 0 0 0 0 Plicatopollis 0 0 0 0 0 0 0 0 0 5 0 magniorbicularis Proteacidites retusus 0 0 3 0 0 0 0 0 0 0 0 Pseudoplicapollis 0 2 0 0 0 0 0 0 0 0 0 serenus Quercoidites sp. 0 0 0 0 0 5 0 4 0 0 0 Rhoipites sp . 0 0 0 0 0 3 0 13 0 0 0 178

Rhoipites pisinnus 12 0 0 0 0 0 0 0 0 0 0 Schizosporis cookonii 0 0 0 0 0 0 0 0 0 0 5 Sequoia sempervirens 1 0 0 0 0 0 0 0 0 1 0 Sphagnum sp. 0 3 0 0 0 0 0 8 0 0 0 Sphagnum regium 0 0 0 0 0 0 3 5 0 0 0 Sphagnum triangularum 0 0 0 0 0 0 0 0 0 3 0 Spirogyra sp . 0 0 0 0 0 0 0 0 0 3 0 Taxodiaceaepollenites 0 0 0 0 2 4 0 0 0 27 0 hiatus Thecaphora sp . 0 0 0 0 0 0 0 0 0 0 3 Todisporites sp. 0 0 0 0 0 1 0 0 0 0 0 Toroisporites major 0 0 0 0 0 1 0 17 0 0 0 Triatriopollenites proprius 0 0 0 0 0 1 0 0 0 11 15 Tricolpites sp. 0 0 0 0 0 5 0 5 0 0 0 Tricolpites 0 0 0 0 0 0 0 0 0 3 0 bathyreticulatus Tricolpites erugatus 0 0 0 0 3 0 0 0 0 0 0 Tricolpites hians 0 0 0 0 0 0 0 0 0 3 0 Tricolpites parvus 0 0 0 0 0 0 3 0 0 0 0 Tricolpopollenites sp. 0 0 0 0 0 3 0 0 0 0 0 Triporopollenites sp. 0 0 0 0 0 0 0 0 0 7 18 Unidentified monolete 0 2 0 0 0 0 0 3 0 0 0 Vacuopollis munitus 0 0 0 0 0 0 0 0 0 0 5 Total 41 29 112 20 109 246 58 265 35 306 156

179

APPENDIX D.

QUANTITATIVE PALYNOMORPH DATA FOR CORE CUTTINGS

IN NEW MADRID COUNTY, MISSOURI: NONMARINE PALYNOMORPHS

180

Quantitative Data: Core cuttings.

Depth (m) 1417 1433' 1544 1646 1672'5 1698'5

Core Section (interval) 1417 1433- 1544' 1646' 1672'5" 1698.5 1435'

Sample # NM01 NM02 NM03 NM04 NM05 NM06

Acer striatellum 4 0 4 0 0 0 Ailanthipites marginatus 0 0 0 0 0 0 Alnus trina 4 0 0 0 0 0 Alsophilidites kerguelensis 0 0 6 3 0 0 Anemia tricornitata 0 0 0 0 0 0 Appendicisporites tricornatus 0 0 4 18 0 0 Arecipites sp. 25 7 6 0 15 19 Arecipites rousei 0 0 0 0 0 0 Baculatisporites sp. 5 0 7 10 0 0 Basopollis obscurocostatus 0 4 11 10 0 2 Betulaceoipollenites sp. 4 0 0 0 0 0 Bisaccates 12 0 0 0 0 7 Boehlensipollis sp. 0 0 0 0 0 0 Boehlensipollis hohlii 0 0 8 0 0 0 Bombacadites sp. 7 0 0 0 0 0 Bombacadites reticulates 0 0 4 0 0 0 Botryococcus sp. 10 4 0 5 4 0 Cardioangulina diaphana 5 0 0 0 0 3 Carpinus subtriangula 0 0 0 0 0 4 Caryapollenites simplex 3 0 0 0 0 0 Caryapollenites imparalis 3 0 0 0 0 8 Caryapollenites veripites 4 0 0 0 0 0 Casauarinidites sp. 5 4 0 0 0 22 Catinipollis geiseltalensis 0 0 0 0 0 0 Chenopodipollis sp. 22 0 0 11 0 3 Chenopodipollis nuktakensis 0 0 0 0 0 0 Cicatricosisporites sp. 2 0 8 0 4 4 Cingulatisporites dakotaensis 2 0 0 0 0 9 Corollina (Classopollis ) sp. 2 0 0 0 0 7 Corylus granilabrata 0 0 5 0 0 0 Cupanieidites speciosus 0 0 0 5 0 0 Cupressacites hiatipites 46 13 10 8 5 28 Cupuliferoipollenites sp . 12 0 0 0 0 0 Cycadopites sp. 0 0 0 5 0 0 Cycadopites scabratus 17 0 12 10 0 27 Cyrillaceaepollenites ventosus 9 0 0 0 0 0 Deltoidospora sp. 2 0 0 0 0 0 Diporopollenites sp. Type A 0 0 0 0 0 4 Emmapollis sp. 13 0 11 12 0 0 Engelhardtia sp. 7 0 0 0 0 0 Engelhardtia microvoveolata 3 0 11 0 10 6 Ephedra sp. 3 0 0 0 3 9 181

Ephedra claricristata 2 0 0 0 0 0 Ephedra volute 2 0 13 0 0 0 Ephedripites sp. 0 0 0 0 0 7 Ericipites redbluffensis 0 0 0 0 0 2 Eucommia sp. 0 0 0 5 0 0 Extremipollis sp. 5 0 0 0 0 0 Extremipollis caminus 0 0 0 0 0 0 Extremipollis versatilis 0 0 0 0 0 0 Extremipollis vivus 0 0 0 0 0 0 Favitricolporites sp. 20 0 0 8 4 14 Foveosporis triangulus 4 0 4 0 0 0 Fraxinoipollenites sp. 7 0 0 0 0 0 Fraxinoipollenites variabillis 2 0 0 0 0 4 Fungi 0 0 0 0 0 0 Gleicheniidites sp. 5 0 0 4 0 7 Gleicheniidites senonicus 0 0 0 0 0 0 Gleichenia circinidites 0 5 0 0 0 0 Gleichenia sp. 5 0 0 0 0 0 Gleichenia triangular 20 8 0 3 7 25 Gothanipollis cockfieldensis 1 0 0 0 0 0 Graminidites sp. 0 0 0 0 0 0 Holkopollenites sp. A 8 0 0 0 0 0 Horniella sp. 0 0 0 0 0 11 Inaperturopollenites sp. Type A 0 0 7 0 0 0 Inaperturopollenites sp. Type C 0 0 0 0 0 0 Inaperturopollenites sp. Type D 0 0 0 0 0 4 Interpollis sp. 0 0 6 0 0 0 Interporopollenites turgidus 0 0 0 0 0 0 Intratriporopollenites sp. 6 0 0 0 0 0 Kyandopollenites sp. 3 0 0 0 0 0 Laevigatosporites sp. 0 0 4 0 0 7 Laevigatosporites haardti 5 7 0 0 0 0 Laevigatisporites pseudomaximus 0 0 0 0 0 0 Lanagiopollis sp. 0 0 0 4 0 0 Lanagiopollis cribellata 0 0 0 0 0 0 Laricoidites magnus 0 6 0 0 0 0 Leptolepidites tenuis 12 0 0 0 4 0 Liliacidites sp. 4 0 0 0 0 0 Lycopodium hamulatum 0 0 0 0 0 0 Lygodiumsporites adriennis 2 0 0 0 0 0 Momipites sp. 16 0 0 0 0 0 Momipites coryloides 7 0 0 12 0 0 Momipites dilates 0 0 0 0 0 0 Momipites inaequalis 5 0 0 0 0 0 Momipites microfovelolatus 16 4 2 0 0 5 Monocolpopollenites sp. 0 0 0 0 0 0 Monoporisporites globusus 2 0 0 0 0 0 Myricipites annulites 0 5 4 2 0 0 Myriophyllum sp. 0 0 0 3 0 0 182

