__p PATTERNS OF DjAGE

LOWER Atfr>MiDDU: PENNS V
Cover. Leached ilmenite grain approximately 60 microns in diameter surrounded by 

quartz overgrowth in Lower Pennsylvanian sandstone in Indiana. Quartz overgrowths 

occlude much of the pore space in these rocks. Sample collected by Paula Hansley, U.S. 

Geological Survey.
Patterns of Diagenesis in Lower and Middle

Pennsylvanian Sandstones of the

Illinois Basin, Illinois, Indiana, and Kentucky

By Paula L. Hansley

EVOLUTION OF SEDIMENTARY BASINS ILLINOIS BASIN 

Jennie L. Ridgley, Project Coordinator

U.S. GEOLOGICAL SURVEY BULLETIN 2094-E

A multidisciplinary approach to research studies of 

sedimentary rocks and their constituents and the 

evolution of sedimentary basins, both ancient and modern

UNITED STATES GOVERNMENT PRINTING OFFICE, WASHINGTON : 1996
U.S. DEPARTMENT OF THE INTERIOR 

BRUCE BABBITT, Secretary

U.S. GEOLOGICAL SURVEY 

Gordon P. Eaton, Director

For sale by U.S. Geological Survey, Information Services

Box 25286, Federal Center

Denver, CO 80225

Any use of trade, product, or firm names in this publication is for descriptive purposes only and 

does not imply endorsement by the U.S. Government

Library of Congress Cataloging-in-Publication Data

Hansley, Paula L.

Patterns of diagenesis in Lower and Middle Pennyslvanian sandstones of the Illinois 

Basin, Illinois, Indiana, and Kentucky / by Paula L. Hansley.

p. cm. (Evolution of sedimentary basins Illinois Basin ; E) 

(U.S. Geological Survey bulletin ; 2094)

Includes bibliographical references.

Supt.ofDocs.no.: I 19.3:2094-E

1. Sandstone Illinois Basin. 2. Geology, Stratigraphic Pennsylvanian. 

3. Diagenesis Illinois Basin. I. Title. II. Series. III. Series: U.S. Geological 

Survey bulletin ; 2094. 

QE75.B9 no. 2094-E 

[QE471.15.S25] 

557 s dc20

[552'5] 95-24635

CIP
CONTENTS

Abstract........................................................................................................................... El

Introduction..................................................................................................................... 1

Geologic Setting.............................................................................................................. 3

Stratigraphy..................................................................................................................... 4

Depositional Environment.............................................................................................. 4

Methods........................................................................................................................... 5

Description of Cores ....................................................................................................... 5

Detrital Petrology............................................................................................................ 13

Caseyville Formation and Mansfield Formation (lower part)................................. 13

Tradewater Formation and Equivalent Sandstones................................................. 14

Authigenic Petrology...................................................................................................... 14

Caseyville Formation and Mansfield Formation (lower part)................................. 14

Tradewater Formation and Equivalent Sandstones................................................. 15

Siderite.................................................................................................................... 19

Carbon and Oxygen Isotopes.......................................................................... 19

Composition.................................................................................................... 19

Interpretation................................................................................................... 19

Discussion....................................................................................................................... 21

Conclusions..................................................................................................................... 22

References Cited............................................................................................................. 22

Appendix Description of Cores ................................................................................... 25

FIGURES

1. Map of Illinois Basin showing major Pennsylvanian-age structural features and locations of coreholes ............ E2

2. Chart showing stratigraphy of Lower and Middle Pennsylvanian strata, Illinois Basin ....................................... 3

3. Generalized depiction of conglomerate of Caseyville Formation filling channel cut into Mississippian strata... 4

4. Photomicrographs of rock fragments in Lower Pennsylvanian sandstones.......................................................... 12

5. Scanning electron micrograph showing dissolution of potassium feldspar .......................................................... 12

6-8. Photomicrographs of:

6. Tar and pyrite at grain contacts .................................................................................................................... 12

7. Tar under quartz overgrowth ........................................................................................................................ 13

8. Tar in dissolution vug in ankerite................................................................................................................. 13

9. Diagram showing paragenetic sequence for authigenic mineral phases in Tradewater Formation

and equivalents............................................................................................................................................. 13

10-12. Photomicrographs of:

10. "Wheat seed" siderite................................................................................................................................... 13

11. Siderite in deformed muscovite flake........................................................................................................... 14

12. Botryoidal siderite after aragonite(?)........................................................................................................... 15

13. Scanning electron micrograph of quartz overgrowths preserving primary porosity.............................................. 15

14. Cathodoluminescence micrograph of quartz overgrowths in sandstone................................................................ 16

15, 16. Photomicrographs of:

15. Detrital quartz grains with corroded edges .................................................................................................. 16

16. Albite overgrowth on sericitized plagioclase ............................................................................................... 16

17, 18. Scanning electron micrographs of:

17. Authigenic kaolinite..................................................................................................................................... 17

18. Authigenic illite on kaolinite........................................................................................................................ 17

III
IV CONTENTS

19. Sketch of siderite concretion.................................................................................................................................. 17

20-22. Photographs of:

20. Siderite laminae in tidalite sequence............................................................................................................ 17

21. Siderite bed ........................................................................................................................................ 18

22. Siderite breccia fragments in channel sandstone ......................................................................................... 18

TABLES

1. Location of cores in the Illinois Basin that were sampled and described ............................................................. E5

2-4. Modal analyses of selected thin sections of sandstones from cores:

2. Indiana.......................................................................................................................................................... 6

3. Illinois....................................................................................................................................................^ 9

4. Kentucky ...................................................................................................................................................... 11

5. Carbon and oxygen isotope analyses of authigenic siderite in cores of the Lower and Middle

Pennsylvanian Tradewater Formation and equivalent rocks, Illinois Basin.......................................................... 18

6. Composition of siderite cement in sandstones of the Lower and Middle Pennsylvanian

Tradewater Formation from the Greene County, Indiana, core............................................................................. 19

7. Composition of siderite from the study area......................................................................................................... 20

8. Composition of ankerite cement in sandstones of the Lower and Middle Pennsylvanian

Tradewater Formation and equivalent rocks, Illinois Basin.................................................................................. 20
Patterns of Diagenesis in 

Lower and Middle Pennsylvanian Sandstones

of the Illinois Basin, 

Illinois, Indiana, and Kentucky

By Paula L. Hansley

ABSTRACT

Rapid facies changes and early diagenetic cementation 

that reduced porosity and permeability limited fluid flow 

through Lower and Middle Pennsylvanian sandstones in the 

Illinois Basin. Basal Pennsylvanian quartzarenites were 

deposited in deep, fluvial channels incised into Mississippian strata. Abundant silica cement in these sandstones 

reflects their simple detrital mineralogy. Younger Pennsylvanian sublitharenites were deposited in a variety of environments on a tidally influenced coastal plain. Abundant 

organic matter, including peat in numerous swamps, created 

an anoxic environment in these sandstones. Early diagenesis 

was dominated by microbially catalyzed reactions such as 

sulfate reduction and methanogenesis. Organic acids produced in these early reactions greatly increased the solubility 

of aluminosilicates and quartz, and high alkalinity and iron 

activity resulted in precipitation of abundant siderite. Sandstones adjacent to those containing siderite developed a high 

volume percentage of quartz overgrowths due to local movement of silica. Ankerite and calcite formed slightly later, and 

kaolinite locally filled in voids. Carbon isotope and compositional analyses of syndepositional and early diagenetic siderite reveal that sandstone pore waters were predominantly 

fresh to brackish and became more saline as burial proceeded.

Early siderite and quartz cements remained stable 

throughout the postdepositional history of these sandstones, 

and they lowered permeability and restricted fluid flow. 

Low diagenetic temperatures due to shallow burial and erosion of overlying strata helped to preserve early cements. As 

a result, diagenetic assemblages in Lower and Middle Pennsylvanian sandstones in the Illinois Basin were controlled 

mostly by the detrital mineralogy of the sandstone and by the 

depositional environment rather than by later diagenesis and 

basinwide fluid flow.

INTRODUCTION

As part of a multidisciplinary effort to examine the geologic evolution of the Illinois Basin (Haney and others, 

1992), Lower and Middle Pennsylvanian sandstones were 

examined for evidence of regional diagenetic and fluid-flow 

patterns. The late Paleozoic was a time of fluid movement 

that resulted in mineralization in the fluorspar district of 

southern Illinois, formation of zinc-lead deposits in the 

Upper Mississippi Valley District of southern Wisconsin, 

and migration of hydrocarbons throughout the Illinois Basin. 

In addition to a number of oil fields in Carboniferous rocks, 

a large tar-sand accumulation in Mississippian and Lower 

Pennsylvanian rocks in west-central Kentucky contains at 

least 3.4 billion barrels of heavy oil in-place (Hamilton-Smith, 1990). Disagreement exists as to whether fluids 

migrated basinwide (Goetz and others, 1992; Goldhaber and 

others, 1994; Pitman and others, 1994) or fluid movement 

was limited to local convection cells (Spirakis, 1994; Spirakis and Heyl, 1995).

Although many aspects of Pennsylvanian sandstones in 

the Illinois Basin have been studied in detail, including the 

detrital petrology and provenance (Potter and Siever, 1956a, 

b), clay mineralogy (Hughes and others, 1985), and depositional environment (Kvale and Barnhill, 1994), their diagenesis has only recently been examined (Hansley, 1992, 1994; 

Barnhill and Hansley, 1993; Hansley and others, 1993). 

Diagenetic mineral assemblages provide clues as to the 

types of fluids that migrated through the sandstones and can 

reveal the timing of petroleum migration. Reconstructing the 

history of fluid movement is important because economically important low-sulfur coals and significant petroleum 

reservoirs in paleovalley deposits are contained within 

Lower and Middle Pennsylvanian rocks throughout the Illinois Basin (Kvale and others, 1992).

Previous petrologic studies show that basal Pennsylvanian sandstones are relatively clean pebbly quartzarenites

El
E2 EVOLUTION OF SEDIMENTARY BASINS ILLINOIS BASIN

96° 94° 92° 90°

0 50 MILES

0 100 KILOMETERS

MISSISSIPPI EMBAYMEIMT KENTUCKY

40° -

38° -

36° -

Figure 1. Map of the Illinois Basin showing the location of major structural features in Pennsylvanian time and coreholes sampled and 

described for this study; shaded area around Illinois Basin represents outcrop of Pennsylvanian rocks. Indiana corehole designations:S, Sullivan County; G, Greene County. Illinois corehole designations: S4, Sangamon County; P, Perry County; PO, Pope County; W4, Williamson County; SAL, Saline County. The four Kentucky coreholes (K) are represented by a single dot because they are close together. Samples 

from 14 coreholes collected in the Naval Surface Warfare Center (NSWC) near Crane, Indiana, were also studied. Locations of coreholes

that grade upward into matrix-rich sandstones (Hopkins, 

1895; Gault, 1938; Siever, 1949; Siever and Potter, 1956; 

Rusnak, 1957; Potter and Glass, 1958; Greenberg, 1960). 

Houseknecht and Wood (1992) concluded that much of the 

matrix constitutes fine-grained metamorphic rock 

fragments; this conclusion is supported by data presented 

herein. The basal quartzose sediments probably originated in 

the northern Appalachians in the area of northern New 

England, northern New York, and southeastern Quebec 

where Proterozoic through Mississippian metaquartzite, 

vein quartz, and quartz sandstone and conglomerate are 

present (Nelson, 1989). Crossbedding measurements and 

petrographic data show that the overlying, more lithic 

sediments were derived from the Canadian Shield (north and

northwest) (Seal, 1990), Appalachian Basin (northeast), and 

(or) the Transcontinental arch (west) (Potter and Pryor, 

1961; Potter, 1962, fig. 9). The relatively high metamorphic 

lithic content signals the beginning of the Alleghanian orogeny.

Acknowledgments. I would like to thank Mark Barnhill and Erik Kvale of the Indiana Geological Survey for 

their help in identifying sedimentary environments in Lower 

and Middle Pennsylvanian rocks. John Nelson of the Illinois 

Geological Survey assisted me in selecting core in Illinois to 

study. Sherry Kazee of the Indiana Geological Survey core 

library and Patrick Gooding of the Kentucky Geological 

Survey core library helped immensely with retrieving core. 

Theresa Cookro of the U.S. Geological Survey kindly read
PATTERNS OF DIAGENESIS IN PENNSYLVANIAN SANDSTONES E3

CO

LU

DC 

LU

co ,

MIDDLE PENNSYLVANIAN

LOWER PENNSYLVANIAN

PROVINCIAL 

SERIES

Desmoinesian

c

CO

^.

o

<

-1

Morrowan

rbondale 

Group

CO

O

0.

Z> 

0

DC 

O

^.

LU 

LU 

DC 

O

~z. 

