Geology of the Eddyville, Stonefort, and Creal Springs Quadrangles, Southern Illinois

Home , Clear Creek Chert, Degonia Formation, Grove Church Shale, Lusk Creek, Saline River (Illinois), Staunton Formation

ILLINOIS GEOLOGICAL 557 IL6b SURVflfc UBRAR? no. 96

GEOLOGY OF THE EDDYVILLE, STONEFORT, AND CREAL SPRINGS QUADRANGLES, SOUTHERN ILLINOIS

Department of Energy and Natural Resources ILLINOIS STATE GEOLOGICAL SURVEY

BULLETIN 96 1991 Digitized by the Internet Archive

in 2012 with funding from

University of Illinois Urbana-Champaign

http://archive.org/details/geologyofeddyvil96nels GEOLOGY OF THE EDDYVILLE, STONEFORT, AND CREAL SPRINGS QUADRANGLES, SOUTHERN ILLINOIS

W. John Nelson, Joseph A. Devera, Russell J. Jacobson, Donald K. Lumm, Russel A. Peppers, Brian Trask, C. Pius Weibel, Leon R. Fbllmer, and Matthew H. Riggs Illinois State Geological Survey

Steven P. Esling, Elizabeth D. Henderson, and Mary S. Lannon Southern Illinois University, Carbondale, IL

BULLETIN 96 1991

ILLINOIS STATE GEOLOGICAL SURVEY Morris W. Leighton, Chief 615 East Peabody Drive Champaign, IL 61820

_A CONTENTS

ABSTRACT INTRODUCTION Location and Climate Topography Geologic Setting Previous Studies Method of Study STRATIGRAPHY OF THE BEDROCK Cambrian Through Devonian Systems Mississippian System Clore Formation Degonia Formation Kinkaid Limestone Chesterian Undifferentiated Mississippian-Pennsylvanian Contact Pennsylvanian System Caseyville Formation Abbott Formation Spoon Formation Carbondale Formation

SURFICIAL GEOLOGY Physiography Methodology Field Methods Laboratory Methods Construction of Stack-Unit Map Stratigraphy Lithostratigraphic Units: Upland Formations 47 Lithographic Units: Valley Formations 53 Pedostratigraphic Units Resources Land Use Appendix A

STRUCTURAL GEOLOGY AND MINERAL DEPOSITS Structural Features Shawneetown Fault Zone Lusk Creek Fault Zone McCormick Anticline New Burnside Anticline Battle Ford Syncline Bay Creek Syncline Geophysical Expression of Anticlines Origin of McCormick and New Burnside Anticlines Time of Deformation of Anticlines Little Cache Fault Zone Other Structures Mineral Deposits Coal Oil and Gas Fluorspar and Related Minerals Stone, Sand, and Gravel

REFERENCES 1

Figures

1 I ocation map 2 Regional geologic setting of stud) area

3 Ski'ti li ol north-south profile through Eddyville Quadrangle

4 Graphic column ol C hesterian Series in study area 5 Graphic logo! Alcoa tesl hole, Eddyville Quadrangle 6 Generalized stratigraphic column of bedrock units exposed in study area 7 Formations! nomenclature ol the Pennsylvanian System in the Illinois B.isin 8 typical Null exposure ol Battery Rock Sandstone

9 Measured sections of ( aseyville Formation 10 Type section ol Abbott Formation, Stonefort Quadrangle

1 ( ieneralized stratigraphic cross section ol Abbott Formation,

I ddyville and Creal Springs Quadrangles 12 Composite section ol basal Abbott shale and sandstone sequence, Eddyville Quadrangle 13 typical planar-bedded sandstone ol the lower Abbott

Formation, I ddyville Quadrangle 14 lateral fades change in middle and lower part of Abbott Formation in Dixon Springs Graben 1^ Trace fossil Conostichus in middle Abbott Formation, Creal Springs Quadrangle 16 Murray bluff Sandstone al its maximum development, Eddy- ville Quadrangle 17 Liesegang banding in Murray Bluff Sandstone 18 Railroad cut showing upward lithologic changes in basal Spoon Formation 19 Profile of railroad cut south of Oidtown, showing New Burn- side Anticline 20 Sketch of surface mine highwall, showing New Burnside Coal, Creal Springs Quadrangle 21 Strata exposed on highwall of Western Mining Company surface mine, Stonefort Quadrangle 22 Section in abandoned railroad cut at type locality of Carrier Mills Shale Member, Spoon Formation 23 Carrier Mills Shale Member at type locality shown in figure 22 24 Composite section of strata exposed in and near Brown Brothers Excavating Company mines 25 Stratigraphic classification of Quaternary deposits in study area 26 Vertical distribution of clay minerals and particle sizes in boring ED8, and general locations of borings mentioned in chapter 27 Cross section showing distribution of Quaternary units in the Sugar Creek valley 28 Cross section showing distribution of Quaternary units in the Pond Creek valley 29 Vertical distribution of clay minerals and particle sizes in boring CS20 30 Vertical distribution of clay minerals and particle sizes in boring SF3 31 Vertical distribution of clay minerals and particle sizes in boring CS25 32 Vertical distribution of clay minerals and particle sizes in boring CS27 33 Vertical distribution of clay minerals and particle sizes in boring CS24 34 Vertical distribution of clay minerals and particle sizes in boring SF14 35 Vertical distribution of clay minerals and particle sizes in boring SF26 36 Cross section showing distribution of Quaternary units in Little Saline River valley Figures

37 Structural features of study area 38 Profile of Lusk Creek Fault Zone, Section 31, T11S, R6E 39 Profile of Lusk Creek Fault Zone, SW, Section 35, T11S, R6E 40 Profile of Lusk Creek Fault Zone southwest of Lost 40 Mine 41 Interpreted history of Lusk Creek Fault Zone 42 Cross section of McCormick structure and Winkleman Fault 43 Cross section through fault on McCormick Anticline 44 Sketch of field relationships, Eddyville Quadrangle 45 Cross-section sketch of field relationships west of McCormick 46 Rose diagrams of joint orientations along and south of McCormick Anticline 47 Profile of New Burnside structure on west side of Blackman Creek, Eddyville Quadrangle 48 Profile of New Burnside structure where it crosses Battle Ford Creek, Eddyville Quadrangle 49 Profile of hillside east of ravine in Eddyville Quadrangle 50 Fault surface exposed by mining in Brown Brothers Excavating No. 2 Mine north of Eddyville Quadrangle 51 Trace-slip fault in Stonefort Quadrangle 52 Rose diagrams of joint orientations on and near New Burnside Anticline, Eddyville Quadrangle 53 Residual vertical magnetic intensity in and adjacent to study area 54 Cross section in western Maryland and West Virginia 55 Profile in Ruhr coal basin, West Germany, showing deformation of Upper Carboniferous strata 56 Example of foreland detachment structure in Anadarko Basin, Oklahoma 57 Hypothetical origin of McCormick and New Burnside Anti- clines and associated faults 58 Sketch of east side of railroad cut south of tunnel portal, Stonefort Quadrangle, showing north-dipping thrust faults

Tables

1 COGEOMAP cored test holes in study area 5 2 Thickness of strata in selected deep wells in and near study area 8 3 Oil test holes in study area 10 4 Thickness of Caseyville Formation in study area 17 5 Analytical data on coal in study area 36 6 Relation between modern soil series and map units of this study 46 7 Locations of borings 50

Stratigraphic columns of cored test holes and measured sections in and near Eddyville, Stonefort, and Creal Spring Quadrangles

_A ABSTRACT

The Eddyville, Stonefort, and Creal The overlying Abbott Formation, Cahokia Alluvium occupies stream Springs 7.5-Minute Quadrangles of late Morrowan and Atokan age, valleys throughout the region. are in southern Saline and William- thickens eastward from 220 to 400 Structurally, the region lies on the son and northern Johnson and Pope feet across the study area. The Abbott southern margin of the Illinois Basin; Counties, Illinois. Most of the study consists of numerous sandstone bedrock strata dip regionally north- area is within the Shawnee Hills bodies, more lenticular than those of ward. Folds and faults in the report section of the Interior Low Plateaus the Caseyville, interbedded, and area represent three major episodes physiographic province; the north- intertonguing with gray to black of deformation. The first was normal ern edge is in the Central Lowlands shale, siltstone, and local coal. faulting related to rifting that oc- province. Sedimentary rocks of Abbott sandstones are mineralogi- curred near the end of Precambrian Mississippian and Pennsylvanian cally less mature than Caseyville time along the Shawneetown and age crop out in the Shawnee Hills, sandstones and generally lack quartz Lusk Creek Fault Zones at the south- and Pleistocene glacial deposits cover pebbles. The proportion of sand- eastern corner of the map area. The

Pennsylvanian bedrock in the Cen- stone in the Abbott increases east- second was Permian (?) compression, tral Lowlands. ward. Shale and siltstone in the which induced high-angle reverse Exposed Mississippian rocks are Abbott locally contain abundant trace faulting in the Lusk Creek Fault Zone assigned to the Clore and Degonia fossils, some indicating marine and detached thrusting and folding Formations and the Kinkaid Lime- sedimentation; some marine body in the McCormick and New Burnside stone, all of upper Chesterian age. fossils have also been found. The Anticlines. The third event was

The Clore contains 95 to 155 feet of Abbott is interpreted as consisting Triassic or Jurassic (?) extension, shale, sandstone, and limestone, of mostly of subaqueous deposits of a during which earlier formed reverse which the upper 30 feet is exposed. series of deltas that prograded west- faults underwent normal movement The Degonia consists of 20 to 64 feet ward and southwestward. and many new normal faults were of shale, siltstone, and very fine- The lower Desmoinesian Spoon formed. The McCormick Anticline grained sandstone. The Kinkaid, 85 Formation thickens eastward from may have begun to rise during to 230 feet thick, consists of lime- 200 to 300 feet. In comparison with Morrowan and Atokan sedimenta- stone, shale, claystone, and sand- the Abbott, the Spoon contains less tion; evidence for the uplift includes stone. A prominent unconformity sandstone, more shale, and thicker paleoslumps, local unconformities, separates the Kinkaid from Pennsyl- and more widespread coal and and facies patterns that appear to vanian strata. limestone beds. The Spoon repre- follow the anticline. The oldest Pennsylvanian forma- sents deltaic and shallow-marine Coal has been extracted in the tion is the Caseyville Formation, of sedimentation in an increasingly study area from surface mines and Morrowan age. About 200 to 450 feet stable regime. from small drift and slope mines. thick, the Caseyville consists primar- The Carbondale Formation, ex- Coals of the lower Abbott and Spoon ily of quartz-arenitic sandstone. Four posed in a small part of the Eddyville Formations, particularly the Del- members are recognized: the Way- Quadrangle, is the youngest bedrock wood and Mt. Rorah Coals, offer side (oldest), Battery Rock Sand- in the study area. The Carbondale prospects to small operators; how- stone, Drury, and Pounds Sand- contains regionally continuous, thick ever, careful exploratory drilling stone. The Battery Rock and the coal and black fissile shale, and must be done because of the variable Pounds are thick (30 to 120 ft), displays pronounced cyclicity. thickness and quality of the coals and cliff-forming, widely traceable, The Glasford Formation, an II- their limited continuity. Twenty-nine thick-bedded sandstones that com- linoian glacial till, covers the north- petroleum test holes have been monly contain quartz granules and western Creal Springs Quadrangle. drilled in the study area; all were dry pebbles. The poorly exposed Way- Adjacent valleys contain Illinoian and were abandoned. Chesterian tar- side Member is composed of gray to ice-margin deposits, which we have gets on major anticlines have been black, silty shale and siltstone, very correlated with the Teneriffe Silt. tested; deeper possibilities are fine-grained, thin-bedded sand- Sediments of Wisconsinan slackwa- speculative. Fluorspar has been stone, and lenses of thick-bedded ter lakes in the northern part of the mined from veins along the Lusk sandstone. The Drury Member is study area are termed Equality Creek Fault Zone, and reserves similar but contains thin, discontinu- Formation. Uplands throughout the probably exist at depth there. Lime- ous coal beds. The Caseyville repre- area are mantled with residuum (Oak stone, sand, and gravel can be quar- sents a variety of depositional envi- formation), colluvium (Peyton For- ried, but poor access and distance to ronments, ranging from estuary or mation), and loesses: the Loveland market limit the potential for de- embayment (shale with goniatites) to (Illinoian), Roxana (Altonian), and velopment. swamp (coal and rooted claystone), Peoria (Woodfordian). The Holocene in an overall deltaic setting. II

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CD g -A INTRODUCTION

This study was conducted as part of northwestern Pope Counties in Escarpment is a moderately rolling the ongoing Cooperative Geologic southeastern Illinois (fig. 1). The upland cut by many deep ravines. Mapping Program (COGEOMAP) of study area is rural; the largest towns Drainage in the study area is rela- the U.S. Geological Survey (USGS) are Creal Springs (population 845), tively youthful: the region has been and the Illinois State Geological Stonefort (population 316), New subjected to erosion for a relatively Survey (ISGS). The USGS initiated Burnside (population 276), and short time. Small streams are well COGEOMAP in 1985 as a national Eddyville (population about 100). adjusted to bedrock structure, but program to revitalize geologic map- Most of the land is privately owned, larger ones cut across structures and ping. The first cooperative agreement but the U.S. Forest Service holds follow incised meanders. Most larger between the ISGS and the USGS, surface and mineral rights in large streams have steep sides and flat, signed in 1985, provided that the tracts in the Shawnee National alluviated bottoms. Small ravines ISGS supply personnel and research Forest, especially in the Eddyville generally have a V-shaped profile. facilities and the USGS supply tech- and Stonefort Quadrangles. Topo- Part of the northwestern Creal nical and financial assistance. Survey graphic maps showing Forest Service Springs Quadrangle is mantled with staff had mapped part of the Creal lands and trails are available from the glacial drift, and in this region the Springs Quadrangle before 1985. The Forest Service office in Harrisburg, topography is gently rolling. Broad, initial COGEOMAP agreement called Illinois. level, swampy areas along streams in for publication of three quadrangles Southern Illinois has a warm tem- the northernmost parts of all three already mapped (Nelson and Lumm perate climate. Rainfall averages 42 quadrangles are underlain by glacio- 1986a,b,c) and for mapping an inches yearly; spring is the wettest lacustrine sediments. These areas are additional twelve 7.5-minute quad- season and fall the driest (Miles and part of the Mt. Vernon Hill Country, rangles.* Weiss 1978). Most of the geologic a division of the Central Lowlands The Eddyville, Stonefort, and mapping was conducted in the cool (Leighton et al. 1948). Creal Springs Quadrangles were months (from late October to early Bedrock outcrops in the study area selected as the initial COGEOMAP May) when vegetation presented less are found mainly along ravines. quadrangles for several reasons: (1) of a problem. Sandstone forms bluffs or ledges the proximity of these quadrangles along valley walls and crops out to quadrangles already mapped or Topography extensively along the beds of small being mapped; (2) the desire to Most of the study area is in the to medium-sized streams. Some follow up challenging structural and Shawnee Hills section of the Interior Pennsylvanian sandstones are resis- stratigraphic problems that had been Low Plateaus physiographic pro- tant enough to produce cliffs away identified during previous mapping vince (Leighton et al. 1948, Horberg from streams. Prominent hogbacks (for instance, several fault zones and 1950). The Shawnee Hills are a strip of these sandstones occur along anticlines that have received little of rugged bedrock hills between the anticlines and faults. Exposures of attention occur in the quadrangles); drift-covered Central Lowlands to shale and siltstone are small and

(3) the exposures of the problematic the north and the Mississippi Embay- generally confined to cutbanks of lower Pennsylvanian succession (be- ment to the south. A southern belt active streams. Shale, siltstone, and low the Carbondale Formation) in of the Shawnee Hills—most of which limestone are grossly underrepre- the quadrangles, and the existence lies south of the study area—is sented in natural exposures because of type localities for many named underlain by Mississippian lime- of the humid climate and extensive units in or near the study area; and stone, shale, and sandstone that pro- soil and vegetation. Railroad cuts, (4) the known existence but poor duce a gently to moderately rolling roadcuts, and exposures in mines delineation of coal resources in the topography and broad, alluviated provide more complete views of the quadrangles, and the unsuccessful stream valleys. The northern belt of strata but are few and far between. oil exploration conducted in the the Shawnee Hills, underlain by region. sandstone and shale of Pennsylvan- Geologic Setting ian age, has a more rugged topog- The study area is on the southern Location and Climate raphy. The Pounds Escarpment, com- margin of the Illinois Basin, a struc- The Eddyville, Stonefort, and Creal posed of massive, conglomeratic, tural and depositional basin (fig. 2). Springs Quadrangles are in south- basal Pennsylvanian sandstones, is The Illinois Basin contains sedimen- western Saline, southeastern Wil- near the southern edge of the map tary rocks ranging in age from Cam- liamson, northeastern Johnson, and area. The area north of the Pounds brian to earliest Permian. The present

*In 1986, geologic maps of the Shawneetown, Equality, and Rudement Quadrangles were published in the new ISGS series, Illinois Geologic Quadrangles (IGQ). The accompanying report was published as Circular 538 (1987). The Eddyville, Stonefort, and Creal Springs IGQs discussed in this report were published in 1990 as IGQ-4, IGQ-5, and IGQ-6. Figure 2 Regional geologic setting of the study area. Stippled region 150 represents Late Precambrian-Early Cambrian rift system (Reelfoot Rift and ° 50 10° km Rough Creek Graben). FAFC = Fluorspar Area Fault Complex; H = Hicks Dome; LC = Lusk Creek Fault Zone; MC = McCormick Anticline; NB = New Burnside Anticline; WV = Wabash Valley Fault System. (Modified from King and Beikman 1974).

configuration of the basin is largely eastern edge of the Eddyville Quad- nian rocks and speculated on the the result of uplift on the south rangle and strikes north-northeast. origin of structures in and near the (Pascola Arch) that developed middle About 12 miles northward the fault present study area, also discussed oil Pennsylvanian time. The system abruptly curves to the east possibilities in southern Illinois. thickest preserved Paleozoic succes- and continues more than 100 miles Smith (1957) mapped strippable coal sion in Illinois (about 15,000 ft) is at into Kentucky. The Rough Creek- reserves and refined the stratigraphy the center of the Fairfield Basin. Shawneetown System contains high- of Pennsylvanian rocks in and Thicker sedimentary rocks—possibly angle reverse and normal faults and around the study area. Potter (1957) 25,000 feet—are found in western bears evidence of several episodes of examined deformed Pennsylvanian Kentucky, south of the Rough Creek- movement (Nelson and Lumm 1984). rocks in railroad cuts in the Stonefort Shawneetown Fault System. The Cottage Grove Fault System, a Quadrangle and theorized on the The southern part of the Illinois right-lateral strike-slip system (Nel- cause of the deformation. His report Basin is extensively faulted (fig. 2). son and Krausse 1981), crosses contains a geologic map of a small A swarm of northeast-striking, high- southern Illinois east to west just part of the Stonefort Quadrangle. angle faults crosses southeastern north of the study area. No geologic maps covering more Illinois and the adjacent part of than a fraction of the study area have Kentucky. The name Fluorspar Area Previous Studies been published at a scale larger than Fault Complex has been applied to The first known report covering part 1:500,000. Klasner (1982, 1983) these faults because many of them of the study area was a description mapped the geology of part of the contain commercial vein deposits of by Cox (1875) of the geology of Saline current study area at a scale of fluorite (Grogan and Bradbury 1968). and Gallatin Counties. Brokaw (1916) 1:24,000. His purpose was to assess The Lusk Creek Fault Zone, which discussed geology and oil possibil- the mineral potential for two pro- crosses the southeastern corner of ities of southern Illinois and mapped posed "wilderness" areas in the the Eddyville Quadrangle, marks the structure, including the McCormick National Forest. The 1982 map covers northwest edge of the Fluorspar Area and New Burnside Anticlines. Cady part of the southeastern Eddyville Fault Complex. The Rough Creek- (1926) mapped the areal geology of Quadrangle; the 1983 map includes Shawneetown Fault System branches Saline County. Weller (1940), who part of the west-central Eddyville and off the Lusk Creek Fault Zone at the described and classified Pennsylva east-central Stonefort Quadrangles. Tkble 1 COGEOMAP cored test holes in the study area

TD (ft) Strata penetrated

Creal Springs Quadrangle

C-l NENENW 35-11S-3E 110 Middle and lower Abbott Formation (fig. 10)

C-2 NENWSW 23-11S-3E 83 Cliffy Creek sandstone, olive shale (fig. 16) C-3 SWNENE 25-11S-3E 151 Middle Abbott Formation including marine limestone; Tunnel Hill Coal Bed (fig. 10) C-4 SENESE 29-10S-3E 101 Sub-Davis sandstone, Carrier Mills Shale Member, Wise Ridge Coal Bed, Mt. Rorah Coal Bed, Creal Springs Limestone Member (fig. 21)

C-5 NESESE 36-11S-3E 256 Middle and lower Abbott Formation; Tunnel Hill and Reynoldsburg Coals (fig. 10) C-6 NWNWSE 15-11S-4E 266 Middle and lower Abbott Formation including marine limestone and Tunnel Hill Coal Bed (fig. 10) C-7 SWSWNE 5-11S-4E 156 Golden sandstone, Delwood Coal Bed, Cliffy Creek sandstone (fig. 20)

C-8 NWNENE 26-11S-3E 81 Cliffy Creek sandstone, olive shale (fig. 16)

Eddyville Quadrangle

E-l SENESE 33-10S-6E 201 Golden sandstone, Mitchellsville Limestone Mem- ber, Delwood Coal Bed, Murray Bluff Sandstone Member (fig. 20)

E-2 NENENW 8-11S-6E 141 Middle and lower Abbott Formation (fig. 10)

E-3 SENENE 9-11S-6E 141 Middle Abbott Foramtion (fig . 16) E-4 SWSWNE 32-11S-6E 181 Pounds Sandstone Member, Drury Member, Bat- tery Rock Sandstone Member (fig. 8)

Harrisburg Quadrangle

H-l SWNWSE 20-10S-4E 300 Sub-Davis sandstone, Carrier Mills Shale Member, Stonefort Limestone Member, Wise Ridge and Mt. Rorah Coal Beds, Mitchellsville Limestone Bed, Delwood Coal Bed, Murray Bluff Sandstone Member (fig. 21)

Stonefort Quadrangle

SWNESE 25-10S-4E 196 Sub-Davis sandstone, Carrier Mills Shale, Stone- fort Limestone, Wise Ridge and Mt. Rorah Coal Beds, Creal Springs Limestone Member (fig. 21) SWNESE 29-10S-5E 265 Delwood Coal Bed, unnamed coals; "golden sandstone" (fig. 20) SESENE 33-10S-5E 136 Golden sandstone, Oldtown Coal Bed, Murray Bluff Sandstone Member (fig. 20) NWSENW 25-11S-4E 346 Murray Bluff Sandstone Member, olive shale, lower Abbott sandstone, Tunnel Hill and Reynoldsburg Coal Beds, uppermost Pounds Sandstone Member (fig. 16)

Waltersburg Quadrangle NWNENE 9-12S-5E 280 Basal Caseyville Formation, Kinkaid Limestone, Degonia Formation and uppermost Clore For- mation

Accompanying the maps are discus- the study area are available for inspec- (1965). Bedrock geology immediately sions of the geology, geochemistry, tion in the ISGS library map room. north of the fluorspar district was and mineral potential for the two The region directly east of our mapped by Nelson and Lumm (1986 areas. Klasner's maps show less de- study area has been mapped geolog- a,b,c). A preliminary geologic map tail than ours, and some of his inter- ically at a scale of 1:24,000 (fig. 1). of the quadrangles directly south of pretations, particularly of faulting, The quadrangles constituting the the study area was published by are not supported by our findings. Illinois part of the fluorspar district Weller and Krey (1939). Lamar (1925) Unpublished geologic maps, man- were mapped by Baxter et al. (1963, mapped the Carbondale Quadrangle uscripts, and field notes of parts of 1967) and Baxter and Desborough (scale, 1:62,500), which is west of the Creal Springs Quadrangle. Quadran- mapped the Creal Springs Quad- COGEOMAP holes range from 81 to l gles immediately south and west of rangle from the fall of 1979 through 2 )l feet. Records of these borings are the present study area are currently the spring of 1987. The Eddyville filed in the ISGS Geologic Records. being mapped at a scale of 1:24,000 Quadrangle was mapped by Nelson Field notes from previous studies as part of COGEOMAP (fig. 1). and Lumm, assisted by Devera, by ISGS geologists were gleaned for Numerous studies have been pub- Weibel, and Stephen K. Danner, from useful information. These notes lished on selected aspects of the the fall of 1984 through the spring of include descriptions of outcrops that geology in and near the Eddyville, 1986. Lumm and Nelson mapped the are now covered by colluvium or Stonefort, and Creal Springs Quad- Stonefort Quadrangle in 1986. otherwise lost to study. rangles. The most important strati- R. A. Peppers conducted palyno- Aerial photography in the study graphic studies are by Weller (1940), logical studies of coal samples col- area was of limited value for the Siever (1951), Kosanke et al. (1960), lected during the mapping, and geologist. Most aerial photography and Peppers and Popp (1979). The invertebrate fossils were identified by in southern Illinois is done during sedimentology and petrology of Devera, Jacobson, and Rodney D. the growing season for use in agricul- Pennsylvanian rocks were examined Norby. tural studies. Few details of bedrock by Potter (1957, 1963), Potter and All available well records for the geology can be discerned through Glass (1958), and Siever and Potter study area were examined. Logs of the dense vegetation that covers (1956). Structural geology and igne- boreholes are filed for public inspec- most of the study area during the ous rocks of the region were covered tion in the 1SGS Geologic Records. summer. by Weller et al. (1952), Records include drillers' logs, sample Field notes from this study are Stonehouseand Wilson (1955), Clegg studies, geophysical logs, and very number-keyed to locations marked and Bradbury (1956), and Nelson and limited core data. on topographic maps and kept on Lumm (1984). During the mapping program 17 public file in the Map Room of the stratigraphic test holes were drilled ISGS library. In this publication, Method of Study in or directly adjacent to the study reference is occasionally made by

This report is based principally on area (table 1; plate 1). All of the test number to specific field notes that the geologic study of bedrock out- holes were cored continuously, and can provide the reader with addi- crops. Jacobson and Trask, assisted geophysical logs were obtained for tional detail. by Lumm, Nelson, and Weibel, most of the holes. Total depths of STRATIGRAPHY OF THE BEDROCK W. J. Nelson, J. A. Devera, R. J. Jacobson, D. K. Lumm, R. A. Peppers, C. B. Trask, and C. P. Weibel

CAMBRIAN THROUGH lines up with the northwest margin borehole data (fig. 4). Mississippian DEVONIAN SYSTEMS of a geophysically defined major formations exposed in the quadran- Strata of the Cambrian, Ordovician, graben within the Reelfoot Rift of gles are described in the following Silurian, and Devonian Systems have southeastern Missouri and north- pages. been penetrated in several deep wells eastern Arkansas (Ervin and McGin- Clore Formation in and near the study area (table 2). nis 1975, Hildenbrand et al. 1977, The general succession in these wells Howe and Thompson 1984). Name and correlation The Clore is similar to the succession in other The other proprietary seismic re- Formation was named by Weller wells in the southern part of the Illi- flection profile runs southward from (1913) for Clore School in Randolph nois Basin (Atherton 1971, Willman Franklin County, across the Cottage County, southwestern Illinois. Weller etal. 1975, Schwalb 1982). However, Grove Fault System, to the northern (1920) redefined the Clore, excluding two proprietary seismic-reflection edge of the Mississippi Embayment the newly named Degonia Sandstone profiles viewed by the authors reveal in Massac County, passing near the and Kinkaid Limestone. The Clore is some stratigraphic conditions not western edge of the present study readily correlated in outcrop and sub- previously recognized. area. This profile showed substantial surface throughout southern Illinois The first profile (fig. 3) through the southward thickening of the Cam- on the basis of its lithology, although Eddyville Quadrangle indicates that brian succession but no indication of the proportion of limestone gradu- the Lusk Creek Fault Zone was active growth faulting. The seismic evi- ally decreases eastward from the type during and possibly before deposi- dence negates Schwalb's (1982) area (Swann 1963, Abegg 1986). tion of the Upper Cambrian Mt. assertion that the Cottage Grove Simon/Lamotte Sandstone. The Lusk Fault System was active during Distribution and thickness The Creek Fault Zone crosses the south- Cambrian sedimentation. only outcrops of the Clore found in eastern corner of the Eddyville the study area were in a southeast- Quadrangle. On the seismic profile, flowing stream and in nearby gullies MISSISSIPPIAN SYSTEM as at the surface, the fault zone dips in NW Section 2, T12S, R4E, near the steeply to the southeast. Offset on Mississippian rocks crop out exten- southwest corner of the Stonefort strata above the Mt. Simon/Lamotte sively south of the study area and Quadrangle. The Clore was observed is slight, but the top of crystalline are known from numerous wells just south of the Eddyville Quad- basement appears to be downthrown (tables 1, 2). The youngest Mississip- rangle on the west side of Lusk Creek several thousand feet on the south- pian strata, representing the Clore, and has been projected a short dis- eastern side of the fault zone. An Degonia, and Kinkaid Formations, tance into the Eddyville Quadrangle. interval of layered reflectors repre- are exposed in the southeastern Well records indicate that the thick- senting the Mt. Simon/Lamotte, and Eddyville and southwestern Stone- ness of the Clore ranges from 95 to possibly older strata, correspond- fort Quadrangles. A composite col- 120 feet in the Eddyville and Stone- ingly thickens southeast of the fault umnar section of Chesterian strata in fort Quadrangles and from 110 to 155 zone. The Lusk Creek Fault Zone the study area was prepared from feet in the Creal Springs Quadrangle.