Nudopollis sp. 0 0 0 3 0 4 Nudopollis endangulatus 0 0 0 0 0 0 Nudopollis terminalis 0 3 0 0 0 0 Nyssapollenites explanata 6 0 0 0 0 3 Osmunda comaumensis 7 0 0 4 0 0 Ovoidites ligneolus 0 0 3 0 0 0 Ovoidites microligneolus 0 0 0 0 0 0 Palaeoisoetes subengelmannii 4 0 0 0 0 0 Pinus scopulipites x 0 0 0 0 0 Pistillipollenites mcgregorii 0 0 0 0 5 0 Platacarya sp. 0 0 0 0 0 24 Platanus occidentaloides 0 0 0 0 0 0 Plicapollis retusus 0 6 0 0 0 0 Plicatopollis sp. 10 0 0 0 5 0 Polycolpites sp. 6 1 0 0 0 0 Proteacidites retusus 6 0 7 0 5 0 Pseudotricolpites sp. 8 0 0 7 0 0 Pseudoculopollis admirabillis 0 0 0 0 0 0 Pseudolplicapollis serenus 0 7 0 0 0 10 Pseudovacuopollis involutus 0 0 0 0 0 3 Quercoidites sp. 2 13 14 3 0 0 Quercoidites genustriatus 0 0 4 0 0 0 Retibrevitricolpites sp. 0 0 0 0 0 3 Rhoipites sp. 27 0 0 0 7 0 Rhoipites globosus 0 0 4 27 0 8 Rhoipites latus 4 0 0 0 0 0 Rhoipites pisinnus 22 13 9 7 7 0 Salixipollenites parvus 0 0 16 0 0 40 Schizosporis cookonii 5 0 0 0 0 0 Schizaeoisporites sp. 0 0 0 4 0 0 Schizaeoisporites eocaenicus 0 2 0 0 0 0 Schizosporis laevigatus 2 4 0 0 0 0 Schizosporis parvus 5 0 0 0 0 0 Selaginella perinata 3 0 0 0 0 0 Sequoiapollenites paleocenicus 18 0 0 0 0 0 Sphagnum sp. 2 0 0 0 4 0 Sphagnum austral 0 0 0 0 0 0 Sphagnum regium 2 7 0 0 0 0 Stereisporites antiquasporites 0 0 0 0 8 0 Striopollenites terasmaei 2 0 0 0 0 0 Subtriporopollenites nanus 0 0 0 0 0 5 Syncolporites sp. 0 0 0 0 0 7 Syncolporites lisamae 1 0 0 0 0 0 Taxodiaceaepollenites hiatus 9 8 0 10 0 3 Thomsoniopollis sp. 4 5 0 0 18 0 Toroisporis major 0 0 0 7 0 6 Tricolpites sp . A (very large) 2 0 0 0 0 0 Tricolpites sp. B (very large) 0 0 0 0 0 2 Tricolpites parvus 0 0 0 0 0 3 183

Tricolpites splendens 0 0 8 0 0 0 Triporopollenites sp. 5 0 0 0 0 0 Triporopollenites? Maternus 2 0 0 0 0 0 Vitis affluens 0 0 0 9 0 0 Total 554 136 212 219 110 369

184

APPENDIX E.

QUANTITATIVE PALYNOMORPH DATA FOR BH-1, BH-9, AND BH-10 IN

SCOTT COUNTY, MISSOURI: DINOFLAGELLATGES AND OTHER MARINE

PALYNOMORPHS

185

Quantitative Data: BH-1.

Depth (m) 7.31 7.62 9.45 11.9 14 17.2 18.1 18.3 18.8

Core-Section (Interval) R- R- R- R- R-1393- R-1470 R-1470- R-1470- R-1393- 1393- 1393- 1393- 1470- 3/COR -3/COR 2/COR 4/COR 4/COR 1/COR 14/COR 2/COR 1/COR

Sample # SC01 SC02 SC03 SC04 SC05 SC06 SC07 SC08 SC09

Acritarchs 0 0 10 0 0 0 3 0 0 Carpodinium granulatum 0 0 0 0 0 0 6 0 0 Cerodinium sp . A 0 0 0 0 0 0 0 0 0 Cleistosphaeridium 0 0 0 0 2 0 0 0 0 insolitum Cordosphaeridium sp . A 0 0 8 0 0 0 0 0 0 Cordosphaeridium 0 0 0 0 0 0 7 0 0 cantharellus Cordosphaeridium 0 0 0 0 0 0 3 0 0 fibrospinosum Dinogymnium sp . 0 0 0 0 0 0 0 0 0 Fibrocysta sp . 0 0 0 3 0 0 0 0 0 Glaphyrocysta intricate 0 0 1 0 0 0 0 0 0 Homotryblium sp . 0 0 5 0 0 0 0 0 0 Nematosphaeropsis sp. 0 0 0 0 0 0 2 0 0 Operculodinium sp . 0 0 0 0 0 0 0 0 0 Palaeocystodinium sp . 0 0 0 1 0 0 2 0 0 Palaeoperidinium 0 0 0 0 0 0 0 0 0 pyrophorum Phoberocysta neocomica 0 0 0 0 2 0 0 0 0 Prolixosphaeridium 0 0 0 0 2 0 10 0 0 parvispinum Protoellipsodinium 0 0 0 0 2 0 0 0 0 spinosum Schematophora speciosa 0 0 0 0 0 0 0 0 0 Spiniferites sp . 0 0 1 0 0 0 0 0 0 Thalassiphora sp . 0 0 0 3 2 0 0 0 0 Trichodinium cilatum 0 0 0 0 1 0 0 0 0 Total 0 0 25 7 11 0 33 0 0

186

Quantitative Data: BH-9.

Depth (m) 16.4 17.3 18.1 18.4 19.5 21.0 22.5 23.7 30.1

B- B- B- B- B- B- B- Core-Section, Interval B-563 564 9565 9570 9562 9570 9566 9571 B-560

Sample # SC14 SC16 SC17 SC18 SC19 SC21 SC23 SC25 SC27 Cordosphaeridium sp. A 0 0 0 0 2 0 0 0 0 Dinogymnium sp. 0 0 3 0 0 0 0 0 0 Palaeoperidinium pyrophorum 0 0 1 0 0 0 0 0 0 Total 0 0 4 0 2 0 0 0 0

187

Quantitative Data: BH-10. 22. Depth (m) 13.5 14.3 15.4 15.8 16.7 19.8 21.3 8 25.9 32 33.5 34.1 34.4 Core- B- B- B- B- B- B- B- B- B- B- B- B- Section, 957 B- 957 957 956 957 957 95 957 957 959 959 959 Interval 2 9573 4 5 7 6 7 61 8 9 7 8 9

SC SC SC SC SC SC SC SC SC SC SC SC SC Sample # 10 11 12 13 15 20 22 24 26 28 29 30 31 Acritarchs 0 0 0 0 0 23 0 0 0 0 0 0 0 Cerodinium sp. A 0 0 0 0 0 1 0 0 0 0 0 0 0 Operculod- inium sp. 0 0 0 0 1 0 0 0 0 0 0 0 0 Palaeocyst- odinium sp. 0 0 0 0 6 0 0 0 0 0 0 0 0 Schemato- phora speciosa 0 0 0 0 5 0 0 0 0 0 0 0 0 Spiniferites sp. 0 0 0 0 0 * 0 0 0 0 0 0 0 Total 0 0 0 0 12 24 0 0 0 0 0 0 0

188

APPENDIX F.

QUANTITATIVE PALYNOMORPH DATA FOR TRENCH 1 IN STODDARD

COUNTY, MISSOURI: DINOFLAGELLATES AND OTHER MARINE

PALYNOMORPHS

189

Quantitative Data: Trench 1.

Depth (cm) 180 160 140 110 110 75 75 60 50 20 0

Core-Section R- B-9568 B-9583 B-9580 R-1393- R-1393- B-9600 B-9582 B-9581 R-1393- B-9584 (interval) 1393- 25/COR 24/COR 23/COR 22/CO R