0 

0 

o 

o 

<

DC

INDIANA

Linton Formation 

(Colchester coal)

Staunton Formation

Brazil Formation

Formation Id 

Mansfie

Upper part

Middle part

"Pinnich" zone

Lower part

KENTUCKY

Carbondale Formation 

(Davis coal)

Tradewater 

Formation

Caseyville Formation

ILLINOIS

Carbondale Formation 

(Seelyville coal)

Tradewater 

Formation

Caseyville Formation

Figure 2. 

fig. I)-

Stratigraphy of Lower and Middle Pennsylvanian rocks in the Illinois Basin. Modified from Purer and Droste (1993,

earlier drafts of this manuscript and offered valuable suggestions. Technical reviews by Dave Macke, Jennie Ridgley, 

and Janet Pitman also greatly improved the manuscript.

GEOLOGIC SETTING

The Illinois Basin, which encompasses parts of Illinois, 

Indiana, and Kentucky, initially developed as a result of the 

formation of the New Madrid rift complex in Late 

Proterozoic to Early Cambrian time (Kolata, 1993). Since 

then, it has evolved as a consequence of various periods of 

tectonic activity from a failed rift basin, to a cratonic embayment, and finally to an interior cratonic basin. The rift 

complex has greatly influenced subsidence, sedimentation 

rate, depositional environment, formation of structures, and 

earthquake activity (Kolata and Nelson, 1993a). The present 

configuration of the basin formed after uplift of the Pascola 

arch just to the south of the Mississippi embayment in

post-Pennsylvanian to Late Cretaceous time (Buschbach 

and Kolata, 1993). One way in which the basin is defined is 

by outcrops of Pennsylvanian rocks, the oldest pre-Quaternary rocks (fig. 1). By this definition, the basin is bordered 

by the Wisconsin arch on the north, the Kankakee arch on 

the northeast, the Cincinnati arch on the southeast, the Mississippi embayment to the south, the Ozark dome on the 

southwest, and the Mississippi River arch on the west. The 

deepest part of the basin (21,000 ft [6,774 m] to the top of 

the Precambrian) is in the Fairfield subbasin, which is in 

northwestern Kentucky just south of the point at which all 

three States join (Buschbach and Kolata, 1993, fig. 1-7). 

During the late Paleozoic, concurrent with the breakup of 

the Pangea supercontinent, the AJleghanian and Wichita 

orogenies created compressional stresses that reactivated 

faults such as the Rough Creek-Shawneetown fault system 

in western Kentucky and the Cottage Grove fault system in 

southern Illinois and caused the La Salle anticline to form 

along the eastern side of the basin and the Mississippi River
E4 EVOLUTION OF SEDIMENTARY BASINS ILLINOIS BASIN

EXPLANATION 

Limestone

Conglomerate

Figure 3. Generalized depiction of conglomeratic sandstone 

of the Casey ville Formation filling channel cut into Mississippian strata in west-central Kentucky. Black areas represent 

tar-saturated sandstone. Modified from McGrain (1976).

arch to emerge along the western margin of the basin (Kolata 

and Nelson, 1993a, b).

Pennsylvanian rocks are overlain by Quaternary glacial 

sediments, which extend southward to the Shawnee Hills of 

southern Illinois, in most of the basin. The maximum thickness (>2,800 ft, >903 m) of Pennsylvanian strata is in western Kentucky. Pennsylvanian rocks include interbedded 

sandstone, siltstone, shale, low-sulfur coal (<1 percent), and 

underclay. Carbonized plant debris is common in most 

facies. An unknown amount of erosion occurred in Permian 

to Early Cretaceous time. Damberger (1971, 1989) 

concluded on the basis of vitrinite reflectance that the

Pennsylvanian section has been buried less than 3 km in the 

deepest part of the basin. In a drillhole in the western Kentucky coalfield, about 390 ft (126 m) of the Mauzy Formation containing Lower Permian fusulinids was intercepted in 

a fault block. Structural data suggest that the formation may 

be as thick as 1,300 ft (419 m) (Kehn and others, 1982).

STRATIGRAPHY

Lower and Middle Pennsylvanian rocks rest 

unconformably on Devonian to Mississippian strata 

throughout the Illinois Basin (Kvale and others, 1989). 

Relief on the unconformity is as much as 434 ft (140 m). In 

Indiana, the interval from the base of the Lower Pennsylvanian to the base of the Carbondale Group is known as the 

Raccoon Creek Group (Purer and Droste, 1993, fig. 1) (fig. 

2). The Casey ville Formation, which locally is present in 

paleochannels filled with conglomeratic sandstone, is the 

oldest Pennsylvanian formation in western Kentucky and 

Illinois (fig. 3). Equivalent strata in western Indiana are 

assigned to the lower part of the Mansfield Formation (Nelson, 1993, fig. 1). In western Kentucky and southeastern Illinois, strata between the Caseyville Formation and the Davis 

No. 6 coal at the base of the Carbondale Group are designed 

the Tradewater Formation. In western Indiana, strata equivalent to the Tradewater Formation above the lower part of 

the Mansfield Formation are designated as, in ascending 

order, the middle and upper parts of the Mansfield Formation 

and the Brazil and Staunton Formations.

The south and southwest paleoslope during earliest 

Pennsylvanian time (Potter, 1962) is reflected by flow directions of fluvial channels filled by quartzose and 

conglomeratic sediments of the Caseyville Formation or 

equivalent lower part of the Mansfield Formation. Pennsylvanian rocks slope 19.6-29.3 ft/mi (3.8-5.7 m/km) from 

western Indiana toward the center of the basin (Hutchison, 

1967). Correlations within Lower and Middle Pennsylvanian 

strata are extremely difficult because of rapid facies changes 

and a lack of good marker horizons. In the past, correlations 

were made using coal beds as marker horizons; however, 

recent mapping shows that most coal beds are not continuous 

over very long distances.

DEPOSITIONAL ENVIRONMENT

The Illinois Basin was located at about lat 5° S. in Early 

to Middle Pennsylvanian time (Kvale and others, 1992). In 

earliest Pennsylvanian time, deep incised valleys were filled 

with quartzose, conglomeratic sediments of the Caseyville 

Formation and the lower part of the Mansfield Formation. 

Recent sedimentologic and paleontologic studies of the 

overlying interval represented by the middle part of the 

Mansfield through the lower part of the Staunton Formation 

in Indiana show that the interval constitutes marine and tidal 

sediments deposited in a coastal setting (Kvale and Archer, 

1990). The interval was originally defined by Potter (1962)
PATTERNS OF DIAGENESIS IN PENNSYLVANIAN SANDSTONES E5

Table 1. Locations of cores in the Dlinois Basin that were sampled and described.

[Locations of coreholes shown in figure 1. Designations for wells in Illinois and Indiana were chosen for this report]

Well name Operator Location

Illinois

P 

PO 

SAL 

S4 

W4

J.H. Forester 

Illinois Geological Survey 

Illinois Geological Survey 

Madison Coal Corporation 

Illinois Geological Survey

NW^SWKNW1/* sec. 5, T. 6 S., R. 1 W., Perry County. 

NEHNWVi sec. 8, T. 1 1 S., R. 6 E., Pope County. 

Sec. 33, T. 10 S., R. 6 E., Saline County. 

NW%SW'/4 sec. 15, T. 13 N., R. 5 W., Sangamon County. 

Sec. 29, T. 10 S., R. 4 E., Williamson County.

Indiana

G 

S

Clarence Haskins 

Indiana Geological Survey

SWttSEttSWVi sec. 27, T. 8 N., R. 6 W., Greene County. 

NW'/^NE^NE1/* sec. 28, T. 7 N., R. 9 W., Sullivan County.

Edmonson County, Kentucky

Vincent No. 13 

Vincent No. 27 

Vincent No. 28 

Raymond Carroll No. 19

Marathon Oil Company 

Marathon Oil Company 

Marathon Oil Company 

Marathon Oil Company

Lat37°lTN.,long86°42'W. 

Lat37°17N.,long86°45'W. 

Lat 37°15' N., long 86°44' W. 

Lat 37° 1 1 1 N., long 86°50' W.

as a fluvial-dominated system characterized by cyclic 

nonmarine sedimentation. Kvale and others (1992) 

demonstrated, however, that tide-dominated estuarine 

deposits (marine and nonmarine) in Morrowan rocks of 

western Indiana include thinly (1 mm) laminated, 

semimonthly (neap-neap) to yearly tidal bundles of siltstone 

and claystone. Herringbone cross-stratification that is 

present in shale-dominated sequences is also characteristic 

of most tidal deposits. Associated depositional environments 

include tidally influenced channels, intertidal-supratidal 

swamps and peat mires, subtidal-intertidal sand- and (or) 

mud-dominated tidal flats, and transgressive marine muds 

(Barnhill, 1992). A marine shale referred to as the "Pinnick 

zone" (Purer and Droste, 1993) (see fig. 2) can be correlated 

throughout western Indiana. The presence of 

saline-dependent invertebrates (Devera and others, 1992) 

and other marine to brackish-water fossils, such as 

conodonts, acritarchs, and linguloid brachiopods, in many of 

the shales is evidence of a marine environment (Fishbaugh 

and others, 1989; Howard and Whitaker, 1990). Low-sulfur 

coals, which formed in this marine-influenced setting, may 

have been preserved by rapid burial of peat (Nelson, 1993).

Facies fluctuations were probably caused by a 

combination of tectonic and eustatic factors. The cyclicity of 

sedimentation in Pennsylvanian to Early Permian time may 

have been due to global fluctuations in sea level caused by 

glacial-interglacial periods in the Southern Hemisphere 

(Ross and Ross, 1985; Heckel, 1986).

METHODS

Sandstone samples were collected from seven cores of 

the Tradewater Formation and equivalent strata in Illinois 

and western Indiana and from four cores of the Caseyville 

Formation in western Kentucky. The Illinois cores were 

selected because they are in a line extending from the 

relatively shallow part of the basin southward to the deepest 

part of the basin (fig. 1). Samples from 14 cores of the

Mansfield Formation, collected in the Naval Surface 

Warfare Center (NSWC) near Crane, Indiana (just southeast 

of the Greene County core), were included as part of the 

study. Descriptions and interpretations of the NSWC cores 

are in Barnhill (1992), Barnhill and Kvale (in press), and 

Barnhill and Hansley (1993).

Petrographic thin sections of sandstone samples from 

these cores were impregnated with blue-dyed epoxy and 

stained with Alizarin-Red S for calcite identification, potassium cobaltinitrite for potassium feldspar identification, and 

potassium ferricyanide for ferroan calcite or ankerite determination. Each sample was given a number that corresponds 

to the depth from which it was taken in the core. Point counts 

(300 per thin section) were made of selected thin sections 

from each core. Siderite cement, beds, and nodules were collected for carbon and oxygen isotope analyses to determine 

the geochemistry of groundwater during deposition and 

early diagenesis. Siderite samples chosen for stable oxygen 

and carbon isotope analyses were drilled from core samples, 

ground, and analyzed by X-ray powder diffraction to determine if they were pure siderite.

Representative samples were examined with the petrographic microcope under transmitted and reflected light, a 

JEOL JSM-840 scanning electron microscope with an 

attached Tracer Northern (TN-5500) energy-dispersive 

X-ray analysis system, a luminoscope, and a JOEL electron 

microprobe with an attached wavelength dispersive analysis 

system. X-ray powder diffraction (bulk, glycolated, and 

550°C) was used to characterize the -2-micron fraction (clay 

fraction) of selected samples.

DESCRIPTION OF CORES

Two cores from Indiana, five cores from Illinois, and 

three cores from Kentucky were described during this study 

(table 1, appendix). The Raymond Carroll No. 19 core (C19
Table 2. Modal analyses of selected thin sections of sandstones from Indiana cores as determined by point counts. 

[Location of core holes shown in figure 1. Core designations given in table 1; number after core designation refers to sample depth (in feet)]

Sample No.

G-23.5

G-31.5

G-67.3

G-71.5

G-91.5

G-93.1

G-94

G-130.5

G-144.5

G-153

G-200

G-210

G-220

G-228

G-237.5

G-240

G-247

G-253

G-269

G-280

G-282.5

G-298

G-318

G-333

G-340

G-353

G-386

G-^06

G-420.3

G-^58

Phi

2.75

3.25

3.5

3.25

2.8

3.1

3.25

3.5

3

3.5

3.25

3.25

3

3

2.5

2.7

2.7

3.1

3.75

3.75

3.25

3.5

3

2.5

2

2.2

3.1

2.5

3.75

2.5

Polycrystalline 

Quartz quartz

191

148

202

190

159

67

187

146

155

163

206

207

195

204

185

226

201

230

180

225

183

211

211

214

201

211

213

200

180

117

13

5

1

12

16

11

10

4

19

25

5

6

6

6

7

0

2

1

1

2

4

5

8

15

7

10

8

16

15

4

Potassium 

feldspar

12

12

2

5

22

5

6

6

5

3

9

5

4

4

0

0

0

2

9

4

5

2

4

4

2

1

3

1

9

1

Plagioclase

1

1

0

1

4

4

2

1

12

4

0

0

2

0

1

1

2

2

3

3

1

2

2

1

1

3

0

3

6

0

Igneous 

rock frag.