McCormick New Burnside Anticline Anticline

Figure 3 Sketch based on north-south seismic reflection profile through the Eddyville Quadrangle. The profile indicates that (1) Lusk Creek Fault Zone is a listric normal fault that penetrates crystalline basement; (2) Lusk Creek Fault was active during pre-Knox sedimentation; (3) Raum Fault Zone, which forms the southeast margin of the Dixon Springs Graben, is a post-Pennsylvanian structure that intersects the Lusk Creek Fault Zone at depth; (4) the prominent reflector representing the base of the Knox is not deformed beneath the McCormick and New Burnside Anticlines, and therefore these anticlines are detached within upper Paleozoic strata; (5) imbricate faults, most of which dip southward and flatten at depth, underlie the two anticlines. Ibble 2 Thickness of strata in selected deep wells in and near the study area

J b c d Streich Wells etal. Mohler Texota Walters'" Farley #l' Boner8

Pennsylvanian 418 695 540 558

Mississippian 3,050 3,197 3,350 3,399 3,292 Chesterian 1,292 1,052 1,528 875? 1,429 Ste. Genevieve 220 340 205?

St. Louis 430? 222 420? Salem 420? 2,113 292

Ullin 480? 1,175

l or) Pa) ne 152?

Spring\ tile 48 20 80 Chouteau 8 12 5

Devonian 1,762 2,060 350 New Albany 320 345 172 Lingle 112 55

Grand Tower 120 1,715 109 Lower Devonian 1,210 14

Ordovician and Knox Maquoketa Galena

Platteville Joachim and Dutch town

St. Peter Knox (Camb-Ord)

Cambrian below Knox 2,384 Eau Claire 1,160 Mt. Simon 1,224

Total Depth 14,942 6,200 4,250 3,172

Texas Pacific, Mary Streich #, SW NW SE, 1-11S-6E, Eddyville Quadrangle. Texas Pacific, Wells etal. #1, N14NWNW, 34-10S-6E, Eddyville Quadrangle. Jenkins, Mohler#l, SWSWNW, 24-11S-3E, Creal Springs Quadrangle. Texota, King #1, NE SE, 32-10S-7E, Saline County.

Texaco, J. M. Walters #1, SWNE SW, 29-9S-9E, Gallatin County. Texas Pacific, Farley et al. #1, SE NW NW, 34-13S-3E, Johnson County.

Tunnel Hill Oil Co., Boner #1, WV2 SW NE, 30-11S-3E, Johnson County.

Lithology Well logs in the study consists of shale and thin limestone The Tygett Sandstone Member area show that the Clore has a con- beds. The shale is mostly dark gray ranges from less than an inch to 20 sistent lithologic sequence correlative to greenish gray, silt free, and partly feet thick in the Eddyville Quad- with that found in outcrop in adja- calcareous; the limestone, mostly rangle and from 15 to 50 feet thick in cent quadrangles (Baxter et al. 1967, very fine to fine-grained, argillace- the Stonefort and Creal Springs Devera, in preparation, Nelson, in ous, and very fossiliferous, is dark Quadrangles. To the east the Tygett preparation, Weibel et al. , in prepara- gray or brownish gray. Limestone consists mostly of gray silty shale and tion). The Cora, Tygett, and Ford Sta- accounts for about one-fourth to siltstone. Westward, the Tygett be- tion Members of Swann (1963) can one-third of the total thickness of the comes sandstone, very fine to fine be identified in most logs (fig. 4). Cora; most of the limestone is in the grained and generally light gray- The Cora Member at the base of upper part of the member in beds a brown to greenish gray. The sample the Clore is 35 to 70 feet thick and few inches to about 5 feet thick. study of well 15 (table 3) indicates about 8 feet of limestone, lithologically similar to limestone of the Cora Member, near the middle of the Tygett. Thin limestone beds also occur in the Tygett in the adjacent Glendale and Bloomfield Quadran- gles (Devera, in preparation, Nelson, in preparation). The Ford Station Member of the upper Clore consists of 23 to 50 feet of interbedded shale and limestone. Shale is generally predominant, but in a few well logs the Ford Station consists mostly of limestone. Litho- logies are similar to those of the Cora Member. The medium to dark gray, fine- to coarse-grained, argillaceous limestone exposed in the southwestern Stonefort Quadrangle is believed to belong to the Ford Station Mem- ber. Fossils include the bryozoans Archimedes, Polypora, and Rhombopora; the brachiopods Composita subquad- rata and Spirifer sp., silicified rugose corals of the genus Trilophyllites, and abundant pelmatozoan fragments. The limestone occurs in beds less than 2 feet thick, separated by covered intervals that probably are Waltersburg mostly shale. Both upper and lower contacts of the Clore Formation appear to be conformable within the study area. Tar Springs The top of the Clore is placed at the top of the highest limestone bed beneath sandstone, siltstone, and silty shale of the Degonia.

Depositional environment The variety of lithologies in the Clore Hardinsburg Formation reflects varying deposi-

sandstone

calcareous sandstone Fraileys siltstone; shale and sandstone interbedded shale Cypress calcareous shale

shaly limestone

limestone -j- red/green >H variegated claystone Bethel —j- coal and underclay Downeys Bluff

a chert Yankeetown

Figure 4 Graphic column, based on well data, of the Chesterian Series in the study area (modified from Swann 1963). Table 3 Oil test holes in the study area

Total Deepest Year depth unit Operator Farm, well no. Location drilled (ft) penetrated

Eddyville Quadrangle

1 Carter Oil Gowdy, #1 NVVNWSE 16 IDS SI 1955 3,034 Ultin

2 li'VIN I'.U lilt Wells etal.,#l NV4NWNW 34 10S-6E 1977 6,200 Silurian 3 Whitlocketal. Anthis, #1 SE NW NE 12 11S-5E 193H 1,760 Chesterian

4 Mid-Egypt I ightfbot, H\ SESWNE 12 11S-5E 1923? 1,670 Chesterian

5 Mid-Egypt Stations, # I SWNWNE 12 ir. ! 1923 1,760 Chesterian

6 Roy Pledger ( libson, # 1 NWNENW 13 11S-5E 1956 2,631 St. Louis 7 Texas Pacific Streich, n\ SWNWSE 2 11S-6E 1976 14,942 Mt. Simon 8 Milo Ditterline Hart,#1 SESENVV 14 HS-61 1957 2,297 St Louis

9 K-Winn Headrich,#l SWNWNE 25 LOS 51 1984 1,530 1 l.miinsburg

Stonefort Quadrangle

ID Ohio Oil Co. I [ancock, #1 SWSESE 33-10S-4E 1917 3,058 Ullin?

11 OhioOiK o. Bynum, # 1 NWNWNE 35-10S-5E 1916 1,281 Chesterian 12 Pierce Camden, #1 NWNWNW 9-11S-5E 1916 3,075 Salem? 13 OhioOiK o Gen. Am. Life, #1 NESESE 10-11S-5E 1940 1,692 Ste. Genevieve

14 Mid-Egj pi Parsons, # 1 NWNENE 15-11S-5E 1923? 660 Chesterian

15 Gardenheir& Smith Peoples, tt\ SESE 19 lis 51 1940 1,160 Menard

16 c laro Moyer, #1 NESENW 29-11S-5E 1941 1,236 Glen Dean

.il 17 Gamier el Peeples # 1 NENENE 30-11S-5E 1940 2,204 Ste. Genevieve? 18 Higgins Trammell, #1 SESENE 36-10S-4E 1955 2,304 Ste. Genevieve

Creal Springs Quadrangle

19 Mitchell &Stanonis Simmons, #1 SENESE 23-11S-3E 1965 1,676 Cypress 20 Mitchell & Hamilton Giver, #1 NESENE 24-11S-3E 1980 2,400 St. Louis 21 Jenkins* Mohler, #1 SWSWNW 24-11S-3E 1941 4,250 Clear Creek (Devonian) 22 Hardin & Harlow McCuan, #1 NENWNE 26-11S-3E 1941 708 Pennsylvanian 23 Witnel-Cunningham SESWSE 3-11S-4E 1,508 Chesterian 24 Fletcher Farrar Horn, #1 SENWNW 5-11S-4E 1956 2,450 St. Louis? 25 ShureOilCo. Evans, #1 SESENW 10-11S-4E 1955 2,230 St. Louis 26 Reeves Gibson, #1 NENESW 15-11S-4E 1908 1,560 Chesterian 27 Mitchell & Hamilton Parson, #1 NENWNE 16-11S-4E 1980 2,130 St. Louis 28 Wrightsman Jackson-Whitnal #1 SE SW NW 17-11S-4E 1917 2,002 Ste. Genevieve 29 Monjeb Minerals Trammel, #1 NENWSE 27-10S-4E 1983 2,461 Ste. Genevieve

tional conditions. Because only having normal salinity, low rates of tween the distinctive limestones of limited data on depositional environ- sedimentation, and low wave turbu- the Clore and Kinkaid Formations. ment are available for the Clore in lence. the study area, our discussion is Distribution and thickness Out- brief; however, Abegg (1986) pro- Degonia Formation crops of the Degonia are confined to vides a good overview of the Clore Name and correlation Weller two small areas within the quadran- in southern Illinois. (1920) defined the Degonia Sand- gles studied. One is along the stream Fossils found in Ford Station Lime- stone as part of an interval of rock at the southwest corner of the Stone- stone Member in the Stonefort previously assigned to the Clore fort Quadrangle, and the other is Quadrangle represent forms adapted Formation. In its type area, about 45 along Lusk Creek at the southern to low turbulence and soft, muddy miles west of the study area, the edge of the Eddyville Quadrangle. substrates. Particularly diagnostic of Degonia is largely massive sand- Well records indicate that the De- this setting are specimens of Archi- stone. Eastward towards the study gonia is present in the subsurface medes with fronds attached, spiriferid area, the Degonia grades to shale, throughout the study area. brachiopods with broad hinge lines, siltstone, and very fine-grained, The Degonia ranges from about 20 and rugose corals. According to thinly bedded sandstone. We define to 64 feet thick in the study area and Abegg (1986), the environment was the Degonia Formation in this publi- generally is about 40 feet thick; it is probably a shallow marine shelf cation as a siliciclastic interval be- thinnest in the southeastern Eddy-

10 :

i;'/: ;±^';;

:;:;-'iv.v-.' Battery Rock and Wayside 7 Members O _ ~" ~.'.- $ ;' ~: > OIT LL -— £ m 5 ?fL^iz^

j~ >^ ^ £ ^

i = i i -~r ,

r ' ' ^!-i _-L- Goreville I' Member — ~o_" .-.•_' 7 green and red quartz pebbles " - • • . . — • . o — sublithographic 300 ft tj^t^t black shale -100 m

__ 9 _ - ~--i~~-S

Negli ^ Creek Pounds Member ? _i Member > > LU <7) < u Drury — . • — _ —

Member ? — • — — -^

Figure 5 Graphic log of Alcoa test hole, SW NW NE NW, Section 2, T12S, R6E, Eddyville Quadrangle. The borehole is in the Dixon Springs Graben, immediately southeast of the Lusk Creek Fault Zone. (Log is based on core descriptions by Paul E. Potter, William H. Smith, and D. B. Saxby 1956).

ville Quadrangle, but otherwise no The Degonia thickens to more than Tbpography The Degonia under- consistent thickness trends are appar- 100 feet and becomes dominantly lies gently to moderately sloping ent. The Degonia-Clore contact is of- clean, crossbedded, fine-grained terrain in its area of outcrop. Discon- ten impossible to determine from well sandstone along a southwest-trend- tinuous sandstone ledges occur in records because the thin limestones ing belt lying northwest of the study areas free of talus from overlying of the upper Clore Formation are area (Potter et al. 1958, Potter 1963). units. Otherwise, outcrops are con- hard to identify in geophysical logs. fined to beds and banks of streams. Lithology The Degonia Formation consists of very fine sandstone, siltstone, shale, claystone, and bedded chert. The lithologic sequence is BED, MEMBER moderately variable. Distinctive, bedded chert is found at the base of the Degonia in the Eddyville Quadrangle. Dull white to brownish gray, opaque, and closely fractured, the chert occurs in tabular Houchin Creek Coal Mbr to irregular beds up to about 1 foot thick. The chert is best exposed in an old road and adjacent streambed Survant Coal Mbr near the center of the NE, Section 3, T12S, R6E. This chert also is widespread in the Herod and Karbers Colchester Coal Mbr Ridge Quadrangles (Baxter and Desborough 1965, Baxter etal. 1967) Dekoven Coal Mbr and in the Waltersburg Quadrangle (Weibel et al. in preparation). The Davis Coal Mbr sample study of well 15 (table 3) in sub-Davis sandstone the Stonefort Quadrangle indicates chert at the base of the Degonia. Carrier Mills Shale Mbr The main part of the Degonia Stonefort Ls Mbr Wise Ridge Coal Bed generally consists ol a thin shale at Mt. Rorah Coal Mbr the base overlain by sandstone that Creal Springs Ls Mbr grades upward to siltstone and silty Murphysboro (?) Coal Mbr shale. The sandstone rarely is thicker golden sandstone than about 10 feet. A few well logs, Mitchellsville Ls Bed as well as outcrops in the Stonefort New Burnside Coal Bed Quadrangle, indicate two thin sand- Delwood Coal Bed stones separated by 10 to 20 feet of shale and siltstone. Shale and siltstone in the Degonia commonly are Oldtown Coal Bed dark gray, olive, or greenish gray. Sandstone exposed in the Eddyville Murray Bluff Quadrangle is bluish green to olive Ss Mbr and weathers light brown to yellow- olive shale ish brown; it is very fine grained and forms ripple-marked beds 1 to 4 inches thick. Exposures are found in the beds of Ramsey Branch and Lusk Creek near the road crossings in NW, Section 3, T12S, R6E, and in the road itself east of Lusk Creek. Degonia sandstone exposed in the Stonefort Quadrangle is light gray to light Tunnel Hill Coal Bed brown, very fine grained, and thin bedded to thick bedded. Sedimen- basal Abbott shale, ss tary structures include faint parallel Reynoldsburg Coal Bed laminations, current ripples, and horizontal tubular burrows. Red to green variegated claystone or soft shale is a distinctive feature The contact of the Degonia with flow differs from one layer to the of the uppermost part of the De- the overlying Kinkaid Limestone is next; this could reflect either shallow gonia. This material can be seen in sharp and apparently conformable. subtidal or nonmarine overbank sed- the bank of Lusk Creek just north of imentation. Crawling traces and fos- the road in NW, Section 3, T12S, R6E; Depositions! environment Only sil plants observed in the Degonia it is also recorded on drillers' logs of limited inferences can be made on south of the study area suggest a many wells in the study area. Accord- depositional environments of the nearshore environment. Variegated ing to Swann (1963), red shale is Degonia because of lack of expo- red and green claystone like that found near the top of the Degonia sures. Body fossils are absent and the found at the top of the Degonia may throughout much of southern Il- few trace fossils observed are not represent a paleosol (Jerzykiewicz linois. diagnostic. Current ripples indicate and Sweet 1986). The bedded chert directional flow, but the direction of at the base of the Degonia may have recorded in well logs in the Creal Springs Quadrangle. In most of the study area 120 to 160 feet of Kinkaid are preserved. Pounds Ss Mbr Topography The Kinkaid com- Drury Mbr monly is obscured by talus on slopes below outcrops of the Caseyville Gentry Coal Bed Formation. Where talus is absent the limestones of the Kinkaid form Battery Rock Ss Mbr ledges or subtle benches separated by slopes underlain by shale; the best example of this type of topography is found in SE, Section 4, T12S, R6E, Wayside Mbr (Caseyville) Eddyville Quadrangle.

Grove Church Mbr (Kinkaid) Lithology The Kinkaid Formation

Goreville Ls Mbr (Kinkaid) consists of limestone and shale and small amounts of siltstone and claystone (figs. 4, 6). The vertical lithologic sequence is consistent Cave Hill Mbr (Kinkaid) throughout the study area, although gradual lateral variation is evident. The Negli Creek Member (Swann

Negli Creek Ls Mbr 1963), almost entirely limestone, ranges from 25 to 38 feet thick. The lower part of the Negli Creek generally is a very fine to fine-grained, dark

Ford Station Mbr gray to brownish gray limestone; it is argillaceous (although distinct shale partings are rare) and in many Figure 6 Generalized stratigraphic column of bedrock units exposed in places it contains blue-gray to brown the study area, with correlations to Western European and North American chert nodules. Weathered surfaces Midcontinental series. are rough, and the rock is generally crumbly or rotten. Beds range from been derived from silicification of of interbedded shale and limestone a few inches to about 2 feet thick and calcareous siltstone (Baxter et al. that are lithologically similar to the are irregular or hummocky. Brachio- 1967). rest of the Kinkaid. The Kinkaid and pods, bryozoans, and echinoderm Regional studies by Potter et al. its four members (fig. 4) are readily fragments are common, but the most (1958) and Potter (1963) suggest that traceable, on the basis of lithologic characteristic fossils are large bel- the Degonia represents distal sedi- content in outcrop and subsurface, lerophontid gastropods, Girvanella ments from a distributary system that from their respective type localities (algal) oncoids, and Chaetetella. The lay northwest of the study area. to the study area. gastropods and Girvanella occur in other Chesterian limestones, but Kinkaid Limestone Distribution and thickness The their occurrence together is definitive Name and correlation Weller Kinkaid crops out along Ramsey for the lower part of the Negli Creek. (1920) named the Kinkaid Limestone Branch and Lusk Creek in the south- Chaetetella, found in one outcrop of for Kinkaid Creek in Jackson County, eastern part of the Eddyville Quad- Negli Creek in the study area, has Illinois, approximately 40 miles west rangle and along the southwest-flow- been reported in no other unit in the of the study area. Swann (1963) re- ing stream near the southwest corner region (Trace and McGrain 1985). The vised the definition of the Kinkaid of the Stonefort Quadrangle. Two upper part of the Negli Creek is gray, to include three newly named mem- small exposures occur at the crest of fine- to coarse-grained, bioclastic bers—the Negli Creek Limestone the McCormick Anticline in SW, Sec- limestone dominated by pelmato- (basal), the Cave Hill, and the tion 11, T11S, R5E, Stonefort Quad- zoan fragments, fenestrate bryo- Goreville Limestone. Swann as- rangle. The Kinkaid is identified in zoans, and brachipods. Cross- signed shale above the Goreville all wells that reach the required bedding was observed in the upper Limestone to a new formation, the depth within the study area. One Negli Creek near the south edge of Grove Church Shale. In this publica- core description from the Eddyville the Eddyville Quadrangle west of tion we have reclassified the Grove Quadrangle is available (fig. 5). Lusk Creek. The overall lithologic Church as a member of the Kinkaid, The thickness of the Kinkaid varies sequence of the Negli Creek in the because it does not meet the require- because of erosion at the base of the study area is very similar to that ment of mappability the North Amer- overlying Caseyville Formation (figs. described by Randall (1970) and ican Stratigraphic Code (1983, article 4, 6). The minimum thickness (about Buchanan (1985). 24d) stipulates for a valid formation. 85 ft) and maximum thickness (about The Cave Hill Member (Swann Also, the Grove Church is composed 230 ft) of the Kinkaid were both 1963) is divisible into three lithologic

13 units in the study area and elsewhere along Ramsey Branch in NW NWSE, The Grove Church Shale Member in southern Illinois. The lower unit Section I, T12S, R6E (Eddyville field occurs in places beneath the pre- is greenish gray shale and siltstone, station 642). Caseyville unconformity. The only the middle unit is mainly sublitho- The middle unit of the Cue I I ill outcrop found is immediately south graphic to fine-grained limestone contains a rich fauna of brachiopods, of the Eddyville Quadrangle in gul- interbedded with shale, and the bryozoans, molluscs, and echino lies about 600 feet from the south upper unit is red and green, varie- derms. Some of the more common line, 1,500 feet from the east line, gated claystone interbedded with fossils are the brachiopods Spirifer Section 4, T12S, R6E, Waltersburg thin limestone. The Cave Hill is as increbescens, Composita sp., and Dia- Quadrangle. A core of the Grove thin as 55 feet where its upper part phragmus sp., the bryozoans Ar- Church was obtained from hole W-l, is missing (the result of pre-Casey- chimedes sp., Fenestellasp., and Eridop- drilled close to this outcrop (plate 1). ville erosion), but is 75 to 95 feet thick orasp., and the gastropods Platyt eras The Grove Church also was identified where fully preserved, and dwarf Bellewphon. The shells are in the logs of six or seven wells in The lower shale unit of the Cave commonly whole and articulated, the Creal Springs Quadrangle and Hill thickens to the northeast across but they do not appear to be in life one well each in the Eddyville and the study area; it is 7 to 24 feet thick position. Most Archimedes axes are Stonefort Quadrangles. A thickness in the Creal Springs and Stonefoii intact, although the fronds are of 71 feet of Grove Church shale Quadrangles, 20 to 30 feet thick in detached. Most echinoderm re- (close to the known maximum thick- the southern part of the Eddys ille mains, except those of a few Ventre ness of the Grove Church) was iden- Quadrangle, and 27 to -4^ teet thick mites calices, are disarticulated. tified in the Jenkins #1 Mohler well in the Mitchellsville oil field just The upper unit of the Cave Hill (well 21, table 3). In outcrops and north of the Eddyville Quadrangle. consists of soft, generally nom alt ar- well samples the Grove Church con- Accompanying the increase in thick- eous, greenish gray and red-green, sists primarily of olive gray to ness is an increase in grain size to variegated shale or claystone contain- greenish gray, lightly mottled, partly the northeast. In the west the lower ing beds of nodular, highly fossilifer- calcareous shale that is silt free to unit consists dI silt-free, dark gray to ous limestone less than 6 inches finely silty. Limestone beds in the greenish gray clay-shale, but in the thick. The bivalves Myalina and lower Grove Church are less than a east, silly shale and siltstone are Edmondia are characteristic of this foot thick, fine to coarse grained, very found, particularly in the upper part unit. Outcrops are visible along shaly, and fossiliferous. An interval of the unit. Outcrops are scarce; the Ramsey Branch in the SESE, Section of limestone up to 18 feet thick is description of the lower unit is based 5, T12S, R6E. The upper unit is indicated on well logs in the upper mainly on well cuttings and geophys- generally 10 to 20 feet thick through- Grove Church. ical logs. The northeastward thicken- out the study area. ing and coarsening correspond to The Goreville Member of the Kin- Depositional environment The regional trends recognized bv Ran- kaid, like the Negli Creek Member, argillaceous limestone of the lower dall (1970). consists almost entirely of limestone part of the Negli Creek Member of The middle unit of the Cave Hill and a few shale partings (Swann the Kinkaid probably was deposited becomes thinner and contains more 1963). The Goreville is thin or missing in relatively deep water with low to shale to the northeast. The thickness in places because of pre-Caseyville moderate turbulence. Abundant Gir- decreases from 50 to 75 feet in the erosion, but where fully preserved it vanella oncoids suggest gently oscil- Creal Springs Quadrangle to about is 35 to 45 feet thick. As exposed in lating currents that rolled fossil 30 feet in the Mitchellsville oil field. the Eddyville Quadrangle and in well grains along the sea bottom. An in-

The middle unit is at least three- cuttings, it is medium to dark gray crease in wave and current energy/ fourths limestone in the Creal or brownish gray and fine to coarse probably related to shoaling, is indi- Springs, Stonefort, and southern grained. Weathered surfaces are cated by the coarse, locally cross- Eddyville Quadrangles but is half rough because of the silicified fossil bedded biosparite of the upper part shale in the Mitchellsville oil field. fragments they contain, and the of the Negli Creek (Buchanan 1985). Limestone in the middle unit is limestone commonly crumbles when The shale and siltstone of the lower sublithographic to fine grained and struck. Some parts of the Goreville part of the Cave Hill Member prob- light to dark gray; most of it weathers are highly argillaceous and contain ably are prodeltaic sediments, from to light gray, smooth, rounded sur- thin layers of olive gray, calcareous a delta that lay northeast of the study faces. The limestone is dense and shale. Chert nodules and bands up area (Randall 1970). Periodic input of rings when struck with a hammer, to 24 inches thick are conspicuous in mud from this source continued unlike limestones of the Negli Creek some horizons. The Goreville is com- through accumulation of the middle and Goreville Members, which gen- posed largely of pelmatazoan frag- part of the Cave Hill. Most limestone erally crumble when struck. Some ments; partly articulated crinoid of the Cave Hill was laid down in beds are dolomitic and weather stem segments are common. Bryo- gently agitated water, as indicated by yellowish orange. Much of the zoans also are common; very large slight to moderate disarticulation of limestone is argillaceous or silty. specimens of Archimedes (with axes delicate fossils. Bedded and nodular chert is abun- up to 12 inches long) are diagnostic The red and green mudstone of the dant. Shale interbedded in the of the Goreville in the report area. upper part of the Cave Hill contains middle unit is medium to dark gray The Goreville generally becomes abundant Myalina (mussels), or greenish gray, and mostly calcar- coarser grained, and contains more suggesting shoaling and possible eous. The most complete exposure sparry cement and less micrite and episodes of subaerial exposure. of the middle unit of the Cave Hill is clay westward.