Sample # ST01 ST02 ST03 ST04 ST05 ST06 ST07 ST08 ST09 ST10 ST11 Acritarchs: various 4 0 8 0 11 25 9 20 0 17 24 Achomosphaera 2 0 0 0 0 0 0 0 0 0 0 sp . Achomosphaera 5 0 0 0 11 0 0 0 0 0 0 alcicornu Achomosphaera 0 0 0 0 0 0 0 0 0 3 0 andalousiensis Adnatosphaerid ium 0 0 0 0 0 2 0 0 0 0 0 sp. Alisocysta sp. 7 0 0 0 6 0 0 0 0 4 0 Alisogymnium 0 0 0 0 0 0 2 0 0 0 0 euclaense Aptea polymorpha 0 0 0 0 0 0 0 0 0 2 0 Apteodinium sp . 3 0 0 0 0 0 0 0 0 0 0 Areoligera 8 0 0 0 0 0 0 0 0 0 0 senoniense Batiacasphaera sp . 0 0 0 0 0 0 2 0 0 0 0 Batiacasphaera 0 0 7 0 0 0 0 0 0 0 0 baculata Batiacasphaera 0 0 0 0 0 0 3 0 0 0 0 micropapillata Cassiculosphaer- 2 0 0 0 0 0 0 0 0 0 0 idia reticulate Cerodinium sp. A 0 0 2 0 0 0 0 0 10 4 0 Cerodinium 0 0 0 0 0 0 0 0 0 2 0 boloniense Cerodinium diebelii 1 0 0 0 0 0 0 0 0 0 0 Cerodinium 0 0 0 0 0 0 0 2 0 0 0 pannuceum Cerodinium 0 0 2 0 0 3 0 0 3 0 0 speciosum Cerodinium 0 0 2 1 0 0 0 0 1 1 0 striatum Cleistosphaeridium 0 0 0 0 15 0 0 0 0 0 0 sp. Cleistosphaeridium 16 0 0 0 0 0 0 0 0 2 0 insolitum Cordosphaeridium 0 1 0 0 7 2 0 0 4 0 0 sp. A Cordosphaeridium 0 0 0 0 0 2 0 0 0 0 0 exilimurum Cordosphaeridium 9 0 0 4 0 0 3 0 10 9 0 funiculatum Cordosphaeridium 0 0 0 0 3 0 0 0 0 0 0 minimum Cribroperidinium 3 0 0 0 0 0 0 0 0 0 0 sp. Deflagymnium sp. 0 0 0 0 1 0 0 0 0 0 0 Deflandrea sp. 3 0 0 0 0 0 0 0 0 1 0 Dinogymnium 0 1 0 0 2 0 0 0 0 0 0 acuminatum Diphyes colligerum 0 0 0 0 0 3 0 3 0 4 0 190

Diphyes spinula 0 0 0 0 4 6 0 0 2 2 0 Distatodinium sp . 5 0 0 0 0 0 0 0 0 0 0 Distatodinium 6 0 0 0 0 0 0 0 0 0 0 ellipticum Fibrocysta sp. 0 0 0 0 9 0 0 3 0 0 0 Fibrocysta 6 0 0 0 0 7 0 0 1 0 0 lappacea Florentinia sp. 1 0 0 0 3 0 0 0 0 0 0 Fromea fragilis 0 0 0 0 0 2 0 0 0 0 0 Gippslandia sp. 4 0 0 0 0 0 0 0 0 0 0 Glaphyrocysta sp. 0 0 0 0 1 3 0 0 0 0 0 Gochteodinia sp. 0 0 0 0 4 0 0 0 0 0 0 Hafniasphaera sp. 1 0 0 2 0 0 0 0 0 0 0 Hafniasphaera 0 0 11 1 0 0 0 0 0 0 0 graciosa Hafniasphaera 18 0 0 0 0 0 1 0 2 2 0 septatus Homotryblium sp. 0 0 3 0 0 3 0 0 2 0 0 Hystrichokolpoma 0 0 0 0 2 0 0 0 0 0 0 sp. Hystrichosphaerid- 0 0 1 0 3 5 0 0 0 0 0 ium tubiferum Melitasphaeridium 0 0 0 0 3 0 0 0 0 0 0 sp. Nematosphaerop- 4 0 0 0 15 0 0 5 0 0 0 sis sp. Oligosphaeridium 0 0 0 0 0 6 0 0 0 1 0 sp. A Oligosphaeridium 9 0 4 3 15 0 0 0 0 0 0 complex Oligosphaeridium 3 0 0 0 0 0 0 0 0 0 0 patulum Operculodinium sp. 3 0 0 0 0 0 0 0 0 4 0 Operculodinium 7 0 6 3 0 5 1 3 7 0 0 centrocarpum Operculodinium 7 0 0 0 0 0 0 0 0 0 0 echigoense Paleocystodinium 2 0 6 4 5 0 3 4 5 0 0 golzowense Palaeoperidinium 1 0 1 0 0 0 5 0 0 0 0 pyrophorum Paucisphaeridium 0 0 0 0 2 0 0 0 0 0 0 Inversibuccinum Pervosphaeridin- 0 0 0 0 8 0 0 0 0 0 0 ium sp. Phthanoperidinium 0 0 0 0 3 0 0 0 0 0 0 sp. Phthanoperidinium 1 0 0 0 0 0 0 0 0 0 0 amoenum Pterodinium spp. 0 0 0 0 1 0 7 0 4 3 0 Pterospermopsis 0 0 6 1 3 0 16 4 18 0 0 sp. Schematophora 1 0 0 0 2 0 0 0 0 0 0 speciosa Senegalinium sp. A 0 0 0 0 5 1 0 0 0 0 0 Senoniasphaera 0 0 0 0 3 0 0 0 0 0 0 sp. Senoniasphaera 2 0 0 0 4 0 0 0 0 0 0 Inornata Spiniferites spp. 24 0 13 16 38 51 6 0 27 9 0 Spiniferites 22 2 16 8 17 6 5 0 9 5 0 ramosus 191

Spiniferites 4 0 0 0 0 0 0 0 0 0 0 supparus Subtilisphaera sp. 0 0 0 0 0 0 0 x 0 0 0 Systematophora 0 0 0 0 0 0 0 0 0 2 2 silybum Tanyosphaeridium 0 0 0 0 7 0 0 0 0 0 0 sp. Tanyosphaeridium 3 0 0 0 0 0 0 0 0 0 0 regulare Thalassiphora sp . 1 0 0 0 0 0 0 0 0 0 2 Thalassiphora 1 0 0 0 0 0 0 0 0 0 0 delicate Thalassiphora 2 0 0 0 0 0 0 0 0 0 0 inflate Thalassiphora 0 0 0 0 7 0 0 0 0 0 0 pelagic Total 201 4 88 43 220 132 63 44 105 77 28

192

APPENDIX G.

QUANTITATIVE PALYNOMORPH DATA FOR CORE CUTTINGS FROM

NEW MADRID COUNTY, MISSOURI: DINOFLAGELLATES AND OTHER

MARINE PALYNOMORPHS

193

Quantitative Data: Core cuttings.

Depth (m) 1417 1433' 1544 1646 1672'5 1698'5 1433- Core-Section (interval) 1417 1435' 1544' 1646' 1672'5" 1699

Samp. # NM01 NM02 NM03 NM04 NM05 NM06 Acritarchs 0 0 0 4 1 9 Achomosphaera sp. 0 0 0 3 0 5 Alterbidinium sp. 0 0 0 0 1 0 Cerodinium sp. A 0 0 0 2 0 13 Cerodinium diebelii 0 0 0 0 0 3 Cerodinium pannuceum 0 0 0 0 3 3 Cerodinium speciosum 0 0 0 0 0 2 Cerodinium striatum 0 0 0 0 0 0 Cleistosphaeridium sp. 0 0 0 0 0 22 Cordosphaeridium sp .A 0 0 0 0 0 3 Cordosphaeridium funiculatum 0 0 0 7 0 14 Deflandrea sp. 0 0 0 0 0 0 Dinogymnium acuminatum 0 0 0 2 0 0 Fibrocysta lappacea 0 0 0 0 0 7 Glaphyrocysta semitecta 0 0 0 0 0 1 Hafniasphaera septatus 0 0 0 0 0 1 Homotryblium sp. 0 0 0 0 0 2 Hystrichosphaeridium tubiferum 0 0 0 0 0 3 Lanternosphaeridium lanosum 0 0 0 0 0 2 Lejeunecysta hyaline 0 0 0 0 0 3 Lejeunecysta izerzenensis 0 0 0 0 0 3 Micrhystridium piliferum 0 0 3 0 2 0 Nematosphaeropsis sp. 0 0 3 0 7 11 Oligosphaeridium sp . A 0 0 0 0 0 2 Operculodinium sp. 0 0 0 0 0 9 Operculodinium centrocarpum 0 0 0 0 0 0 Palaeocystodinium sp. 0 0 0 0 0 1 Palaeocystodinium golzowense 0 0 0 1 3 2 Palaeoperidinium pyrophorum 0 0 0 0 0 2 Phelodinium sp. A 0 0 0 0 0 3 Phelodinium magnificum 0 0 0 0 0 3 Pterospermopsis sp. 0 0 0 0 0 2 Senegalinium sp . A 0 0 0 0 0 2 Spiniferites sp . 0 0 0 6 0 19 Spiniferites ramosus 0 0 0 0 0 0 Sumatradinium druggii 0 0 0 0 0 9 Total 0 0 6 25 17 161

194

APPENDIX H.