0

4

0

0

11

1

0

0

3

1

2

1

1

4

0

1

1

0

5

2

0

1

0

2

1

0

0

0

0

0

Meta. 

rock frag.

1

9

5

4

15

4

10

5

3

9

7

10

7

4

8

5

3

11

5

5

10

7

6

11

6

8

0

0

2

0

Sed. 

rock frag.

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

1

0

0

0

1

1

0

0

0

0

Altered 

rock frag.

5

7

2

3

1

4

8

3

11

1

5

6

3

4

6

1

2

1

9

5

6

5

5

2

10

2

0

0

1

1

Chert

3

6

2

2

3

1

0

0

20

1

2

2

2

1

5

1

1

0

5

3

3

4

3

0

1

3

2

2

6

0

Detrital 

clay

5

98

1

10

1

29

1

4

21

6

2

2

0

1

14

0

0

1

5

5

8

1

5

6

2

2

47

4

12

46
Table 2. Modal analyses of selected thin sections of sandstones from Indiana cores as determined by point counts Continued.

Sample No.

G-23.5

G-31.5

G-67.3

G-71.5

G-91.5

G-93.1

G-94

G-130.5

G-144.5

G-153

G-200

G-210

G-220

G-228

G-237.5

G-240

G-247

G-253

G-269

G-280

G-282.5

G-298

G-318

G-333

G-340

G-353

G-386

G-406

G-^20.3

G-^58

Organic 

matter

0

1

10

0

1

50

3

2

0

0

0

1

1

0

0

0

0

0

0

0

0

0

5

0

0

0

8

0

6

3

Iron 

oxide

0

0

0

1

0

4

0

2

0

0

0

0

0

0

2

0

0

0

0

2

0

0

0

0

0

0

0

0

0

4

Kaolinite

7

0

2

3

0

10

2

0

9

4

8

1

2

2

7

3

10

2

1

0

0

4

0

3

5

3

0

1

1

1

Authigenic 

chlorite

0

1

14

0

4

0

0

0

0

0

1

0

4

0

0

0

1

1

1

1

3

0

0

0

0

0

0

0

0

7

Sericite

0

0

0

0

0

0

0

2

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

Calcite

0

0

2

3

1

0

0

0

2

13

0

0

0

0

0

4

1

3

0

0

1

3

0

0

0

5

0

6

0

0

Ankerite

0

0

0

0

0

0

24

0

0

0

0

0

1

0

0

0

0

0

0

0

0

0

0

0

4

0

0

0

0

0

Siderite

0

0

6

0

0

95

0

121

0

0

0

0

19

0

8

0

38

2

16

1

0

0

0

0

0

0

3

0

1

95

Quartz 

overgrowth

30

0

9

9

15

0

7

0

11

16

13

14

4

7

6

10

2

8

1

2

1

5

2

10

15

3

6

36

37

8

Albite 

overgrowth

0

0

0

0

0

0

0

0

6

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

Pyrit

0

0

0

0

0

0

0

0

0

1

0

1

0

0

0

0

0

0

0

0

0

0

1

1

0

0

0

0

11

0
Table 2. Modal analyses of selected thin sections of sandstones from Indiana cores as determined by point counts Continued.

Polycrystalline Potassium

Sample No.

S-726.5

S-741

S-744

S-754

S-788

S-789.5

S-825.5

S-879

S-881.2

S-924

S-942

Sample No.

S-726.5

S-741

S-744

S-754

S-788

S-789.5

S-825.5

S-879

S-881.2

S-924

S-942

Phi

2

2

3.25

2.75

2

2.75

3.25

2.75

2.75

3.5

2.5

Organic

matter

0

0

1

1

0

0

1

0

0

12

0

Quartz

191

191

159

218

201

181

226

194

229

197

234

Iron

oxide

0

0

0

0

0

0

0

0

0

0

0

quartz

2

0

1

8

15

10

5

13

3

2

1

Kaolinite

0

4

7

0

10

7

9

0

0

3

1

feldspar

7

0

0

0

0

0

3

0

0

1

0

Authigenic

chlorite

0

2

0

1

0

0

0

0

0

0

0

Plagioclase

0

4

1

0

1

4

1

3

4

0

0

Sericite

0

0

0

0

0

0

0

0

0

0

0

Igneous

rock frag.

0

3

3

0

0

1

0

0

3

0

0

Calcite

0

0

0

0

9

9

0

0

0

0

0

Meta.

rock frag.

2

2

8

2

1

10

0

1

4

0

0

Ankerite

0

1

2

0

0

0

0

0

0

0

0

Sed.

rock frag.

0

0

0

0

0

0

0

0

0

0

0

Siderite

67

68

101

0

25

2

0

3

3

41

0

Altered

rock frag.

8

10

8

1

1

8

2

1

1

1

1

Quartz

overgrowth

3

0

1

10

0

8

48

17

1

0

2

Chert

1

2

4

0

0

2

2

1

2

0

1

Albite

overgrowth

0

0

0

0

0

0

0

0

0

0

0

Detrita

clay

0

1

0

1

9

8

1

3

2

35

32

Pyrite

0

0

0

3

2

0

0

1

0

2

0
Table 3. Modal analyses of selected thin sections of sandstones from Illinois cores as determined by point counts. 

[Location of core holes shown in figure 1. Core designations given in table 1; number after core designation refers to sample depth (in feet)]

Sample No.

PO-43

PO-55

PO-62

PO-70

PO-86.5

PO-93

PO-106

PO-136

P-200

P-271

P-282

P-299

P-318

P-318

P-332

P-334

P-387

P-392

P^Ol

S4-437

S4-479

S4-554

S4-566

S4-568.5

S4-583.5

S4-598

S4-609

S4-620

S4-626

S4-675.1

W4-8

W4-21.5

W4-94.8

W4-100

W4-200

SAL-11

SAL-22

SAL-31

SAL-37

SAL-91.5

SAL-94.5

SAL-108

SAL-189

Phi

1.75

2.75

2.5

1.5

3

2.8

3.75

3.2

2

2.25

2.5

2.5

2.2

2.2

2.5

2.2

2.5

1.5

1.75

3

3.9

2.3

2.6

3

3

2.6

2.9

3.25

3.5

2.5

2.25

2.2

3

3

2.2

2.8

2.5

2.2

2.2

2.8

3.25

3

1.5

Polycrystalline 

Quartz quartz

194

205

205

168

199

233

196

212

148

128

115

191

155

169

161

179

174

220

166

190

146

181

187

196

197

190

150

208

197

194

160

165

160

162

182

141

153

120

134

96

125

155

170

31

18

18

19

18

8

9

13

33

39

34

20

22

19

19

16

11

17

23

22

10

6

9

7

3

4

12

8

2

7

5

10

6

5

4

8

25

59

48

14

5

35

18

Potassium 

feldspar

2

1

1

6

0

0

0

0

32

23

17

13

15

5

14

10

1

0

9

9

7

3

0

1

2

1

0

3

6

5

15

0

15

17

0

11

16

23

25

1

0

0

0

Plagioclase

1

3

0

1

0

0

0

0

11

4

9

0

0

1

0

0

2

0

3

5

0

1

0

1

1

4

0

0

2

3

10

12

11

10

0

0

0

0

0

1

4

7

2

Igneous 

rock frag.

1

0

0

0

0

0

0

0

0

0

5

0

0

0

0

0

0

0

0

1

1

0

0

0

0

1

0

0

0

1

1

2

1

0

2

0

1

3

1

1

1

2

0

Meta. 

rock frag.

8

7

6

3

0

5

0

10

0

9

17

10

5

6

9

4

9

4

13

4

10

1

4

0

1

1

2

0

5

1

18

10

13

8

3

7

10

9

12

0

6

9

7

Sed. 

rock frag.

0

4

2

1

0

3

0

0

0

0

2

0

3

0

0

0

0

0

0

0

0

1

0

0

0

0

0

0

0

1

0

2

0

0

5

0

3

1

0

5

15

3

0

Altered 

rock frag.

6

11

10

8

0

6

3

4

0

8

5

2

6

7

1

1

9

0

7

1

2

1

1

2

3

3

1

6

2

2

7

2

6

2

6

8

5

9

7

2

10

10

7

Chert

1

2

2

4

2

1

2

1

0

7

7

4

8

9

6

9

10

3

4

5

7

10

0

1

0

6

3

4

1

1

8

8

9

8

3

3

2

6

4

2

6

4

5

Detrital 

clay

9

5

14

10

65

13

46

27

28

2

1

0

2

0

36

0

24

2

10

19

107

61

53

56

0

67

29

57

62

0

2

11

41

42

16

56

5

2

10

164

7

38

8
Table 3. Modal analyses of selected thin sections of sandstones from Illinois cores as determined by point counts 

Continued.

Sample No.

PO-43

PO-55

PO-62

PO-70

PO-86.5

PO-93

PO-106

PO-136

P-200

P-271

P-282

P-299

P-318

P-318

P-332

P-334

P-387

P-392

P^31

S4-437

S4-479

S4-554

S4-566

S4-568.5

S4-583.5

S4-598

S4-609

S4-620

S4-626

S4-675.1

W4-8

W4-21.5

W4-94.8

W4-100

W4-200

SAI^ll

SAL-22

SAL-31

SAL-37

SAL-91.5

SAL-94.5

SAI^IOS

SAL- 189

Organic 

matter

0

0

0

7

0

0

0

0

0

0

0

0

0

0

0

0

0

1

0

0

0

2

8

0

2

2

0

0

0

0

0

1

0

1

0

0

0

0

0

2

1

2

0

Iron 

oxide

0

0

0

0

0

0

0

0

0

0

0

0

0

0

2

0

0

0

0

0

0

4

1

0

0

0

7

8

1

0

0

0

0

0

0

0

0

0

0

0

0

0

0

Kaolinite

1

1

3

4

0

0

2

1

7

10

8

7

5

8

6

1

1

1

2

1

0

0

0

0

0

0

1

0

0

0

6

5

0

1

1

1

19

30

0

0

1

4

26

Calcite

0

0

0

0

0

0

0

0

0

0

1

7

0

0

0

1

0

0

0

1

0

0

0

1

1

0

2

0

0

2

0

0

2

0

17

0

0

0

1

0

1

0

2

Iron 

calcite

0

0

0

0

0

0

0

1

0

7

58

9

8

8

4

51

0

0

0

7

0

0

3

0

0

0

5

0

0

15

0

0

1

0

23

9

6

4

21

0

108

6

32

Siderite

24

0

0

15

13

0

19

0

2

47

0

0

55

42

38

0

0

4

0

0

0

1

3

2

27

0

62

0

0

0

0

0

0

0

3

39

0

0

0

0

0

1

0

Quartz 

overgrowth

8

5

7

0

1

9

7

14

1

1

9

30

0

0

0

25

7

0

1

6

0

4

4

0

1

0

0

0

0

21

9

15

13

2

7

0

8

2

1

0

0

1

6

Pyrite

0

0

4

47

0

0

2

0

0

0

0

2

0

0

0

2

16

0

0

0

2

0

1

1

0

1

0

0

4

0

0

0

0

0

0

0

20

0

2

0

0

0

2

Void

14

36

12

5

1

21

6

14

9

1

9

12

12

15

2

0

33

47

47

26

12

21

21

17

25

12

15

0

6

46

44

34

2

5

24

2

16

15

15

0

0

8

9
Table 4. Modal analyses of selected thin sections of sandstones of the Caseyville Formation from cores in Edmonson County, Kentucky, 

as determined by point counts.

[Location of core holes shown in figure 1. Core designations: V13, Vincent No. 13; V27, Vincent No. 27; V28, Vincent No. 28; C19, Raymond Carroll No. 19; 

number after core designation refers to sample depth (in feet)]

Sample No.

V13-110.8

V13-113.7V13-133.5

V13-286.5V27-20.5

V27-24.5

V28-101

C19-150C19-155.5

Sample No.

V13-110.8V13-113.7V13-133.5

V13-286.5

V27-20.5V27-24.5

V28-101

C19-150C19-155.5

Phi

1

2.2

1.751.251.51.251.5

2.5

1.75

Detrital 

clay

0

2

00006

20

0

Polycrystalline 

Quartz quartz

207

238231

186

207210200242238

Muscovite

00

1

00

00

2

0

31

10

12

54

2

1110

1

4

Heavy 

mineral

000

0

00

1

00

Potassium 

feldspar

23

300005

0

Kaolinite

62

1

2

5

1

8

1

4

Plagioclase

1

000

1

0

1

00

Calcite

000

14

00000

Sed. 

rock frag.

0

1

11

0

1

000

Ankerite

000

0

00002

Igneous 

rock frag.

00

00000

00

Quartz 

overgrowth

30

0

0

1913

2

12

5

Meta 

rock frag.

0

42

0

1

0

00

1

Pyrite

0

00

20

000

00

Altered 

rock frag.