14 —

The Goreville Member represents Within our study area, the Casey- Caseyville is highly unlikely. Al- a return to open marine sedimenta- ville Formation overlies the Grove though the age of the Grove Church tion and a slight input of terrigenous Church, Goreville, and Cave Hill has not been completely established, clay from the east or northeast. The Members of the Kinkaid Formation Jennings and Fraunfelter (1986) re- water was moderately agitated, more (fig. 6). Total relief on the contact is ported significant floral and faunal so than during Cave Hill deposition. about 150 feet. Just south of the study breaks between Grove Church and The fossils of the Grove Church area in the northeastern part of the basal Caseyville and suggested that also signify marine sedimentation. Glendale Quadrangle, the Kinkaid Caseyville conodonts described by and Degonia Formations are locally Rexroad and Merrill may have been Chesterian Undifferentiated absent, and the Caseyville rests reworked from Mississippian strata. Outcrops of steeply tilted, shattered, directly on strata of the Clore Forma- No clear exposures of the Kinkaid- and mineralized limestone and tion (Devera in preparation). Caseyville contact were found in the quartzitic sandstone within the Lusk The Kinkaid Formation in the study area. In quarries a short dis- Creek Fault Zone have been mapped study area is characterized by a con- tance to the south, the contact is as "Chesterian undifferentiated." sistent vertical sequence having only sharp and gently undulating. Pre- Most of the fault slice lies in Sections minor and gradual lateral variations. Pennsylvanian downcutting is 2 and 3, T12S, R6E, Eddyville Quad- This "layer cake" stratigraphy of the shown best in the southern part of rangle. The best exposures are along Kinkaid contrasts sharply with the the Eddyville Quadrangle. Grove the east side of a deep ravine and in lateral lithologic variability of the Church Shale is preserved in SE, a logging road (not shown on the Caseyville Formation. Section 4, T12S, R6E; along the map) southwest of the Lost 40 Mine, Variations in thickness of the Kin- Ramsey Branch near the southwest- in NE SE, Section 3. kaid clearly are the result of erosion ern corner of the same section, the Limestone in the fault slice litho- of the upper members and replace- Caseyville rests on the lower part of logically resembles limestone of the ment by Caseyville sediments. If the Goreville Member. Pennsylva-

Kinkaid, and much of it probably is depositional continuity between the nian rocks overlie the upper part of Kinkaid; it is medium to dark gray, Kinkaid and the Caseyville exists the Cave Hill Member in the outcrops medium bedded, and fine to coarse anywhere in the Illinois Basin, it in the southwestern Stonefort Quad- grained. No diagnostic fossils or must occur where the Grove Church rangle. other distinctive features were noted. Member is most complete (it would The limestone is thoroughly frac- be unusual for the contact to be con- tured and is shot through with vein- formable at one or a few sites but PENNSYLVANIAN SYSTEM lets of calcite and small amounts of unconformable everywhere else in The Pennsylvanian System of the fluorite, galena, and sphalerite. the basin). Only the lower shale of Illinois Basin—particularly the lower Sandstone in the fault slice resem- the Grove Church is present at local- part of the system in the study area bles quartzite and is highly shat- ities about 8 miles west of the report is difficult to subdivide into litho- tered. The grain size, bedding, and area, where Rexroad and Merrill stratigraphic units. The system is sedimentary structures have been (1985) collected their fossils. The composed mostly of sandstone, silt- obscured in places. The sandstone is upper limestone of the Grove stone, and shale, which generally mostly a white to light gray (altered Church, observed in boreholes with- form lenticular bodies that intergrade to red or orange), very fine-grained, in the study area, is absent at the laterally and vertically. Intercalated nearly pure quartzose sandstone that type locality. with the siliciclastic rocks are thin contains dark shale partings or inclu- Lateral intertonguing of Caseyville beds of coal, limestone, and black sions in places. Bedding, where vis- and Grove Church lithologies, which fissile shale. In the lower part of the ible, is thin and planar. The sand- would be expected if the units repre- Pennsylvanian (Morrowan and Ato- stone does not resemble Degonia sented continuous deposition, never kan Series) these beds are mostly sandstone, which crops out in the has been reported. Rexroad and Mer- lenticular, but in Desmoinesian and vicinity; some of the sandstone in the rill asserted that the Caseyville and younger strata they become widely fault slice may be from older Cheste- Grove Church are lithologically simi- traceable and useful as marker beds. rian formations, but part may be lar, but this is not true. The lower Most Pennsylvanian formations in Pennsylvanian. part of the Caseyville is dominantly the Illinois Basin were defined partly sandstone and siltstone, but these on the basis of observable lithic char- lithologies are absent in the Grove acteristics (primarily by differences MISSISSIPPIAN- Church. Limestone, greenish gray in the composition and texture of PENNSYLVANIAN CONTACT shale, and calcareous shale, which sandstones) and partly on the basis Controversy exists over the nature of make up the bulk of the Grove of marker beds (especially coals and the Mississippian-Pennsylvanian Church, are rare in the Caseyville. limestones). Many problems have boundary in southern Illinois. Most Some of the olive, mottled, silty shale arisen because lithic features and geologists (Siever, 1951, Bristol and of the Grove Church does resemble marker beds that are well developed Howard 1971, Howard 1979, Jen- certain shales in the Caseyville, but in type areas cannot be recognized nings and Fraunfelter 1986) regard the former is fissile or platy and the in other parts of the basin. As a this boundary as a basinwide uncon- latter is weakly laminated and com- result, the formations currently re- formity. However, Rexroad and monly interlayered with sandstone. cognized by the Illinois, Indiana, and Merrill (1985), in a conodont study, To summarize, lithologic evidence Kentucky Geological Surveys differ proposed that the sedimentation was indicates that depositional continuity substantially (fig. 7). Recent efforts continuous across the boundary. between the Grove Church and the of the three state surveys to stan-

15 .

W. KENTUCKY INDIANA ILLINOIS Caseyville on the Ohio River in U.S. & Ky THIS REPORT Shaver et al. 1986 Kosanke et al. 1960 Union County, Kentucky. Lee (1916) Geol. Surveys revised the name to Caseyville Danville Coal Mbr Danville Coal Mbr Formation and described tin' type section on the Illinois side of the Ohio Herrin coal bed eroded River opposite Caseyville. Later, SOme geologists/ such as Wcllcr

Carbondale Fm 1 (I ' Hi), referred to the Caseyville as Carbondale Group a group. Kosanke etal. (I960) ranked the Caseyville as a formation in Carbondale Fm Illinois and described a reference Carbondale Fm so tion along the Illinois Central fColchester Coal Mbr Railroad in the south-central part of theStonefort Quadrangle. The Casey- ville has been mapped extensively in Seelyville Coal Mbr Davis coal bed Davis Coal Mbr Spoon Fm western Kentucky and is equivalent Staunton Fm to the lower part of the Mansfield Spoon Fm Formation in Indiana (fig. 7). Minshall Coal Mbr Correlation of the Caseyville Murray Bluff Ss Mbr Murray Bluff Ss Mbr Formation into the study area is Tradewater Fm based on its lithologic similarity to Brazil Fm the type Caseyville and on the physical continuity of the Pounds Bell Battery Lower Block Coal Abbott Fm Abbott Fm and Rock Sandstone Mem- bers from their type localities into these quadrangles.

Distribution and topography The Pounds Ss Mbr Pounds Ss Mbr Caseyville Formation crops out extensively in the southern parts of all

three quadrangles of this study. It Mansfield Fm also is exposed in many places along the crest of the McCormick Anticline, Caseyville Fm which runs westward across the cen- Caseyville Fm Caseyville Fm tral part of the Eddy ville Quadrangle and thence southwestward to the southwest corner of the Stonefort Quadrangle. The Caseyville produces rugged topography; massive sandstones, more than 100 feet thick MISSISSIPPIAN AND OLDER STRATA in places, form bold cliffs, ledges, and steep slopes (fig. 8). A line of Figure 7 Formational nomenclature of the Pennsylvanian System in the Illinois cuestas marks the Caseyville outcrop Basin, as used by the three state geological surveys and in this report. The top of the in the southern part of the study Caseyville Formation in western has either at Kentucky been mapped the highest area. Intervals of shale, siltstone, and occurrence of sandstone containing quartz pebbles or at the base of the Bell coal bed shaly sandstone between the mas- The Seelyville Coal Member (Staunton Formation of Indiana) commonly is a split sive Caseyville sandstones erode to seam; the lower bench is equivalent to the Davis Coal and the upper bench correlates gentle slopes and strike-valleys. with the Dekoven Coal (Jacobson 1987). Talus from the sandstone cliffs com- dardize stratigraphic terminology (1986a,b,c 1990a,b) and Trask and monly covers the nonresistent inter- have led to the adoption of several Jacobsen (1990) in geologic map- vals of the Caseyville. common terms for members (Jacob- ping of quadrangles east of the pre- son etal. 1985). A basinwide classifi- sent study area. The formations rec- Thickness The Caseyville Forma- cation of the Pennsylvanian into ognized are the Caseyville (oldest), tion varies from about 170 to more formations was proposed during a Abbott, Spoon, and Carbondale. Sev- than 450 feet thick in the report area. meeting of the Tri-State Correlation eral members and beds have been re- Thickness values were obtained from Committee for the Pennsylvanian in vised or redefined, others have been well records and from composite April 1989 for eventual adoption by deleted, two new formal members sections measured on outcrops (table the three surveys. have been proposed, and several 4). This limited evidence suggests In this study we adopt, with revi- informal units are introduced. that the Caseyville is generally sions, the formational nomenclature thicker in synclinal areas than it is on Caseyville Formation proposed by Kosanke et al. (1960) the McCormick and New Burnside and used by Baxter et al. (1963), Name and correlation Owen Anticlines and adjacent to the Lusk Baxter and Desborough (1965), Bax- (1856, p. 48) named the Caseyville Creek Fault Zone. ter et al. (1967), Nelson and Lumm conglomerate after the settlement of

16 stones contain more mica, feldspar, lithic fragments, and clay matrix and are classified as subgraywackes (Siever and Potter 1956, Potter and Glass 1958). Quartz granules and pebbles are much more abundant in the Caseyville than in younger Penn- sylvanian formations. The Pounds Sandstone Member is the youngest sandstone that consistently displays the lithic character of the Caseyville. Therefore, following the practice of most geologists who have worked in southern Illinois and western Ken- tucky, we have mapped the top of the Caseyville at the top of the Pounds Sandstone. The contact is drawn at the top of the highest ledge of thick-bedded sandstone; any overlying thin-bedded sandstone is assigned to the Abbott. In a small part of the Eddyville Quadrangle where the Pounds Sandstone was not iden- Figure 8 Typical bluff exposure of Battery Rock Sandstone Member, Caseyville tified, the top of the Caseyville was Formation at Cedar Creek, near the southeast corner of the Creal Springs Quadrangle, placed at the highest occurrence of Section T12S,R4E. Note the larg talus block of sandstone near the stream SWSW, 3, clean quartzose sandstone. (right). Four previously named members Baxter et al. (1967) reported a the Caseyville and the overlying of the Caseyville Formation are thickness of 300 to 500 feet for the Abbott Formation are subtle and recognized in the study area. These Caseyville in the Herod Quadrangle gradational. The chief difference is are (in ascending order) the Wayside, east of the study area. Nelson and in the character of the sandstones. the Battery Rock Sandstone, the Lumm (1986c) reported a thickness Caseyville sandstones (both fine and Drury, and the Pounds Sandstone. of 250 to 300 feet in the Rudement coarse grained) are relatively clean, The Gentry Coal Bed, which occurs Quadrangle. sparkly, quartz sandstones generally within the Drury Member, has also classified as quartz arenites; Abbott been identified. Lithology The Caseyville Forma- and younger Pennsylvanian sand- tion is characterized by white to light gray, relatively clean quartzose sandstone commonly containing well- Tkble 4 Thickness of the Caseyville Formation in the study area rounded granules and small pebbles Location Thickness (ft) (up to 1 inch) of white quartz. Sandstone in the Caseyville varies from very fine to very coarse grained Eddyville Quadrangle and from very thin bedded to mas- Outcrop section SE 34-11S-6E 200 sive. In most places, one-half to Water well, Eddyville village 257 three-fourths of the thickness of the Oil-test holes 12-11S-5E 235-310 Caseyville is sandstone. The remain- Milo Ditterline #1 Hart SESENW 14-11S-6E 300 der of the formation consists of light Roy Pledger #1 Gibson NWNENW 13-11S-5E 405 to dark gray or brownish gray siltstone; medium to dark gray (rarely Stonefort Quadrangle black), silty shale; olive gray to Outcrop sections near brownish gray claystone; thin, dis- southwest corner of quadrangle continuous beds of shaly coal; and Gamier etal. #1 Peeples NENENE 30-11S-5E localized, dark gray, calcareous shale Pierce #1 Camden NWNWNW 35-10S-5E containing thin beds and nodules of Ohio Oil Co. #lBynum NWNWNE 35-10S-5E limestone. The only place in the report area Creal Springs Quadrangle where the Caseyville Formation can- Mitchel and Stanonis # 1 SENESE 23-11S-3E not be differentiated confidently Bessie Mohler #1 SWSWNW 24-11S-3E from Chesterian strata is within the Biver#l NWSWNE 24-11S-3E small fault slice labeled "Chesterian Charles Wrightsman #1 SESWNW 17-11S-4E undifferentiated" (described previ- Parson #1 NENWNE 16-11S-4E ously). The upper contact of the Evans #1 SESENW 10-11S-4E Caseyville is more problematic, be- Horn #1 SENWNW 5-11S-4E cause lithologic differences between Wayside Member Lamar (1925) tures in thin-bedded sandstones are channel was eroded into Mississip- applied the name, Wayside Sand- current and interference ripples and pian strata (Devera, in preparation). stone and Shale Member, to basal small load casts. The Wayside con- Cliffs of Wayside sandstone up to 40 Caseyville strata below Ins Lick Creek tains a greater abundance and variety feet high are present along Hayes (now Battery Rock) Sandstone Mem- of load structures than any other unit Creek at the southern edge of the ber in the Carbondale 15-minute in the study area. Trace fossils in the Eddyville Quadrangle and south of Quadrangle, about 8 miles west of Wayside include simple, branching, the stream near the center of Section ourstudyarea. Kosankeetal. (1960) or curving horizontal burrows, crawl- 2, T12S, R4E in the Stonefort Quad- shortened the name to Wayside ing traces and feeding traces, and rangle. Sandstone Member. Weller (1940) escape burrows inclined to bedding. The upper contact of the Wayside applied the name Lusk Formation I he only organic remains found in Member is well exposed only in the (Caseyville Group) to the same thin-bedded Wayside in the study railroad cut south of the tunnel in interval of strata in the Waltersburg area are poorly preserved plant Section 31, T11S, R5E, Stonefort Quadrangle immediately south of fragments. Quadrangle. Here, as in outcrops in the Eddyville Quadrangle. Kosanke Good exposures of thin-bedded adjacent quadrangles, the contact of et al. (1960) revised the name to Lusk Wayside strata are along the west- the Wayside with the overlying Bat- Shale Member, without giving rea- flowing stream in the NW SE, Section tery Rock Sandstone Member is sons for the change or clearly outlin- 2, T12S, R4E, in the southwestern sharp and appears to be erosional. ing the difference between the Lusk part of the Stonefort Quadrangle. The Wayside varies in thickness and the Wayside. Mapping in pro- The upper part of the Wayside is from less than 30 feet to more than gress demonstrates that the type exposed in the railroad cut south of 150 feet. The Wayside is at least 150 Wayside and the type Lusk an 1 litho- the tunnel in Section 31, T11S, R5E, feet thick in W 1/2, Section 1, and in logically similar units of interbedded Stonefort Quadrangle (fig. 9). In the E 1/2, Section 2, T12S, R4E, in the shale and sandstone and are strati- Eddyville Quadrangle the Wayside southwestern part of the Stonefort graphically equivalent. The name crops out along the Ramsey Branch Quadrangle. Within a mile south- Lusk is therefore abandoned in favor and adjacent gullies. west of this area the Wayside thins of Wayside, which has priority. Also, A minor but distinctive lithology to 35 to 50 feet. In the Eddyville the lithic term "sandstone" is omit- found only in the Wayside is con- Quadrangle the Wayside thickens ted, because the Wayside contains glomerate consisting of clasts, up to from less than 30 feet along the upper large proportions of shale and silt- several inches in diameter, of sand- part of Ramsey Branch to at least 80 stone. stone, ironstone, and chert in a feet along the lower part of the same

The Wayside Member is generally matrix of highly ferruginous sand- stream; it is as thick as 115 feet in the nonresistant, but in places it contains stone and claystone. Such conglom- subsurface in the Eddyville Quad- cliff-forming sandstones. Much of erate occurs as beds or lenses up to rangle. We do not have enough data the Wayside is concealed by talus and a few feet thick interlayered with to determine whether or not these colluvium on slopes below the thin-bedded sandstone and shale. variations are related to irregularities Battery Rock Sandstone. The Way- Outcrops were observed near the on the sub-Pennsylvanian surface. side is not known to be absent any- center of Section 35, T11S, R6E, where in the study area, but in some Eddyville Quadrangle, and in the Battery Rock Sandstone areas exposures are too poor to stream bed in SW SE NE, Section 2, Member The Battery Rock Sand- permit mapping this member. T12S, R4E, Stonefort Quadrangle. stone Member was named by Cox The Wayside Member consists of Thick-bedded to massive cliff- (1875) for Battery Rock, a bluff along variable proportions of shale, forming sandstones up to 40 feet the Ohio River in eastern Hardin siltstone, and thin- to medium-bed- thick occur in the Wayside Member County, Illinois. Mapping in the ded sandstone, along with minor in the Stonefort and Eddyville Quad- fluorspar district (Baxter et al. 1963, conglomerate and lenticular bodies rangles. These sandstones are nota- Baxter and Desborough 1965, Baxter of massive sandstone. Coal has been bly lenticular in comparison with the et al. 1967) established the physical reported in the Wayside in other widely traceable Pounds and Battery continuity of the type Battery Rock areas, but none was found in our Rock Sandstones higher in the Casey- with sandstone in our study area. three quadrangles. Shale in the ville. Massive Wayside sandstones The Battery Rock has been identified Wayside is medium to dark gray or are generally fine grained and lack as far west as Jackson County, Illinois brownish gray, silty, finely micace- the quartz pebbles that are abundant (Desborough 1961, Sonnefield 1981). ous, and noncalcareous. Thin inter- in the Battery Rock and Pounds. The Battery Rock is a resistant, vals of black carbonaceous shale also Crossbedding is seldom as conspicu- cliff-forming sandstone (fig. 8); it is occur. Wayside siltstone, light to ous in Wayside sandstones as in well exposed along the drainages of medium gray or olive gray, com- younger Caseyville sandstones. Lusk Creek and Hayes Creek in the monly occurs as lenses or laminae in Fossils include rare coalified logs, Eddyville Quadrangle, Bay Creek shale. Thin-bedded sandstones of along with silicified corals and and Little Bay Creek in the Stonefort the Wayside are white to light gray crinoid fragments reworked from Quadrangle, and Cedar Creek in the or brown, very fine-grained, Mississippian limestones. Wayside Creal Springs Quadrangle. It also is quartzose, and very well indurated. sandstone is thickest south of the exposed in several places along the Bed thickness is quite variable; most study area in the northwestern part McCormick Anticline. The sandstone thin-bedded intervals include some of the Waltersburg Quadrangle and is exposed in railroad cuts along the layers that are several feet thick. The northeastern part of the Glendale Illinois Central tracks in the southern most common sedimentary struc- Quadrangle, where a deep paleo- part of the Stonefort Quadrangle.

18 field station 402 field station 506 COGEOMAP hole E-4 field station 617 W 1/2 SW NE SVfe SW NW SW SW NE SE SE SE 11-11S-5E 6-12S-6E 32-11S-6E 23-11 S-6E Eddyville Eddyville Eddyville Eddyville

'/ss/sy.

concealed, probably shale

slumped concealed" fossil wood

Drury Drury

Wayside^

angul r - ^M? unconformity (?)

Figure 9 Measured sections of the Caseyville Formation.

The Battery Rock is a thick-bedded to be Skolithos were observed near the R6E and in an east-flowing small to massive, conglomeratic, quartzose railroad just south of the Stonefort tributary of Little Lusk Creek just sandstone. Nearly all outcrops of Quadrangle (NW NW, Section 17, north of the SE corner, Section 23, Battery Rock contain abundant T12S, R4E). T11S, R6E, also in the Eddyville quartz pebbles 1/4 to 1 inch in diam- The contact of the Battery Rock Quadrangle. eter. Lenses of quartz-pebble con- with thin-bedded sandstone and The Battery Rock is 30 to 60 feet glomerate are common, especially shale of the overlying Drury Member thick in most places; it may reach 100 near the base of the unit. Pebbles are is abrupt in most places. In the Illin- feet or more along Bear Branch and larger and more numerous in the ois Central railroad cut (SE, Section Lusk Creek in the Eddyville Quad- Battery Rock than in the younger 31, T11S, R4E) the Battery Rock is rangle, but at these locations it Pounds Sandstone Member. directly overlain by the underclay of cannot be easily differentiated from Nearly white when fresh, Battery the Gentry Coal Bed. Near the south- massive sandstones of the Wayside Rock sandstone weathers to light to ern boundary of the Stonefort Quad- Member. The Battery Rock becomes medium gray. Weathered surfaces are rangle in the railroad cut, the upper thin and lenticular east of Lusk Creek smooth and rounded; the sandstone part of the Battery Rock grades later- and has not been mapped . It is prob- has a sugary texture. Large-scale ally to siltstone and thinly laminated, ably 75 to 100 feet thick along Burden planar and trough crossbedding is shaly sandstone. Gradational Battery Creek and Caney Branch, near the common, and ripple marks occur Rock-Drury contacts are exposed in crest of the McCormick Anticline in locally. The only fossils are trans- a gully alongside a trail west of the east-central part of the Stonefort ported logs of Lepidodendron and Eddyville (fig. 9, third column), near Quadrangle; well records here indi- Calamites. Vertical burrows believed the center, W 1/2, Section 6, T12S, cate as much as 145 feet of massive

19 sandstone in the lower Caseyville, sandstone and conglomerate are Drury here consists of 25 to 30 feet but part of this may be Wayside rare. Local lenses of crossbedded of yellowish gray, very fine-grained, sandstone. sandstone up to about 15 feet thick silty sandstone having herringbone produce small ledges. One such crossbedding; its base is concealed. Drury Member Lamar (1925) sandstone lens is well exposed on The Pounds-Drury contact is ero- named the Drury Shale and Sand- the south side of Cedar Creek in SE sional, showing sharp truncation of stone Member of the Pottsville NE NE, Section 5, T12S, R4E, Creal bedding and 12 to 15 feet of vertical Formation for Drury Creek, about 20 Springs Quadrangle. Coal and car- relief. Small sandstone dikes from miles west of the present study area, bonaceous shale occurring in the the Pounds penetrate the uppermost in the Carbondale L5-minute Quad- Drury will be discussed in a separate Drury near the back of the "cave" rangle. Lamar's Drury was an inter section. Dark gray to bl.u k calcareous (actually a rock shelter). val of nonresistant shale

Sandstones. Kosanke et al. ( I960) Quadrangle. ber ol the south-central part of the recognized the Drury as a member I lu' most complete exposure oi the Eddyville Quadrangle. The sites are

I of the Caseyville Formation and >rury Member is along a north-flow- (1 ) gullies beside an abandoned road redefined it as the Drury Shale Mem- ing tributary oi Caney branch (fig. 9, near the center of the west line of ber. Weare herein changing the name column 2). At the top ol the unit, Section 33, T11S, R6E (field station to Drury Member because in many about 8 feet of dark gray clay-shale, 519); (2) a cutbank on a tributary of places half or more of the interval containing plant fossils, overlies 2 the Bear Branch, near the center of consists of sandstone. feet of soft, gray claystone. Below the S 1/2, Section 32, same township

The continuity of the Drurj from claystone is 27 feet of medium-dark (field station 518); (3) gullies beside the area mapped by Lamar to our gray, silty shalecontaining thin lami- a dirt road, NW SE NW, Section 5, study area has been verified In map nae and lenses of light gray siltstone T12S, R6E (field station 515); and (4) ping (in progress) in the intervening and sandstone. Both the upper and a drill core from borehole E-4, near Goreville Quadrangle, west of the lower contacts of the Drury are sharp center Section 32, T11S, R6E. In the Creal Springs Quadrangle (Jacobson, at this locality. A nearly complete outcrops a maximum of 8 feet of shale in preparation). exposure of the Drury occurs along was exposed in the upper part of the Mapping in our three quadrangles a small gully beside a trail just west Drury. The drill core (fig. 9, column shows the Drury overlying the Bat- of Eddyville (fig. 9, column 3). Here 4, and plate 1) includes 82 feet of tery Rock Sandstone in nearly all the the member is 65 to 70 feet thick, and medium dark gray to black, partly area where the Battery Rock is pre- both upper and lower contacts are calcareous shale containing thin sent. One exception is in E 1/2, gradational. The Drury at this site bands or nodules of argillaceous

Section 1, T12S, R4E, Stonefort consists of thin- to medium-bedded limestone. The shale grades upward Quadrangle, where the Drury has sandstone interbedded with siltstone to sandstone of the Pounds and been eroded and replaced by Pounds and shale. Burrows and other trace downward to sandstone of the Sandstone. The same situation may fossils are abundant in the lower part Battery Rock. Fossils in the shale exist in the southwestern part of the of the Drury and casts of fossil wood include the goniatites Axinolobus,

Creal Springs Quadrangle. In the occur near the middle part. Gastrioceras, and Wiedeyoceras (?), southwestern part of the Eddyville The lower part of the Drury is well nautiloids, bivalves, gastropods, Quadrangle, thick talus deposits that exposed along a ravine west of Little brachiopods, conodonts, and conceal the Drury interval have been Lusk Creek (fig. 9, column 5). Near palynomorphs (Devera et al. 1987). mapped. the mouth of the ravine about 30 feet The only other reported occur- Where strata are horizontal or of sandstone is present. This sand- rence of calcareous marine strata in gently dipping, the Drury erodes to stone, transitional from Battery Rock the Drury Member is from a bluff of a topographic bench between the to Drury, occurs in beds a few inches the Ohio River near the abandoned Pounds and Battery Rock escarp- to 4 feet thick and contains scattered community of Sellers Landing, east- ments. Along the McCormick Anti- quartz pebbles. The sandstone beds ern Hardin County, Illinois (Wanless cline where the beds are tilted, the have planar crossbedding in which 1939, 1956, Baxter et al. 1963). The Drury underlies strike-valleys. In the foreset beds consistently dip limestone, which occurs near the both situations most of the Drury is southwest and pass into ripple- base of the Drury Member, is thought hidden by talus and colluvium de- marked bottomset beds. The lower to be slightly older than the Gentry rived from the Pounds Sandstone. unit grades upward to about 20 feet Coal Bed (Wanless 1956). The marine Outcrops of the Drury thus generally of ripple-marked siltstone containing shale in the Eddyville Quadrangle are fragmentary except along a few laminae of fine-grained sandstone. lies near the top of the Drury and is streams where downcutting is espe- At the top of the Drury is an interval palynologically younger than the cially rapid. about 20 feet thick that contains float Gentry Coal; therefore, the marine The Drury, like the Wayside, con- and small, slumped exposures of shale of the Eddyville Quadrangle sists principally of variable propor- dark gray shale. probably is younger than the Sellers tions of light to dark gray clay-shale The upper part of the Drury and Limestone. The Drury is thin to and silty shale, light gray, thinly the overlying Pounds Sandstone are absent where it was cut out and laminated siltstone, and light gray, exposed at Peter Cave near the replaced by the Pounds Sandstone very fine-grained, thin- to medium- southwest corner of the Eddyville and as thick as 120 feet in the south- bedded, shaly sandstone. Pebbly Quadrangle (field station 508). The eastern part of the Creal Springs

20 .