NONMARINE PALYNOMORPH TAXA IN THE OWL CREEK: NEW MADRID,

SCOTT, AND STODDARD COUNTIES, MISSOURI

195

Owl Creek Taxa

Arecipites rousei Frederiksen 1973 Arecipites sp. Basopollis obscurocostatus Tschudy 1975 Bisaccates (various) Cardioangulina diaphana Wilson & Webster 1946 Carpinus subtriangula Stanley 1965 Caryapollenites imparalis Nichols & Ott 1978 Casuarinidites sp Chenopodipollis sp Cicatricosisporites sp. Cingulatisporites dakotaensis Stanley 1965 Compositoipollenites sp. Corollina (Classopollis ) sp. Cupressacites hiatipites (Wodehouse 1933) Krutzsch 1971 Cupuliferoipollenites sp. Cycadopites giganteus Stanley 1965 Cycadopites scabratus Stanley 1965 Diporopollenites sp. Type A Engelhardtia microvoveolata Stanley 1965 Ephedra voluta Stanley 1965 Ephedripites sp. Ericipites redbluffensis Frederiksen 1980 Extremipollis caminus Tschudy 1975 Favitricolporites sp. Fraxinoipollenites variabillis Stanley 1965 Gleicheniidites senonicus Ross 1949 Gleicheniidites sp. Gleichenia triangular Stanley 1965 Graminidites sp. Holkopollenites sp. A Horniella sp. Inaperturopollenites sp. Type C Inaperturopollenites sp. Type D Laevigatosporites sp. Lycopodium hamulatum (Krutzsch 1959) Frederiksen 1980 Lycopodium heskemensis (Pflanzl 1955) Frederiksen 1980 Maceopolipollenites amplus Leffingwell 1971 Momipites coryloides Wodehouse 1933 Nudopollis terminalis (Pflug in Thomson in Thomson & Pflug 1953) Elsik 1968 Osmundacidites sp. Pistillipollenites mcgregorii Rouse 1962 Platacarya sp. Plicatopollis sp. Proteacidites retusus Anderson 1960 196

Pseudoplicapollis serenus (Krutzsch 1967) Tschudy 1975 Pseudovacuopollis involutus (Krutzsch & Pacltová 1967) Tschudy 1975 Retibrevitricolpites sp. Rhoipites globosus Stanley 1965 Rhoipites pisinnus Stanley 1965 Rhoipites sp. Salixipollenites parvus Frederiksen 1980 Sphagnum sp. Stereisporites antiquasporites (Wilson & Webster 1946) Dettmann 1963 Syncolporites sp. Thecaphora sp. Thomsoniopollis sp. Triatriopollenites paradoxus Tricolpites parvus Stanley 1965 Triporopollenites sp. Vacuopollis munitus Stanley 1965

197

APPENDIX I.

NONMARINE PALYNOMORPH TAXA IN THE CLAYTON: NEW MADRID,

SCOTT, AND STODDARD COUNTIES, MISSOURI

198

Clayton Taxa

Ailanthipites marginatus Frederiksen 1983 Alnus trina, Stanley 1965 Annutriporites tripollenites (Rouse) Sepúlveda & Norris 1982 Aquilapollenites murus Stanley 1961 Araliaceoipollenites profoundus Frederiksen 1980 Arecipites columellus Leffingwell 1971 Arecipites sp. Aster sp. Baculatisporites sp. Basopollis obscurocostatus Tschudy 1975 Basopollis sp. Betula infrequens Stanley 1965 Bisaccates undifferentiated Bombacadites reticulatus (Couper 1960) Krutzsch 1970 Botryococcus sp. Caprifoliipites longus Stanley 1965 Cardioangulina diaphana Wilson & Webster 1946 Carya paleocenica Stanley 1965 Caryapollenites imparalis Nichols & Ott 1978 Casauarinidites sp. Catinipollis geiseltalensis Krutzsch 1966 Chenopodipollis sp. Chenopodipollis nuktakensis Norris 1986 Choanopollenites sp. Cicatricosisporites sp. Cingulatisporites dakotaensis Stanley 1965 Corollina (Classopollis ) sp. Corylus granilabrata Stanley 1965 Corylus sp. Cupanieidites speciosus Stanley 1965 Cupressacites hiatipites (Wodehouse1933) Krutzsch 1971 Cupuliferoipollenites sp. Cyathidites minor Couper 1953 Cyathidites sp. Cycadopites scabratus Stanley 1965 Cycadopites sp. Deltoidospora sp. Diporopollenites sp. Type A Engelhardtia microvoveolata Stanley 1965 Ephedra sp. Ephedra voluta Stanley 1965 Ephedripites sp. Ericipites redbluffensis Frederiksen 1980 Extremipollis versatilis Tschudy 1975 199

Favitricolporites sp. Foveosporites triangulus Krutzsch 1959 Fraxinoipollenites sp. Fraxinoipollenites variabillis Stanley 1965 Gleichenia circinidites (Cookson 1953) Dettmann 1963 Gleichenia sp. Gleichenia triangular Stanley 1965 Gleicheniidites sp. Graminidites sp. Holkopollenites sp. A Horniella sp. Inaperturopollenites sp. Type A Inaperturopollenites sp. Type C Inaperturopollenites sp. Type D Interporopollenites turgidus Tschudy 1975 Intratriporopollenites crassipites Norris 1986 Kyandopollenites sp. Laevigatosporites haardti (Potonié & Venitz 1934) Thomson & Pflug 1953 Laevigatosporites sp. Leptolepidites tenuis Stanley 1965 Liliacidites dividuus Brenner 1963 Microreticulatisporites sp. Momipites coryloides Wodehouse 1933 Momipites microfovelolatus (Stanley 1965) Nichols 1973 Momipites sp. Monoporisporites globusus Clarke 1965 Monoporisporites singularis Sheffy & Dilcher 1971 Monoporisporites sp. Myricipites annulites (Martin & Rouse 1966) Norris 1986 Nudopollis terminalis (Pflug in Thomson in Thomson & Pflug 1953) Elsik 1968 Nyssapollenites albertensis Singh 1971 Nyssapollenites explanata Anderson 1960 Nyssapollenites pulvinus (Potonié 1931) Frederiksen 1980 Osmunda comaumensis (Cookson 1953). Platacarya sp. Plicapollis sp. Plicatopollis magniorbicularis Frederiksen 1983 Plicatopollis sp. Proteacidites retusus Anderson 1960 Pseudoplicapollis serenus (Krutzsch 1967) Tschudy 1975 Pseudovacuopollis involutus (Krutzsch & Pacltová 1967) Tschudy 1975 Quercoidites sp. Retibrevitricolpites sp. Rhoipites globosus Stanley 1965 Rhoipites pisinnus Stanley 1965 Rhoipites sp. 200

Salixipollenites parvus Frederiksen 1980 Sequoia sempervirens Zalkinskaya 1953 Sphagnum regium Drozhastchich 1961 Sphagnum sp. Sphagnum triangularum (Mamczar 1960) Frederiksen 1980 Spirogyra sp. Subtriporopollenites nanus (Pflug & Thomson in Thomson & Pflug 1953) Frederiksen 1980 Syncolporites sp. Taxodiaceaepollenites hiatus (Potonié 1931) Kremp 1949 Todisporites minor Todisporites sp. Toroisporis major (Pflug in Thomson in Thomson & Pflug 1953) Stanley 1965 Triatriopollenites paradoxus Tricolpites bathyreticulatus Stanley 1965 Tricolpites erugatus Tricolpites hians Stanley 1965 Tricolpites parvus Stanley 1965 Tricolpites sp. Tricolpites sp. Type B (large pollen) Tricolporopollenites sp. Triporopollenites sp.

201

APPENDIX J.

NONMARINE PALYNOMORPH TAXA IN THE PORTERS CREEK: NEW

MADRID, SCOTT, AND STODDARD COUNTIES, MISSOURI

202

Porters Creek Taxa

Abies balsamea Leopold 1969 Abies sp. Acer striatellum (Takahashi 1961) Frederiksen 1980 Aglaoreidia pristine Fowler 1971 Ailanthipites berryi Wodehouse 1933 Ailanthipites marginatus Frederiksen 1983 Ailanthipites speciipites Wodehouse 1933 Alnipollenites scoticus Simpson 1961 Alnus trina Stanley 1965 Alnus vera (Potonié 1931) Martin & Rouse 1966 Alsophilidites kerguelensis Cookson 1947 Anemia tricornitata (Weyland & Greifeld) Stanley 1965 Appendicisporites tricornatus (Weyland & Greifeld 1961) Groot et al. 1963 Aquilapollenites bertillonites Funkhouser 1961 Aquilapollenites murus Stanley 1965 Araliaceoipollenites profoundus Frederiksen 1980 Arecipites columellus Leffingwell 1971 Arecipites rousei Frederiksen 1973 Arecipites sp. Baculatisporites sp. Baculatisporites quintus (Thomson & Pflug 1953) Krutzsch 1959 Basopollis obscurocostatus Tschudy 1975 Basopollis sp. Betula infrequens Stanley 1965 Betulaceoipollenites sp. Bisaccates (various) Boehlensipollis hohlii Krutzsch 1962 Boehlensipollis minimus (Leffingwell 1971) Pocknall & Nichols 1996 Boehlensipollis sp. Bombacadites reticulatus (Couper 1960) Krutzsch 1970 Bombacadites sp. Botryococcus sp. Bullasporis sp. Cardioangulina diaphana Wilson & Webster 1946 Caryapollenites imparalis Nichols & Ott 1978 Caryapollenites simplex (Potonié 1931) Tschudy & van Loenen 1970 Caryapollenites veripites (Wilson & Webster 1946) Nichols & Ott 1978 Casauarinidites sp. Catinipollis geiseltalensis Krutzsch 1966 Celtipollenites gracillis Nagy 1969 Chenopodipollis nuktakensis Norris 1986 Chenopodipollis sp. Choanopollenites sp. Cicatricosisporites sp. 203