13

2300

02

00

Oil

000

0

51

41

0

1114

Chert

1

032

6

3

2

0

1

Void

353841

21

8

20

68

4

31

O

T1DO WW0000Z

m

r

O

OT3

won
E12 EVOLUTION OF SEDIMENTARY BASINS ILLINOIS BASIN

Figure 4. Photomicrographs of rock fragments in Lower Pennsylvanian sandstones from the Illinois Basin. Locations of coreholes shown 

in figure 1. A, Schist (s) from the Tradewater Formation; Saline County, Illinois, core, 91.5 ft; field length, 0.8 mm. B, Chloritic rock fragment (c) from the Caseyville Formation; Vincent No. 13 core, Kentucky, 98.5 ft; field length 1.4 mm.C, Metaquartzite from the lower part 

of the Mansfield Formation; Greene County, Indiana, core, 237.5 ft; field length 1.4 mm. D, Igneous fragment with feldspar grains (f) from 

the Caseyville Formation; Vincent No. 13 core, Edmonson County, Kentucky, 98.5 ft; field length 1.4 mm, crossed polars.

Figure 5. Scanning electron micrograph of detrital potassium 

feldspar (k) showing evidence of dissolution in a sandstone from 

the Lower and Middle Pennsylvanian Mansfield Formation in a 

core from the Naval Surface Warfare Center near Crane, Indiana 

(fig. 1). Field length 0.4 mm.

Figure 6. Photomicrograph of tar (t) and pyrite (p) at contacts between quartz grains (q) in the Lower Pennsylvanian Caseyville 

Formation; Vincent No. 27 core, 24.5 ft, Edmonson County, Kentucky (fig. 1). Calcite (c) fills pores. Plane-polarized light, field 

length 3.3 mm.
PATTERNS OF DIAGENESIS IN PENNSYLVANIAN SANDSTONES

EARLY DIAGENESIS

Figure 7. Photomicrograph of black tar (arrows) under quartz 

overgrowths (qo) in the Lower Pennsylvanian Caseyville Formation; Vincent No. 27 core, 20.5 ft, Edmonson County, Kentucky 

(fig. 1). Tar fills voids, and some quartz grains show dissolution 

(arrow). Plane-polarized light, field length, 1.4 mm.

Figure 8. Photomicrograph of tar (t) in dissolution vug in ankerite (blue-green area) in the Lower Pennsylvanian Caseyville Formation; Raymond Carroll No. 19 core, 155.8 ft, Edmonson County, 

Kentucky (fig. 1). q, detrital quartz grains; qo, quartz overgrowths. 

Plane-polarized light, field length 0.4 mm.

Organic acids 

Siderite 

Dissolution 

Calcite 

Pyrite 

Ankerite

Quartz overgrowths 

Albite overgrowths -1

Kaolinite Meteoric water

Illite/smectite

E13

LATER DIAGENESIS

C03 

Dolomite

Meteoric water

Figure 9. Paragenetic sequence for authigenic mineral phases in 

the Lower and Middle Pennsylvanian Tradewater Formation and 

equivalent rocks.

Figure 10. Photomicrograph of brown "wheat seed" siderite 

rhombohedra (s), some of which contain dark, organic-rich cores, 

and detrital quartz grains (q), from the Lower Pennsylvanian Mansfield Formation; Sullivan County, Indiana, core, 726.5 ft (fig. 1). 

Blue-dyed epoxy fills voids. Plane-polarized light, field length 2.7

facies characteristic of these rocks are discussed in detail in 

Barnhill and Hansley (1993).

in table 4) from Edmonson County, Kentucky, was sampled 

and point counted, but it was not described. The Indiana and 

Illinois cores include part or all of the Tradewater Formation 

and equivalent rocks, and the Kentucky cores sample part of 

the Caseyville Formation. A rock-color chart (Rock-Color 

Chart Committee, 1948) was used to describe the color of 

some cores. Rapid, cyclic facies changes characteristic of a 

coastal environment can be clearly seen in the vertical 

sequences of Tradewater or equivalent strata in the cores. 

Facies include marine shale, tidal and fluvial sandstone, siltstone, marine limestone, coal, and underclay. Sedimentary

DETRITAL PETROLOGY

CASEYVILLE FORMATION AND MANSFIELD 

FORMATION (LOWER PART)

The Caseyville Formation and the lower part of the 

Mansfield Formation constitute poorly sorted, conglomeratic 

quartzarenite characterized by quartz pebbles. Major detrital 

constituents are quartz, polycrystalline quartz, and chert. 

Modal analyses of selected samples are listed in table 2.
E14 EVOLUTION OF SEDIMENTARY BASINS ILLINOIS BASIN

Figure 11. Photomicrograph of siderite (s) that has deformed a muscovite flake (m) from the Lower and Middle Pennsylvanian Mansfield 

Formation; Greene County, Indiana, core, 458 ft (fig. 1). Crossed polars, field length 0.4 mm.

TRADEWATER FORMATION AND 

EQUIVALENT SANDSTONES

According to Folk's (1980) classification, sandstone of 

the Tradewater Formation and equivalent sandstones is 

sublitharenite. It is generally very fine grained to fine 

grained and poorly to moderately well sorted. Quartz, 

polycrystalline quartz, and rock fragments are the major 

detrital constituents. Complete modal analyses of the cores 

are given in tables 3 and 4. The major rock fragments are 

chert, schist (fig. 4A), chloritic varieties (fig. 4#), and metaquartzite (fig. 4C). Other rock fragments include siltstone, 

shale, fine-grained igneous (fig. 4£)), and micrite. Unidentifiable grains were classified as altered rock fragments. 

Other detrital constituents include muscovite, illite, potassium feldspar, plagioclase, and heavy minerals (zircon, 

tourmaline). Potassium feldspar shows marked dissolution 

in most samples (fig. 5).

AUTHIGENIC PETROLOGY

CASEYVILLE FORMATION AND MANSFIELD 

FORMATION (LOWER PART)

In west-central Kentucky, Mississippian rocks contain 

tar-sand deposits, and sandstones of the Caseyville Formation are commonly saturated with tar where they infill channels cut into Mississippian strata (see fig. 3). Tar and pyrite 

are at grain contacts and completely surround some detrital 

grains in the Vincent No. 27 and Raymond Carroll No. 19 

cores (fig. 6). Quartz overgrowths are locally abundant. Oil 

is present between the overgrowths and detrital grains; however, tar more commonly is on the overgrowths (fig. 7). 

Kaolinite, which is present in isolated pores, is oil stained in 

oil-saturated sandstone. In the Raymond Carroll No. 19 core, 

oil is in dissolution vugs in ankerite (fig. 8) that fills pores 

rimmed with quartz overgrowths.
PATTERNS OF DIAGENESIS IN PENNSYLVANIAN SANDSTONES E15

Figure 12. Photomicrograph of botryoidal siderite (s) after aragonite(?) from the Lower and Middle Pennsylvanian Mansfield Formation; 

Greene County, Indiana, core, 458 ft (fig. 1). Matrix is detrital clay. Crossed polars, field length 0.8 mm.

Figure 13. Scanning electron micrograph of quartz overgrowths 

(qo) that have preserved primary porosity (p). Some quartz grains 

are covered with detrital clay (c). Sample is from the Middle Pennsylvanian Mansfield Formation; WES-10C^7 core, 82.8 ft, Naval 

Surface Warfare Center near Crane, Indiana (fig. 1). Field length 

0.1 mm.

TRADEWATER FORMATION AND 

EQUIVALENT SANDSTONES

The paragenesis of diagenetic alterations in the Tradewater Formation and equivalent sandstones (fig. 9) is more 

complex than that of the older Pennsylvanian quartzarenites. 

Quartz, siderite, ankerite, nonferroan calcite, and kaolinite 

are the most abundant authigenic minerals. Ankerite is 

present where siderite is not, and both may contain pyrite 

inclusions. Tiny "wheat-seed" siderite crystals may completely rim detrital grains, indicating that they precipitated 

before compaction (fig. 10). Hard, dense siderite concretions, which commonly are present at the base of a channel, 

are throughout the section. Deflection of bedding by many 

concretions indicates that the concretions were syndepositional. Siderite also is present as rhombohedra in pores and 

is commonly interlocked as a cement. The presence of siderite between deformed muscovite flakes suggests that siderite growth pushed the flakes apart before compaction (fig. 

11). Boytryoidal siderite in the Greene County core may be 

a replacement of aragonite (fig. 12), which commonly
E16 EVOLUTION OF SEDIMENTARY BASINS ILLINOIS BASIN

Figure 14. Cathodoluminescence micrograph showing dark, nonluminescent quartz overgrowths (qo) on detrital (reddish) quartz grains 

(q) from the Lower Pennsylvanian Mansfield Formation; Sullivan County, Indiana, core, 825.5 ft (fig. 1). Blue-dyed epoxy fills pores (p). 

Field length 1.4 mm.

Figure 15. Photomicrograph of detrital quartz grains (q) with 

corroded edges from the Middle Pennsylvanian Brazil Formation; 

Green County, Indiana, core, 93.1 ft (fig. 1). Matrix is calcite. 

Plane-polarized light, field length 1.4 mm.

Figure 16. Photomicrograph of albite overgrowth (a) on 

sericitized plagioclase grain in the Lower Pennsylvanian Mansfield 

Formation; Sullivan County, Indiana, core, 825.5 ft (fig. 1). Other 

grains are detrital quartz with quartz overgrowths (qo). Crossed 

polars, field length 0.7 mm.
PATTERNS OF DIAGENESIS IN PENNSYLVANIAN SANDSTONES E17

Figure 17. Scanning electron micrograph of authigenic vermicular kaolinite (k) from the Lower and Middle Pennsylvanian Mansfield Formation; Greene County, Indiana, core, 144.5 ft (fig. 1). 

Detrital illite, I; field length 0.4 mm.

Figure 18. Scanning electron micrograph of authigenic illite (i) 

on kaolinite (k) from the Lower and Middle Pennsylvanian Mansfield Formation; Greene County, Indiana, core, 144.5 ft (fig. 1). 

Field length 0.04 mm.

grows in this form in subtidal zones (Scholle, 1978). Anhedral calcite and ankerite cements fill pores rimmed by euhedral quartz overgrowths, pyrite, and siderite.

As much as 12 volume percent syntaxial quartz overgrowth is present in some sandstones. In many instances 

quartz overgrowths preserved primary porosity by preventing compaction; however, at the same time they lowered the 

permeability (fig. 13). Cathodoluminescence studies reveal 

that more authigenic silica is present as overgrowths than is 

apparent under transmitted light (fig. 14). Abundant authigenic silica tends to be present in samples that do not contain siderite (table 4), and sandstone that contains quartz 

overgrowths commonly lies above or below sandstone that 

contains siderite. Detrital quartz grains in sandstone that has 

a high volume percentage of siderite show widespread

10 cm

Figure 19. Sketch of siderite concretion that was sampled for 

carbon and oxygen isotope analyses. Concretion is from the Lower and Middle Pennsylvanian Mansfield Formation in the Greene 

County, Indiana, core at 420 ft (fig. 1). Numbers next to sampled 

areas are keyed to isotope values given in table 5. Number 7 is on 

the back of the concretion on the rim.

Figure 20. Photograph of siderite (dark) interlaminated with silty 

clay (light) in tidalite sequence from the Lower and Middle Pennsylvanian Mansfield Formation; Greene County, Indiana, core, 158 

ft (fig-1).

evidence of dissolution (fig. 15). Rare authigenic albite is in 

sandstones containing quartz overgrowths (fig. 16).

Vermicular kaolinite, which is commonly in apparently isolated pores, dominates the authigenic clay mineralogy. Kaolinite coats siderite rhombohedra (fig. 17) and 

detrital illite. Tiny (1-2 (im) illite overgrowths that are 

visible only with the scanning electron microscope (fig. 18) 

are present locally on early(?) kaolinite. Much kaolinite is
E18 EVOLUTION OF SEDIMENTARY BASINS ILLINOIS BASIN

Figure 21. Photograph of siderite bed (dark) from the Lower and 

Middle Pennsylvanian Mansfield Formation; Sullivan County, Indiana, core, 540 ft (fig. 1).

Figure 22. Photograph of siderite breccia fragments (s) in a 

channel (tidal?) sandstone from the Middle Pennsylvanian Brazil 

Formation; Greene County, Indiana, core, 125 ft (fig. 1).

Table 5. Carbon and oxygen isotope analyses of authigenic siderite in cores of the Lower and Middle Pennsylvanian 

Tradewater Formation and equivalent rocks, Illinois Basin.

[Location of core holes shown in figure 1. Core designations given in table 1; number after core designation refers to sample depth (in feet). All 

values (in per mil) are relative to the PDB belemnite standard. Analyses by Global Geochemistry (Canoga Park, Calif) and Augusta Warden 

(U.S. Geological Survey). The WES-10C-23 core is within the Naval Surface Warfare Center]

Sample No.