Quadrangle. In general, the Drury T12S, R5E (Stonefort field station 781) top of the Caseyville Formation in thins where the Pounds thickens, and in a small gully in NE NW SW, Illinois. This definition has been used and vice versa. The Pounds-Drury Section 36, T11S, R4E (field station by numerous mappers working in contact tends to be sharp and ero- 775) . At all these localities the coal is southern Illinois and adjacent parts sional where the Drury is thin and 14 to 24 inches thick and is very shaly, of western Kentucky (Amos 1965, gradational where the Drury is thick except for the uppermost 4 to 6 1966, Baxter et al. 1963, Baxter and

(fig. 9; plate 1). inches, which is brightly banded. Desborough 1965, Baxter etal. 1967, The coal, found about 3 to 10 feet Desborough 1961, Nelson and Lumm Gentiy Coal Bed A coal bed that above the top of the Battery Rock 1986a,b,c) and is used in this report. crops out near Battery Rock on the Sandstone, is separated from the The Pounds Sandstone is a cliff- Ohio River in Hardin County, Illi- Battery Rock by soft shale and clay- forming unit in much of southern nois, was named the Battery Rock stone; it is overlain by silty shale and Illinois. Cliffs of this sandstone,

Coal by Owen ( 1856) . Kosanke et al siltstone in the natural exposures and which are relatively continuous from (1960) renamed the coal the Gentry by thin- to medium-bedded sand- the Ohio River to the Mississippi, are Coal Member to avoid duplicating stone in the railroad cut. popularly called the Pounds Escarp- the name used for the Battery Rock Coal identified palynologically as ment. Many scenic cliffs of Pounds, Sandstone. We are in this report Gentry was sampled from wastepiles and deep gorges, waterfalls, and changing the rank of the Gentry Coal of two collapsed drift mines along- rockshelters are found in the study from a member to a bed (1) because side a northeast-trending stream in area; these include Double Branch a member cannot contain another SW NW NE, Section 7, T11S, R6E, Hole, Jackson Hole, and Peter Cave member (North American Strati- Eddyville Quadrangle (field station in the Eddyville Quadrangle, and graphic Code, 1983, Article 26), and 387). Coal also is recorded in drillers' Bell Smith Springs, Burden Falls, (2) to establish a hierarchy in which logs of two oil-test holes in NE, Cedar Falls, and Jackson Hollow in local or lenticular coals like the Gen- Section 12, T11S, R5E, about 3/4 mile the Stonefort Quadrangle. Large try are ranked as beds, and widely west of the drift mines. Both logs areas of bare rock are common at the continuous coals like the Davis and indicate that the coal occurs at the tops of cliffs and knobs capped by Herrin are ranked as members. In so base of the Drury Member. A weath- Pounds. Bold hogbacks of Pounds doing, we depart from previous ISGS ered outcrop of coal was found near Sandstone mark the north and north- practice, in which all coals were the base of the Drury in a stream in west flanks of the McCormick Anti- ranked formally as members (e.g., SE NE SW, Section 12. Black shale cline, especially in the area northeast Davis Coal Member) and from cur- containing plant fossils was found at of Burden Falls. In contrast, the rent USGS and Kentucky Survey pol- the position of the Gentry Coal in NE Pounds forms gentle slopes on some icy, in which all coals are ranked SWSE, Section 33, T11S, R6E, Eddy- of the drainage divides (for example, informally as beds (e.g., Bell coal ville Quadrangle. in the village of Eddyville). bed, with coal bed in lower case). The The Pounds is similar lithologically distinction between a coal bed and a Unnamed coal in Drury Member to the Battery Rock Sandstone, but coal member, in our usage, will be Thin, shaly coal about 5 feet below generally has fewer and smaller decided on a case-by-case basis. In the top of the Drury was sampled quartz pebbles than the latter. Some general, we are ranking as members from a small ravine in SW NW NE, Pounds outcrops contain no pebbles. those coals that are traceable across Section 3, T12S, R5E (Stonefort field In most places quartz granules and several counties, and ranking as beds station 6). This bed, 18 to 24 inches pebbles less than 1/2 inch in diameter the less traceable coals. thick, is palynologically distinct from are scattered throughout the Pounds The Gentry Coal has been iden- the Gentry Coal. Shale that contains or concentrated along certain bed- tified in parts of Hardin County, plant fossils and may either overlie ding planes. Conglomerate is rare. Illinois (Baxter et al. 1963, Baxter and or be laterally equivalent to a coal has Bedding and sedimentary structures Desborough 1965), and Crittenden been observed in upper Drury strata of the Pounds resemble those of the and Livingston Counties, Kentucky at three sites in the study area. One Battery Rock. Occasional fossil logs (Amos 1965, 1966). This coal is not site is at Eddyville field station 402 of Calamites and Lepidodendron have physically traceable from these sites (fig. 9, col. 2). A second is near the been observed. Bivalve resting traces to the study area, where it is probably stream junction in SW SE NW, Sec- (Pelecypodichnus) were found in float lenticular. The coal we are calling tion 36, T11S, R4E (Stonefort field believed to be from the Pounds along Gentry is in the same stratigraphic station 758). The third is a ravine in Bear Branch in the Eddyville Quad- position as the type Gentry and is SW NW SE, Section 4, T12S, R4E, rangle. similar in palynological content. Creal Springs Quadrangle (Nelson's The Pounds is thin to absent in The Gentry Coal is exposed at field station 9). some places and more than 120 feet several places in the southwestern in others. It is at least 100 feet thick part of the Stonefort Quadrangle, but Pounds Sandstone Member The in Jackson Hollow in the southwest- its crop line has not been plotted on Pounds Formation in the Caseyville ern part of the Stonefort Quadrangle, the geologic map because of space Group was introduced by Weller where the Drury Member underlies constraints. The best exposures are (1940); its type locality is Pounds the Pounds. Westward, where the in railroad cuts in the southwestern Hollow in southern Gallatin County, Drury Member apparently was part of the Stonefort Quadrangle (fig. Illinois. Kosanke et al. (1960) revised eroded, the Pounds rests directly on 9, column 1). The coal was also the name to Pounds Sandstone Mem- the Battery Rock Sandstone. Con- observed near the head of Jackson ber, Caseyville Formation, and tinuous exposures of sandstone are Hollow in NE NW NW, Section 6, defined the top of the Pounds as the present from the 510-foot to the

21 .

700-foot contour in SE, Section 1, Deposit ional environment Previ- fossils by marcasite are evidence of T12S, R4E. More than 120 feet of ous Studies of lower Pennsylvania!! dysaerobic conditions (Devera et al. sandstone, probably all Pounds, sandstones in the Illinois Basin 1987). The herringbone crossbedding .is crops (Hit cliffs east ol the stream (Potter and Siever 1456, Potter and in the I )im v Member at Peter Cave in E 1/2, Section 3, T12S, R3E, Creal Glass 1958, Potter 1963) established indicates tidal currents. Nonmarine Springs Quadrangle. The Pounds is a dominant southwesterly paleo- conditions elsewhere in the Drury 60 to 105 feet thick on the McCormk k currenl direction. This direction are indicated by the presence of coal, Anticline northeast ol Burden Falls. conforms to the trend of sub-Pennsyl- rooted underclay, and shale contain- Between bell Smith Springs and vanian paleovalleys (Bristol and ing unbroken plant fossils.

Edd) ville the sandstone ranges from 1 low, ud 1<-)71). Most geologists, Marine sedimentation in the Way- 40 to 75 feet thick. Eastward from the including those cited above and side Member has been documented center oi Section 32, T11S, R6E, Ethridgeetal. (1975) and Koeninger to the west (Rexroad and Merrill Eddyville Quadrangle, the Pounds and Mansfield (b>79), have inter- 1985, Jennings and Fraunfelter 1986) thins abruptly (within 1/2 mile) from preted the Caseyville as primarily the and to the south (Devera, in prepara- about 50 feel to 5 feet, [he bounds product ol fluvial and deltaic sedi- tion) of the present study area. was not recognized in the two small mentation fhese authors also attri- Abbott Formation exposures ol Caseyv ille on the bute the ijuartz-arenitic character of McCormick Anticline in Section 2, ( aseyville sandstones to derivation Name and definition The Abbott T11S, R6E, Eddyville Quadrangle. from sedimentary and low-grade Formation was proposed by Kosanke The lower contact of the bounds metamorphic rocks in the northern et al. (1960) and named for Abbott, was discussed previously. The upper Appalachians or southeastern Cana- an abandoned station on the Illinois boundary of the Pounds, and thus of dian Shield. Central Railroad near the center of theCaseyville Formation, is mapped I he transport of such a quantity of the Stonefort Quadrangle. (The at the top oi the highest clifl or ledge sand and gravel (particularly as much name is spelled "Abbot" on the cur- of sandstone. The cliff tops corre- .is that seen in the Battery Rock and rent 7 1/2-minute topographic map, spond with the highest occurence ol Pounds Sandstones) such a distance but was spelled "Abbott" on the older thick-bedded to massive sandstone. from the source area would seem to 15-minute Harrisburg Quadrangle Fine-grained, thin-bedded, flaggy require a relatively steep gradient map). The type section consists of sandstone, commonly overlying the and a wet climate. Orogenic uplift of railroad cuts north and south of cliff- <\nd ledge-forming sandstone, the source area would provide the Abbot (fig. 10). The Abbott Formation is classified as Abbott Formation. increased gradient. Early Pennsylva- was defined there as comprising In the small area in the east-central nian tectonism in the northern Appa- strata from the top of the Caseyville part of the Eddyville Quadrangle lachians has been well documented Formation to the top of the the Mur- where the Pounds is absent, the top in West Virginia (Englundetal. 1986), ray Bluff Sandstone Member. The of the Caseyville was mapped at the eastern Pennsylvania (Wood et al. type locality of the Murray Bluff highest occurence of sandstone 1986), New England (Skehan et al. Sandstone is at Murray Bluff, near having typical Caseyville lithology. 1986), and Nova Scotia (Bell 1938, the northwest corner of the Eddyville Caseyville sandstone in this area is Rust et al. 1987). The paleoclimate of Quadrangle about 4 miles east of the white to light gray, nearly pure the Morrowan Epoch evidently was Abbott type section. The Murray quartz containing small quartz wet (Phillips and Peppers 1984, Cecil Bluff Sandstone is present (although pebbles; it varies from thin to thick et al. 1985), although not as wet as incorrectly identified by Kosanke et bedded but does not produce a that of the late Desmoinesian Epoch al. 1960) in the Abbott type section continuous ledge. Although they are not continuous (fig- 10). deposits, the Pounds and Battery Kosanke et al.'s definition of the Age of the Caseyville Formation Rock Sandstones in the study area upper boundary of the Abbott Forma- Evidence for the age of the Caseyville are more like "blanket" sandstones tion has caused difficulties for Formation is based on fossil pollen than like the linear or "shoestring" geologists attempting to map this and spores from coal and shale and sands typically associated with flu- formation. Kosanke et al. defined on goniatites from the marine shale vial or distributary channels. These overlying Spoon Formation in west- of the Drury Member in the Eddyville sandstones have some characteristics central Illinois more than 200 miles Quadrangle. Palynological data indi- of braided channel systems (Brown from the Abbott type area. Abbott cate that the Caseyville is of Morro- etal. 1973). Another possibility is that and Spoon lithologies grade into one wan age, according to the standard Pounds and Battery Rock sands were another in both areas. The base of series terminology in the Pennsyl- reworked by marine processes. De- the Spoon was defined as the top of vanian System of the North Ameri- tailed sedimentological work will be the Bernadotte Sandstone Member, can Midcontinent region (fig. 6) . The required to test these hypotheses. which Kosanke et al. believed equiva- Morrowan corresponds to the Namu- The presence of goniatites in the lent to the Murray Bluff Sandstone. rian C and Westphalian A stages of Drury Member in the southern part That equivalence has never been the Upper Carboniferous Series in of the Eddyville Quadrangle estab- verified; Kosanke et al. did not western Europe. The goniatites lishes marine influence there. Low provide a means of differentiating confirm the findings of palynology. diversity of fauna, large numbers of Abbott and Spoon Formations in The genus Axinolobus, identified in juvenile goniatites, and lateral facies areas where the Bernadotte/Murray the Drury, is associated with late relations suggest a drowned distribu- Bluff is absent or unidentifiable. In Morrowan or Westphalian A strata tary channel. High content of organic spite of these difficulties, we have (Devera et al. 1987). carbon (1.7%) and replacement of elected to retain the Abbott and

22 bott-Spoon contact has been projected and is indicated by a dashed line on the geologic maps.

Distribution and topography The Abbott Formation covers most of the Eddyville Quadrangle except (1) the southeastern and extreme southwestern parts and a narrow strip along the McCormick Anticline

where it is eroded; and (2) parts of the northern quarter of the quadrangle where the Spoon Formation overlaps it. In the Stonefort Quad- rangle the Abbott crops out southeast of the McCormick Anticline and on the structurally higher parts of the New Burnside Anticline. It also is exposed along all the ravines between the two anticlines and is thinly covered by the Spoon Formation on the intervening uplands. The Abbott is at the surface in most of the southern half of the Creal Springs Quad- rangle and in the valleys of Wagon

and Larkin Creeks; it is eroded along the large streams in the extreme south and is covered by thin, irregular patches of Spoon Formation on uplands in the southeast. The Abbott produces a topography of broad, gently rolling uplands deeply incised by ravines. The break in slope between valleys and uplands generally forms at the top of a sandstone. Ledges and local cliffs of sandstone line the valley walls, but no long escarpments like those of the Pounds Sandstone are developed. Alternating sandstones and shaly intervals produce hogbacks and strike valleys, respectively, on the flanks of anticlines.

Thickness Few reliable thickness measurements of the Abbott Forma- tion are available because of the absence of continuous sections and the difficulty of picking the contacts in subsurface logs. Composite sections Figure 10 Type section of Abbott Formation, Illinois Central Railroad cuts, Stonefort must be used with caution because Quadrangle, et al. this report. with nomenclature of Potter (1957), Kosanke (1960), and individual units vary considerably in thickness. The Abbott is estimated to Spoon Formations in the present ray Bluff itself is traceable through be 350 to 400 feet thick in the Eddy- study. The interval of rock between most of the report area, although its ville Quadrangle; it may be thicker the Murray Bluff Sandstone and the character varies considerably from in the Dixon Springs Graben at the Pounds Sandstone is noticeably place to place. southeast corner of the quadrangle, sandier and produces a more rugged We mapped the Abbott-Spoon con- where the upper part of the Abbott topography than the interval above tact at the top of the highest ledge of is eroded. The Alcoa core (fig. 5) the Murray Bluff, particularly in the thick-bedded Murray Bluff Sand- indicates 350 feet as a minimum eastern part of the study area. With stone. Overlying thin-bedded sand- thickness. practice, geologists can generally stone,- present in many places, was The Abbott thins abruptly from distinguish sandstones from above assigned to the Spoon Formation. In about 350 to 250 feet in the eastern and below the Murray Bluff in out- some areas where the Murray Bluff half of the Stonefort Quadrangle. crop and hand specimen. The Mur- is absent or unrecognized, the Ab- Approximately 200 feet is exposed in

23 SSW CREAL SPRINGS STONEFORT Sandbu rn hole C-5 Reynoldsburg Ozark Creek hole S-4 IC railroad

o • o quartz granules 1 2 mi coal 1 2 3 km x x rooted zone M marine fossils including ichnofossils dark gray to black shale j--*--*- calcareous shale

Figure 11 Generalized stratigraphu cross section ofAbbott Formation from the northeastern part of the Kddyville Quadrangle to the southwestern part of the Creal Springs Quadrangle. Datum, top of Caseyville. Stippled pattern represents a ledge-forming sandstone; unpatterned areas represent shale, siltstone, and thin-bedded sandstone. the railroad cuts of the type section do not occur. Conglomerates of shale Siltstones and shales of the Abbott along the north-south centerline of pebbles or molds of pebbles—and and Caseyville are generally indistin- the quadrangle (fig. 10), and an addi- less commonly, coal and ironstone guishable. Bioturbation is more tional 50 feet or so is concealed .it the clasts—in sandstone matrix are fairly widespread in Abbott shale and silt- base. Test hole S-4 (plate 1) cored the widespread. Petrologic maturity of stone than in the Caseyville. Certain entire Abbott Formation. The lower sandstones decreases upward intervals in the Abbott that are contact is fairly definite; the upper through the Abbott. Lower Abbott pervasively bioturbated serve as local part of the Abbott grades from thin- sandstones closely resemble Casey- markers in the western part of the to medium-bedded sandstone (hav- ville sandstones except that they study area. Dark gray to black calcar- ing shale breaks) to crossbedded generally lack quartz pebbles and eous shale containing marine fossils sandstone. If the top of the crossbed- have slightly more mica, dark grains, and thin layers or nodules of lime- ded sandstone is defined as the top and interstitial clay. Upward in the stone are locally present. of the Abbott, the unit is about 250 Abbott, mica grains, feldspar, and The Abbott Formation is not com- feet thick. Estimated to be 220 to 300 rock fragments become increasingly pletely classified into members in feet thick in the Creal Springs Quad- common, and clay matrix occurs this publication. Several previously rangle, the Abbott continues to thin instead of silica cement. Iron oxide named sandstone members and coal westward in the Goreville Quad- is prominent, especially in the mid- beds or members have proved to be rangle (Jacobson, in preparation). dle part of the Abbott. These sand- lenticular and are difficult or impos- stones weather dark brown and com- sible to identify away from their type Lithology The Abbott Formation, monly have iron-oxide boxwork, areas. Only the Reynoldsburg Coal lithologically transitional between fracture-fillings, and Liesegang Bed and the Murray Bluff Sandstone the Caseyville and Spoon Forma- banding. Because of their clay matrix Member, which have type localities tions, has greater lateral variability and weak cementation, Abbott sand- within the study area, can be iden- than either. It consists almost entirely stones are generally more friable and tified with assurance. All other units of siliciclastics and a few lenses of less resistant to erosion than Casey- within the Abbott shown on the geo- coal and rare limestone, but the pro- ville sandstones. logic maps and described herein are portions and vertical distribution of Abbott sandstones are not as wide- named informally. Correlations of sandstone, siltstone, and shale vary ly traceable as the Pounds and Bat- some of these informal units around widely from one place to another. tery Rock Members of the Caseyville; the study area are tenuous, and in Sandstones of the Abbott are very some are traceable only a few tens to some areas one or more of the units light gray to medium gray when fresh hundreds of yards. Larger sandstone cannot be identified. The following and typically weather brown. Grain bodies locally are more than 100 feet units have been mapped and are size ranges from very fine to coarse. thick but in most places are less than discussed in this report: Widely scattered quartz granules and 50 feet. Relatively tabular Abbott small pebbles up to about 1/4 inch sandstones typically range from less Murray Bluff Sandstone Member are present, but abundant large peb- than 10 to about 40 feet thick. (youngest) bles like those found in the Caseyville Olive shale (informal)

24 EDDYVILLE NNE cycles of strata were observed; each begins with dark gray clay-shale at Bill Hill Hollow Blackman Creek Cochran Hollow the base and coarsens upward through silty shale and siltstone to sandstone. Two of the cycles are topped off by gannister (extremely hard, fine-grained, orange-weathering sandstone with a lumpy appearance) that is thoroughly penetrated by Stigmaria. Thin coal was observed overlying one of the gannisters. The entire interval is about 15C Teet thick, and individual cycles are 30 to 70 feet thick. Some lenticular sandstones within the basal member are thick enough to have been mapped. One such sandstone occurs along Bear Branch (SW NW, Section 32, T11S, R6E, Eddyville Quadrangle). This sandstone, 12 to 15 feet thick at most, lies about 25 feet above the base of the Abbott; it is light gray, very fine grained, and thickly bedded. Sand- Middle Abbott sandstone lentils, grades upward from the Pounds stone of similar lithology, mapped as including Cedar Creek sandstone Sandstone. Sugar Creek sandstone lentil, crops lentil (informal) The basal unit has been mapped out about 70 feet above the base of Lower Abbott sandstone lentils, only in an area along the McCormick the Abbott along Ozark Creek, SW, including Ozark sandstone lentil Anticline in the Eddyville Quad- Section 27, T11S, R4E, Creal Springs (informal) rangle, where overlying lower Abbott Quadrangle. Up to 40 feet of fine- Basal Abbott shale and sandstone, sandstones are relatively continuous. grained, nearly massive sandstone, including Sugar Creek sandstone In areas where lower Abbott sand- also mapped as Sugar Creek sand- lentil (informal) stone is absent, the basal unit cannot stone lentil, is exposed in ledges and Tunnel Hill Coal Bed be separated lithologically from railroad cuts along Sugar Creek in Reynoldsburg Coal Bed younger strata; such areas are map- SW NE SW, Section 17, T11S, R4E. ped simply as Abbott Formation, The Tunnel Hill Coal directly overlies The geometric relationships of these undifferentiated. For discussion pur- this sandstone. A persistent sand- units across the study area are poses, the basal unit includes that stone not on the map forms a small illustrated in figure 11. part of the Abbott Formation beneath ledge 30 to 40 feet above the base of lower Abbott Sandstone lentils in the the Abbott along the northwest flank Basal Abbott shale and sand- Stonefort Quadrangle and beneath of the McCormick Anticline between stone The ba sal unit of the Abbott the Tunnel Hill coal and Ozark sand- McCormick village and Burden Falls Formation in our study area consists stone in the Creal Springs Quad- in the Stonefort Quadrangle. of shale, siltstone, thin-bedded sand- rangle. The railroad cut north of the tunnel stone, and local lenses of thick-bed- The total thickness of the basal unit in Section 19, T11S, R5E, Stonefort ded sandstone (figs. 5, 12). The of the Abbott is about 50 to 80 feet Quadrangle, reveals unusual lithol- Reynoldsburg Coal Bed occurs near in the Creal Springs Quadrangle and ogies in the basal unit of the Abbott the base and the Tunnel Hill Coal 50 to 150 feet in the Eddyville and (fig. 10) . The basal unit here consists near the top; both coals are discon- Stonefort Quadrangles. of numerous lenses of sandstone tinuous. The basal unit erodes to gentle interbedded with shale-pebble con- The dominant lithologies of the slopes and strike valleys and com- glomerate. The sandstone in the basal unit are shale, siltstone, and monly is covered with talus and lenses is relatively clean, fine- thin-bedded sandstone. Medium colluvium derived from younger grained, and quartzose. Sandstone gray to dark gray clay-shale and silty sandstones. Thick-bedded sand- lenses 15 feet thick and as long as 100 shale commonly is thinly interlami- stones produce ledges or small cliffs feet terminate abruptly, locally inter- nated with light gray siltstone or in places; otherwise the interval is fingering with the conglomerate. The sandstone. The thin-bedded sand- exposed only in ravines and artificial conglomerate consists of gray shale stones, which closely resemble those excavations. clasts in carbonaceous siltstone and of the Caseyville, consist of white to Among the few relatively complete sandstone. In most places the bed- very light gray, very fine, slightly exposures of the basal unit are sev- ding is subhorizontal, but locally the impure, well-indurated quartz sand. eral in cutbanks and gullies along rock has undergone small-scale fold- Bedding is typically flaggy and may tributaries of Blackman Creek, in NW ing and faulting. Up to about 30 feet display ripple marks and trace fos- SW, Section 2, and E 1/2 SE, Section of sandstone/conglomerate is sharp- sils. Flaggy sandstone, especially 3, T11S, R6E, Eddyville Quadrangle ly and irregularly overlain by cross- common at the base of the Abbott, (fig. 11). Several coarsening-upward bedded to massive sandstone. Potter

25 (1957) described the exposure in sandstone-very line, well sorted, detail and called the sandstone/con- clean quartz; massive to thick o-pO bedded and crossbedded glomerate a breccia. He interpreted it as the product of subaqueous slumping or gravity flow triggered by tectonic movements along the McCormick Anticline, south of the railroad cut.