Cingulatisporites dakotaensis Stanley 1965 Cingulatisporites radiatus Stanley 1965 Corollina (Classopollis ) sp. Compositoipollenites grandiannulatus Frederiksen 1983 Confertisulcites fusiformis Frederiksen 1973 Confertisulcites sp. Corylus granilabrata Stanley 1965 Cupanieidites speciosus Stanley 1965 Cupressacites hiatipites (Wodehouse 1933) Krutzsch 1971 Cupuliferoipollenites sp. Cyathidites minor Couper 1953 Cycadopites giganteus Stanley 1965 Cycadopites scabratus Stanley 1965 Cycadopites sp. Cyrillaceaepollenites ventosus (Potonié) Frederiksen 1980 Deltoidospora concava Takahashi 1975 Deltoidospora sp. Diporopollenites sp. Type A Diporopollenites sp. Type B Diporopollenites sp. Type C Diporicellaesporites retipilatus Elsik 1968 Endoinfundibulapollis sp. Engelhardtia microvoveolata Stanley 1965 Engelhardtia sp. Ephedra claricristata Shakhmundes 1965 Ephedra exiguua Frederiksen 1983 Ephedra hungarica (Nagy 1963) Frederiksen 1980 Ephedra sp. Ephedra voluta Stanley 1965 Ephedripites sp. Ericipites redbluffensis Frederiksen 1980 Eucommia sp. Extremipollis caminus Tschudy 1975 Extremipollis sp. Extremipollis versatilis Tschudy 1975 Extremipollis vivus Tschudy 1975 Faguspollenites sp. Favitricolporites sp. Foveosporites sp. Foveosporites triangulus Krutzsch 1959 Fraxinoipollenites medius Frederiksen 1980 Fraxinoipollenites sp. Fraxinoipollenites variabillis Stanley 1965 Gleichenia circinidites (Cookson 1953) Dettmann 1963 Gleichenia sp. Gleichenia triangular Stanley 1965 204

Gleicheniidites senonicus Ross 1949 Gleicheniidites sp. Graminidites gramineoides (Meyer 1956) Krutzsch 1970 Graminidites sp. Holkopollenties sp. A Horniella sp. Inaperturopollenites sp. Type A Inaperturopollenites sp. Type B Insulapollenites rugulatus Leffingwell 1971 Interpollis sp. Interporopollenites turgidus Tschudy 1975 Intratriporopollenites crassipites Norris 1986 Intratriporopollenites sp. Jarzenipollenites trinus (Stanley 1965) Kedves 1980 Juglans nigripites Wodehouse 1933 Kyandopollenites sp. Laevigatosporites haardti (Potonié & Venitz 1934) Thomson & Pflug 1953 Laevigatosporites pseudomaximus Pflug and Thomson in Thomson & Pflug 1953 Laevigatosporites sp. Lanagiopollis sp. Lanagiopollis cribellata (Srivastava) Frederiksen Laricoidites magnus Potonié 1958 Leiotriletes adriennis pseudomaximus (Pflug & Thomson 1953) Krutzsch 1959 Leptolepidites tenuis Stanley 1965 Libopollis jarzenii Farabee et al. 1984 Liliacidites complexus (Stanley 1965) Leffingwell 1971 Liliacidites inaequalis Singh 1971 Liliacidites intermedius Couper 1953 Liliacidites sp. Liliacidites tritus Frederiksen 1980 Liliacidites vittatus Frederiksen 1980 Longapertit es sp. Lycoperdon sp. Lycopodium hamulatum (Krutzsch 1959) Frederiksen 1980 Lycopodium sp. Lygodiumsporites adriennis (Potonié & Gelletich 1933) Potonié 1956 Milfordia incerta (Pflug & Thomson in Thomson & Pflug1953) Krutzsch 1961 Milfordia minima Krutzsch 1970 Momipites coryloides Wodehouse 1933 Momipites dilatus Fairchild in Stover et al. 1966 Momipites fragilis Christopher 1979 Momipites inaequalis Anderson 1960 Momipites marylandicus Groot & Groot 1962 Momipites microfovelolatus (Stanley 1965) Nichols 1973 Momipites sp. Momipites strictus Frederiksen & Christopher 1978 205

Momipites tenuipolus Anderson 1960 Monocolpopollenites sp. Monoporisporites globusus Clarke 1965 Monoporisporites singularis Sheffy & Dilcher 1971 Monoporisporites sp. Myocolpopollenites reticulatus Elsik in Stover et al. 1966 Myricipites annulites (Martin & Rouse 1966) Norris 1986 Myriophyllum sp. Nudopollis endangulatus (Pflug & Thomson in Thomson & Plug 1953) Pflug 1953 Nudopollis sp. Nudopollis terminalis (Pflug & Thomson in Thomson & Pflug 1953) Pflug 1953 Nyssapollenites explanata Anderson 1960 Nyssapollenites paleocenicus Frederiksen 1980 Nyssapollenites pulvinus (Potonié 1931) Frederiksen 1980 Osculapollis sp. Osmunda comaumensis Cookson 1953 Osmundacidites stanleyi Douglas 2002 Ovoidites ligneolus (Potonié 1951) Thomson & Pflug 1953 Ovoidites microligneolus Krutszch 1959 Palaeoisoetes subengelmannii (Elsik 1968) Pediastrum boryanum Reinsch 1867 Pinus cembraeformis Frederiksen 1983 Pinus scopulipites (Wodehouse 1933) Krutzsch 1971 Pinus semicircularis Stanley 1965 Pinus sp. Pinus strobipites Wodehouse 1933 Pistillipollenites mcgregorii Rouse 1962 Platacarya sp. Platanus occidentaloides Frederiksen 1980 Platanus sp. Plicapollis retusus Tschudy 1975 Plicapollis sp. Plicapollis usitatus Tschudy 1975 Plicatopollis magniorbicularis Frederiksen 1983. Plicatopollis sp. Polyatriopollenites stellatus Pflug 1956 Polycolpites sp. Polypodiaceoisporites sp. Polyvestibulopollenites verus (Potonié 1931) Thomson & Pflug 1953 Porosipollis porosus (Mtchedlishvili in Samoilovitch et al. 1961) Krutzsch 1969 Proteacidites retusus Anderson 1960 Pseudoculopollis admirabillis Tschudy 1975 Pseudoplicapollis serenus (Krutzsch 1967) Tschudy 1975 Pseudoplicapollis sp. Pseudotricolpites sp. Pseudovacuopollis involutus (Krutzsch & Pacltová 1967) Tschudy 1975 206

Quercoidites genustriatus Stanley 1960 Quercoidites inamoenus (Takahashi 1961) Frederiksen 1980 Quercoidites microhenricii (Potonié 1931) Potonié 1960 Quercoidites sp. Retibrevitricolpites sp . Reticuloidosporites pseudomurii Elsik 1968 Retitriletes sp. Rhoipites globosus Stanley 1965 Rhoipites latus Frederiksen 1980 Rhoipites pisinnus Stanley 1965 Rhoipites sp. Rhoipites subprolatus Frederiksen 1980 Rousea linguiflumena Pocknall & Nichols 1996 Rousea monilifera Frederiksen 1980 Salixipollenites parvus Frederiksen 1980 Schizaeoisporites eocaenicus Potonié 1956 Schizaeoisporites sp. Schizosporis cookonii Pocock 1962 Schizosporis laevigatus (Cookson & Dettmann 1959) Stanley 1965 Schizosporis microfoveatus (Cookson & Dettmann 1959) Stanley 1965 Schizosporis parvus (Cookson & Dettmann 1959) Selaginella perinata (Krutzsch et al. 1963) Frederiksen 1980 Semioculopollis sp. Sequoia sempervirens Zalkinskaya 1953 Sequoiapollenites paleocenicus (Thiergart 1938) Stanley 1965 Sphagnum australe (Cookson 1947) Drozhastchich 1961 Sphagnum regium Drozhastchich 1961 Sphagnum sp. Spirogyra sp. Stereisporites antiquasporites (Wilson & Webster 1946) Dettmann 1963 Stereisporites sp. Stereisporites stereoides (Potonié & Venitz-Pflug 1953 Striopollenites terasmaei Rouse 1962 Subtriporopollenites nanus (Pflug & Thomson in Thomson & Pflug 1953) Frederiksen 1980 Syncolporites lisamae Potonié 1960 Syncolporites rugulosus Syncolporites sp. Taxodiaceaepollenites hiatus (Potonié 1931) Kremp 1949 Thecaphora sp. Thomsoniopollis sp. Tilia instructa (Potonié 1931) Frederiksen 1980 Todisporites minor Toroisporites major (Pflug in Thomson & Pflug 1953) Stanley 1965 Toroisporites sp. Triatriopollenites sp. 207