G-420-2

G-420-3

G-420-4

G-420-5

G-420-6

G-420-7

WES-10C-23-190.8

WES-10C-23-121.2

WES-10C-23-203

SAL-125

SAL-123

PO-96A

PO-96B

S-540

S-767-1

S-767-2

S-767-3

S-869

G-177.8

G-85

G-158.5

813C

-9.97

-6.91

-10.30

-9.33

-9.63

-12.74

+3.33

+11.06

+2.64

-3.59

-4.93

-0.69

+0.58

-2.94

-1.57

-1.58

-1.66

+5.69

+0.23

-0.07

-10.65

8I80

-3.1

-3.91

-3.01

-3.12

-3.4

-3.04

-3.05

-3.3

-3.3

-5.49

-6.44

-0.69

-3.00

-2.40

-3.6

-3.6

-3.51

-3.92

-6.1

-4.52

-3.43

Description

Concretion.

Concretion.

Concretion.

Concretion.

Concretion.

Concretion.

Concretion.

Concretion.

Concretion.

Concretion in tidalite.

Bed.

Bed.

Bed.

Bed.

Bed.

Bed.

Bed.

Bed.

Bed.

Cement in sandstone.

Laminae in tidalite.
PATTERNS OF DIAGENESIS IN PENNSYLVANIAN SANDSTONES E19

Table 6. Composition of siderite cement in sandstones of the

Lower and Middle Pennsylvanian Tradewater Formation from

the Greene County, Indiana, core.

[Location of core shown in figure 1 and described in table 1. Samples were

obtained from depths of 144.5, 153, 237.5, 247, and 406 ft. Oxide weight

percent values were determined using a JOEL JSM-840 scanning electron

microscope and attached Tracor Northern (TN-5500) standardless

quantitative analysis program (SQ). Accelerating voltage 20 kV; dead

time 30 40; spot size 6; LaB6 filament; takeoff angle 31°; ZAP correction

program. Semiquantitative analyses are accurate to

±5 percent for major elements and to ±10 percent for minor elements]

No. of points FeO MgO MnO CaO

Magnesium-rich siderite

1

1

5

2

1

75.12

73.16

77.83

64.12

77.38

12.99

21.24

14.01

28.23

17.61

6.22

3.92

4.30

3.36

3.40

5.67

1.68

3.87

4.31

1.61

Iron-rich siderite

5

4

5

2

2

89.22

89.93

89.03

88.36

90.63

2.71

2.85

3.17

3.42

2.54

5.81

5.88

4.81

5.50

0.89

2.26

2.67

2.99

2.74

5.95

Iron- and magnesium-rich siderite

1 

4 

2 

2

(la, center) 

(Ib, margins) 

(3 a, center) 

(3b, margins)

90.37 

73.06 

88.41 

66.16

2.17 

18.03 

4.45 

26.25

1.07 

5.10 

2.67 

4.56

6.38 

3.81 

5.23 

3.03

contained in underclays, which are clay-rich beds underlying coal beds (Hughes, 1993).

SIDERITE

highly variable: some thin siderite beds (fig. 21) have 8 C 

values just above or below 0 per mil; another siderite bed at 

869 ft (272 m) in the Sullivan County core has a more positive 8^C value (+5.7 per mil). Samples from other beds, 

one at 540 ft (169 m) in the Sullivan County core and one 

from 123 ft (38 m) in the Saline County core, have more 

negative 8 C values, -2.9 and -4.9 per mil, respectively. A 

sample of a siderite concretion from a channel sandstone in 

the Saline County core is from a depth of 125 ft (39 m) (fig. 

22). Siderite cement in a channel sandstone from a depth of 

85 ft (27 m) in the Greene County core has a S^C value of 

-0.1 per mil.

COMPOSITION

The composition of early diagenetic siderite provides a 

strong indication of whether the depositional environment 

was marine or nonmarine (Pye, 1984; Mozley, 1989). Semiquantitative analyses of siderite concretions, beds, and 

cement were obtained with the scanning electron microscope energy-dispersive system standardless analysis program (tables 6, 7). Most of the concretions and beds contain 

very little magnesium; however, siderite rhombohedra from 

a sandstone sample from the Greene County core at 247 ft 

(77 m) contain as much as 28.2 mole percent MgO. Many 

rhombohedra are iron rich in their centers and magnesium 

rich near their edges.

Ankerite cement was also analyzed by the standardless 

analysis program (table 8). Patches of ankerite cement are 

more iron rich toward their centers or in the centers of the 

pores.

INTERPRETATION

CARBON AND OXYGEN ISOTOPES

The various morphological types of siderite from the 

Lower and Middle Pennsylvanian Raccoon Creek Group 

and equivalent rocks were analyzed isotopically to aid in 

interpretation of depositional environment. Isotopic analyses of seven concretions showed both positive and negative 

813C values, and all S18O values were near -3 per mil (table 

5). A concretion from a channel sandstone at 420 ft (191 m) 

in the Greene County core displayed the most negative S 13C 

values (-6.9 to -12.7 per mil) in a series of six samples taken 

from spots across the concretion. The most negative 8 C 

value (-12.7 per mil) was from the edge (spot seven) of the 

concretion, and the other very negative 8 13C value (-10.3 

per mil) was from near the center (spot four) of the concretion. A sketch of the concretion and sampled areas shows 

that there is no apparent isotopic trend outward from the 

center to the margin of the concretion (fig. 19). Siderite laminae in a tidalite sequence from 158.5 ft (50 m) (fig. 20) in 

the Greene County core have a distinctly negative 813C 

value (-10.7 per mil). Isotope values from siderite beds are

Siderite commonly precipitates either syndepositionally or during early diagenesis, and therefore its isotopic 

values and composition can be an indication of depositional 

environment (Poppe and others, 1988). Isotope values are 

reliable because siderite has no unstable polymorphs and it 

does not undergo recrystallization or reequilibration during 

diagenesis. The presence of siderite is diagnostic of an 

alkaline, reducing environment (Berner, 1981). It forms 

under slightly reducing (suboxic) or strongly reducing, 

methanogenic conditions (Mozley and Wersin, 1992). 

According to Berner (1981), a dissolved Ca:Fe ratio less 

than 20 is required for siderite precipitation. In past studies, 

siderite was assumed to form only in nonmarine or 

brackish-water environments where sulfate is present in 

very low concentrations. When sulfate is present, bacterially 

mediated sulfate reduction in the presence of organic matter 

produces sulfur that combines with available iron to form 

sulfides rather than siderite. Siderite also forms in estuarine 

and marine settings (Postma, 1981; Mozley, 1989; Pye and 

others, 1990; Mozley and Wersin, 1992). In a study of intertidal sediments, Mozley and Wersin (1992) showed that
E20 EVOLUTION OF SEDIMENTARY BASINS ILLINOIS BASIN

Table 7. Composition of siderite from the study area.

[Location of core holes shown in figure 1. Core designations given in table 1; number after core designation refers to sample

depth (in feet); number in parentheses is number of analyzed spots. The WES-10C-23 core is in the Naval Surface Warfare Center.

Oxide weight percent values determined using a JOEL JSM-840 scanning electron microscope and attached Tracor Northern

(TN-5500) standardless quantitative analysis program (SQ). Accelerating voltage 20 kV; dead time 30-40; spot size 6; tungsten filament;

takeoff angle 31°; ZAP correction program. Semiquantitative analyses are accurate to ±5 percent for major elements and to ±10 percent

for minor elements]

Sample

8-540(11)

S-869 (10)

PO-96 (8)

S-767 (5)

G-158.5(8)

G-177.8 (6)

SAL-123 (10)

WES-10C-23-190.8 (10)

FeO

95.6

93.8

93.8

95.6

93.0

92.9

96.8

92.3

CaO

1.5

2.8

1.9

2.3

2.1

2.6

0.6

5.2

MgO

0.9

0.4

1.3

0.3

0.6

1.2

0.3

1.5

MnO

2.0

3.0

3.0

1.8

4.3

3.3

2.3

1.0

Description

Bed.

Bed.

Bed.

Bed.

Tidalite.

Bed.

Bed.

Concretion.

Table 8. Composition of ankerite cement in sandstones of the

Lower and Middle Pennsylvanian Tradewater Formation and

equivalent rocks, Illinois Basin.

[Location of cores shown in figure 1. Core designations given in table 1;

number after core designation refers to sample depth (in feet). Oxide

weight percent values determined using a JOEL JSM-840 scanning

electron microscope and attached Tracor Northern (TN-5500) standardless

quantitative analysis program (SQ). Accelerating voltage 20 kV; dead

time 30 40; spot size 6; LaB6 filament; takeoff angle 31°; ZAP correction

program. Semiquantitative analyses are accurate to

±5 percent for major elements and to ±10 percent for minor elements]

Sample no.

G-153

G-153

G-247

G-458

G-^58

SAL-94.5

SAL-94.5

CaO

56.43

46.60

55.61

56.33

52.41

54.80

55.61

FeO

16.11

11.26

25.09

25.77

23.71

20.28

25.09

MgO

26.42

40.38

16.82

15.34

21.57

22.79

16.82

MnO

1.04

1.76

2.47

2.57

2.32

2.23

2.47

siderite rather than pyrite can form, even if sulfate concentrations are high, if the rate of iron reduction exceeds the rate of 

H2S production. In marine environments, siderite also precipitates in suboxic conditions in the presence of relatively 

low concentrations of organic matter. Gautier (1986) proposed that siderite forms by methanogenesis in continental 

sediments if sulfate has been depleted from formation 

waters; however, methanogenesis also occurs (less commonly) in marine sediments.

Although there is some overlap, siderite that has 8 13C 

values less than -8 per mil (relative to PDB) is probably 

marine, and siderite that has positive 8 13C values and 8 18O 

values less than -13 per mil is nonmarine (Mozley and 

Wersin, 1992). Pye and others (1989) found that actively 

forming siderite concretions in marsh and sandflat sediments 

on the Norfolk coast have 8 C values ranging from -3.0 to 

-11.8 per mil and S 18O values ranging from -6.4 to +0.8 per 

mil. They attributed the range in 8 C values as indicating 

that carbon was derived from marine sources and

degradation of organic matter, and they concluded that the 

SO values suggest carbonate precipitated in water ranging 

in composition from seawater to seawater diluted with meteoric water. Mozley and Carothers (1992) explained that 

anomalously low (less than +0.1 per mil) 8 18O values probably reflect seawater-meteoric water mixing or are the result 

of water-sediment interaction, such as precipitation of 

8O-enriched minerals.

The relatively low negative values of 813C in a carbonate concretion in a channel sandstone from the Greene 

County core at 420 ft (131 m) suggest that the sandstone was 

deposited in a tidal channel. The positive 8 C values of the 

other siderite concretions indicate formation in a freshwater 

environment. The distinctly negative 8 13C value (-10.7 per 

mil) of siderite laminae in the tidalite from the Greene 

County core at 158.5 ft (50 m) suggests formation in marine 

water. The S 13C values just above or below 0 per mil of thin 

siderite bands probably indicate precipitation from brackish 

water. The siderite bed from the Sullivan County core at 869 

ft (272 m) has a more positive 5 C value (+5.7 per mil) and 

therefore probably formed in fresher water. The more negative S 13C values, -2.9 and -4.9 per mil, of concretions from 

the Sullivan County core at 540 ft (169 m) and from the 

Saline County core at 123 ft (38 m), respectively, reflect an 

input of marine water. The sample of siderite cement from a 

channel sandstone in the Green County core at 85 ft (27 m) 

has a 8 C value of-0.1 per mil that is suggestive of formation in brackish water.

All of the 818O values are lower than that of seawater 

(about 0 per mil), indicating meteoric-seawater mixing and 

(or) precipitation of 8O-rich minerals. The former possibility is more likely because siderite is usually the earliest 

authigenic mineral to form.

Nonmarine siderite is usually very pure (>90 mole percent FeO), whereas marine siderite contains variable 

amounts of MgO substituting for FeO (Mozley and Wersin, 

1992). Therefore, all of the siderite beds and concretions 

analyzed for this study would be classified as nonmarine
PATTERNS OF DIAGENESIS IN PENNSYLVANIAN SANDSTONES E21

because of their lack of magnesium; however, the presence 

of magnesium in the siderite cement indicates a marine 

influence. Scanning electron microscope analyses indicate 

that pore waters became fresher as the siderite cement grew, 

because the cement rim is magnesium poor. This trend may 

be the result of a regression of marine waters or a byproduct 

of water-rock reactions. Coleman (1993) suggested that laterally extensive siderite beds result from the mixing of components derived from shallow reduction of manganese and 

iron with the byproducts of methanogenesis and decarboxylation. The slight enrichment of manganese in the siderite 

beds of this study may indicate that this process was operative during early diagenesis. The enrichment of iron in the 

youngest part of ankerite cement patches reflects the same 

geochemical trends as seen in the siderite.