Fossils found in basal Abbot I strata include plant remains and trace fossils. The ichnofossil Conostichus sp. was collected from this interval along

«i tributary of Lusk Creek in NWNE N W, Section 28, T11S, R4E, Eddyville Quadrangle. graphic analysis. Hower (written communication 1988) described the Reynolds burg Coal Bed Wellei sample as a torbanite (boghead coal) (1940) named the Reynoldsburg Coal and gave its composition as follows: for the village of Reynoldsburg in the biturninite, 63.2 percent; alginite southwestern part ol the Creal {Bolryococcus), 28.8 percent; inerti- Springs Quadrangle. No tvpe section nite, 3.6 percent; exinite, 2.1 percent; was designated, but reference was vitrinite, 1.2 percent; and resinite, 0.1 made to mines in Section 32, T11S, percent. R4E, just west of the village. Kosanke Farther east, a thin coal was found etal. (1960) ranked the Reynoldsburg at five sites along the drainage of

Coal as a member. We are revising it Hunting Branch, in Sections 27 and to a bed because of its limited extent 28,T11S, R5E, Stonefort Quadrangle. and discontinuous nature. We have This coal is 50 to 60 feet above the mapped the Reynoldsburg Coal in S top of the Pounds Sandstone, where- 1/2, Sections 31 and 32, and in parts as the type Reynoldsburg is 20 to 30 of adjacent sections, along Cedar feet above the Pounds. The coal along Creek. The coal is known from a few Hunting Branch ranges in thickness outcrops and numerous abandoned from less than an inch to about 10 drift mines and prospect pits. This inches; it is dull and shaly and in coal was also extracted from two places consists of discontinuous commercial strip mines. The Herod lenses or stringers of coal in shale or Figure 12 Measured composite section Mining Company had a pit in SE, sandstone. No rooting was observed of basal Abbott shale and sandstone Section 32, and Energy Exploration below the coal. The palynological sequence as exposed in Blackman Creek, Company's Ozark Mine was in SW assemblage is abnormal and differs SE SE NE, Section 3 to SW NW SW, SE, Section 31. to NE According Section 2, T11S, R6E, Eddysville from that of type Reynoldsburg Coal. annual coal reports of the Illinois Quadrangle. Abundant herbaceous lycopod Department of Mines and Minerals, spores and Laevigatosporites in two the Herod mine was operated from East of Reynoldsburg, the Rey- samples suggest that the coal formed May through July, 1965, and pro- noldsburg Coal crops out along on a flood plain or in a similar, duced 1,938 tons of coal; the Ozark Ozark Creek in S 1/2, Section 27, relatively dry setting rather than in Mine operated from July through Tl IS, R4E, and has been traced along a peat swamp. A third sample con- December, 1978, and turned out the north side of Cedar Creek to NW, tained acritarchs (marine microfossils 10,417 tons of coal. Secbon 36, same township, in the possibly related to planktonic algae), The Reynoldsburg Coal was 27 to Stonefort Quadrangle. On Ozark which are rare in coal. These find- 31 inches thick at the Ozark mine and Creek, the dull, hard, finely lami- ings, plus the field setting, indicate 15 to 17 inches at the Herod Mine nated coal has been described as can- that the coal on Hunting Branch was (ISGS field notes, open files). Field nel or oil shale. Barrett (1922) deformed from transported plant mate- notes on other mines, prospect pits, scribed the deposit and ran distilla- rial rather than from an in situ peat and outcrops indicate that the coal tion tests on the samples. A maxi- deposit. Whether it is equivalent to reaches a maximum thickness of mum yield of 48.8 gallons of oil per the Reynoldsburg is problematic. about 36 inches in the Reynoldsburg ton was recovered. Barrett reported A shaly coal about 5 inches thick area. The coal thins rapidly west of that local farmers mined the material occurs about 10 feet above the the Cedar Creek drainage; it is only and burned it in their cookstoves and Pounds Sandstone on a tributary of 3 inches thick in the core of borehole fireplaces; no attempts at commercial Bear Branch, SW SE NW, Section 32, C-5 in SE SE, Section 36, T11S, R3E mining and distillation have been T11S, R6E. Sandstone below this coal (plate 1). The coal was not seen in made. is thoroughly rooted. Coal palyno- the southwestern Creal Springs A sample of the Reynoldsburg can- logically similar to Reynoldsburg coal Quadrangle, but it occurs farther nel from Ozark Creek was submitted was sampled from underwater at the west in the Goreville Quadrangle to James C. Hower of the Kentucky stream junction in the SE NE SE, (Jacobson, in preparation). Energy Cabinet Laboratory for petro- Section 5, same township.

26 Tunnel Hill Coal Bed A coal that has been applied widely to sand- and in Katy Reid Hollow south and crops out 40 to 70 feet above the stone in the lower part of the Abbott. southeast of Abbot probably is part Reynoldsburg has been mined at The type Grindstaff Sandstone is in of the same sand body. In this area several places in the Creal Springs southwestern Gallatin County, Illi- quartz granules and small pebbles Quadrangle. It is herein named the nois (Butts 1925). Baxter and Des- are fairly common in the sandstone. Tunnel Hill Coal Bed, for the nearby borough (1965) and Baxter et al. The sandstone is well exposed and community of Tunnel Hill. This coal (1967) mapped the Grindstaff in the about 40 feet thick in the railroad cut is palynologically equivalent to the fluorspar district east of our study in Section 19, T11S, R5E, which is Bell (IB) coal bed of western Ken- area. Potter (1957, 1963) and Kosanke part of the Abbott type section (fig.

tucky, but it is lenticular and prob- et al. (1960) called the lowest sand- 10). Its lower contact is sharp and ably not continuous with the Bell stone in the Abbott type section appears to be erosional, and the Coal. A surface mine was operated Grindstaff. However, no sandstone upper contact of the exposure also is in the Tunnel Hill Coal by the Holly in our study area can be linked with sharp; in places the upper surface of Mining Company in NW NW, Sec- the Grindstaff Sandstone of the fluor- the sandstone undulates strongly. A tion 6, T12S, R4E. According to spar district, and the lower Abbott strongly rolling upper surface along records of the Illinois Department of sandstones here are too discontinu- Allen Branch explains the intermit- Mines and Minerals, the mine oper- ous to warrant formal naming. We tent exposure of the sandstone in the ated only in August, 1970, and therefore refer to these sandstones stream bed. The overlying shale produced 2,542 tons. Judging by the informally as lentils within the lower contains small folds, which probably size of the area mined, the tonnage Abbott. reflect compactional adjustments to figure appears too small; another The lower Abbott sandstones are the rolling surface of the sandstone. company may have worked the mine consistently white to light gray when Several small lenses of lower before or shortly after Holly Mining fresh and light to medium gray when Abbott sandstone have been mapped Company. Several open cuts expose weathered. Iron-enriched zones and in the southeastern Stonefort Quad- the overburden strata and remnants Liesegang bands are common. Most rangle, along Bay Creek near Watkins of the coal. of the sand is fine grained, but small Ford and along Hunting Branch and Several caved drift mines and pros- granules are scattered throughout. its tributaries. Three lenses of sand- pect pits for the Tunnel Hill Coal were Quartz pebbles as large as 1/4-inch stone occur south of Hill Branch in found along the valley of Cedar in diameter are uncommon. The rock Sections 32 and 33, T11S, R5E. Cliffs Creek near the Holly strip mine. is massive to thick bedded; cross- up to 40 feet high are present just Evidence of digging also exists bedding and slumped or contorted north of the center of Section 32. around the head of the south-trend- laminations are common. Toward the Conglomerate of pea-sized quartz ing ravine in Section 1, T12S, R3E. A lateral edges of lentils the sandstones granules is exposed on the small collapsed adit containing fragments becomes more thin bedded and inter- knob in NW NE, Section 32. The of coal was noted in a steep side tongue with enclosing shales. stratigraphic position of the sand- ravine of Sugar Creek, SE NW SW, The most extensive lower Abbott stones in this area ranges from 20 to Section 17, T11S, R4E. Thin coal sandstone body crops out along the more than 100 feet above the base of sampled at two localities in the McCormick Anticline from Section 2, the Abbott. Eddyville Quadrangle is palynologi- T11S, R6E, Eddyville Quadrangle, A lower Abbott sandstone mapped cally similar to the Tunnel Hill (and westward to NE SE, Section 10, T11S, as the Ozark sandstone lentil crops Bell) Coals. The sites are a small ra- R5E, Stonefort Quadrangle. This out near the head of Ozark Creek in vine near the NW corner, Section 33, sandstone, 50 to 60 feet thick in most Section 27, T11S, R4E and on the T11S, R6E, and a steep gully in SE of this area, is especially prominent north sides of Cedar and Sugar NWNE, Section 23, same township. on the north flank of the anticline, Creeks in the Creal Springs Quad- The Tunnel Hill Coal is 12 to 14 where it forms large hogbacks. rangle. This sandstone also has been inches thick where it is exposed in Westward, this sandstone gradually mapped on the New Burnside Anti- the Holly strip mine. Three test holes thins and pinches out. Eastward, it cline from Section 17, T11S, R4E, encountered the coal (plate 1), which splits into two benches, and both Creal Springs Quadrangle, to SE, was 12 inches thick in hole C-6, 20 become thin bedded and grade later- Section 3, same township, western inches thick in hole C-3, and 28 ally into shale east of Cochran Hol- Stonefort Quadrangle. inches thick in hole C-5. The coal low (fig. 11). The northward extent The lower Abbott sandstone lentils from all three cores is dull and shaly. is unknown because the sandstone intergrade laterally with thin-bedded dips below drainage. On the south sandstone, siltstone, and shale (fig. Lower Abbott sandstone lentils it intergrades with flaggy, thin-bed- 12). The sandstone typically occurs Prominent cliff- and ledge-forming ded sandstone. in flaggy beds less than 4 inches sandstones are widespread above the Another lentil of lower Abbott thick, but some beds are as thick as basal unit in the lower part of the sandstone is well exposed on the 3 feet (fig. 13). Current ripples and Abbott Formation. These sandstones west side of Burden Creek, along oscillation ripples are common. Gray are as thick as 100 feet, and their Ogden Branch, and near the top of siltstone and silty shale are interbed- bases lie 50 to 150 feet above the base the ridge between Burden Falls and ded with the sandstone. Good expo- of the Abbott Formation. They do not McCormick in the Stonefort Quad- sures of these lithologies are found form a single tabular body of sand- rangle. This lentil, 40 to 100 feet thick along Bear Branch and in adjacent stone, but rather a series of lenses at near Ogden Branch, thins rapidly to roadcuts beside Rt. 145 north of similar stratigraphic position (fig. the southeast. Sandstone in the bed Eddyville, and in the vicinity of 11). The name Grindstaff Sandstone of Allen Branch west of McCormick Watkins Ford. All of these thin-

27 A single sandstone body 80 to 100 feet thick is present along Lusk Creek in Sections 16 and 21, T11S, R6E.

Eastward along Dog I lollow the sandstone splits into two distinct ledges separated by a covered interval. Farther north and east, several sandstone lentils appear at differen) levels within the middle part of the Abbott. A middle Abbott sandstone up to about 60 feet thick occurs in the southwestern part of the Eddy- ville Quadrangle, from Section 29, T11S, R6E westward. Below this thick-bedded sandstone is an interval of thin- to medium-bedded sandstone interbedded in places with shale and siltstone. Good exposures are available in roadcuts along Rt. 145 and in the bed of Bear Branch east of Figure 13 l\ pica] planar of the lower Abbott Formation in

Abbott Formation, undifferentiated, stones in our report area are too of Section 2, T12S, R6E, it is mostly or as lower Abbott on the Creal lenticular to warrant formal names. thick-bedded sandstone; eastward, Springs Quadrangle. Middle Abbott sandstones are shale and siltstone interfinger with thick And widespread in the Eddy- the sandstone (fig. 14). Black shale Middle Abbott sandstone lentils ville and easternmost Stonefort containing abundant plant fossils The middle part of the Abbott Forma- Quadrangles; they crop out along the and coal stringers occurs between tion contains many mappable len- New Burnside and McCormick Anti- sandstone tongues along the three- ticular bodies of sandstone that clines and in the drainages of Bay, forked ravine in Section 1, T12S, R6E, underlie and interfinger laterally Lusk, and Little Lusk Creeks. In most and along the south bluff of Little with fine-grained clastic strata (fig. of the central and western Stonefort Lusk Creek. Several horizons of 12). The fine-grained strata, desig- Quadrangle no mappable sandstones plant-bearing shales can be seen nated as the "olive shale" unit, are occur in the middle Abbott. A wide- along a steep ravine in SE SW SW, discussed and mapped separately spread but generally thin sandstone Section 36, Tl 1 S, R6E (Eddyville field from the sandstone lentils. informally named the Cedar Creek station 576). Middle and lower The sandstones described in this lentil can be traced through most of Abbott sandstones cannot be dif- section represent part of wha t Weller the area along and southeast of the ferentiated in this area, so the entire (1940) called the Delwood Formation New Burnside Anticline in the Creal interval is mapped as middle and (in theTradewater Group). The Del- Springs Quadrangle. lower Abbott sandstone. wood Formation was named for the Middle Abbott Sandstones form The marine trace fossil Zoophycos is village of Delwood in the Eddyville prominent cliffs in only a few places, common in a middle Abbott sand- Quadrangles, but no type section notably along Cochran Hcllow and stone that crops out along the stream was designated. Kosankeetal. (1960) Spring Valley Creek in the northeast- in N 1/2, NE SW, Section 10, T11S, recognized three sandstone mem- ern part of the Eddyville Quadran- R6E, Eddyville Quadrangle. Below bers in the Abbott Formation of gle. More commonly, a series of sand- the sandstone is black shale contain- southern Illinois: the Grindstaff, stone ledges separated by talus- ing the inarticulate brachiopod Orbi- Finnie, and Murray Bluff Sand- covered benches (presumably shale culoidea. This shale overlies dark gray stones. The Finnie Sandstone, in the and siltstone) is found in an interval shale that contains pyrite and sele- middle Abbott, was named by 90 to 135 feet thick. Individual sand- nite crystals and has stigmarian root- Owen (1856) in southwestern Union stone bodies have been mapped lets near its base. Trace fossils (prob- County, Kentucky. Kehn (1974) stated where the map scale permits (e.g., ably marine), including Torrowangia, that the Finnie is discontinuous Cedar Creek sandstone lentils on the complexly bifurcating burrows, and within the Dekoven (Kentucky) Creal Springs Quadrangle map), but domicile traces were observed near Quadrangle, which contains the type elsewhere the entire interval of sand- the same stratigraphic position in NE section. Palynological studies of coal stone and shale is mapped as middle NE, Section 10. by Peppers and Popp (1979) deter- Abbott sandstone, as in the drainage In general, the middle Abbott mined that the type Finnie is approx- area of Bay Creek and along the sandstone succession of the Eddy- imately equivalent to the Grindstaff McCormick Anticline from Cochran ville and eastern Stonefort Quad- Sandstone. Correlation of the Finnie Hollow westward. Individual cliff- rangles becomes coarser and less into southern Illinois (Kosanke et al. and ledge-forming sandstones have mature upward. The lower part typi- 1960, Baxter etal. 1963, 1967, Baxter been distinguished in the area south cally consists of light gray, very fine and Desborough 1965), therefore is of the anticline and east of Rt. 145. to fine-grained, well-indurated,

28 plant fossils

Figure 14 Lateral fades change in the middle and lower part of the Abbott Formation in Dixon Springs Graben, southeast of Little Lusk Creek, in the extreme southeastern part of the Eddyville Quadrangle. Lateral distance is approximately 1.2 miles (2 km). Numbers along the top of the figure designate field stations. quartzose sandstone in tabular, thin indicates approximate correlation The Cedar Creek sandstone gener- to thick beds. Upward, the sandstone with the Tarter or Willis Coal, which ally is light gray to buff when fresh, becomes medium to coarse grained occurs in the middle part of the weathering to brown. Iron oxide is and poorly sorted and contains some Abbott. A coal seam 6 inches thick abundant. Grain size is fine to medi- quartz granules. Mica, lithic frag- was encountered at a depth of 130 um, rarely coarse; granules are ments, and interstitial clay content feet in borehole E-3 (plate 1), SE NE absent. Mica, lithic fragments and increase upward. Iron oxide is preva- NE, Section 9. Several thin, carbon- clay matrix are noticeable. Bedding lent; the sandstones weather dark aceous shales or coaly stringers were varies from medium to very thick and brown, and Liesegang bands and logged in borehole E-2, near the is generally irregular. Where the heavy surface crusts of iron oxide are center of the north line, Section 8, sandstone is thick, planar crossbed- prominent on cliffs and ledges. Sedi- same township (plate 1). ding is conspicuous. mentary structures of the upper part Middle Abbott sandstones inter- The Cedar Creek sandstone and of the middle Abbott include planar finger westward with the olive shale underlying shaly strata in the Creal and trough crossbedding, scour-and- unit in the eastern Stonefort Quad- Springs Quadrangle contain abun- fill, and slumped bedding. rangle. The middle part of the Abbott dant ichnofossils and local body fos- Light gray, thinly laminated silt- thins markedly as the sandstones sils, both of which indicate marine stone and shaly sandstone, gray to pinch out. The interval from the top sedimentation. The sandstone is black shale, and thin lenses of coal of lower Abbott sandstones to the strongly bioturbated in many places, are interbedded with middle Abbott base of the Murray Bluff Sandstone particularly in the railroad cut at sandstones in the central part of the decreases from about 200 to 230 feet Tunnel Hill and the highwall of the Eddyville Quadrangle. Dark gray to in the Eddyville Quadrangle to 80 to abandoned strip mine in NW NW, black carbonaceous shale was found 100 feet in the central Stonefort Section 6, T12S, R4E. The ichnofossils near the base of the interval in several Quadrangle. Conostichus broadhcadi (fig. 15), places; a good outcrop is near the The sandstone mapped as Cedar Rhizocorallium, and Pekcypodichnus fork of Blackman Creek in SE NE NE, Creek sandstone lentil in the Creal were identified here and in nearby Section 3, T11S, R6E (Eddyville field Springs Quadrangle is equivalent to outcrops. Calcareous, dark gray to station 108) . A 2-inch coal bed crops the lower part of the olive shale to black shale containing thin bands out in the stream bed in NW SW SW the east; it has been traced over a and nodules of argillaceous to sandy, of the same section (field station 183). large area that includes the New very fossiliferous limestone occur in Several coal outcrops and collapsed Burnside Anticline and the drainage the same interval. Outcrops are com- adits were observed in the stream areas of Cedar, Sugar, and Little mon in the Sugar Creek drainage area southwest of Zimmer Cemetary near Cache Creeks south of the anticline. southeast of the New Burnside Anti- the boundary of Sections 9 and 16 in Although thin and poorly exposed cline, and fossiliferous strata were the same township. Stream cuts re- in most places, the sandstone marks cored in boreholes C-3 and C-6 (plate veal 12 to 14 inches of coal overlain by the abrupt change in slope at the tops 1). The following fossils were iden- sandstone and underlain by rooted of the steep-walled valleys and tified from limestone in the Creal underclay. Palynological analysis ravines of these three creeks. Springs Quadrangle:

29 .

Bi.h huipoils Sjinili-irlluni oiiiipcs

tris; Pum tospirifei morrowensis I to

/m/i)/(/('s N(7'M*.sAi'((.s/s; AlllitjllillDlliil s;i.;

/ inoprodm tusplaniventralis ( omposita sp.

/ Crinoids: Hphuu rinus i / i roneisi (2 calyces); Sepacocrinus plates Conodonts: Idiognathoides ouachitensis;!. noduliferous;L sin uosis,

Idioproniodus i onjuru tws; Hideodus minutus

Trilobites: c./, Paladin morrowensis Bryozoans, bivalves, ostracodes, and nautiloid cephalopods.

In addition, the inartic ulate brachiopods Lingula and Orbiculoidea, productid bra< huopods, and the trace fos-

sil Zoophyi us are found in black shale associated with the limestone [Tie conodonts suggest late Morrowan to early Atokan age (Jacobson 1983).

The Cedar Creek sandstone is so Figure 15 I he traee tossil ('(»;,>>/ u /;/<•., interpreted as a nesting-trace of a sea anemone poorly exposed at must places that and ,\n indicator of marine deposition, in shaly siltstone of middle Abbott Formation, near the south end ol the railroad cut south ol runnel Hill, Creal Springs Quadrangle its thickness is difficult to estimate. (SE NE SE, Section 35, T11S, R3E). Ravine cuts and artificial exposures typically show 15 to 20 feet ol sandstone. The sandstone thickens ab- unknown; the color of the shale is lent to the Cedar Creek sandstone. ruptly to 40 feet or more in some not noticeably olive. Other common ichnofossils are Pe/e-

places, forming cliffs. I he elongate, In the Eddyvilleand eastern Stone- cypodichnus and Cochlichnus; these north-trending bodies ol this sand- fort Quadrangles the olive shale types are especially common in the stone display planar crossbedding forms slopes and strike-valleys lower part of the olive shale along with foresets consistently dipping between the middle Abbott sand- Ogden Branch and in drainage ditch- southward. One such body lies along stones and the Murray Bluff. Expo- es beside the railroad tracks south of the east side of the large ravine in sures, generally confined to small Abbott (Stonefort Quadrangle). A SW, Section 20, T11S, R4E. Another gullies, are small and fragmentary. specimen of Conostichus was found is near the head of Cache Creek in The exposed rocks consist mainly of in shale in the ditch east of the SW, Section 27, T11S, R3E. The sand- medium to dark gray, silty shale railroad. stone varies greatly in thickness and interlaminated with light- to medi- Calcareous sandstone and impure, interfingers with shale. The exposure um-gray siltstone and very fine sand- sandy limestone containing fragmen- in the ravine near the SE corner of stone. In a narrow northeast-trend- tary marine fossils were observed in Section 36, T11S, R3E is almost en- ing ravine in SE NW, Section 35, the olive shale at field station 86 in tirely sandstone; 2,000 feet south- T10S, R5E, Stonefort Quadrangle, the Eddyville Quadrangle. The out- ward a thin sandstone bed overlies about 25 feet of siltstone in the lower crop lies along the base of the bluff siltstone, shale, and thin-bedded, part of the olive member is exposed on the west side of Blackman Creek, shaly sandstone at the same eleva- The siltstone, ripple marked and just south of the mouth of a small tion. North of Cedar Creek in SW, shaly in the lower part, becomes ravine that runs east from the center Section 31, T11S, R4E, sandstone has intensely bioturbated and less shaly of Section 34, T10S, R6E. Old field been cut down almost to the Tunnel upward. Exposures of part of the notes (ISGS, open files) reported Elill Coal, but fine-grained strata over- olive shale also can be found in small other unconfirmed exposures of lie the coal at the abandoned Holly ravines just east of Murray Bluff in limestone nearby. Fossils in the lime- surface mine south of the creek. the Eddyville Quadrangle. stone consist of broken brachiopod Numerous ichnofossils are found shells and crinoid fragments. The Olive shale An interval consisting in the olive shale throughout the limestone underlies and grades into mostly of shale and siltstone and study area. The most common form 10 to 12 feet of sandstone that forms some thin beds of sandstone partly is Planolites, a simple horizontal, a small ledge along the west side of overlies and partly is laterally equiva- straight to slightly curved, tubular the valley. Solution channels are lent to middle Abbott sandstones de- burrow 1/4- to 3/8-inch in diameter. developed in the lower part of the scribed previously (fig. 11). Several These burrows, typically filled with limestone. Limestone and dark gray geologists working in the early 1900s sand, weather out of their shale or shale containing gastropods, cepha- (unpublished field notes, open files, siltstone matrix. Planolites was ob- lopods, and other marine fossils were ISGS) referred to this interval as the served in all three quadrangles in found in the upper part of the olive

"olive shale," and we have adopted more than a dozen localities; it is shale in the cores of boreholes C-2 this term as an informal mapping found in the upper part of the olive and C-8 (plate 1). unit. The origin of the name is shale in strata approximately equiva-

30 .

A 1-inch layer of weathered coal In the Creal Springs Quadrangle, sandstone. Farther west the sand- and underclay were noted near the the Cedar Creek sandstone and the stone reappears and becomes as thick top of the olive shale near the mouth shaly interval between the Cedar as 80 feet along Cliffy Creek and the of a ravine south of Battle Ford Creek, Creek and Murray Bluff Sandstones Little Saline River in the northwest- SW NE NE, Section 32, T10S, R6E are equivalent to the olive shale ern part of the Stonefort Quadrangle. (Eddyville field station 289). farther east. The olive shale was not Much shale and siltstone are inter- The olive shale thickens westward designated on the Creal Springs bedded with the sandstone in this in the Eddyville Quadrangle from as geologic map. The interval between area. In the southwestern Stonefort little as 10 feet along Cochran Hollow the Cedar Creek and Murray Bluff Quadrangle and throughout the to about 55 feet near Murray Bluff. Sandstones is 20 to 70 feet thick and Creal Springs Quadrangles, the In the Stonefort Quadrangle the is largely covered with colluvium. Murray Bluff ranges from less than olive shale is mapped along the New Test holes C-2, C-6, and C-8 cored 10 feet to about 40 feet thick. Burnside Anticline and along Ogden this interval (plate 1). The Murray Bluff splits into two Branch, Allen Branch, and Katy Reid sandstone benches separated by a Hollow south of the anticline. The Murray Bluff Sandstone Mem- parting of shale or siltstone on the olive shale in the Stonefort Quadran- ber Weller (1940) named the Mur- north flank of the New Burnside gle consists mainly of medium to ray Bluff Sandstone and assigned it Anticline in the Eddyville Quad- dark gray, silty, carbonaceous shale, to the Macedonia Formation in the rangle (fig. 11). The parting appears and light- to medium-gray, thinly Tradewater Group. Murray Bluff is about 1 mile east of the type locality laminated siltstone. In most of the the name of a hill near the northwest and thickens eastward to about 30 quadrangle the olive shale is 60 to corner of the Eddyville Quadrangle, feet. The upper sandstone bench is 100 feet thick. Thin, tabular beds of where the sandstone is especially generally 20 to 25 feet thick; the lower light gray, very fine-grained sand- prominent. Kosanke et al. (1960) bench is 50 to 80 feet thick. Good stone occur in the lower part of the reclassified the Murray Bluff as the exposures are present in ravines in unit. Ripple marks and small load uppermost member of the Abbott NE SE Section 28, T10S, R6E, and in casts are common. Bioturbation is Formation in southern Illinois. roadcuts along Rt. 145 in Section 27, especially prevalent, and abundant The Murray Bluff Sandstone has same township. The core of borehole and diverse ichnofossils are present been mapped in all three quadran- E-l also indicates two benches of in sandstone and siltstone in the gles northwest of the McCormick Murray Bluff (plate 1). The splitting lower part of the olive shale. The best Anticline but has not been positively is not indicated on the geologic map. places to observe ichnofossils are identified southeast of the anticline Sandstone similar in lithology and along the south fork of Ogden Branch Westward, it continues into the Gore- stratigraphic position to the Murray in SW NE, Section 16, T11S, R5E ville Quadrangle (Jacobson, in prep- Bluff occurs south of the McCormick (field stations 647 and 648), and in a aration) and appears to die out in the Anticline in the Eddyville Quad- large ditch just west of the Illinois eastern Lick Creek Quadrangle rangle. Because of its uncertain Central Railroad, south of Abbott (Weibel and Nelson, in preparation). correlation with the Murray Bluff, (field station 696). Desborough (1961) did not identify this sandstone is designated as upper The upper part of the olive shale the Murray Bluff in the Pomona Abbott. It has been mapped on hill- can be seen in railroad cuts at both Quadrangle, Jackson County. East of tops near Oak and in the area south- ends of the short tunnel in NW, our study area, Baxter et al. (1965) east of Bay Creek and west of Rt. 145. Section 18, T11S, R5E. The cuts reveal and Baxter and Desborough (1967) Outcrops are small, and most are up to 18 feet of dark gray, sideritic traced the Murray Bluff through confined to stream cuts, roadcuts, shale, overlain by underclay and the Herod and Karbers Ridge Quad- and discontinuous ledges. The most thin, shaly coal. Coal also crops out rangles. Nelson and Lumm (1984, accessible exposure is a roadcut nearby along Katy Reid Hollow. Paly- 1986a,b,c) were unable to identify the along Rt. 145 in NW SW NW, Section nologically, the coal is considered Murray Bluff north of the Fluorspar 29, T11S, R6E. younger than the Tunnel Hill (Bell) District. The topography of the Murray Coal and older than the Smith coal The thickest known occurrence of Bluff is less consistent than that of bed of western Kentucky. The coal is Murray Bluff is at the type locality; older Pennsylvanian sandstones.

overlain by dark gray clay-shale, here it is 115 feet thick, and the top Where it is thick and massive, the upon which the Murray Bluff Sand- is eroded. Along Battle Ford Creek sandstone commonly forms cliffs stone rests with erosional contact. in the Eddyville Quadrangle and (fig. 16) separated by steep slopes

The lower contact of the olive shale along the Little Saline River from having float and small outcrops . The is either sharp and irregular, as along Sand Hill eastward in the Stonefort distribution of outcrops could give Allen Branch, or gradational, as Quadrangle, the Murray Bluff is 100 the impression that the Murray Bluff along Ogden Branch. Sandstone feet or thicker. The sandstone be- consists of a series of lenses; how- beds in the olive shale generally are comes shaly southward and thins to ever, fresh exposures in gullies com- thicker and more numerous near the less than 50 feet on the flank of the monly reveal thick sections of mas- base. This sandy lower part is later- McCormick Anticline. The Murray sive or thick-bedded sandstone in ar- ally equivalent to middle Abbott Bluff grades laterally to shale, silt- eas where no cliffs or ledges are pre- sandstone lentils to the east and stone, and thin-bedded sandstone in sent. The lithology of the Murray west. The contact of the olive shale Sections 6, 8, and 16, T11S, R5E, Bluff in such areas does not differ no- with the overlying Murray Bluff Stonefort Quadrangle. The Spoon- ticeably from that of the cliff-forming Sandstone is erosional in the few Abbott contact here is mapped at the Murray Bluff. Differential resistance places it is well exposed. projected position of the top of the to erosion may be related to differ-

31 The upper boundary of the Murray Blufl generally isgradational through an interval of thin- to medium bed tied, shaly sandstone to the overlying siltstone and shale of the Spoon

I Formation (plate I). he contai I is mapped al the top ol thick-bedded sandstone.