Tricolpites bathyreticulatus Stanley 1965 Tricolpites hians Stanley 1965 Tricolpites splendens van der Hammen 1954 Tricolpites sp. Tricolpites sp. Type A Tricolpites sp. Type B Tricolporpollenites sp. Triplanosporites sinuosus Pflug 1952 Triplanosporites sp. Triporopollenites maternus Frederiksen 1980 Triporopollenites sp. Trudopollis plenus Tschudy 1975 Trudopollis sp. Trudopollis variabilis (Pflug 1953) Tschudy 1975 Tschudypollis retusus Anderson 1960 Ulmipollenites sp. Ulmipollenites undulosus Wolff 1934 Undulatisporites concavus Kedves 1979 Vacuopollis munitus Vitis affluens Stanley 1965

208

APPENDIX K

GLOSSARY OF TERMS USED FOR PALYNOMORPH DESCRIPTIONS

209

Pollen and Spores

Angiosperm: A plant that bears seeds enclosed in a fruit, characterized by double fertilization producing the zygote and the endosperm. Angiosperms and Gymnosperms produce pollen. Other plants produce spores.

Annulus: Thickening or thinning of the pollen wall around a pore.

Aperture: A thinning of the pollen or spore wall, typically covered with a membrane, that allows shrinking and swelling of the pollen grain; and where the pollen tube may exit; e.g., a furor or pore. Arci: Distinctive surface ridges in the pollen wall; very prominent in pollen of aided.

Baculate: Elements post or rod-like, higher than broad, > = 1 µm long.

Bisaccate (pollen): Pollen bearing two bladders or sacci, common in the pine family. “s” saccus, “B” body.

Bladders: The wings or air sacs (sacci) found in bisaccate pollen.

Clavate: Elements higher than broad with a constricted base or club shaped tip, > = 1 µm long.

Colpus (colpi): A pollen aperture that is more than twice as long as broad.

Columellae: Rod-like ektexine elements that extend from the foot layer to the tectum.

Dicolpate: Pollen grain with two furrows (colpi).

Diporate: Pollen grain having two pores.

Echinate: Elements in form of pointed spines, sometimes called spinulate (with spinules) if between 1-3 µm long. Spiny sculpturing.

Ektexine: The outer portion of the exine, comprised of the tectum and columellae.

Equator or equatorial: The line or plane that is usually half way between the proximal and distal poles of a pollen grain.

Exine: A resistant wall layer outside the cell wall of a pollen grain.

Furrow: Boat-shaped aperture, more than twice as long as broad.

Fusiform: Spindle-shaped, broad at center and tapered at each end. 210

Gemmate: Diameter of elements equal to, or greater than, height, constricted bvase, > = 1 µm wide. Sculptural elements with constricted bases.

Gymnosperm: Seed plant which does not produce fruits; that is, the seeds are not enclosed in an ovule.

Inaperturate: A palynomorph without apertures (alete).

Monocolpate: Pollen grains with a singlue furrow (colpus).

Monolete: Spores having a single scar in the exine surface.

Monoporate: Having a single pore in the exine surface.

Muri: Wall-like raised portion of reticulate sculpturing.

Operculum: An exinous covering over a pore.

Palynomorph: A generalized term for spores, pollen and other microfossils of similar size and composition.

P/E Index: The ratio of polar to equatorial diameter.

Pollen (pollen grains): Multicellular or multinucleate products of the microsporangia of seed plants.

Porate: Pollen grains with pores.

Pore: A pollen aperture that is nearly round less than twice as long as broad.

Psilate: Surface smooth with no discernible sculpturing.

Reticulate: Horizontally elongated elements forming a net-like pattern of lacunae (holes) and muri (walls). Bearing a net-like (reticulum) surface sculpture pattern.

Rugulate: Horizontally elongated elements in an irregular patern.

Scabrate: Small sculptural elements, less than 1 µm in any dimension.

Sculpture: The surface features of the pollen or spore wall.

Spore: The haploid cell, often with resistant wall, which is produced by meiosis in the sexual life cycle or as an asexual propagule.

Striate: Horizontally elongated elements in a more or less parallel pattern. 211

Structure: The structural features of the palynomorph wall, especially those characteristics due to the form and arrangement of the exine elements inside the tectum.

Sulcate: Having a furrow, particularly of gymnosperms and monocots. The sulcus is formed on the distal face of monocot grains. W – width, L – Length.

Tricolpate: A pollen type with three equatorial furrows.

Tricolporate: A pollen type with three equatorial furrows, each containing a pore.

Trilete: Spore having a tri-radiate scar in the wall.

Triporate: A pollen type with three equatorial pores.

Verrucate: Elements as broad as, or broader than, high, > = 1 µm wide. Sculpturing type characterized by verrucae.

Dinoflagellate Cysts (Illustrations in Figures 1-4)

Acavate: Term for a cyst having no cavities between the wall layers.

Accessory archeopyle suture: A partially developed suture between paraplates around the archeopyle or operculum margin.

Aculeate: Term for a process that has a pointed ending that is drawn out into pointed spinelets, usually of equally length.

Acuminate: Term for a process that has a pointed ending.

Annulate: Term for processes or other features that are arranged in a circle.

Apiculocavate: Term for a cyst wall with cavities at the base of or throughout the length of the processes.

Archeopyle: The excystment opening in a dinocyst.

Arcuate: Term for processes or other features that are arranged in an arc.

Attached operculum: An operculum that remains partially attached to the main body after excystment.

Autophragm: The single-layered wall of acavate dinocysts, or the inner wall of holocavate dinocysts.

212

Bifid: Term for a closed or solid process that is angularly divided into two short, equal parts.

Bifurcate: Term for a process that is divided distally into two branches.

Bulbous: Term for a solid or closed process that is distally swollen and has the appearance of a club.

Cavate: Term for a cyst with a cavity or cavities between wall layers.

Central body: The body from which arise the processes or septa in a chorate or proximochorate cyst.

Chorate: Term for a cyst with processes or septa that in height are more than 30% of the shortest diameter of the central body.

Cingulum: In motile dinokont dinoflagellates, the furrow (or equivalent feature on cysts) that divides the episome and hyposome and in which, in the motile stage, lies the transverse flagellum.

Circumcavate: Term for a cyst with two wall layers that are continuously separated around the ambitus.

Cornucavate: Term for a cyst with two wall layers that are separated in the vicinity of the horns only.

Cyst: A coccoid cell with a cell wall and a reproductive or dormancy function; in the context of this study, the term cyst is equivalent to dinoflagellate cyst, or dinocyst.

Digitate: Term for an open process in which the distal margin is drawn out to form finger-like extensions.

Distal: Towards the outside, for example the free ends of processes.

Dorso-ventral: Term referring to the view when either the dorsal or the ventral surface is uppermost.

Ectophragm: The wall layer external to the periphragm or autophragm and supported by processes, membranes or other structures.

Endophragm: The innermost wall layer of a dinocyst with two or more walls that are not connected by supporting structures.

Epicyst: The area of a dinocyst anterior to the cingulum. Equivalent to the epitheca in the motile stage; the term episome can refer to epitheca or epicyst.

213

Fusiform: Term describing a spindle-shaped cyst, in which single horns are developed at apical and antapical poles.

Holocavate: Term referring to a situation in which there are supporting structures between the two wall layers (usually ectophragm and autophragm) of a cavate dinocyst.

Horn: An extension of the cell or cyst wall into a blunt or pointed structure which protrudes from the ambitus.

Hypocyst: The area of a dinocyst posterior to the cingulum. It is equivalent to the hypotheca in the motile stage. The term hyposome can refer to both theca and cyst.

Intratabular: Features that are within the parasutures of individual paraplates.