DISCUSSION

The abundance of metamorphic rock fragments in the 

Tradewater Formation and equivalent rocks contrasts with 

the quartz-rich sandstones of Caseyville age. The authigenic 

mineral assemblage (see fig. 10) of the Tradewater and 

equivalent rocks reflects their more varied detrital mineralogy and the presence of organic matter. To a large degree, 

the authigenic mineral assemblage formed as a result of 

early diagenetic reactions, such as sulfate reduction and 

methanogenesis, that commonly occur in organic-rich sediments (Curtis and Coleman, 1986). Pyrite formed very early 

as a byproduct of microbial sulfate reduction in the presence 

of organic matter (Berner, 1984). The rarity of pyrite was 

apparently due to a lack of sulfate rather than to a lack of iron 

because siderite is an abundant authigenic mineral. In addition, pyrite is rare because of a very high bicarbonate activity 

due to microbial reactions and because it was locally 

replaced by siderite, which precipitated when sulfate had 

been depleted in the groundwater. The abundant organic 

matter in these sandstones lowered the Eh such that the concentration of Fe ions in solution was raised, favoring precipitation of siderite when the sulfate concentration became 

low. Siderite concretions formed syndepositionally near the 

bases of fluvial channels. Unstable micaceous lithic fragments and detrital clay and iron oxyhydroxide grain coatings 

provided an iron-rich environment during early diagenesis. 

The presence of abundant low-magnesium siderite is strong 

evidence for formation of many of these sandstones in fresh 

to brackish water. Where siderite precipitated it apparently 

inhibited quartz overgrowth formation. Ankerite precipitated instead of siderite when the chemical activity of iron 

was not high enough for siderite to form.

The precipitation of authigenic silica is interpreted to 

have occurred during early diagenesis because where overgrowths are abundant detrital grains have point contacts and 

quartz overgrowths protrude into areas that have high values 

of minus cement porosity (primary?). In inorganic solutions,

silica has a very low solubility if the pH is below 9; however, the solubility of silica rises dramatically at near-neutral pH because of the stability of organic-silica complexes 

(Bennett and Casey, 1994). Recent peat bogs have high 

organic acid concentrations, near-neutral pH, increasing silica concentration with depth, and etched quartz and aluminosilicate grains (Bennett and others, 1991). During early 

diagenesis of the Pennsylvanian sandstones described 

herein, conditions were favorable for the production of 

organic acids from the plant debris. These organic acids, 

such as oxalate and citrate, complexed with silica and corroded the edges of detrital quartz grains. Silica was mobilized by the organic-silica complexes, which remained in 

solution until they were destabilized due to changes in ionic 

strength or pH (Bennett and Casey, 1994). At this time, the 

silica nucleated on detrital quartz grains as quartz overgrowths. Detrital quartz grains in sandstones that have 

abundant quartz overgrowths show no corrosion, indicating 

that authigenic silica was extrinsically derived.

Conditions were favorable for kaolinite precipitation 

during both early and late diagenesis. During early diagenesis, indigenous organic matter and organic-acid-rich 

waters from swamps created an acidic environment favorable for kaolinite precipitation. After erosion of overlying 

strata, meteoric water infiltrated these rocks, creating an 

acidic environment in which kaolinite precipitated.

The lack of metamorphic rock fragments and detrital 

organic matter distinguishes the tar-bearing sandstones of 

the Caseyville Formation and equivalent strata from those 

of the Tradewater Formation and equivalent rocks. The 

monomineralic nature of Caseyville-age sandstones is 

reflected in the authigenic mineralogy. The absence of siderite reflects the lack of detrital organic matter and 

iron-bearing minerals in these quartzarenites. The presence 

of tar at grain contacts indicates that the migration of oil 

took place before significant compaction. Pyrite precipitated in the reducing environment associated with the oil. 

Oil migration coincided with the deposition of quartz overgrowths, but most oil entered the sandstones after quartz 

precipitation. The abundance of early quartz overgrowths in 

sandstones of the Caseyville Formation and equivalents 

may be due to the mobility of silica in organic-acid-rich 

brines associated with oil migration.

Others have also concluded that oil migration occurred 

during the late Paleozoic (Davis, 1990). Rose (1963) attributed the oil in the Caseyville Formation to west to east 

migration along the Rough Creek-Shawneetown fault 

system (Buschbach and Kolata, 1993, fig. 1-6) in western 

Kentucky. The source rock for the oil is unknown (Noger, 

1984). Fisk (1978) suggested that the oil came from the 

Devonian Chattanooga Shale, but Hamilton-Smith (1994) 

presented geochemical data that suggest the oil was derived 

from the Devonian and Mississippian New Albany Shale. 

More conclusive geochemical studies have yet to be done to 

determine a definitive oil-source rock corrrelation.
E22 EVOLUTION OF SEDIMENTARY BASINS ILLINOIS BASIN

CONCLUSIONS

Basin wide fluid movement through these Lower and 

Middle Pennsylvanian rocks of the Illinois Basin was 

restricted due to rapid facies changes characteristic of a 

coastal environment. Detrital clay grain coatings, early 

siderite and quartz cements, and organic laminae were also 

barriers to fluid flow. Fluvial channels of the Caseyville Formation and lower part of the Mansfield Formation may have 

provided the best pathways for fluid movement, better than 

the overlying matrix-rich sandstones of the Tradewater Formation and equivalent units. Faults or unconformities as 

fluid conduits were not considered as part of this study; however, Nelson (1992) found that tripolitic or hydrothermal silica deposits in southern Illinois were the result of the 

movement of warm silica-bearing solutions along faults, and 

therefore the possibility that diagenesis in a local area may 

have been influenced by fault-related fluids cannot be ruled 

out.

Diagenetic alterations, which afford one of the best 

ways to track fluid movements, were directly related to the 

host sandstone mineralogy and to the geochemistry of the 

local, early depositional environment. Carbon isotope values and the compositions of siderite nodules, cement, and 

beds in the Raccoon Creek Group and equivalent rocks 

indicate that early pore waters were reducing and fresh to 

brackish. The early authigenic mineral assemblage reflects 

the alkaline, anoxic pore waters of these organic-rich 

sandstones. The fluctuations in salinity are evidence of the 

coastal environment in which these sandstones were deposited. As diagenesis proceeded, pore waters became fresher, 

as indicated by the tendency of both siderite and ankerite to 

become more iron rich with time. Etched and skeletal quartz 

and aluminosilicate grains show the effects of 

organic-acid-complexation on silica solubility. Local movement of organic-silica complexes between sandstones during early diagenesis contributed to the large volume 

percentage of quartz overgrowths. In many areas, the quartz 

overgrowths lowered permeability but preserved primary 

porosity. Shallow burial, erosion of overlying strata, and the 

stabilities of early cements preserved early authigenic 

assemblages.

REFERENCES CITED

Barnhill, M.L., 1992, Subsurface sedimentology of the Pennsylvanian (Mansfield) rocks, Naval Surface Warfare Center, Crane, 

Indiana: Indiana Geological Survey Open-File Report, 93 p.

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McComish Gorge, Old Burn Pit, Pest Control site, and Mustard Gas burial grounds A preliminary investigation: Indiana 

University, Indiana Geological Survey Administrative Report, 

67 p.

Barnhill, M.L., and Kvale, E.P., in press, Tide-influenced estuarine, 

deltaic, and open-coast deposits of the Mansfield and Brazil 

Formations (Lower Pennsylvanian), southwestern Indiana: 

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Coleman, M.L., 1993, Microbial processes Controls on the shape 

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Paleontologists and Mineralogists Special Publication 38, p. 

23-33.

Damberger, H.H., 1971, Coalification pattern of the Illinois Basin: 

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 1989, Overview of the Pennsylvanian in the Illinois Basin, 

in Cecil, C.B., and Eble, C., eds., Carboniferous geology of the 

eastern United States: Washington, D.C., American Geophysical Union, p. 20-37.

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PATTERNS OF DIAGENESIS IN PENNSYLVANIAN SANDSTONES E23

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E24 EVOLUTION OF SEDIMENTARY BASINS ILLINOIS BASIN

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Published in the Central Region, Denver, Colorado 

Manuscript approved for publication June 15, 1995 

Edited by Judith Stoeser 

Graphics and photocomposition by Gayle M. Dumonceaux
APPENDIX
E26 EVOLUTION OF SEDIMENTARY BASINS ILLINOIS BASIN

APPENDIX DESCRIPTION OF CORES

[Locations of coreholes are shown in figure 1 and described in table 1. Depths are in feet below the surface. Color classification is from Rock-Color Chart 

Committee (1948)]

Appendix table 1. Vincent No. 28 core, Edmonson County, Kentucky.

___Depth_______________________________________Description___________________________________

______________________________________Caseyville Formation_____________________________________

94.0-95.0 Sandstone, 10YR 6/2; fines upward; pebbly layers at 94.5 ft (most are <0.12 in. thick); fine to medium grained at top,

pebbly and medium to coarse grained at base 

95.0-99.0 Sandstone, 10YR 6/2, medium- to coarse-grained, poorly to moderately well sorted, calcite-cemented; scattered

pebbles as large as 0.25 in.; less porous than interval above 

99.0-100.0 Sandstone, 5Y 6/1, coarse-grained, very poorly sorted, vuggy, 0.25-0.5-in., subrounded to rounded, white quartz and

chert pebbles; pebbly layers at high-angle crossbedding; spotty calcite cement; top 2.0 in. very pebbly

100.0-101.0 Sandstone, 10YR 6/2, coarse-grained, vuggy, poorly sorted; rare pink feldspar, 0.25-in. pebbles; sample at 101.0 ft 

101.0-102.9 Sandstone, 10YR 6/2, coarse-grained; finer grained than interval above; pebbly layer at base 

102.9-103.0 Sandstone, 5Y 4/1, coarse-grained, poorly sorted, calcite cemented; scattered pebbles as large as 0.75 in.; oil(?); 

___________sample at 103.0 ft_____________________________________________________

Appendix table 2. Vincent No. 27 Core, Edmonson County, Kentucky.

___Depth_______________________________________Description___________________________________ 

______________________________________Caseyville Formation_____________________________________

17.0-18.5 Sandstone, Nl, fine- to medium-grained, oil saturated; finer grained at top; moderately well sorted

18.5-19.5 Sandstone, Nl, medium-grained, moderately well sorted, pebbly, oil-saturated; most pebbles <0.25 in.; iron oxide in

pores

19.5-22.0 Sandstone, Nl, silty to medium-grained, poorly sorted, oil-saturated; sample at 20.5 ft 

22.0-24.0 Sandstone, Nl, medium- to coarse-grained, moderately well sorted, pebbly, oil-saturated 

24.0-25.0 Sandstone; Nl, medium- to coarse-grained, oil-saturated; pebbles as large as 0.5 in. but most <0.25 in.; pockets of

pale-brown clay and (or) iron oxide

25.0-26.5 Sandstone; Nl, fine- to medium-grained, oil-saturated 

26.5-27.0 Sandstone; Nl, medium- to coarse-grained, poorly sorted, very pebbly; oil-saturated matrix; gray (barite?) matrix;

sharp basal contact

27.0-27.4 Sandstone, 10YR 7/4, fine- to medium-grained, poorly sorted; scattered pebbles (<0.25 in.) 

27.4-28.4 Sandstone, 10YR 7/4, coarse-grained; scattered pebbles; spotty tar, samples at 27.6 and 28.0 ft____________

Appendix table 3. Vincent No. 13 Core, Edmonson County, Kentucky.

___Depth_______________________________________Description___________________________________ 

______________________________________Caseyville Formation_____________________________________ 

97.7-98.5 Sandstone, 10YR 6/2, fine- to coarse-grained, poorly sorted; 0.25-in. pebbles; sample at 98.5 ft 

98.5-108.5 Sandstone, 5YR 4/1, fine- to coarse-grained, poorly sorted, pebbly, basal 4 ft vuggy; finer grained; tarry layer 101.0-

105ft

108.5-110.5 Sandstone, 5Y 6/1,very fine grained, silty; sparse black, wavy laminae 

110.5-110.7 Sandstone, 5Y 6/1, very fine grained, vuggy, pebbly (white pebbles <0.12 in.); tarry stain 

110.7-115.1 Sandstone, 5Y 6/1, medium- to coarse-grained; sparse pebbles (O.12 in.); calcite and iron oxide cement; oil stained

113.5-113.8 ft; pebbles as large as 0.5 in. in basal foot; samples at 110.8 and 113.7 ft 

115.1-121.7 Sandstone, 5Y 6/1, fine-grained; sparse pebbles

121.7-121.8 Same as interval above but more pebbly and tarry; moderately well sorted

121.8-136.5 Sandstone, 5 Y 4/1, medium-grained, moderately well sorted; color changes gradually downward as oil saturation

increases; scattered pebbles; several 1.0-in. pebbles 133.1 ft; very pebbly zone 136.1-136.5 ft; sample at 133.5 ft 

136.5-139.5 Sandstone, 5Y 4/1, medium-grained; many pebbles at base of interval; sample at 137.5 ft________________ 

______________________________________Oil-water contact(?)______________________________________ 

139.5-140.5 Sandstone, 5Y 6/4, very coarse grained to conglomeratic, pebbly, oxidized 

140.5-142.5 Sandstone, SYR 8/2, fine-grained, moderately well sorted 

142.5-147.9 Conglomerate, SYR 8/2; shale rip-up clasts 

147.9-148.2 Conglomerate, 10YR 5/4; many rip-up clasts and pebbles
PATTERNS OF DIAGENESIS IN PENNSYLVANIAN SANDSTONES E27

Appendix table 3. Vincent No. 13 Core, Edmonson County, Kentucky Continued.