Age of the Abbott Formation The Reynoldsburg Coal, near the base of the Abbott, is late Morrowan (latest

Westphalian A) (fig. 6), on the basis oi palynological study. The Tunnel Hill Coal, slightly above the Rey- noldsburg and palynologically distinct from the Reynoldsburg, is

c lassified as latest Morrowan (early Westphalian B stage). Conodonts indicative of late Morrowan or early Atokan age were recovered from Figure 16 Murray Blufl Sandstone at its maximum development just east of the type locality in NENWNF, Section J5, T10S, R5E, in the north westernmost pari ol limestone above the Tunnel Hill Coal tin- 1 ilds \ ille On. ulianeje 1 he sandstone dips 15 to 20 northwest on the Hank in the Creal Springs Quadrangle of the New Bumside Anticline. (Jacobson 1983). The Oldtown Coal, which lies just above the Abbott in ences in cementation of the sand becomes less prominent and ripple the basal Spoon Formation, is paly- stone. On cliffs and ledges the Mur- marks more numerous. In the west- nologically correlative with the Rock ray Bin II tends to be heavily impreg- ern Stonefort and Creal Springs Island Coal and is classified as very nated with iron compounds and has Quadrangles the Murray Bluff is late Atokan (latest Westphalian C). conspicuous Liesegang banding (fig. generally finer grained, more shaly, The Seville Limestone, which direct-

17). This sandstone is case hardened: and less massive than it is to the east. ly overlies the Rock Island Coal, con- the impregnated crust protects the Quartz granules have not been tains fusulinids that also indicate late more friable rock beneath. Else- noted, but lenses of shale- and Atokan age. The Seville is considered where, notably on Sand Hill in the coal-pebble conglomerate are found equivalent to the Curlew Limestone Stonefort Quadrangle, the Murray in the east-central Creal Springs of western Kentucky (Thompson et

Bluff disintegrates to sand. Where it Quadrangle. Gray, silty shale and al. 1959, Douglass 1987). is thin, the Murray Bluff erodes to siltstone commonly interfinger with occasional ledges on moderately the sandstone. Ripple marks, load Depositional environment Our sloping, float-covered hillsides. casts, and bioturbation can be seen preliminary findings, based largely Lithologically, the Murray Bluff is in the shale and siltstone. on study of trace fossils, indicate that less mature than older Pennsylva- The contact of the Murray Bluff most shale and siltstone and much nian sandstones. Quartz is the main with the underlying olive shale unit of the sandstone in the Abbott For- constituent, but mica, feldspar, rock is sharp and is probably erosional in mation were deposited under marine fragments, and interstitial clay occur most places. The best exposures of a conditions. Marine body fossils have in greater quantities than in older clearly erosional lower contact are in been found in the Creal Springs and sandstones. When fresh, the sand- railroad cuts in NW, Section 18, T11S, Eddyville Quadrangles within the stone is light gray to medium gray, R5E, Stonefort Quadrangle. A sand- olive shale and equivalent sand- or brown; it weathers golden brown stone body that is probably a paleo- stones of the middle part of the to dark brown and commonly dis- channel or paleoslump is exposed Abbott. Abundant, diverse ichnofos- plays Liesegang bands. Where the along the ravine near the center of sils are found in the same rocks in all

Murray Bluff is thick, it is generally NW, Section 4, T11S, R5E (Stonefort three quadrangles. The forms Aster- fine to coarse grained and contains field station 608) and is indicated on osoma, Conostichus, Rhizocorallium, scattered small, rounded, quartz the geologic map. This sandstone is Teichichnus Torrawangia, and granules, especially in the upper part approximately 1,400 feet long and Zoophycus, in particular, have strong of the unit. Thinner Murray Bluff 200 feet wide where exposed and is marine affinities (Chamberlain 1971). normally is very fine to fine grained incised 30 to 40 feet into the olive The broad diversity of ichnogenera and lacks granules; its bedding shale. It is linear (or nearly so) and observed at many middle Abbott differs according to thickness of the strikes N20°E. The western contact sites is an additional indicator of unit. Thick Murray Bluff is thick resembles a fault surface dipping 60° marine sedimentation (Miller 1984). bedded to massive. Planar foreset to 70° east; however, no indication of Environmental indicators are beds in sets as thick as 6 feet are tectonic faulting was found. The sparse in the basal Abbott shale and conspicuous in many outcrops. As eastern margin is concealed. Bedding sandstone interval, but an occur- the Murray Bluff thins, its bedding in the sandstone is horizontal, or rence of Conostichus in this interval also thins, and shale or siltstone nearly so, and the adjacent shale is and the presence of acritarchs in Rey- interbeds are seen. Crossbedding poorly exposed. noldsburg (?) coal indicate marine

32 deposition in these strata also. With- thickening may reflect accelerated Quadrangle and caps uplands in the in this framework, the thick-bedded, tectonic subsidence of the area at the Battle Ford Syncline west of Black- mappable Abbott sandstones seem junction of the Reelfoot Rift and the man Hollow. It occurs north and best interpreted as distributary-chan- Rough Creek Graben; this junction south of the New Burnside Anticline nel or distributary-mouth bar de- was a center of subsidence during in the Stonefort Quadrangle and posits. The largest body of lower much of Paleozoic time (Kolata and overlaps the crest of the anticline Abbott sandstone, which follows the Nelson, in press). Deltas may have from Old Town nearly to the western McCormick Anticline from the east- prograded into this area from the edge of the quadrangle. The Spoon ern part of the Eddyville Quadrangle east, depositing mostly sand on the covers most of the northern three- to the southwestern part of the east and mud and silt offshore to the quarters of the Creal Springs Quad- Stonefort Quadrangle, probably re- west. Some middle Abbott distribu- rangle except the valleys of larger presents a distributary channel. This tary channels, however, advanced as streams and an area along the New sand body trends west to west-south- far as the Creal Springs Quadrangle. Burnside Anticline northeast of west; some of its features, including The best example of one of these Sugar Creek, where it has been erod- its erosional base, abundant trough channels is the south-trending linear ed. The Spoon is covered by glacial crossbedding, and slumped lamina- body of Cedar Creek sandstone, with drift in the northwestern part of the tions, are typical of distributary its unidirectional, south-facing fore- Creal Springs Quadrangle and by channels (Brown et al. 1973). Unfor- set beds, in Section 20, T11S, R4E. Quaternary alluvial and lacustrine tunately, too few paleocurrent indi- The thickest Murray Bluff Sand- sediments in much of the northern cators were recorded to establish any stone lies in a west- to southwest- part of the Stonefort Quadrangle. trend. The location of this sandstone trending belt parallel to the McCor- A gently to moderately rolling to- along the anticline suggests that mick Anticline. Enclosed in shaly pography developed in the Spoon structural movements may have con- marine strata, it thins and becomes Formation. Sandstones in the Spoon trolled its deposition. Potter (1957) shaly as it approaches the flank of rarely produce ledges. Locally the interpreted deposits immediately the anticline. Our own limited paleo- sandstones cap low dissected pla- below this sandstone in the Illinois current data, and data of Potter (1963, teaus, of which Wise Ridge and the Central railroad cut as subaqueous p. 46), indicate westerly to southwes- hills north of Stonefort village are the gravity slides triggered by contem- terly flow. (Potter's map shows cross- best examples. Natural exposures of poraneous uplift of the McCormick bed orientation of the "Finnie Sand- the Spoon are limited in size and Anticline. stone" in the west-central part of the quantity. The lithologic sequence is The middle Abbott section thick- Stonefort Quadrangle. The outcrop known mainly from subsurface data ens substantially and becomes san- pattern indicates that the sandstone and exposures in quarries and strip dier eastward in the study area. The is Murray Bluff.) The Murray Bluff mines. fines upward from an erosional base and in places has slumped into un- Thickness The upper portion of derlying shale. All these features the Spoon Formation is eroded in all support interpretation of thick Mur- but a small area of the Eddyville ray Bluff as a distributary channel in Quadrangle, so the original thick- a high-constructive, elongate delta ness of the formation within the (Brown et al. 1973). Contemporane- study area is unknown. Boreholes ous structural movement on the north of the study area and compo- McCormick Anticline may have site measurements from outcrops in- influenced the course of the channel. dicate that the original thickness increased eastward from about 200 feet Spoon Formation in the Creal Springs Quadrangle to Name and definition Kosanke et 225 to 300 feet in parts of the Stone- al. (1960) proposed and named the fort and Eddyville Quadrangles. formation for the Spoon River in Fulton County, west-central Illinois, Lithology The Spoon Formation where the type section was de- consists primarily of gray sandstone, scribed. As originally defined, the siltstone, and shale (fig. 6) and gen- Spoon comprises strata from the top erally contains a lower proportion of of the Bernadotte/Murray Bluff sandstone than the Abbott Formation Sandstone Member to the base of the in the eastern part of the study area. Colchester Coal Member. We have In the western part of the area the revised the upper boundary of the Abbott becomes shalier, so the con- Spoon Formation in the study area trast between the Abbott and Spoon downward to the base of the Davis is less marked. Coal Member for reasons explained Sandstones of the Spoon Forma- in the section on name and definition tion, like most Abbott Sandstones, Figure 17 Liesegang banding, a of the Carbondale Formation. are classified as subgraywackes common feature of thick-bedded to (Potter 1963,Potter Glass 1958). massive sandstone (especially in middle and Abbott Formation), in Murray Bluff Distribution and typography The Coarse mica flakes and carbonaceous Sandstone at same locality shown in Spoon Formation crops out along the plant fragment grains are conspicu- figure 16. northern edge of the Eddyville ous in most Spoon sandstones and

33 thickly coat the bedding planes. The stone Bed OCCUr within (his basal N 1

matrix is dominantly < lay, and < e interval ol the Spoon Formation Z nu'nt is weak or absent (Potter and l he basal Spoon Formation com- 5l Thus, is Glass 1958). Spoon sandstones monly thin-bedded sandstone, grade crossing C/)| are less resistant and more friable gradationaJ the at ' from underlying Oldtown dip 5" a than most older Pennsylvanian sand- Murra) Bluff Sandstone. Ripple / stones. Unweathered sandstone is laminated sandstone .it the base lighl to medium gray or bull and commonly grades upward to gray

.1 commonly has speckled or salt siltstone oi silty shale. I he upper and pepper appearam c due to 1 .11 pari oi the Murray Bluti appears to bonaceous grains. Weathered stu grade laterally to thin bedded sand- fa< es generally are yellowish graj to stone and shale southeastward along deep orange brown. Hie grain size Bill Hill Hollow and also southwest- varies from very fine to coarse. Small ward from the type locality to the quartz granules are rare and found railroad cuts south ol Oldtown. turn bv the Oldtown Coal. Trace onlj in the lowesl part ol the Spoon. I hus, the Spoon '\nd Abbott Forma- lossils are common in the thin-bed- Shale, coal,

3 to 4 feet thick and can be tra< ed stone. I Ins shaly standstone is the present study include Teich- through large parts ot the report area. overlain bj 40 to45 feel ol interlami- ichnus, Asterosoma, Aulichnites, Phy- Some of these coal beds may extend nated, dark gray, silty shale and coides, Planolites, Beaconichnus, Tas- into several counties in southern siltstone (tig. 18), having some thin manadia, and Stellascolites (?). Illinois. sandstone interbeds, overlain in In the core of borehole S-2 (plate

Thin but widely traceable lime- 1), the Murray Bluff Sandstone stone and black fissile shale contain- grades upward to 50 feet of intensely ing marine fossils are present in the burrowed and flaser-bedded, silty Spoon Formation, particularly the shale resembling that observed in the upper part. railroad cut. Crinoid fragments and The following members, beds, and productid brachiopods occur 65 to 73 informal subdivisions of the Spoon feet deep in a thin limestone and Formation are recognized in this overlying sandstone. Poorly pre- study (fig. 6): served bivalves and corals (?) were noted 56 feet deep in shale above the Sub-Davis sandstone (youngest) thin coal. Strata between sub-Davis and L. G. Henbest (ISGS, unpublished golden sandstones field notes, 1926) reported calcareous Carrier Mills Shale Member sandstone containing marine fossils Stonefort Limestone Member north of Buzzard Roost Hollow near Wise Ridge Coal Bed the center of Section 35, T10S, R5E, Mt. Rorah Coal Member Stonefort Quadrangle. Fossils listed Creal Springs Limestone Member include Bellerophon, Marginifera, Avi-

Murphysboro (?) Coal Member culopecten, spiriferid brachiopods, horn corals, and crinoid columnals. Golden sandstone Henbest was unsure of the strati- Strata below golden sandstone graphic position of his find. We were Mitchellsville Limestone Bed unable to locate the exposure of cal- New Burnside Coal Bed careous sandstone, but we mapped Delwood Coal Bed the area as basal Spoon Formation. Oldtown Coal Bed (oldest) The interval between the Murray transition Figure 18 Upward from Bluff and golden sandstones is 100 thin-bedded, shaly sandstone to shale Strata below golden sandstone to 130 feet thick in ravines on the containing marine trace fossils, in basal An interval of dominantly fine- north flank of the New Burnside Spoon Formation. This railroad cut is grained strata, 30 to more than 130 Anticline near the western edge of south of Oldtown, Stonefort Quadrangle feet thick, separates the Murray Bluff the Stonefort Quadrangle. The inSWNWNW, Section 5, T11S, R5E.The is and golden sandstone. The Old- staff is 5 feet (1.5 m) long. The trace fossil Murray Bluff Sandstone less than town, Delwood, and New Burnside Conostichus broadheadi, a marine form, is 30 feet thick, and its identity is Coal Beds and the Mitchellsville Lime- common here. uncertain in some exposures. The

34 golden Oldtown sandstone Coal shale; marine sandstone sandstone trace fossils dip 10-J5^V^^^>^ (basal Spoon Fm) (basal Spoon Fm) .dip 2-3° dip 0°

Figure 19 Profile of east side of Illinois Central railroad cut south of Oldtown, showing New Burnside Anticline, here a

faulted monocline . (a) Fracture zone striking N80°W and dipping 90°, having horizontal slickensides and no measureable displacement, (b) Hinge of flexure; maximum dip about 35°N; two high-angle normal faults, each striking N75° - 80°W and

having roughly 5 feet ( 1 . 5 m) of throw down to north . (c) Normal fault trending N60°E/60°NW, with about 10 feet (3.0 m) of throw. Not shown: many small, high-angle normal and some reverse faults or flexures, all having less than 1.0 feet (0.3 m) of throw; most are located between B and C or a short distance south of C. Location: along border of Sections 5 and 6, T11S, R5E. overlying strata consist of medium to is slightly older than the Delwood of Durfee's drift mine. The Oldtown dark gray silty shale and siltstone and and closely correlates with the Rock Coal may be entirely eroded in these thin planar-bedded and ripple-lami- Island Coal of northwestern Illinois, boreholes and the coal penetrated nated sandstone, along with lenticu- the Litchfield and Assumption Coals may be slightly below the position of lar intraformational conglomerates. of central Illinois, and the Minshall the Oldtown. Table 5 lists results of The Oldtown Coal is 10 to 20 feet Coal of Indiana. chemical analysis from the Oldtown beneath the golden sandstone. The The Oldtown Coal, as thick as 36 Coal at the E. and L. Mine. basal Spoon Formation is substan- inches in the railroad cut (figs. 10, tially thinner in the northeastern part 19), is partly cut out by the overlying Delwood Coal Bed Weller (1940) of the Stonefort Quadrangle and in golden sandstone. M. E. Hopkins named the Delwood Coal for the the Eddyville Quadrangle, where the and Neely Bostick (ISGS, unpub- village of Delwood; Wanless (1956) Murray Bluff is thickest. The basal lished field notes, 1970) reported that described the type section in NW Spoon is as thin as 30 feet along the just west of the railroad, in the E. NW, Section 3, T11S, R6E, Eddyville west side of Bill Hill Hollow, near the and L. Coal Company surface mine, Quadrangle. These authors, as well border of the two quadrangles. The the coal was 34 to 35 inches thick and as Kosanke et al. (1960), misidentified interval is 40 to 60 feet thick along overlain by 4 to 10 feet of medium to the golden sandstone as the Murray Battle Ford Creek and its tributaries dark gray, smooth, well-laminated Bluff and assigned the Delwood Coal farther east. As elsewhere, the inter- shale, containing Lingula and plant to the Abbott Formation. Our map- val generally becomes finer-grained fragments near the base. The golden ping, borehole data, and palynologi- upward and is in gradational contact sandstone overlies the shale. cal study (by Peppers) demonstrate to the Murray Bluff. A thin coal, The Oldtown Coal also was mined that the Delwood Coal is above the overlain by shale containing plant prior to 1916 at Frank Durfee's drift Murray Bluff Sandstone and that it fossils, was observed 10 to 20 feet mine in SW SW SE, Section 2, Tl IS, is equivalent to the Bidwell Coal below the base of the golden sand- R5E, western edge of Eddyville named by Kosanke et al. (1960). We stone on the west side of Bill Hill Quadrangle. At the time of mapping, believe the correlation of the two Hollow. We did not see any marine the coal was partly exposed in the coals is strong enough to warrant fossils between the Delwood Coal caved adits of this mine. A. D. abandoning the name Bidwell and and the Murray Bluff Sandstone in Brokaw (ISGS, unpublished field retaining Delwood, which has prior- the Eddyville Quadrangle. However, notes, 1916) stated that the coal was ity. The Delwood is assigned bed drillers' logs of coal test holes north 26 to 28 inches thick and directly status because it appears to be a local of Delwood report limestone in this overlain by sandstone (the golden coal, not traceable very far beyond interval, and unpublished ISGS field sandstone). Smith (1957) reported 42 the present study area. notes record marine fossils, which inches (?) of coal. West of Oldtown, In most of the study area the Del- we failed to locate during a specific coal float and adits or prospect pits wood Coal is 24 to 42 inches thick. search in Buzzard Roost Hollow. occur in several places along the The maximum thickness, 71 inches, north flank of the New Burnside is in a borehole in NE NE, Section 8, Oldtown Coal Bed A coal bed up Anticline. The westernmost expo- T11S, R4E, Creal Springs Quadran- to about 3 feet thick crops out and sure of the Oldtown Coal is in the gle. This coal has been mined out. has been mined at several places in bank of Pond Creek, near the south- Forty-seven inches of coal was ob- the northern part of the Stonefort west corner of Section 3, Tl IS, R4E, served in a stream cut in NW NW Quadrangle. We have named this Creal Springs Quadrangle. At this NE, Section 4, T11S, R6E (Eddyville coal the Oldtown Coal Bed. The type locality the Oldtown Coal is 8 to 12 field station 110). The Delwood Coal locality is the railroad cut just south inches thick and very shaly. Thin coal crops out and has been mined at of Oldtown (Old Stonefort) in SW at widely scattered localities farther several places in the northeastern NW NW, Section 5, T11S, R5E (figs. west possibly is equivalent to the part of the Eddyville Quadrangle and 10, 19). Kosanke etal. (1960) referred Oldtown, but correlations could not in the Creal Springs Quadrangle to the coal in the railroad cut as the be confirmed. Only underclay and a northwest of New Burnside. Several Delwood Coal Member, which they very thin coal occur at the expected boreholes, including hole H-l (plate placed in the Abbott Formation. Our position of the Oldtown Coal in bore- 1), have penetrated the coal in the mapping and palynological study holes E-l and H-l (plate 1), and in southern Harrisburg Quadrangle demonstrate that the Oldtown Coal four proprietary test holes northwest (just north of the Eddyville Quadran-

35 c 5 An.ilvin.il data i>n coal in the stud) area

Fixed Volatile Heating carbon matter Moisture Ash Sulfur value, Coal seam Location (%) (%) (%) (%) (%) (Btu/lb)

•dh '

Reynoldsburg Mine dumps 18.6 3.2 2.9 0.88 14,067 SW,32-11S-4E

in Reynoldsburg Mine dumps 51.8 I 4.2 3.7 1.90 14,045 NWSI-si n 11S-41

Reynoldsburg 1 Kind Mine 56.1 3.82 4.17 0.85 13,849 SE,32-11S-4E

Reynoldsburg l Kmd Mine (9.6 I n 3.53 0.66 14,077

SE,32-11S ii

Reynoldsburg l lerod Mine 53.2 sin. 5.19 0.55 12,158 SE,32-11S-4E

Re) noldsburg i lerod Mine (8.9 3.82 0.95 14,109 SE,32-11S-4E

Re) noldsburg 1 lerod Mine 3 is 3.76 1.18 14,165

SE,32-Iis 11

Re) noldsburg" Ozark Mine On 1 i 7.0 3.22 13,525 si SWNI . H lis 11

Reynoldsburg l.st holeS-4 33.7 1.0 13.0 II). OK 12,354 (uppei split)

Re) noldsburg Ust holeS-4 28.5 1.0 31.8 6.22 10,375 (lowei split) b Bell (?) Rest pil 45.3 32.8 16.7 5.2 0.60 10,488 SWSESW,31-11S-4E

rest pit 44.7 33.3 17.6 4.4 0.63 10,344 SWSESW,31-11S-4E

Oldtown" E. & L.Coal Co. 51.6 31.9 9.1 7.5 1.12 12,076 Strip Mine, NENE, 6-11S-5E d 01dtown Test hole S-3 47.3 28.6 1.9 22.2 1.86 11,152

New Burnside J. C. Jennings Mine 48.6 37.8 8.6 5.0 2.12 12,971 SW NENE, 8-1 1S-4E Wise Ridge° Test hole S-l 45.7 35.2 2.2 16.9 4.69 11,915 SWSENE,25-10S-4E Mt. Rorah Western Mining Co. 46.7 32.7 3.6 17.0 7.73 - SESE,34-10S-4E Mt. Rorah' Test hole S-l 41.3 29.6 2.2 26.9 8.27 10,025 SWSENE,25-10S-4E

Delwood8 Test hole S-2 53.6 30.6 5.1 10.8 2.65 12,241 SWNESE,29-10S-5E

Composite of three face-channel samples. Coal 0.6 foot thick. Weathered sample. Two claystone partings included in sample. Composite of two face-channel samples. One claystone parting included in sample. Coal 0.4 foot thick. gle). Test hole S-l was cored in 42 and 6 to 18 inches thick in the Creal sandstone overlain by the New Burn- inches of Delwood Coal in the north- Springs Quadrangle. The parting is 30 side Coal. The shale above the Del- central part of the Stonefort Quad- inches thick in borehole H-l (plate 1). wood Coal is thin or absent in places rangle (plate 1). The Delwood Coal In the Eddyville and Harrisburg because of erosion at the base of the may have been eroded and replaced Quadrangles the Delwood Coal is golden sandstone. Table 5 gives by the golden sandstone in the overlain by 30 to 35 feet of dark gray analytical data on the Delwood Coal. northwestern part of the Eddyville shale, which contains plant fossils in Quadrangle and in the outcrop belt the lower portions and coarsens up- New Bumside Coal Bed The New in the Stonefort Quadrangle. A ward to siltstone. This siltstone is Burnside Coal was named by Weller claystone parting occurs near the overlain by the Mitchellsville Lime- (1940). Its type section is west of New middle of the Delwood Coal at most stone. In the Creal Springs Quadran- Burnside village, for which it was sites. It is commonly 3 to 4 inches gle the Delwood Coal is overlain by named, in SE SE SW, Section 5, T11S, thick in the Eddyville Quadrangle, 8 to 25 feet of shale, siltstone, and R4E, Creal Springs Quadrangle. This

36 o-J-o I Delwood Coal

Figure 20 Drawing of surface-mine highwall (since reclaimed) in SW SE, Section 5, T11S, R4E, Creal Springs Quadrangle. New Burnside Coal is discontinuous and locally split with shale. The sequence above the New Burnside Coal, with sandstone on northwest grading laterally to siltstone and then silty shale with inclined foreset bedding, suggests a delta that prograded toward the southwest. The "rider" coal may be equivalent to the Murphysboro Coal Member, and is laterally equivalent to part of the golden sandstone. (From field sketches by John T Popp 1977)

coal is restricted to the northeastern limestone of southern Illinois is The limestone contains abundant part of the Creal Springs Quadran- younger than the type Curlew Lime large nodules of chert. It weathers to gle. It has been mapped around the stone from Indian Hill, Union a yellow-brown porous residiuum low hills west of New Burnside and County, western Kentucky. Palyno- containing hollow casts of brachi- in small areas of Section 4, T11S, R4E, logical study confirmed the conclu- opods and other fossils. The cherty and Section 32, T10S, R4E. sions based on fusulinids (Peppers residiuum of the Mitchellsville is The New Burnside Coal is discon- and Popp 1979); therefore, we pro- easy to recognize in float and thus tinuous and varies in thickness from pose the name Mitchellsville Lime- the limestone can be mapped where a few inches to about 54 inches. Part- stone Bed for the limestone formerly outcrops do not exist. ings of shale, claystone, and bone coal called "Curlew" in Illinois. The name In most places the Mitchellsville is are common. On strip-mine high- is taken from the village of Mitchells- directly overlain by the golden sand- walls, the New Burnside Coal undu- ville, about 6 miles south of Harris- stone and has a contact that appears lates, pinches, and swells. The strata burg, Saline County. The type section to be erosional. The limestone has overlying the coal also are highly of the Mitchellsville is in a north- not been found west of the Eddyville variable (fig. 20). William H. Smith trending ravine in SW NW NW, Sec- Quadrangle. Directly below the (ISGS, unpublished field notes, 1956) tion 27, T10S, R6E, Harrisburg Quad- Mitchellsville at some sites is a very described sandstone with lenses of rangle (just north of the Eddyville thin coal streak or coaly shale, with shale-pebble conglomerate up to 6 Quadrangle). This ravine exposes underclay beneath. The claystone feet thick directly overlying the New about 5 feet of the limestone directly grades downward to siltstone or Burnside Coal near the type locality. overlain by the golden sandstone. shale, previously described in the Kosanke et al. (1960, p. 65) noted The lower contact of the limestone is section on the Delwood Coal. conglomerates overlying both Bid- concealed at the type locality; com- well (Delwood) and New Burnside plete exposures have not been found. Golden sandstone The golden Coals in their description of the type Cores from drillholes H-l and E-l sandstone* was called the Curlew

sections. Table 5 lists analytical data (table 1), in permanent storage at the sandstone in early reports, and on the New Burnside Coal. ISGS samples library, provide useful renamed the Granger Sandstone by reference sections. The limestone is Kosanke et al. (1960). The type Mitchellsville Limestone Bed A 1 foot thick at a depth of 41 to 42 feet Granger Sandstone overlies the distinctive, cherty marine limestone in hole E-l, and 1.7 feet thick at a Curlew Limestone in Union County, occurs about 35 feet above the Del- depth of 164.0 to 165.7 feet in hole Kentucky. Wanless (1939)correlated wood Coal in the northern part of H-l (plate 1). the "Curlew sandstone" of Kentucky the Eddyville, and the southern part Fresh samples of Mitchellsville with the "Granger sandstone" in of the Harrisburg and Rudement Limestone are medium to light gray southern Illinois. Correlation of Quadrangles (fig. 6). Although Butts or brownish gray. The limestone is sandstones was based on the as- (1925) and Weller (1940) called this sublithographic to fine grained and sumption that the type Curlew rock the Curlew Limestone, contains numerous crinoid frag- Limestone was equivalent to Illinois Thompson et al. (1959) established, ments, corals, whole brachiopods, "Curlew" (now called Mitchellsville). on the basis of fusulinids, that the and other fossils. Bedding is nodular. This correlation, is incorrect. The

*Comparison of maps and measured sections in the Creal Springs, Eddyville, and Stonefort Quadrangles indicates that the "golden sandstone" of the lower Spoon Formation represents at least two different sandstone bodies. What is described as the golden sandstone in this publication overlies the Delwood Coal along the north-central edge of the Eddyville Quadrangle; but in the Stonefort Quadrangle and in the northwestern part of the Eddyville Quadrangle, the sandstone mapped as "golden" probably underlies the Delwood Coal (not mapped)—a conclusion based on thickness considerations. In the Creal Springs Quadrangle, a sandstone occurs below the Delwood Coal and another sandstone occurs, at least locally, above the Delwood Coal; their positions are shown on the stratigraphic column, but their outcrops were not mapped in the quadrangle. The lower sandstone is equivalent to the golden sandstone as mapped in the Stonefort Quadrangle and the northwestern part of the Eddyville Quadrangle; the upper sandstone occurs in the same stratigraphic position as the golden sandstone along the north-central edge of the Eddyville Quadrangle. It has not been confirmed that the sandstones mapped as "golden" merge, as suggested by the stratigraphic columns of the Eddyville and Stonefort Quadrangles and in figures 6 and 20 of this report. Certainly, the lithology of all sandstone mapped as "golden" is similar.