Nontabular: Term referring to a situation in which the processes or other ornamentation of a dinocyst do not show any relationship to paratabulation.

Paraplate: That area on the cyst equivalent to a plate on the theca.

Paratabular: Refers to a situation in which a cyst shows paratabulation.

Paratabulation: The cyst equivalent of thecal tabulation; reflected tabulation on the cyst.

Peridinoid: Having the outline of Peridinium; that is, dorso-ventrally compressed and with a single apical horn and generally two antapical horns. The left antapical horns may be reduced or absent.

Periphragm: The outer layer in dinoflagellate cysts with two wall layers that are unconnected by supporting structures, or the outermost layer where the middle layer is termed the mesophragm, again with no supporting structures.

Process: A structure which arises generally from an external surface and is columnar or spine-like. Processes may be simple or intricately branched and interconnected.

Proximate: Term for a feature that is at or close to the point of origin of a process, crest or similar structure.

Septum: A delicate linear projection on the wall of a dinoflagellate cyst, which is a partial synonym of crest.

Tabulation: The arrangement of the plates on the theca. In situations where both the tabulation and paratabulation are implied, the term tabulation is used in the general sense to include both.

Trifurcate: Term for a process that divides, usually distally, into three branches. 214

Trifurcate process: A process that distally divides into three branches.

Figure 1. Principal features of the theca in a dinoflagellate.

Figure 2. Schematic diagrams illustrating formation of various archeopyle types (Archeopyle shaded); o = operculum, st = parasulcal tongue, sn = parasulcal notch, aas= accessory archeopyle parasuture, pas = principal archeopyle suture.

215

Figure 3. Some examples of surface relief. 216

Figure 4. Schematic illustrations of process shapes and process tip terminology. (1) conical, (2) subconical, (3) tapering, (4) cylindrical, (5) infundibular, (6) flared, (7) tubiform, (8) buccinate, (9) lagenate, (10) bulbose, (11) acuminate, (12) evexate, (13) bulbous, (14) capitate, (15) cauliflorate, (16) bifid, (17) foliate, (18) oblate, (19) digitate, (20) branched, (21) bifurcate, (22) trifurcate, (23) entire, (24) fenestrate, (25) aculeate, (26) secate, (27) denticulate, (28) recurved, (29) patulate, (30) dirigate, (31) orthogonal, (32) acicular, (33) tubiform, (34) bifid, (35) branched-bifid, (36) trifurcate gonal, (37) bifurcate intergonal.

217

APPENDIX L.

ILLUSTRATIONS OF SELECTED PALYNOMORPHS: PLATES 1 TO 8

218

PLATE 1

Names of illustrated specimens on all the plates are followed by focus level, slides numbers, sample numbers, and location coordinates on the Lovins universal slide field finder.