Depth Description

Caseyville Formation Continued

148.2-201.8 

201.8-202.0 

202.0-204.0 

204.0-204.8 

204.8-221.0 

221.0-291.0

Conglomerate, 10YR 5/4; scattered pebbles; white to reddish-brown areas; coarsens downward; sample at 173.8 ft 

Conglomerate, 10YR 5/4, vuggy; large white pebbles (1.0 in.); base of channel (?) 

Siltstone to very fine grained sandstone; 5YR 5/2 

Limestone, 5Y 6/1

Sandstone, 10YR 5/4, very fine grained, silty; grades downward into pebbly, fine- to medium-grained sandstone 

Sandstone, 5YR 6/4, medium- to coarse-grained, poorly sorted, oxidized, calcite cemented; white quartz pebbles; 

possible tar 286.5 ft; pebbly zone (1.0-in.pebbles) 234.0-235.0 ft; pyritized area 281.0 ft; sample at 286.5 ft 

__________________________Mississippian limestone___________________________________

Appendix table 4. Sangamon County, Dlinois, core.

Depth Description

Tradewater Formation

302.0-328.8 Claystone and shale, gray to dark-gray, massive; calcareous concretions in middle 5.0 ft; siltstone at base

328.8-330.4 Limestone, brownish-gray, massive, siliceous, fossiliferous; chert concretions

330.4-339.4 Shale, light-gray to black, fissile to massive, carbonaceous

339.4-342.6 Coal

342.6-344.4 Claystone, dark-gray, noncalcareous, massive

344.4-344.7 Limestone, brownish-gray

344.7-347.8 Sandstone, dark-gray, micaceous, argillaceous; plant impressions; calcareous at top

347.8-3 53.8 Siltstone, dark-gray, micaceous; many plant impressions

353.8-354.9 Sandstone, dark-gray, micaceous; many plant impressions; black shale partings

354.9-355.3 Shale at top of interval and siltstone at base; dark gray, micaceous, calcareous

355.3-355.8 Coal; sandy in middle

355.8-386.1 Siltstone, dark-gray, calcareous, argillaceous, micaceous; very fine grained sandstone middle 4.0 ft; black shale

sample at 358.0 ft, coaly sample at 359.6 ft, and sandstone sample at 358.6 ft 

386.1-388.9 Shale, black, carbonaceous, micaceous, fissile; conodonts 

388.9-389.3 Coal

389.3-390.1 Shale, black, fissile, fossiliferous, calcareous

390.1-390.8 Siltstone, greenish-gray, micaceous, poorly bedded; plant impressions 

390.8-392.0 Claystone, gray-brown, massive, calcareous

392.0-394.6 Sandstone, medium-gray, very fine grained, massive, micaceous, calcareous 

394.6-396.0 Shale, black, carbonaceous, well-bedded

396.0^108.8 Shale, dark-gray to black; 1.0-in.-thick coal 400.0 ft; 5.0-in.-thick sandstone 404.4 ft; sandstone sample at 404.5 ft 

408.8-410.9 Limestone, white, massive

410.9-433.0 Shale (upper 5.5 ft), dark-gray to black; noncalcareous at top, calcareous at base; missing core (lower 18.5 ft) 

433.0^38.0 Sandstone, light-gray, very fine grained, massive, micaceous, calcareous; plant impressions; 8.0-in.-thick shale 436.4

ft; sample at 437.0 ft 

438.0-494.8 Shale, gray to black, nonbedded to well-bedded; conodonts; coal 463.3 ft; two thin (2.0 in.) sandstone intervals (479.0

and 480.0 ft), medium-gray, massive; sandstone sample at 480.0 ft 

494.8-508.6 Siltstone, light-gray, micaceous, bedded

508.6-509.6 Shale, dark-gray to black, carbonaceous, poorly bedded, micaceous

509.6-511.2 Sandstone, medium- to dark-gray, very fine grained, micaceous; carbonaceous sample at 510.0 ft 

511.2-513.0 Shale, dark-gray, poorly bedded; many plant impressions; missing core 

518.9-521.0 Sandstone, light- to medium-gray, micaceous 

521.0-555.8 Siltstone, gray to very dark gray, micaceous; some alternating sandstone beds; siderite 541.0 ft; coaly partings 543.0

ft; siderite nodules near base; very burrowed 539.0-542.0 ft, 549.0-550.0 ft; sample at 554.8 ft; missing core 

555.8-631.7 Sandstone, light- to dark-gray, very fine grained to fine-grained, micaceous; near base dark-gray claystone and

ironstone containing plant fragments; coaly shale sample at 558.0 ft; sandstone samples at 566.0, 568.6, 598.0,

609.0, 620.0, and 626.0 ft; pyrite sample at 583.6 ft.; siderite beds as thick as 1.25 in.; missing core 

631.7-634.8 Sandstone, light-gray, fine-grained, micaceous, massive to irregularly bedded 

634.8-648.0 Shale and claystone, light- to dark-gray, hard, carbonaceous, calcareous; many plant impressions; 2.0-in.-thick coal

bed 646.0 ft; missing core (10.0 ft)

648.0-660.9 Limestone, light-greenish-gray, fossiliferous, massive 

660.9-675.0 Shale, dark-gray, calcareous; sandstone laminae; missing core (12.0 ft) 

675.0-682.8 Sandstone, gray, medium-grained, calcareous, clean; Caseyville(?) Formation; sample at 675.8 ft
E28 EVOLUTION OF SEDIMENTARY BASINS ILLINOIS BASIN

Appendix table 4. Sangamon County, Dlinois, core Continued.

Depth Description

Mississippian(?) limestone

682.8-697.9 Limestone, oolitic, light-grayish-brown

Appendix table 5. Saline County, Dlinois, core.

Depth Description

Tradewater Formation

10.0-39.8 Sandstone, light-gray, micaceous; wavy bedding; shale partings in basal 2.0 ft; coal and black shale stringers;

sandstone samples at 31.0 and 37.0 ft

39.8^41.0 Alternating siltstone and sandstone, light- to dark-gray, argillaceous and carbonaceous, burrowed 

41. 0^42.0 Limestone, brownish-gray, massive 

42.0^6.0 Claystone, olive-gray, black at top with trace of coal

46.0-51.0 Siltstone, medium- to light-gray, micaceous; massive at top, laminated toward base 

51.0-57.0 Alternating dark-gray shale and light-gray sandstone, micaceous, burrowed 

57.0-71.7 Shale with sandstone laminae, dark-gray, plant fossils; grades downward to very dark gray shale at base; pyritic at

base

71.7-73.6 Delwood Coal Member 

73.6-75.6 Missing core

75.6-81.2 Claystone, dark-olive-gray, carbonaceous; plant debris; 1.0-2.0-in. siderite nodules 

81.2-90.2 Mudstone and siltstone, greenish to dark-olive; organic-rich mudstone sample at 83.0 ft 

90.2-91.3 Claystone, very dark gray; sandy at base; plant debris

91.3-93.5 Sandstone, medium- to dark-olive-gray, fine-grained, micaceous, argillaceous, bioturbated; sample at 91.5 ft 

93.5-128.1 Sandstone, very light gray, fine- to medium-grained; coarsens downward; massive in upper part, carbonaceous and 

micaceous in lower 15.0 ft; rip-up clasts of underlying dark gray shale 121.0-123.0 ft; siderite lens 123.0 ft; 

samples at 108.0, 115.0,116.0, and 123.0 ft

128.1-140.3 Shale, medium- to dark-gray, well-laminated; plant fossils; coaly near top; some very fine sandstone laminae 

140.3-145.4 Sandstone, light-gray, very fine grained, micaceous; dark-gray shale laminae 

145.4-165.7 Shale, dark-gray; sandstone laminae throughout; sandstone sample at 146.0 ft 

165.7-190.1 Sandstone, light-gray to very light gray, fine- to medium-grained, micaceous; dark shale laminae; coal 177.0-178.0 ft;

samples at 189.5 and 190.0 ft 

190.1-192.7 Alternating dark-gray shale and very light gray sandstone, micaceous, burrowed; ripple laminae; 0.5-in. siderite

pebbles 192.7-193.0 ft; 0.5-in.-thick coal bed 189.6 ft

192.7-201.0 Sandstone, light-gray, very fine grained to fine-grained, micaceous; dark-gray shale laminae; thin zone of shale and 

siderite clasts 194.6 ft

Appendix table 6. Pope County, Illinois, core.

Depth Description

Tradewater Formation

21.0-25.5 Siltstone and interbedded very fine grained sandstone, orange to light-gray, micaceous, oxidized; clay clasts

25.5-26.0 Shale, dark-gray, laminated with fine-grained sandstone

26.0-29.5 Shale, dark-gray, alternating with sandstone

29.5-31.6 Sandstone, reddish, medium-grained, carbonaceous, micaceous; clay clasts at base; 0.25-in.-thick coal 31.6 ft; sample

at 30.6 ft

31.6-3 3.5 Sandstone, gray, medium-grained, black-stained 

33.5-33.7 Mudstone, gray, massive; roots(?); coaly nodules 

33.7-51.0 Sandstone, gray-brown, medium-grained, micaceous, hematite-stained; shale clasts; carbonaceous layers; sandstone

samples at 43.0 and 55.0 ft

51.0-68.7 Sandstone, gray, fine- to medium-grained; shale clasts; siderite clasts throughout; siderite sample at 62.0 ft 

68.7-76.7 Shale and siltstone, dark-gray, laminated; carbonaceous to coaly layers; pyrite and siderite 76.5 ft; plant impressions

in black shale near base

76.7-84.4 Siltstone, gray, carbonaceous; plant debris; many siderite beds; deformed bedding 

84.4-86.0 Coal

86.0-94.6 Sandstone, white to light-gray, silty, pyrite at 90.3 ft; samples at 86.6 and 93.0 ft 

94.6-97.9 Shale and interbedded siltstone, dark-gray to black, laminated 

97.9-99.6 Siltstone, dark-gray, carbonaceous, burrowed 

99.6-106.0 Sandstone, white to light-gray, very fine grained, laminated, micaceous; sample at 106.0 ft
p

Appendix table 6. Pope Counft

Depth

106.0-107.6 Mudstone, gree 

107.6-109.5 Shale,dark-gray 

109.5-1 15.0 Mudstone and s 

115.0-115.7 Underclay(?), si 

1 1 5.7-1 1 7. 1 Siltstone, gray, 

117.1-128.2 Sandstone, ligh 

128.2-128.5 Sandstone, ligh 

128.5-141.0 Sandstone, light

Appendix table 7. Perry Count

Depth

190.0-202.2 Sandstone, light 

202.2-2 12.7 Siltstone and sh 

212.7-213.6 Coal 

213.6-269.7 Siltstone and sh 

shale in basa 

269.7-271.7 Sandstone, light 

271.7-282.8 Shale, dark-gray 

282.8-285.5 Sandstone, light 

285.5-314.8 Shale, mediumbase; plant d 

314.8-334.5 Sandstone, light 

cement 328.C 

334.5-383.1 Shale, medium383. 1-385.0 Sandstone, brov 

385.0-386.7 Sandstone, gray 

gray shale be

386.9-392.2 Sandstone, gray 

Caseyville(T 

392.2^137.1 Conglomerate,! 

394.4 ft; son 

Core continues to 450.0 ft, but n

Appendix table 8. Williamson

Depth

8.0-18.3 Sandstone, yelk 

base of inter 

2 1 .0-22.7 Sandstone, brov 

grained at ba 

27.0-92.4 Shale, mediumpyritic; coal 

68.3-68.5 ft; 

92.4-93.5 Sandstone, light 

93.5-94.7 Shale, dark-broA 

94.7-94.9 Sandstone, light 

94.9-97.7 Shale, dark-grec 

97.7-101.0 Sandstone, light

STTERNS OF DIAGENESIS IN PENNSYLVANIAN SANDSTONES £29 

, Dlinois, core Continued.

Description

Tradewater Formation Continued

ish-gray; noncalcareous white nodules 

to black, silty, carbonaceous, micaceous 

tale, dark-gray, silty; plant fragments 

ty, carbonaceous; plant debris 

aminated 

 gray, fine-grained, carbonaceous, micaceous 

 gray, fine-grained, very hard and smooth 

 gray, fine-grained, massive, micaceous; some coaly layers; sandstone sample at 136.0 ft

', Dlinois, core.