37 informal name/ golden sandstone/ 1 he contai t ol the golden Band east of Creal Springs village, in NE used m tins report/ refers to th< stone with underlying strata is ero- SE SE, Section 25, THIS, R3E (Kos golden brown color ol the rock o\i sional. In the Eddyvilleand southern ankeetal. I960). The limestone also

some weathered surfaces. l larrisburg Quadrangles the golden is exposed in gullies north of Route

The golden sandstone oc< urs in the sandstone overlies or tills an ero- 166 at the east edgeoi ( real Springs

syn< line northeast ol I >elwood and sional < hannelt ut into the Mitchells- village; at the junction ol an un-

can be seen in .1 road< ul on Route villel Imestone. Westward the sand named north-flowing stream and

1 15 neai the centei ol the easl line/ stone cuts into the Delwood Coal; il Brushy Creek in SI Nl SI , Se< tion

l corner/ Section J3, nns, R6E, dire< tly overlies the Oldtown Coal at 30, T10S, R4E; and in the bed ol the

Eddyv ille Quadrangle. It also caps 1 rank l hirfee's drift mine (western- north-trending ravine near the center

the drainage divide north and west most edge ol the l ddyville Quad N 1/2SW/ Section 28, same township.

ni Rock) Branch and forms a cuesta rangle)and along theouft rop belt in I he limestone is less than 2 feet thick along the northern edgeoi the quad- the Stonefort Quadrangle. The Old- in most places. In the core ol borehole

rangle near Route 145. in the Stone town Coal is partly eroded in the rail- C-4 it is 2.8 ft thick (plate 1). Litho-

tort Quadrangle the golden sand road cut south ol Oldtown. North- logically the ( real Springs is similar

stone caps the lull between ( anej ward in the Stonefort Quadrangle/ to the Mitchellsville Limestone. The

Brant h and Bill I [ill I lollow and well data suggest that the golden Creal Springs Limestone is medium forms small hogbacks on the north- sandstone may pinch out. in the to dark gray, argillaceous, and com- ern flank ol tin.- New Burnside Anti c real Springs Quadrangle the golden posed of whole brachiopods, gastro-

cline. 1 in-- is the sandstone thai sandstone overlies the New Burnside pods, tusulinids, and echinoderm

Kosanke et al. (1960) erroneously Coal and CUtS into it loiallv. I he fragments in micritic matrix. Chert called the Murray Bluii in the Abbott uppei contact ol the golden sand- nodules are abundant and the lime- type section (tig. 10). The golden stone is gradational in the core ol stone is totally silicifed in places. The

sandstone was not mapped in the borehole ill (plate I). conspicuous chert float aids in

Creal Springs Quadrangle/ but it mapping. The Creal Springs Lime-

crops out in many places. It is found Strata between golden sandstone stone occurs above the golden sand-

near the tops of many lulls north and and sub-Davis sandstones I he stone. Its position relative to the west of New Burnside/ and along the interval between the golden and sub- Murphysboro (?) Coal west of New bed ol Sugar Creek east ol the village Davis sandstones consists largely ol Burnside could not be determined. of Creal Springs. shale/ siltstone/ and claystone, with In Franklin and Perry Counties, Unweathered golden sandstone is some shaly sandstone. Three named northwest of the study area, marine

light gray to buff; it weathers golden coal seams, two limestone members, black shale and limestone overlie the or orange brown to very dark brown, and one newly named shale member Murphysboro Coal in drill cores. This with coatings of iron oxide. Grain occur within this interval. The total limestone may be the Creal Springs, size ranges from fine to coarse with thickness of the interval varies from although continuity to the type area rare granules, and sorting is poor. approximately 70 to 120 feet. has not been established (Jacobson This is the youngest sandstone in 1983). which quartz granules were ob- Murphysboro (?) Coal Member served. Mica is abundant; clay mat- Coal probably equivalent to the Mt. Rorah Coal Member Kosanke rix, feldspar grains, and carbonace- Murphysboro Coal Member (Worth- et al. (1960) introduced the name Mt. ous flakes are conspicuous. The en 1868) formerly was mined in Rorah Coal Member for a coal previ- sandstone tends to be friable and several small drift and strip mines ously called the Bald Hill Coal. The erodes to smooth, rounded forms. It west of New Burnside, in E 1/2 Sec- name Mt. Rorah was taken from a seldom forms ledges, except in a few tion 8, T11S, R4E, Creal Springs church, now called Mt. Moriah places near Murray Bluff, where the Quadrangle. Identification of the Church, near the northeastern corner rock is pervasively impregnated with coal is on the basis of its strati graphic of the Creal Springs Quadrangle.

iron oxide. Bedding is generally thick position and a palynological study of Kosanke et al . listed the type locality to massive, with crossbedding com- coal fragments collected from waste of the Mt. Rorah Coal as being in the mon. In the northern part of the piles of mines. No outcrops of the SE, Section 35, T10S, R4E, but this Stonefort Quadrangle the golden coal were found in the study area. appears to be a misprint. The coal sandstone grades laterally to thin- or The coal occurs 20 to 30 feet above does not crop out in this locality now, medium-bedded shaly sandstone, the New Burnside Coal and directly and no mention of it appears in ISGS siltstone, and silty shale. Drill hole overlies the golden sandstone. On field notes for the locality. The in- S-l, north of Stonefort village, en- the highwall of a reclaimed strip mine tended type locality probably is the countered mainly siltstone at the west of New Burnside, we observed ravine just east of the road at the expected position of the golden a thin "rider coal," possibly the northern edge of Stonefort village, sandstone (plate 1). Murphysboro, in a shale sequence SW NE SE, Section 25, T10S, R4E; the The golden sandstone is about 20 that laterally interfingers with the coal is no longer well exposed here to 50 feet thick in most places, and golden sandstone above the New either, but it is well described in ISGS the top of the sandstone is eroded or Burnside Coal Bed (fig. 20). field notes (open files). covered nearly everywhere. It is at The Mt. Rorah Coal is widespread least 50 feet thick in the railroad cut. Creal Springs Limestone in southern Illinois. It has been cor- Kosanke et al. (1960) estimated 60 to Member The type locality of the related in subsurface with coal in 70 feet of golden ("Granger") sand- Creal Springs Limestone Member is Perry and Jackson Counties (Jacob- stone near Creal Springs. in an abandoned quarry about 1 mile son 1983) and, less confidently, with

38 contains the type Mt. Rorah Coal. The Wise Ridge Coal is thin, but fairly persistent across the northern edge of the study area. Its extent outside the mapped area is unknown; the coal is difficult to recognize in subsurface except in cores. It is therefore lowered in rank from member to bed in this report. As far as we know, the Wise Ridge Coal does not exceed a thickness of 12 inches, and has not been mined. The few known exposures include several gullies on the hill northwest of Stonefort, and the quarry east of Creal Springs in NE SE SE, Section Mt. Rorah Coal Mbr T10S, R3E. coal also (mostly concealed) 25, The occurs on the east side of Brushy Creek and Figure 2 1 Strata exposed on highwall of reclaimed Western Mining Company surface on the north side of the hill east of mine, NE SE, Section 34, T10S, R4E, Stonefort Quadrangle. The Mt. Rorah Coal was Mt. Moriah Church. The Wise Ridge mined here. Note lenticular body of light gray shale above the Wise Ridge Coal. was exposed, prior to reclamation, on the highwall of the Western coal as far northeast as Lawrence acres. No production figures are Mining Company surface mine, NE County (Jacobsen 1987). In this available. Nelson visited the site in SE, Section 34, T10S, R4E (fig. 21). report we have retained the Mt. 1977, after mining had ceased, and Wise Ridge Coal also was recovered Rorah Coal as a member rather than described strata in the highwall (fig. in cores of drill holes C-4, H-l, and a bed because of its apparent con- 21). The coal was largely concealed S-l (plate 1). tinuity. The Mt. Rorah crops out and and the pit has since been backfilled. In these cores and outcrops the has been mined on a small scale in Three small surface mines are known Wise Ridge Coal is 6 to 12 inches many places between the towns of in the Creal Springs Quadrangle. The thick, bright-banded, and blocky to Creal Springs and Stonefort. It is Oxford Construction Company thinly laminated. A soft, rooted visible in the quarry at the type mined a small amount of Mt. Rorah claystone generally underlies the locality of the Creal Springs Lime- coal in NE NE SW, Section 29, T10S, coal. A thin, shaly, nodular-bedded stone and in ravines northeast of R4E during 1977. Two other small limestone was observed directly Brushy Creek (Section 29, T10S, surface mines, dates and operators below the coal on the highwall of the R4E), where it was dug in numerous unknown, are in NW SW SW, Section Western Mining Company surface small surface and drift mines. The 28 and NW SW NW, Section 33, both mine. Overlying the coal is 3 to 10 coal also crops out around Wise in T10S, R4E. feet of moderately soft to firm dark Ridge and around the hills north and Cores and limited surface expo- gray, black or green-black, mottled, west of Stonefort. The Mt. Rorah sures indicate that the Mt. Rorah thinly laminated clay-shale, which is Coal was mined in the reclaimed Coal is separated from the Creal overlain by the Stonefort Limestone Western Mining Company strip Springs Limestone by 10 to 20 feet of Member. On the highwall of this strip mine, NE SE , Section 34, T10S, R4E medium gray, soft, smooth to silty mine two distinct shales were ob- (fig. 21). In addition, Mt. Rorah Coal shale, grading upward to rooted served above the Wise Ridge Coal. was recovered in cores of drill holes claystone. The coal generally is over- The lower unit was a soft, medium

H-l, S-l, and C-4 (plate 1). lain by dark gray to black, silt-free, gray clay-shale in lenses up to about Within the study area, the Mt. carbonaceous shale, which grades 2 feet thick directly above the coal. Rorah Coal ranges from less than a upward to gray silty shale, siltstone, Sharply overlying the lower unit was foot to about 45 inches thick, but it and sandstone. Topping the se- about 3 feet of dark gray, thinly is commonly split with shale or clay- quence is the underclay of the Wise laminated shale (fig. 21). stone partings. Good exposures of Ridge Coal. The Mt. Rorah to Wise the coal split by claystone are visible Ridge interval is 20 to 26 feet thick. Stonefort Limestone Member along the west-flowing stream just In the core of hole C-4 a dark gray to Henbest (1928) named the Stonefort east of the center of Section 29, T10S, black, highly carbonaceous shale Limestone Member; Kosanke et al. R4E, Creal Springs Quadrangle. The occurs about 6 feet below the Wise (1960) established its type section in claystone partings contain coal Ridge Coal Bed (plate 1). the same ravine (just north of Stone- stringers and range up to at least 12 fort village) that contains the type inches thick. The coal in these expo- Wise Ridge Coal Bed The Wise Mt. Rorah and Wise Ridge Coals. The sures also is penetrated by several Ridge Coal, formerly called the Stonefort Limestone, thin but wide- nearly vertical claystone dikes. Stonefort Coal, was named a spread throughout southern Illinois, Little information is available on member of the Spoon Formation is readily identifiable on geophysical mines from which the Mt. Rorah Coal by Kosanke et al. (1960) for Wise logs of oil test holes (Jacobson 1983; was extracted. The Western Mining Ridge, a hill in the northeastern part 1987) . It is probably the most widely Company pit was active during 1975 of the Creal Springs Quadrangle. Its traceable and useful subsurface and covered an area of roughly 20 type locality is the same ravine that marker unit below the Davis Coal in

39 three quadrangles mapped, and in

adja< enl quadrangles north >>i the study area, also is widely traceable in subsurface, lacobson (1987) has sub-Davis sandstone, light gray, weathers yellowish tra< eil thi' bla< k shale on geophysical gray to orange-brown, very fine to (me, slightly triable, logs through much ot southern and highly micaceous, slightly carbonaceous, much Inter- east Illinois. stitial clay. Mostly thick-bedded, locally crossbedded; central This shale is some thin-bedded portions with parallel to undulating therefore useful in both lot al and bedding planes Coal and shale rip-up clasts near base. regional correlation, lacobson (1987) Lower contact erosional noted that the shale appears to underlie the Seahorne Limestone Member ol the Spoon Formation in west central Illinois, hut the: oi tela turn has not been confirmed. We propose the name Carrier Mills shale, medium gray, silt-free to finely silly, well laminated, moderately firm, sidentic bands and nodules Shale Member lor the black sink'. softer common. Becomes darker and near base, grades I he name is taken from the town of rapidly to underlying unit Carrier Mills, located about midway Stonefort and Harrisburgin Carrier Mills Shale Member, black, smooth, hard, fis- between sile, well jointed. Large septanan limestone concretions southwestern Saline County (fig. 1). near base in places Lower contact sharp and planar I he type locality is an abandoned claystone, medium gray to olive gray. soft, not rooted railroad cut in NW NW NE, Section Zone of small, dark gray limestone nodules about 2 ft 30, T10S, R5E, Carrier Mills Quad- (0 6 m) from top Lower contact sharp rangle. The Carrier Mills Shale in this Stonefort Limestone Member, medium gray, very fine to fine, large shell fragments; shaly near top and base, locality is 2.5 to 4.0 feet thick and upper contact undulates, lower contact planar overlies soft, light gray claystone dark gray, silt-free, well laminated, lower part shale, with a sharp contact (figs. 22, 23). appears burrowed Sharp contact The black shale grades upward to 1 shale, light to medium gray, soft, silt-free, moderately to 10 feet of medium dark gray, silty, laminated, no fossils noted Sharp contact. sideritic shale, which in turn is dis- Wise Ridge Coal Bed, bright to dull-banded, shaly, conformably overlain by the sub- thinly laminated. Sharp contact. Davis sandstone. Reference sections claystone, medium gray to olive gray, soft, heavily rooted near top, lower part silty. Contact gradational. of the Carrier Mills Shale (plate 1) are sandstone, very light gray, very fine, friable, mica- contained in cores of borehole S-l argillaceous, ripply or lenticular thin to ceous, medium (depth 69.5 to 73.8 ft), hole H-l bedding Sharp contact (depth 48.0 to 51.3 ft), and hole C-4 shale, light "to medium gray, soft, weakly laminated, (depth 32.2 to 36.1 ft). i_ silt-free Poorly exposed, base covered The shale is very dark gray to black,

Figure 22 Section in abandoned railroad cut, NW NW NE, Section 30, T10S, R5E, hard, and very thinly laminated. Un- Carrier Mills Quadrangle. This is the type locality of the Carrier Mills Shale Member like any older shale in the study area, of the Spoon Formation. it splits readily into sheets that are brittle to slightly flexible. Pyrite is southern Illinois. In our study area the Stonefort Limestone and the over- common, and pyritized fossil frag- the Stonefort is found in many of the lying Carrier Mills Shale. Shales and ments can be found. Fossils include same cores and surface exposures as claystones above the Stonefort can be Lingula, Orbiculoidea, and Dunbarella. the Wise Ridge Coal (figs. 22, 23; light gray to greenish gray, some The shale weathers to a silvery plate 1). mottled with red. They are common- sheen, or occasionally to orange As observed, the Stonefort Lime ly calcareous, and nodules of argil- where pyrite is present. Because it is stone varies from a few inches to a laceous limestone may be present. A more resistant than adjacent gray little less than 2 feet thick. It is medi- thin bed of very shaly, nodular lime- shale, it generally projects slightly um to dark brownish gray, shaly, and stone was seen about 6 feet above from banks or gully walls. Float of fine grained with scattered coarse the Stonefort on the highwall of the the Carrier Mills Shale is distinctive fossil fragments and whole fossils. Western Mining Company surface in many places just below the sub- The fauna includes brachiopods, mine (fig. 21), and in the core of bore- Davis sandstone.

pelecypods, gastropods, rugose hole C-4 (plate 1) . The nodular lime- Thinly laminated, very shaly coal, corals, and crinoid fragments. The stone and claystone, in core and high- or thin streaks of coal, occur locally limestone typically forms a single wall, showed evidence of rooting. at the base of the Carrier Mills Shale. bed or two beds separated by a shale The Carrier Mills Shale is overlain by parting. In some places it is nodular. Carrier Mills Shale Member A as much as 10 feet of medium to dark The Stonefort Limestone does not distinctive hard, black, fissile shale, gray, smooth to silty, well-laminated leave a cherty residuum, as do the 2.5 to 5 feet thick, occurs 5 to 15 feet shale. In many places this shale is older Mitchellsville and Creal above the Stonefort Limestone and missing, and the sub-Davis sand- Springs Limestones. at or near the base of the sub-Davis stone lies directly on Carrier Mills About 5 to 15 feet of soft shale or sandstone, which has been mapped. Shale. claystone generally occurs between This shale, which crops out in all

40 per part of the Spoon Formation lie near the middle of the Desmoinesian Series and near the middle of the Westphalian D Stage on the basis of palynology (Peppers 1988).

Depositional environment De- position of the Spoon Formation began with a pronounced transgression, which drowned the Murray Bluff delta. The transgression pro- gressed eastward or northeastward, as shown by shaly strata that contain marine ichnofossils and body fossils, and interfinger with the upper part of the Murray Bluff Sandstone. Following this incursion, a period of regression allowed widespread coal formation. Repeated minor fluctuations in base level allowed accumulation and burial of the Old- Figure 23 Carrier Mills Shale Member (behind staff) at the type locality (same town, Delwood, and New Burnside locality shown in fig. 22). A thin layer of soft, gray shale overlies the hard, black Coals, along with several thin, Carrier Mills Shale; the sub-Davis sandstone disconformably overlies the gray shale. unnamed coals and rooted horizons. The Stonefort Limestone Member forms a broken ledge about 6 feet ( 1 . 8 m) beneath The patchy extent of coals suggests the Carrier Mills Shale and is separated from the latter by claystone . Staff is graduated in feet. that the minor fluctuations were related mainly to local causes, such Sub-Davis sandstone The young- and weakly cemented. Grain size is as structural movements or differen- est recognizable unit of the Spoon fine to medium and locally coarse; tial compaction of lenticular sedi- Formation in our study area is a sorting is poor. Lenses of conglomer- ments at depth. For example, a basin sandstone that caps many hills along ate, composed of shale, coal, and of deposition developed in the the northern edge of the study area. siderite pebbles in a matrix of sand- Eddyville Quadrangle after accumu- The base of this sandstone is a map- stone are common, especially at the lation of the Delwood Coal. This pable horizon, easily identified by base. Such conglomerates can be basin was filled successively by the presence of the Carrier Mills seen in the cores of boreholes S-l and upward-coarsening elastics, a coal

Shale just beneath (figs. 22, 23, 24). H-l (plate 1). Bedding typically is horizon or paleosol, and marine We are calling it informally the thick; crossbedding is common. limestone (Mitchellsville). A much sub-Davis sandstone, because it The lower contact of the sub-Davis thinner clastic interval, and the New underlies the Davis Coal. The sub- sandstone is sharp and erosional Burnside coal, were deposited at the

Davis sandstone commonly is 30 to everywhere it has been observed. same time in the Creal Springs Quad- 40 feet thick, and locally it reaches 60 The upper contact is gradational to rangle, where no evidence of marine feet. The sub-Davis sandstone caps the underclay of the Davis Coal. incursion exists. Wise Ridge and several other hills The erosive base and rafted coal and divides in the northeastern Creal Age of the Spoon Formation The stringers of the golden sandstone Springs Quadrangle. It also is be- Oldtown Coal, near the base of the suggest that it is a fluvial or distri- lieved to occur west of Creal Springs Spoon Formation, is of latest Atokan butary-channel deposit. village, where it is concealed by or latest Westphalian C age, on the The widely persistent, uniform glacial drift. All the hills northwest basis of palynology (Peppers 1988). layering of the upper Spoon Forma- of U.S. Rt. 45 in the Stonefort Quad- Douglass (1987) placed the Mitchells- tion reflects increasing regional sta- rangle are capped by sub-Davis sand- ville Limestone in the early Des- bility, transitional to the widespread stone. In the Eddyville Quadrangle moinesian fusulinid zone of Beedeina cyclic sedimentation of the Carbon- the sandstone was mapped along the leei. The Delwood Coal below the dale Formation. Two extensive ma- ravine southeast of Brown Brothers Mitchellsville Limestone contains rine incursions (Stonefort Limestone No. 1 Mine in NE, Section 30, T10S, spores and pollen, indicating Des- and Carrier Mills Shale) and a more R6E. The base of the sub-Davis sand- moinesian age. Apparently the localized incursion (Creal Springs stone is plotted on the Eddyville and boundaries of both the Atokan-Des- Limestone) are indicated in the Stonefort geologic maps. moinesian Series and the Westpha- upper Spoon. Lithologically the sub-Davis sand- lian C and D Stages fall between the stone resembles the golden sand- Oldtown and Delwood Coals in our Carbondale Formation stone, except that it lacks quartz study area (fig. 6). Definition The Carbondale Forma- granules. Large mica flakes and Douglass (1987) placed the Stone- tion was named for Carbondale, Illi- finely divided carbonaceous matter fort Limestone Member (as sampled nois, by Lines (1912) and Shaw and are concentrated on the bedding at its type locality) in the fusulinid Savage (1912). As originally defined, planes. The sandstone contains zone of Wedekindellina, or early-mid- the Carbondale Formation comprised much feldspar and clay; it is friable dle Desmoinesian. Coals in the up- strata from the Murphysboro Coal,

41 stream exposures. exposures along faults in mines

Figure 24 Composite section of strata exposed in and near Brown Brothers Excavating Company mines, illustrating lateral variability (Sections 19, 20, and 30, T10S, R6E, Eddyville Quadrangle). at the base, to the Herrin Coal at the which has been traced throughout Member (fig. 6). The Colchester is top. Later, geologists who extended southern Illinois and western Ken- the oldest widely mappable and min- the Carbondale Formation away from tucky and correlates with the lower able coal bed in the area of west-cen- its type area selected different boun- bench of the Seelyville Coal in west- tral Illinois where Kosanke et al. dary beds. The Carbondale Forma- central Indiana (Jacobson 1987). defined the Spoon Formation. It re- tion is currently recognized through- Moreover, the Davis Coal in south- mains to be seen whether the defin- out the Illinois Basin, but its defini- eastern Illinois marks the base of a ition of the Spoon Formation should tion varies slightly from place to succession characterized by widely change in western Illinois, or place (fig. 7). continuous coal beds, each typically whether a different classification Neither Lines nor Shaw and Sav- overlain by coarsening-upward elas- should be introduced there. age designated a type section for the tics that commence with black fissile The upper boundary of the Car- Carbondale, and suitable exposures marine shale and terminate with bondale Formation lies at least 8 probably do not exist in southern sandstone and the underclay of the miles north of the present study area, Illinois. Kosanke et al. (1960) desig- next coal. The regularity of this and is not an issue in this study. nated a series of exposures near succession contrasts with the local Canton, Illinois (more than 200 miles variability of coals and inter-coal Extent The Carbondale Formation north of Carbondale), as a principal strata below the Davis Coal. has been mapped in a downwarped reference. Therefore, we have adopted the area at the northern edge of the Within the current study area the base of the Davis Coal as the base of Eddyville Quadrangle in NE, Section Murphysboro Coal, originally de- the Carbondale Formation in our 30, T10S, R6E. Lowermost Carbon- fined as the basal member of the study. This necessitates moving the dale strata possibly occur elsewhere Carbondale Formation, is discontinu- Spoon-Carbondale Formation boun- atop hills rimmed by sub-Davis ous and of doubtful identity. The dary proposed by Kosanke et al. sandstone, but they do not crop out. oldest widely continuous and min- (1960) about 70 to 80 feet downward Carbondale Formation occurs north able coal in the area is the Davis Coal, from the base of the Colchester Coal of the study area and is known there

42 in great detail from mine exposures other marine fossils, commonly was feet of black shale, grading up to gray and coal-test borehole data. found at the base of the shale. shale or siltstone. Overlying the black shale was 20 A small area of Carbondale Forma- Thickness The maximum thick- to 25 feet of medium to dark gray, tion is mapped northwest of the No. ness of the Carbondale Formation silty shale, medium gray siltstone, 1 Mine in SW NE, Section 30, T10S, within the Eddyville Quadrangle is and light gray, shaly sandstone (fig. R6E, Eddyville Quadrangle. Identifi- approximately 225 feet, as estimated 24). The sequence was laterally and cation of these rocks is based on test from boreholes. Another 175 to 250 vertically variable. In some places it drilling by Brown Brothers and paly- feet of upper Carbondale strata has coarsened upward, but elsewhere nological analysis of coal exposed been eroded. sandstone was near the base. Cap- northwest of the fault zone on the ping the sequence was the underclay highwalloftheNo. 1 Mine (fig. 24). Lithology The Carbondale Forma- of the Dekoven Coal Member. A small area of coal believed to be tion has been removed by surface The Dekoven, 36 to 42 inches thick, the Houchin Creek Coal Member mining in the Brown Brothers No. 1 was, like the Davis, clean, bright- (formerly Summum Coal, Jacobson Mine southeast of the northeast- banded, and free of notable partings. et al. 1985) was strip-mined immedi- trending fault that runs through the The Dekoven Coal was overlain by ately north of the Eddyville Quad- center of Section 30, T10S, R6E. approximately 50 feet of gray silty rangle boundary by the Brown Broth- Geologic notes made while the mine shale, siltstone, and sandstone. Dark ers Company. The coal was about 24 was active, and on the recently closed gray to black silt-free, hard shale was to 30 inches thick, and overlain by Brown Brothers No. 2 Mine immedi- found locally immediately above the shale, then sandstone. The Survant ately to the north, indicate that the Dekoven. Fossils in the shale in- Coal, formerly Shawneetown Coal, Davis and Dekoven Coal Members cluded Lingula, Orbiculoidea, chone- (Jacobson et al. 1985), below the were mined. The Davis Coal mea- tid and productid brachiopods, and Houchin Creek, is known only from sured 54 to 57 inches thick in the No. various pelecypods, including prob- drilling records, which indicate a 1 Mine and 48 to 54 inches in the No. able Dunbarella. Elsewhere the roof thickness of about 36 inches. 2 Mine (fig. 24). The Davis was a was medium to dark gray, smooth to bright-banded, blocky coal, with no silty sideritic shale or siltstone. In the Age The portion of the Carbondale significant shale partings. The floor upper half of the 50-foot interval was Formation within the study area is in was soft, rooted claystone, and the a sandstone up to about 20 feet thick the middle to middle-upper part of immediate roof was 2 to 3 feet of (fig. 24). both the Desmoinesian Series and

hard, black, fissile shale, similar to The Colchester Coal was less than the Westphalian D stage (see fig. 6), the Carrier Mills Shale. A coarse shell 12 inches thick in the Brown Brothers on the basis of both fusulinids hash, composed of brachiopods and mines. Overlying the coal was 2 to 3 (Douglass 1987) and palynology (Peppers 1988).