A. Lygodiumsporites adriennis , high focus, slide TLE-4a, sample SC06, 34 J/K.

B. Todosporites sp., high focus, slide TLE-4a, sample SC06, 7 J/K.

C. Todosporites minor , high focus, slide P1-DG-20, sample ST09, 2 V/W.

D. Inaperturate pollen, high focus, slide TLE-4a, sample SC06, 19 C/D.

E. Cyathidites minor , high focus, slide GL-L, sample ST06, 8 E/F.

F. Sphagnum australe , high focus, slide P1-DG-40, sample ST08, 26 J/K.

G. Gleicheniidites senonicus , high focus, slide P1-DG-40, sample ST08, 10 N/P.

H. Gleicheniidites senonicus , high focus, slide GL-L, sample ST06, 16 E/F.

I. Toroisporites sp., high focus, slide TLE-4a, sample SC06, 10 L/M.

J. Cicatricosisporites sp., high focus, slide TLE-4a, sample SC06, 17 J/K.

K. Cicatricosisporites sp., high focus, slide GL-L, sample ST06, 6 G/H.

L. Cyathidites sp., high focus, slide GL-G, sample ST05, 17 E/F.

M. Cyathidites sp., low focus, slide GL-G, sample ST05, 17 E/F.

N. Cicatricosisporites dorogensis , high focus, slide TLE-3, sample SC03, 7 L/M.

219

220

PLATE 2

A. Osmundacidites sp., high focus, slide TLE-4a, sample SC06, 22 J/K.

B. Milfordia incerta , high focus, slide TLE-4a, sample SC06, 3 K/L – 4 K/L.

C. Appendicisporites tricornatus , high focus, slide TLE-4a, sample SC06, 27 C/.D.

D. Unidentified trilete spore, high focus, slide GL-G, sample ST05, 17 G/H.

E. Hamulatisporis hamulatis sp., mid focus, slide TLE-4a, sample SC06, 26 M/N.

F. Graminidites sp., high focus, TLE-4, sample SC05, 8 G/H.

G. Ephedripites sp., high focus, slide CL-2, sample ST10, 3 D/E.

H. Ephedripites sp., high focus, slide GL-G, sample ST05, 12 U/V.

I. Bisaccate pollen, possibly Pinus sp., low focus, slide TLE-4, sample SC05, 26 J/K.

J. Triatriopollenites paradoxus , low focus, TLE-4a, sample SC06, 2 N/P.

K. Triatriopollenites paradoxus , high focus, TLE-4a, sample SC06, 2 N/P.

L. Cupressacites hiatipites , high focus, slide PC10-16.7, sample SC15, 6 L/M.

M. Unidentified tricolporate pollen, high focus, slide TLE-4a, sample SC06, 1 J/K.

N. Betula infrequens, high focus, slide P1-DG-40, sample ST08, 1 F/G.

O. Triatriopollenites sp., high focus, slide GL-L, sample ST06, 22 F/G.

P. Caryapollenites simplex , high focus, slide TLE-4, sample SC05, 10 U/V.

Q. Caryapollenites simplex, high focus, slide TLE-3, sample SC03, 15 G/H.

R. Triatriopollenites proprius , high focus, slide GL-L, sample ST06, 2 D/E.

221

222

PLATE 3

A. Botryococcus braunii , high focus, slide TLE-4a, sample SC05, 15 E/F.

B. Momipites coryloides , mid focus, slide TLE-3a , sample SC04, 14 D/E.

C. Platanus occidentaloides , high focus, slide TLE-4, sample SC05, 7 G/H.

D. Extremipollis sp., mid focus, slide TLE-25, sample SC02, 12 S/T.

E. Chenopodipollis sp., high focus, slide PC10-16.7, sample SC15, 26 K/L.

F. Semioculopollis sp., high focus, slide PC10-25.9, sample SC26, 5 K/L.

G. Cassiculosphaeridia reticulata , mid focus, slide CL-1, sample ST01, 4 B/C.

H. Spiniferites sp., mid focus, slide CL-1, sample ST01, 5 L/M.

I. Dinogymnium acuminatum , mid focus, slide GL-G, sample ST05, 27 D/E.

J. Fibrocysta lappacea , high focus, slide CL-1, sample ST01, 9 J/K.

K. Cleistosphaeridium insolitum , high focus, slide CL-1, sample ST01, 9 R/S.

L. Tricolporopollenites sp., mid focus, slide TLE-4, sample SC05, 26 C/D.

M. Vitis affluens , high focus, slide TLE-4a, sample SC06, 3 J/K.

N. Subtilisphaera sp., mid focus, slide P1-DG-40, sample ST08, 1 F/G

223

224

PLATE 4

A. Palaeocystodinium sp., mid focus, slide P1-DG-20, sample ST09, 2 Q/R.

B. Palaeocystodinium golzowense , mid focus, slide 1698.5, sample NM06, 10 M/N.

C. Palaeocystodinium golzowense , mid focus, slide 1698.5, sample NM06, 16 E/F.

D. Achomosphaera alcicornu , mid focus, slide CL-1, sample ST01, 7 J/K.

E. Senoniasphaera inornata? , high focus, slide 1698.5, sample NM06, 20 H/J.

F. Hafniasphaera septatus , high focus, slide CL-1, sample ST01, 8 L/M.

G. Senoniasphaera inornata , mid focus, slide P1-DG-40, sample ST08, 15 S/T.

225

226

PLATE 5

A. Spiniferites sp., high focus, slide CL-1, sample ST01, 13 Q/R.

B. Operculodinium echigoense , high focus, slide GL-G, sample ST05, 13 T/U.

C. Spiniferites sp., high focus, slide CL-1, sample ST01, 8 T/U – 9 T/U.

D. Spiniferites ramosus , high focus, slide CL-1, sample ST01, 11 U/V.

E. Spiniferites ramosus , high focus, slide CL-1, sample ST01, 7 T/U.

F. Areoligera senoniense , mid focus, slide CL-1, sample ST01, 5 B/C.

227

228

PLATE 6

A. Cerodinium striatum , high focus, slide NM 1698.5, sample NM06, 18 Q/R.

B. Cerodinium pannuceum , high focus, slide NM1698.5, sample NM06, 26 C/D.

C. Cerodinium diebelii , high focus, slide P1-DG-40, sample ST08, 17 F/G.

D. Cordosphaeridium fibrospinosum ., high focus, slide CL-1, sample ST01, 7 B/C – 7 C/D.

E. Cordosphaeridium sp. A, mid focus, slide GL-G, sample ST05, 11 K/L.

F. Deflandrea sp., mid focus, slide NM 1698.5, sample NM06, 28 M/N.

G. Lejeunecysta izerzenensis , mid focus, slide NM1698.5, sample NM06, 24 Y/Z.

H. Lejeunecysta izerzenensis , high focus, slide NM1698.5, sample NM06, 28 Y/Z.

I. Cerodinium sp. A, high focus, slide P1-DG-20, sample ST09, 11E/F.

229

230

PLATE 7

A. Oligosphaeridium complex , mid focus, slide CL-1, sample ST01, 9 R/S.

B. Palaeoperidinium pyrophorum , mid focus, slide GL-G, sample ST05, 10 J/K.

C. Oligosphaeridium complex , high focus, slide CL-1, sample ST01, 9 R/S.

D. Palaeoperidinium pyrophorum , mid focus, slide GL-G, sample ST05, 1 W/X.

E. Oligosphaeridium sp. A, low focus, slide CL-1, sample ST01, 11 S/T.

F. Phelodinium sp. A, mid focus, slide CL-1, sample ST01, 18 Q/R.

231

232

PLATE 8

A. Senegalinium sp. A, low focus, slide P1-DG-40, sample ST08, 15 L/M.

B. Micrhystridium piliferum , low focus, slide GL-G, sample ST05, 15 D/E.

C. Pterospermopsis sp., mid focus, slide P1-DG-40, sample ST08, 13 R/S.

D. Veryhachium sp., high focus, slide P1-DG-40, sample ST08, 14 L/M.

E. Unidentified dinocyst, slide 1698.5, high focus, sample NM06, 12 T/U.

F. Forminiferal inner lining, high focus, slide P1-DG-40, sample ST08, 16 M/N.

G. Pterodinium sp., mid focus, slide CL-1, sample ST01, 5 B/C.

H. Unidentified specimen, possibly a monoporate pollen polyad, high focus, slide 1698.5, sample NM06, 16 K/L.

I. Unidentified specimen, possibly a monoporate pollen polyad, low focus, slide 1698.5, sample NM06, 16 K/L.

233

234

APPENDIX M.

QUANTITATIVE FORAMINIFERA DATA FOR THE OWL CREEK,

CLAYTON, AND PORTERS CREEK FORMATIONS

235

Sample FOC1 FOC2 FOC3 FOC4 FOC5 FOC6 FGLG FCL1 FGLL FKT4

Formation OC OC OC OC OC OC CL CL CL PC

Anomalina 2 2 2 1 3 0 1 3 1 1 elementiana Bathysiphon sp. 0 0 0 0 1 0 0 0 0 0

Bolvina incrassate 0 2 2 0 0 0 0 0 3 0

Dentalina 0 1 0 0 0 0 3 0 0 2 Gardnerae Discorbis 0 0 6 0 0 0 0 1 6 0 Midwayensis Globigerina 1 1 2 2 0 0 0 8 4 7 Compressa Globulina 0 0 0 0 0 0 0 0 1 0 Gibba Globulina 0 0 6 1 0 0 0 7 9 5 Rotundata Gyroidina 2 3 4 0 2 7 0 14 51 28 Depressa Nodogenerina 2 2 2 0 1 2 0 0 1 8 bradyi Nodosaria 2 3 1 0 0 2 5 0 0 0 latejugata Nodosaria affinis 3 0 0 0 0 2 0 0 0 0

Parrella expansa 7 3 2 0 0 5 10 1 0 0

Pyrgo sp. 0 0 2 0 10 0 0 0 0 0

Quinquloculina 0 0 0 1 0 0 0 0 0 0 Sp. Vaginulina 3 1 0 1 0 2 1 0 0 1 Midwayana Tritaxia pyramidata 0 2 0 0 0 0 0 0 0 0

Turritellela sp. 0 0 1 0 0 0 0 2 2 0

Total 22 20 30 6 17 20 20 37 78 52

236

APPENDIX N.

FORAMINIFERA TAXA IN THE OWL CREEK, CLAYTON, AND PORTERS

CREEK FORMATIONS

237

Owl Creek, Clayton, and Porters Creek Taxa

Anomalina elementiana (D’Orbigny) Franke Bathysiphon spp. M. Sars 1872 Bolvina incrassata (Reuss) Cushman, 1926 Dentalina gardnerae (Plummer) Cushman & D’Orbigny 1826 Discorbis midwayensis (Cushman) Lamarck 1804 Globigerina compressa (Plummer) D’Orbigny 1826 Globulina gibba D’Orbigny 1839 Globulina rotundata (Bornemann) Cushman and Ozawa Gyroidina depressa (Church) Cushman 1946 Nodogenerina bradyi Cushman 1927 Nodosaria latejugata (Gümbel) Lamarck 1812 Nodosaria affinis (Reuss) Cushman 1946 Parrella expansa (Toulmin) Finley 1939 Pyrgo spp. Quinqueloculina spp. D’Orbigny 1826 Vaginulina midwayana (Fox and Ross) D’Orbigny 1826 Tritaxia pyramidata Cushman 1926 Turritellela spp.

238

APPENDIX O.

ILUSTRATIONS OF FORAMINIFERA: PLATES 1 AND 2

239

PLATE 1 (Photomicrographs taken by Tambra Eifert)

A. Nodosaria affinis , slide CC0C-6, sample, FOC6, Owl Creek Formation.

B. Vaginulina midwayana , slide GL-G, sample FGLG, Glauconite Zone, Clayton Formation.

C. Nodosaria latejugata , slide GL-G, sample FGLG, Glauconite Zone, Clayton Formation.

D. Nodogenerina bradyi , slide GL-L, sample FGLL, Glauconite Zone Clayton Formation.

E. Parrella expansa , slide GL-G, sample FGLG, Glauconite Zone, Clayton Formation.

F. Gyroidina depressa , slide CL-1, sample FCL1, Coquina Zone, Clayton Formation.

G. Dentalina gardnerae , slide CCOC-2, sample FOC2, Owl Creek Formation.

240

241

PLATE 2 (Photomicrographs taken by Carl Campbell)

A. Anomalina sp., slide GL-L, sample FGLL, Glauconite Zone, Clayton Formation.

B. Parrella expansa , slide CCOC-1, sample FOC1, Owl Creek Formation.

C. Gyroidina depressa , slide GL-L, sample FGLL, Glauconite Zone, Clayton Formation.

D. Discorbis midwayensis , slide GL-L, sample FGLL, Glauconite Zone, Clayton.

E. Globulina rotundata , slide CL-1, sample FCL1, Coquina Zone, Clayton Formation.

F. Tritaxia pyramidata , slide CCOC-2, sample FOC2, Owl Creek Formation.

242

A B

C D

E F

243

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VITA

Tambra Lynn Eifert was born in Cape Girardeau, Missouri on September 13,

1959. She is the daughter of Charles Leon Eifert and Delores Selena Keesee-Eifert.

After completing her degree at Illmo-Scott City High School, Scott City, Missouri in

1978, Tambra worked as a secretary for the Department of Home Economics at Southeast

Missouri State University in Cape Girardeau, Missouri. During the fall of 1983, she entered Southeast Missouri State University as a major in the Department of Physical

Education and Recreation and completed her first Bachelor of Science degree in 1987.

From 1988 to the summer of 1992, Tambra worked for the Kansas City Missouri Mental

Health Department in Kansas City, Missouri as a Recreational Therapist and evening supervisor. During the fall of 1992, she chose to return back to Southeast Missouri State

University and begin working on a second Bachelor of Science degree in Geosciences.

In May of 1996, Tambra completed her second degree and graduated with Academic

Distinction. Tambra received both local and national recognition for her bachelor’s research project and appeared on the Discover Magazine program called ‘Hidden

Worlds’. Following her graduation in May of 1999, she entered graduate school at

Baylor University in Waco, Texas and completed her Master’s Degree in Geology.

Tambra served as a part-time instructor for the Geosciences Department at Southeast

Missouri State University from 1999 to 2000. In 2001, she began her graduate work for her doctorate in Geology at the University of Missouri Science and Technology in Rolla,

Missouri.