Description

Tradewater Formation

 gray, fine-grained, micaceous; shale laminae; sample at 200.0 ft 

lie, light- to medium-gray, laminated, carbonaceous

lie, light-greenish-gray to olive-gray, siderite cemented in places; underclays 214.5 ft; mostly pyritic 

1 10.0 ft; plant impressions 252.0-254.0 ft; coaly layers 259.0 ft 

 gray, fine-grained; some interbedded shale; siderite layers; sandstone sample at 271.0 ft 

to black, laminated; some gray crossbedded sandstone lenses; sandstone sample at 282.0 ft 

-gray, fine-grained, micaceous, interbedded with dark-gray shale; sandstone sample at 285.0 ft 

5ray to black; siltstone laminae top 7.0 ft; 3-in.-thick sandstone bed 299.0 ft; interbedded sandstone 

:bris 314.0 ft; sandstone sample at 299.0 ft 

 gray, medium-grained, micaceous, argillaceous; granule-size pebbles (not quartz); some siderite 

-330.0 ft; sandstone samples at 318.0, 332.0, and 334.0 ft 

jray, silty; plant debris; calcareous 353.0-359.0 ft; scattered siderite nodules 

n, fine- to medium-grained; siderite concretions (1 in.); shale laminae; sandstone sample at 385.0 ft 

brown, medium-grained; siderite concretions (1 in.) and sandstone rip-up clasts; 4-in.-thick mediumds at top and bottom

Caseyviile(?) Formation

to light-brown, fine-grained, micaceous; siderite concretions; conglomeratic near base; typical 

lithology; sandstone sample at 392.0 ft 

ght-gray; 0.5-in. pebbles of quartz and chert; some siderite cement; Caseyville(?); coal fragments at 

e sandstone beds; sandstone samples at 400.0 and 43 1 .0 ft 

o sampling was done

County, Illinois, core.

Description

Tradewater Formation

w-brown to brown, fine- to coarse-grained, iron-stained; clay and oxidized siderite clasts (1.0 in.) at 

al; sandstone samples at 8.0 and 19.0 ft; core loss 2.2 ft 

n to yellowish-brown, medium-grained, iron-stained, micaceous; black organic(?) areas; coarse 

se; sandstone sample at 21.5 ft 

to dark-gray; silty in parts; scattered siderite nodules as large as 1.0 in.; carbonaceous; rootlets; 

>eds 52.6-53.1 ft, 75.7-77.2 ft, 78.1- 78.6 ft; siderite lenses 32-32.1, 32.6-32.8, 65.4-66.7, and 

limestone beds 37.7-38.4, 44.2^15.6, 45.5- 45.7, 89.2-90.8, and 91.0-92.1 ft.; core loss 4.9 ft 

to medium-gray, fine- to medium-grained, massive 

vnish- to medium-gray 

to medium-gray, fine-grained, micaceous; sample at 94.7 ft 

nish-gray, silty, micaceous; siderite at top 

to medium-gray, fine-grained, wavy to massive, micaceous; sample at 100 ft; core loss, 0.2 ft
E30 EVOLUTION OF SEDIMENTARY BASINS ILLINOIS BASIN

Appendix table 9. Sullivan County, Indiana, core.

Depth Description

Brazil and Mansfield Formations, Raccoon Creek Group

720.0-724.6 Sandstone, very light gray, fine- to medium-grained

724.6-727.3 Sandstone, pale-yellowish-brown, fine-grained; sideritic with clay clasts and pyrite; abundant kaolinite in spots;

	sample at 726.5 ft

727.3-733.0 Sandstone, very light gray, fine-grained, slightly sideritic

733.0-740.9 Sandstone, very light gray, fine- to medium-grained; siderite nodules; kaolinite specks

740.9-742.6 Sandstone, very light gray, fine-grained, calcareous; occasional siderite nodules; shaly toward base; sample at 741.0

	ft; 0.7 ft missing near base 

742.6-791.8 Sandstone, very light gray, fine- to medium-grained; dark-gray shale laminae are micaceous and carbonaceous in top

	0.7 ft; brown siderite beds and nodules; samples at 744.0, 754.0, 782.0, 788.0, and 789.5 ft 

791.8-793.3 Shale, dark-gray, sideritic

793.3-800.8 Sandstone, very light gray, fine- to medium-grained, micaceous; dark-gray shale laminae; siderite nodules

800.8-802.0 Coal; calcite in cleats

802.0-803.4 Siltstone, medium-gray; carbonized plant debris; tidalite

803.4-804.7 Sandstone, very light gray, fine-grained; coal and carbonaceous stringers at top and bottom of interval

804.7-805.1 Carbonate rock, medium-dark-gray, very fine grained, brecciated; carbonized plant impressions

805.1-807.2 Sandstone; very light gray, fine-grained, locally brecciated; coal stringers and carbonaceous shale laminae

807.2-818.5 Siltstone, gray, locally sideritic and brecciated; shaly in top 1.5 ft; carbonized plant material; clay clasts near base

818.5-820.5 Sandstone, very light gray, very fine grained; gray shale laminae; sample at 817.5 ft

820.5-857.1 Shale, dark-gray to black; dark-brown siderite beds; carbonate bed 845.3 ft; carbonized plant impressions; thin

	sandstone laminae at base

857.1-877.6 Shale, dark-gray, sideritic, laminated with very light gray, fine-grained sandstone

877.6-879.3 Siltstone, light-gray, calcareous, clayey; carbonized plant debris; sample at 879.0 ft

879.3-919.5 Sandstone,white, fine-grained; paper-thin dark laminae; thin micaceous and carbonaceous laminae in lower part;

	sample at 881.0 ft

919.5-923.2 Shale, dark-gray, interbedded with very light gray sandstone

923.2-924.2 Siltstone, very light gray; dark shale laminae; pyrite band at top; sample at 924.0 ft

924.2-928.5 Shale, medium-dark-gray, pyritic; sandy specks of carbonaceous material

928.5-930.0 Missing core

930.0-931.2 Coal; calcite in cleats; pyrite band in middle of interval

931.2-935.5 Shale, grayish-black, interbedded with medium-gray clay; carbonaceous

935.5-939.5 Coal; laminated with shale

939.5-940.0 Underclay, light-gray; carbonized rootlets

940.0-946.0 Sandstone, white, fine-grained, clayey; sample at 942.0 ft _____________

Appendix table 10. Greene County, Indiana, core.

Depth Description

Brazil Formation, Raccoon Creek Group

20.0-34.2 Sandstone, light-gray, fine-grained, micaceous; wavy carbonaceous laminae; samples at 23.5 and 31.5 ft

34.2-50.3 Sandstone, gray to dark-gray, fine-grained; carbonaceous and coaly lenses

50.3-52.5 Shale, black, very carbonaceous, interbedded with gray, fine-grained sandstone

52.5-52.9 Coal, banded; pyrite cleat fillings

52.9-53.6 Sandstone, gray, fine-grained, micaceous, carbonaceous

53.6-55.0 Shale, gray, slightly carbonaceous; sandy near base

55.0-71.6 Sandstone, light-gray,very fine grained to fine-grained, micaceous, carbonaceous; calcareous toward base; black 

siderite nodules; samples at 67.3 and 71.5 ft

71.6-73.3 Coal, banded; pyrite lenses; calcite cleat fillings

73.3-76.3 Underclay, gray; carbonized plant fragments; siderite nodules near base

76.3-82.0 Shale, dark-gray, carbonaceous; interbedded with light-gray, fine-grained sandstone in upper part, grades downward 

into silty shale with tan siderite nodules at base

82.0-82.3 Coal, banded

82.3-87.6 Shale, dark-gray, silty, carbonaceous at top; siderite nodules at base

87.6-100.0 Sandstone, gray, fine-grained, micaceous, interbedded with carbonaceous shale; coaly lenses; samples at 91.5, 93.1,

and 94.0 ft

100.0-110.0 Shale, dark-gray, silty, carbonaceous; sandy laminae; tan siderite beds 

110.0-118.1 Shale, dark-gray, carbonaceous; tan siderite beds
PATTERNS OF DIAGENESIS IN PENNSYLVANIAN SANDSTONES E31

Appendix table 10. Greene County, Indiana, core Continued.

Depth Description

Brazil Formation, Raccoon Creek Group Continued

118.1-121.9 Lower Block(?) Coal; shiny

121.9-123.1 Underclay, gray, carbonaceous; sandy near base; scattered siderite nodules_______________________ 

______________________________Mansfield Formation, Raccoon Creek Group_____________________________ 

123.1-127.5 Sandstone, gray, very fine grained, micaceous, carbonaceous; gray shale laminae

127.5-134.0 Sandstone, gray, fine-grained, micaceous, carbonaceous; tan siderite pebbles; silty near base; sample at 130.5 ft 

134.0-137.6 Shale, gray; slightly silty siderite nodules; white to light-gray, fine-grained sandstone nodules and bands;

carbonaceous in basal foot 

137.6-148.7 Sandstone, light-gray, fine-grained, micaceous; dark-gray shale lenses in upper part; carbonaceous streaks; tan

siderite lenses in lower part; sample at 144.5 ft

148.7-156.2 Sandstone, gray, fine-grained, micaceous; carbonaceous streaks and bands 

156.2-163.9 Sandstone, light-gray, fine-grained, micaceous, burrowed, interbedded with carbonaceous shale; siderite bands in

lower part; sample at 158.5 ft

163.9-165.1 Shale, black, carbonaceous, clayey, pyritiferous, thin; light-gray; fine-grained sandstone bands near top 

165.1-190.6 Shale, gray; silty near base; carbonized plant debris and tan siderite beds and nodules; pyritiferous 

190.6-192.4 Shale, dark-gray, pyritiferous; carbonized plant debris 

192.4-193.7 Coal, banded, bright, pyritiferous; shaly near base 

193.7-194.9 Shale, clayey, gray, carbonaceous

194.9-199.5 Siltstone, gray, carbonaceous, interbedded with light-gray, fine-grained siltstone

199.5-203.9 Sandstone, light-gray to gray, fine-grained, interbedded with gray, carbonaceous siltstone; sample at 200.0 ft 

203.9-246.4 Sandstone, gray, fine- to medium-grained, micaceous, carbonaceous; bands of gray to dark-gray, silty, carbonaceous

shale; samples at 210,228,237.5, and 240.0 ft 

246.4-250.7 Shale, gray to dark-gray, silty, micaceous, carbonaceous, interbedded with light-gray, fine- to medium-grained

sandstone 

250.7-290.0 Sandstone, light-gray, fine-grained, micaceous, carbonaceous, interbedded with bands of dark-gray, silty,

carbonaceous, micaceous shale containing a few tan siderite beds; samples at 253.0,269.0,280.0, and 282.5 ft 

290.0-292.1 Shale, dark-gray, interbedded with light-gray, fine-grained sandstone

292.1-315.2 Sandstone, light-gray, fine-grained, micaceous; dark-gray, carbonaceous shale laminae; sample at 298.0 ft 

315.2-330.3 Sandstone, light-gray, fine-grained, micaceous, slightly carbonaceous, friable; scattered dark-gray shale bands in

upper part; sample at 318.0 ft 

330.3-338.6 Sandstone, light-gray to gray, fine-grained; irregularly shaped, dark-gray, carbonaceous shale galls and tan siderite

nodules; sample at 333.0 ft

338.6-340.4 Sandstone, light-gray, fine-grained, micaceous; sample at 340.0 ft

340.4-349.6 Sandstone, light-gray, fine- to medium-grained, slightly micaceous; dark-gray, carbonaceous shale galls 

349.6-363.8 Sandstone, light-gray, medium-grained, micaceous, carbonaceous; tan siderite nodules; gray siltstone bands; thin

carbonaceous laminae; sample at 353.0 ft 

363.8^413.0 Sandstone, light-gray, fine- to medium-grained, micaceous; black carbonaceous laminae; dark-gray, dense siderite

nodules; samples at 386.0 and 406.0 ft

413.0-418.4 Siltstone, gray, interbedded with fine-grained sandstone 

418.4^20.0 Sandstone, light-gray, fine-grained, carbonaceous; sample at 420.0 ft 

420.0^30.0 Siltstone, light-gray, micaceous; carbonaceous laminae

430.0^52.2 Shale, dark-gray, silty; carbonized plant debris; tan siderite bed at base of interval 

452.2^54.5 Sandstone, light-gray, fine-grained, micaceous; carbonaceous streaks; silty at base of interval 

454.5^56.6 Siltstone, dark-gray, carbonaceous, interbedded with light-gray sandstone 

456.6^59.4 Sandstone, gray, medium-grained, micaceous, carbonaceous; pyrite in lower part; siltstone and siderite fragments;

siderite cement

459.4-479.8 Siltstone, gray, carbonaceous, interbedded with light-gray sandstone; black pebbles; zones of shaly siltstone 

479.8^95.8 Sandstone, light-gray, medium-grained and conglomeratic, pyritiferous, carbonaceous; contorted bedding; gray

siderite nodules

495.8-516.0 Shale, gray, pyritiferous; fine-grained sandstone laminae; shale and siderite nodules in lower part of interval_____

Mississippian limestone __ _____________________

" 'RINTING OFFICE: 1996 - 774-045 / 20021 REGION NO. 8