SURFICIAL GEOLOGY Steven P. Esling, Leon R. Follmer, Elizabeth D. Henderson, ' s / Mary S. Lannon, and Matthew H. Riggs

The surficial deposits of the Creal PHYSIOGRAPHY 50 ft deep. Samples were generally Springs, Eddyville, and Stonefort The Creal Springs, Eddyville, and collected with a slotted tube, yielding 7.5-Minute Quadrangles were stud- Stonefort Quadrangles are in the cores approximately 7.6 or 5 centimet- ied as a part of a cooperative project Shawnee Hills Section of the Interior ers in diameter, or with a flight auger by the Department of Geology, South- Lowland Province of Illinois (Leigh- 5 centimeter in diameter. We selected ern Illinois University at Carbondale ton and others 1948). The area is 87 drilling sites on the basis of land- (SIUC), and the Illinois State Geolog- maturely dissected and is dominated scape position and accessibility and ical Survey (ISGS). The surficial de- by narrow upland ridges. The high- looked for stable positions where posits include all the relatively soft, est point in the three quadrangles complete stratigraphic sequences nonlithified sediments that cover the (approximately 840 ft above sea level) might be preserved. Paleozoic bedrock of the region. The is just south of the town of Oak, Cores were described in detail deposits formed during the Quater- along the eastern edge of the under field-moisture conditions. nary Period, the most recent part of study area; the lowest point (about Munsell color, mottles, soil structure, geologic time, including the present. 380 ft above sea level) is where the texture, presence or absence of car- The Quaternary deposits cover a Little Saline River and Pond Creek bonate minerals, manganese oxide major unconformity, a break in the leave the study area at the north and iron oxide concretions, and other geologic record that represents mil- boundary. This gives a total relief of features characteristic of a particular lions of years between the Quater- about 460 feet, and maximum local stratigraphic unit were described. nary and Paleozoic Periods. relief is about 240 feet. The study area The texture of the deposits was deter-

During the Quaternary period, contains the headwaters of the Saline mined by the U. S . Department of Ag- glaciers advanced from Canada to as River, Cache River, Bay Creek, and riculture textural classification. The far south as Creal Springs. In the Lusk Creeks. All of these streams weathering zone terminology used is study area the surficial deposits con- drain into the Ohio River; however, that of Follmer, Tandarich, and sist of loess, alluvium, colluvium, a prominent drainage divide trends Darmody (1985). Geologic samples weathered residual material derived east across the southern part of the were collected at 10- to 15-centimeter from bedrock, and minor amounts of quadrangles, separating streams intervals from the cores and saved for glacial deposits (till and related flowing northward into the Saline laboratory analysis. sediments). Surficial materials can River from those flowing southward contain natural resources, including into the Ohio River. Laboratory Methods groundwater and sand and gravel Most of the study area, except for The particle-size distribution of the aggregates. Their composition, thick- the far northwest corner of the Creal samples was determined at the SIUC ness, and physical characteristics Springs Quadrangle, lies south of the Department of Geology, using a pi- determine the suitability of a site for Illinoian glacial boundary (Willman pette method described by Graham specific land uses, such as a munici- and Frye 1980). However, north of (1985). Particle-size classes include pal landfill or industrial complex. The the prominent drainage divide the clay (less than 0.002 mm); fine silt characteristics of surficial deposits valleys show the effects of glaciation. (0.002 to 0.02 mm), coarse silt (0.02 also affect drainage, groundwater They generally are broader than val- to 0.62 mm), and sand (0.062 to 2 recharge, and the impact of certain leys south of the drainage divide, mm). environmental hazards, including and they are filled with sediment Clay mineralogy of the samples flooding and earthquakes, on a originating partly from processes was determined at SIUC by X-ray region. associated with Illinoian and Wiscon- analysis of orientated slides of the In this investigation we (1) charac- sinan glaciation. South of the divide less than 0.002-mm fraction. The clay terized the surficial materials in the valleys are generally narrow, and fraction was placed on glass slides, terms of particle-size distribution, the streams flow on rock or on thin dried, glycolated, and analyzed for clay mineralogy, and thickness; (2) alluvial deposits. peak heights of standard minerals. summarized the stratigraphy of the The clay mineral suite recognizes surficial deposits within the three METHODOLOGY peaks in the region of 17A as expand- quadrangles; (3) prepared detailed able clay minerals, 10A as illite, and stack-unit maps of the surficial Field Methods 7A as kaolinite and chlorite. Graham deposits in each of the quadrangles; Because exposed Quaternary sec- (1985) described a method, modified (Riggs in prep., Henderson in prep., tions are rare in southern Illinois, from Hallberg and others (1978b), and Lannon in prep.); (4) assessed samples of the surficial materials which is based on a routine method the resource potential of the Quater- were collected with a hydraulic soil used by the Illinois State Geological nary deposits, and (4) evaluated the probe (Giddings Machine Company). Survey to scan large numbers of suitability of the surficial materials The soil probe recovers core and samples for stratigraphic and classifi- for specific land uses. auger samples 6 to 15 meters (20 to cation purposes. This method yields useful clay mineralogy data for Table 6 Relation between modem soil series and map units of this study characterizing Quaternary sediments; however, many factors other UPLAND SOILS than clay mineralogy may affect peak Unglaciated areas Glaciated areas height, and the accuracy of the Alford (generally slopes less than 12%) Ava (generally slopes less than 12%) method is not well documented. Therefore, conclusions based on ( Irantsburg (generally slopes less than 12%) Bluford (slopes less than 4%)

I losmer (generally slopes less than 127,,) comparisons between clay mineral- (Irantsburg (generally slopes less ogy data from this report and clay Robbs than 12%) mineralogy data determined by simi- Stoy Robbs lar methods on different instruments should be used with caution. SIDESLOPES Unglaciated areas Glaciated areas Construction of the Stack-Unit Map Alton.) (generally slopes more than 12%) Ava (generally slopes more than 12%) Alford- Baxter Complex (generally slopes Grantsburg (generally slopes more The distribution ot surficial deposits more than 12%) than 12%) (lithostratigraphic units) is a function Beasley Hickory of the depositional conditions and Bedford Hickory-Ava Complex the postdepositional erosional his- Berks Wellston tory of each unit. These two factors have caused complex relationships Creal Zanesville (generally slopes among the stratigraphu units in the Grantsburg more study area. A stack-unit map (Kemp- than 12%) ton 1981) illustrates the areal and Hosmer (generally slopes more than 12%) vertical distribution ot geologic Muskingum materials to a given depth below the Wellston surface. A generalized stack-unit Wellston-Berks Complex map was prepared by combining in- Wellston-Muskin Complex formation obtained from 87 borings Zanesville made in the area, field observations, and hand augering. Principal sources LOWLANDS ROCK OUTCROPS of additional information were the Banlic Burnside Sandstone Rock Land county soil survey reports (Miles and Belknap Creal Wellston-Berks complex Weiss 1978, Parks 1975, Fehrenbacher Bonnie Sharon 1964, Fehrenbacher and Odell 1959) and well logs on file at the Illinois State Geological Survey. Soil reports provided information on the distribu- and (2) in geologic mapping, data chronostratigraphic (time relation- tion and nature of the near-surface from deep borings must be integrat- ships), (2) lithostratigraphic (litho- materials. Maps included in the ed with near-surface data. In gen- Iogic or compositional relationships), county soil reports show the distribu- eral, geologic material more than 5 and (3) pedostratigraphic (soil devel- tion of particular soil series in the feet below ground surface has little opment history or relationships of study area and are useful in distin- effect on the type of soil series at a pedogenic attributes). guishing major landscape and geo- site. Most of the stratigraphic units in logic boundaries. The surficial litho- A detailed srack unit map for each the area correlate with units de- stratigraphic units were interpreted quadrangle was prepared at a scale scribed by Willman and Frye (1970) from the soil map units (table 6). of 1:24,000 (Henderson in prep, and Lineback (1979). One new infor- The preparation of a stack-unit Lannon in prep, Riggs in prep). mal lithostratigraphic unit, the Oak map requires some subjective deci- These maps are useful for general formation, is proposed; this forma- sions: in many cases, map bound- planning purposes, but do not tion is a widespread weathered aries cannot be drawn with certainty provide sufficient information for material (principally residuum) that because of insufficient data. The site-specific interpretations. These directly overlies the bedrock in the vertical sequence of deposits from a three maps will be placed in the ISGS region. Because many of the charac- borehole is first related to the soil Open File Series when they are teristics of the Oak formation are series and landscape position; topo- completed. pedogenic in origin, this formation graphic features are then used as a presents a classification problem; guide to drawing map-unit bound- STRATIGRAPHY however, it has lithologic properties aries. A boundary between geologic Stratigraphic studies facilitate under- on which to base correlations and units can cross a soil-map boundary standing of the origin of the units occupies a consistent stratigraphic for two reasons: (1) the soils maps and provide a framework for correlat- position throughout the region. and the 7.5-minute topographic base ing and predicting their character The distribution of lithostrati- of the stack-unit maps are at different and occurrence. The relationships of graphic units in the study area is scales, and the topographic base the surficial deposits of the Creal controlled to a large extent by geo- does not show the subtle changes in Springs, Eddyville, and Stonefort morphic processes of erosion and slope identified on the soils maps; Quadrangles can be classified as (1) eolian deposition; this explains the

46 CHRONOSTRATIGRAPHY LITHOSTRATIGRAPHY PEDOSTRATIGRAPHY

Holocene Stage Modern Soil

Valderan/Greatlakean Peyton Fm Cahokia Fm en Substage LU CO Wh- Twocreekan Substage > q3 c CO W > c Woodfordian Substage Peoria Silt Equality Fm (Mbr B) DC C o < (D O Farmdalian Substage Farmdale Soil o cc 1 LU '53 Altonian Substage Roxana Silt Equality Fm (Mbr A) D!c 0. o Sangamonian Stage Sangamon Soil

lllinoian Stage Glasford Fm Teneriffe Silt Loveland Silt

Pre-lilinoian Oak fm Yarmouth Soil

Figure 25 Stratigraphic classification of Quaternary deposits in the study area. Chronostratigraphic names are commonly used for the deposits (substage) that formed during an interval of time (subage).

•25 6 f 22 23,22 24 25 in lithostratigraphic classification. 2*—f fig. 28 •27 3# 21*^16 Because a residuum has attributes of • 28 fig. 27 both a soil and a lithologic (material) 21.23.24 ^ig. 36 20—26 26t unit, it has often been excluded from 14 lithostratigraphic classification. The Oak formation in the study area is lat-

erally continuous and it has lithologic properties distinctly different from those of the underlying indurated • 8 bedrock. The term residuum is restricted in this discussion to material formed in situ on a bedrock substrate. CREAL SPRINGS STONEFORT EDDYVILLE The term formation may include in situ and redeposited material. Figure 26 Vertical distribution of clay minerals and particle sizes in boring ED8, The Oak formation is named for and general locations of borings mentioned in this chapter. the town of Oak in Pope County, near the eastern boundary of the Eddy- distinction between the sequence of underlies some valley deposits. The ville Quadrangle. A boring (ED8 in surficial deposits constituting the Oak formation is weathered material; the Eddyville Quadrangle) that present upland and the sequence in most of it is the product of in situ contains a typical example of the Oak lowland positions. weathering, but it includes redepos- formation serves as a reference sec- ited, stratified material in places. All tion. In this section the Roxana Silt Lithostratigraphic Units: other Quaternary units overlie it (fig. overlies the Oak formation, which Upland Formations 25). We propose that the informal rests on bedrock. Figure 26 sum- Oak formation This formation is name, Oak formation, be used to re- marizes laboratory data for ED8, and dominated by fine-grained material place a variety of common names appendix A (page 59) describes the with a soil fabric (peds or natural (i.e., residual material, weathered ED8 section. General locations of aggregates and biological pores); it bedrock, paleosol, geest, clay, and borings discussed in this chapter are overlies bedrock on stable upland pedisediment), and that the Oak for- shown in figure 26; precise locations and some hillslope surfaces and mation be recognized as a minor unit are listed in table 7.

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[lj] Mldep T&ble 7 Location oi borings The texture (particle-size distribu- added and weathered. The residual tion) refle< is the composition ol the material on bedrock probably de-

Elev. underlying bedrock, ranging from velops in episodes; it could be eroded Boring Location (ft) loam and sandv loam to sandy clay during periods of landscape instabil-

loam where it overlies sandstone/ ity and could form again during silt Creal Springs Quadrangle and from loam and i lav loam to periods of stability. We have not

i lay where it overlies shale. The high determined when Oak development CS20 SWNESE 2-11S-3E 185 concentrations of clay and sand show began. It could have started when CS21 NWNWSE 2-11S-3E 495 the effect of pedologu alteration and the Pennsylvanian rocks were first CS23 SENESE 2-11S-3E 485 the predominance oi sandstone lith- exposed to weathering more than 200

CS24 NWNWSE 1-11S |] 510 ologies "i the bedrock in the study million years ago, but we have no

area [Tie sand and pebble content it is older late CS25 NWNWSW ! 10S 11 590 evidence that than generally increase with depth, rhe Tertiary (several million years old). CS26 SWNESW l lis }] 525 unit is leached oi carbonates in all Landscape evolution models sug- CS27 SWNENW 34-10S-3E 61 i luit one observed location in a valley. gest that in regions having appreci- CS28 NWSWSE M ins »] 545 In most cases the unit is oxidized, able relief, erosion would remove or and reddish brown, brovy n. and \s chlorite clay minerals, reflecting the are recognized as remnants of laterite clay mineralogy of the parent rock. weathering. Lateritic iron ore or ED24 SWSENW 29-10S-6E 390 At some locations the percentage of bauxite occurs at the top of deep ED25 NWSWNW 28-10S-6E 370 expandable clay minerals is high near weathering profiles where erosion the top of the unit, indicating possi- has not occurred. Rare observations Stonefort Quadrangle ble mixing with the overlying Roxana of lateritic material have been noted 25-10S-4E SF2 SESWSE 150 Silt. In other regions the residuum in Illinois, Indiana, Arkansas, and a SF3 SWSENE 6-10S4E 490 on carbonate rocks is rich in expand- few places in the western part of the SF6 SWSENE 25-10S-4E 570 able (smectitic) clays, such as the United States and in Canada. No la- geest in northwestern Illinois de- teritic materials have been found in SF7 NESENE 1-11S-5E 620 scribed by Willman et al. (1989). the study area. SF1 NWNWNW 9-11S-5E 400 The Sugar Creek and Pond Creek The Oak formation is not weath- SF1 SESESW 31-11S-5E 480 transects, summarized in figures 27 ered to the degree of a laterite. It SF1 SENESW 31-10S-5E 442 and 28, show the physical relation- contains a mixed clay-mineral as- SF21 NENWSW 31-10S-5E 405 ship between the Oak formation and semblage that includes expandable valley and clay. evolution SF22 SESESW 30-10S-5E 393 the other upland Quater- The landscape models nary-age units in the study area. The and the degree of weathering in the SF26 NWSESE 5-11S-5E 405 Oak formation is not shown in the Oak suggest that most of the forma- cross sections of valleys because of tion is of Quaternary age. Most of The Oak formation is generally scale limitations and lack of data. A the Oak appears to be about 300,000 continuous on uplands of low relief. type of material included in the Oak to 2 million years old, on the basis

On valley slopes it is discontinuous formation found in valley positions of its stratigraphic occurrence below and occasionally exposed; it may is the unoxidized and unleached correlated Illinoian units (Loveland occur under alluvium in valleys. The sediment overlying bedrock in the Silt, Glasford Formation, and Oak formation is uncemented and Maple Branch of Sugar Creek Valley Teneriffe Silt). Although the Oak softer than the underlying bedrock. (fig. 29). directly underlies the Wisconsinan

The lower boundary, gradational in Figures 30, 31, and 32 summarize deposits in many places, it often most cases, is defined by a distinct the vertical trends in particle size and appears to be an erosional remnant change in consistence or an increase clay mineralogy of borings SF3, of older, weathered material. The in hardness. The upper contact is an CS25, and CS27. These borings serve residuum would thicken between unconformity that ranges from as additional reference sections for times of erosion, and the actual time abrupt to gradational into the overly- the Oak formation. of formation is not a critical factor for ing younger units that commonly Interpreting the age of a litho- mapping its distribution. contrast in color, fabric, and texture. stratigraphic unit that accumulated The Oak formation usually shows On the uplands in the study area the primarily from weathering processes pronounced pedologic features, in- Oak formation is overlain by the presents a unique classification cluding well-developed soil fabric Loveland Silt, the Glasford Forma- problem. As the weathering front (structure) and clay films on ped faces tion, or the Roxana Silt. In the progresses and the contact between (coatings on aggregates), the evi- valleys, it is overlain by the Cahokia the lithified and nonlithified units dence for interpreting an old soil or Formation, the Equality Formation, moves downwards, the residuum paleosol. Where overlain by the or the Teneriffe Silt. becomes thicker. Therefore, the Roxana Silt, this paleosol is corre- The Oak formation is 0.66 meters softened part of the bedrock becomes lated with the Sangamon Soil; where thick at the reference section (appen- residuum. In addition, when the overlain by the Loveland Silt, the dix A) and ranges from 0.3 to 2.7 residuum is at ground surface, it can paleosol is correlated with the Yar- meters thick across the study area. thicken upward as new deposits are mouth Soil. Although the paleosol in

50 SECTION: CS20 CLAY MINERALOGY (%) PARTICLE SIZE (%) 2,0 40 60 80 DEPTr 20 40 60 80 UNIT [SOIL] HORIZON . Cahokia [Modern} A; Bw ^ — M

r ? y* coarse > ^ l silt *•>» Bt expand^

Teneriffe B [Sangamon] Btb 4. CBg^ -T -p *=^- p CB p clay a jt 9 Teneriffe A «T kaolinite ' ^* and Ku ~==^=d chlorite P p \ * ^x^ L illite > 3 > J J XT Si r i p / | Silt \ J E^ <0 Sand 1 °> < \ I p 7 ^ > «u p fa { < - 10 - "? ^ %, / J > > V, Jd > 40,800 RCYBP — p .

13 ~"*™ Oak CD** eT ^^"* o

Figure 29 Vertical distribution of clay minerals and particle sizes in boring CS20 (for location see fig. 26).

the Oak formation represents a major zon. The Loveland Silt was not found examined, it is weathered. In the de- unconformity (a long period of ero- on the narrow upland divides in the scribed geologic sections the Love- sion and weathering) between the study area, but was observed on a land Silt ranges from 0.5 to 1.25 Pennsylvanian and Quaternary Per- lower, distinct, gently sloping up- meters thick and commonly is red- iods, the boundaries between units land surface along the Pond Creek dish brown to yellowish brown. are gradational because of continu- valley in the upper reaches of the The Loveland Silt probably man- ing soil-forming processes over time. Saline River basin. Apparently the tled the upland in the study area at

upland divides were too narrow to one time, but it has been largely re- Loveland Silt Willman and Frye be stable, and erosion occurring after moved by erosion, remaining as a (1970) applied the term Loveland Silt deposition of the Loveland Silt re- deposit of colluvium and loess only to the undifferentiated silt deposits moved most of the deposit. Detailed on protected, stable landscape posi- of Illinoian age that occur south of logs of borings SF2 and SF16 (fig. 28) tions. Weathered Loveland Silt and the Illinoian glacial limit. The Love- show the Loveland Silt on the land- Roxana Silt are similar in appearance land Silt is primarily loess. It overlies scape positions adjacent to Pond and composition and and can be the Oak formation and is buried by Creek. Although the lower upland easily differentiated only when the the Roxana Silt. Sangamon Soil deposition is broader than the divides, Sangamon Soil is recognized in the velopment has altered the entire the Loveland Silt was encountered in Loveland Silt. unit, creating blocky structure and only three of the eight borings drilled The texture of the weathered Love- biological pores typical of a B hori- at this position. At all locations land Silt ranges from a silt loam to

51 SECTION CS25 CLAY MINERALOGY (%) PARTICLE SIZE (%) UNIT [SOIL] HORIZON 20 40 60 80 DEPTH 20 40 60 80 "" 1 ' A Bw cf illite ^* M Peoria [Modern] Bt expandables ^ \ /coarse Roxana [Farmdale] AEb

Figure 31 Vertical distribi and particle sizes in boring CS25 (tor loca

SECTION: CS27 CLAY MINERALOGY (%) PARTICLE SIZE (%) UNIT [SOIL] 20 40 60 80 DEPTH 20 40 60

Peoria [Modern]

Roxana [Farmdale]

Glasford [Sangamon]

Oak [Yarmouth]

Figure 32 Vertical distribution of clay minerals and particle sizes in boring CS27 (for location, see fig. 26).

silty clay loam, and its clay content southern boundary marks the south- undifferentiated Glasford Formation increases somewhat with depth ernmost extent of continental glacia- and reserve the correlation question within the Bt (clay-enriched) horizon tion in North America (William and for further investigation. of the Sangamon Soil. The sand con- Frye, 1980). In the study area the In the study area the diamicton tent also increases with depth as a Glasford Formation is found only in appears to have a patchy distribu- result of mixing with the underlying the extreme northeast corner of the tion. Only two of the four borings Oak formation. The Loveland Silt in Creal Springs Quadrangle. Where north of the glacial boundary encoun- the study area contains high percen- present, it overlies the Oak formation tered the unit. The deposit is highly tages of kaolinite plus chlorite clay and is buried by the Roxana Silt. The weathered and thin, and in both de- minerals. Figure 30 summarizes the development of the Sangamon Soil scribed sections the unit is oxidized vertical distribution of clay minerals has altered all of the Glasford Forma- to a brown or yellowish brown and and particle size of a typical Loveland tion in upland positions; glacial de- leached of carbonates. In boring

Silt section (SF3) in the study area. posits may fill bedrock valleys, and CS27 (fig. 32), the Glasford Forma- unweathered diamicton might be tion is 3.4 meters thick. The base of Glasford Formation The Glasford found in these valleys. the Glasford Formation was not en- Formation mainly consists of Illi- The map compiled by Lineback countered in boring CS28, from noian-age diamicton (a mixture of (1979) shows the Vandalia Member, which 3.3 meters of diamicton was clay silt, sand, and pebbles). Diamic- a middle member of the Glasford recovered. ton that is dense and has uniform Formation, covering the study area. The Glasford Formation in the

characteristics is interpreted as till, a Willman and Frye (1970) interpreted study area generally has a silt-loam sediment directly deposited from a the southern limit of the Glasford as texture but ranges to silty clay loam glacier. Other types of diamicton in- forming during the oldest part of the and loam. Erratic igneous and meta- clude deposits that have been locally Illinoian. The limited information morphic pebbles are rare, and the redeposited by water action or mass acquired in this study has not re- coarser clasts are mainly sandstone, wasting. The Glasford Formation is solved this correlation question. coal, and chert derived from the local the most extensive Quaternary litho- Therefore, we classify all observed bedrock. Typically the Glasford stratigraphic unit in Illinois, and its glacial deposits in the study area as Formation contains high percentages

52 of kaolinite plus chlorite and illite, a pedologic alteration from modern Peyton Formation The Peyton characteristic expected of glacial soil development. Expandable clay Formation includes all sediment de- deposits from a northeastern source minerals dominate the clay fraction posited by mass wasting and collu- that have been mixed with local near the top of the Roxana and gradu- vium at the base of slopes that has material. Figure 32 summarizes the ally diminish with depth as the accumulated from the end of the vertical distribution of clay minerals kaolinite plus chlorite fraction in- Wisconsinan to the present. The and particle size for a Glasford creases. This vertical trend may Peyton consists of reworked loess, Formation section (CS27) in the study indicate a change in source area as residuum, and clasts of bedrock. The area. well as mixing of the Roxana Silt and unit, generally thin, is commonly

Basal till throughout the midwest the underlying Oak formation. Frye associated with bedrock outcrops. generally has a uniform matrix. and others (1962) attributed the high The Peyton generally is yellowish However, the diamicton in the study percentage of expandable clay miner- brown to brown and is leached of area at borings CS27 and CS28 does als to a northwest source area. Fig- carbonate minerals in the study area. not have uniform clay mineralogy or ures 26, 30, 31, and 32 summarize The Peyton colluvial material on texture either laterally or with depth, typical vertical trends in particle-size slopes grades into alluvium that is suggesting that these sections may distribution and clay mineralogy of stratified and better sorted in the have originated from superglacial the Roxana Silt in the study area. valley bottoms. An arbitrary vertical mass movement. Willman and Frye line separates deposits that origi- (1980) described an exposure in the Peoria Silt The Peoria Silt, also nated mostly from fluvial processes study area (near the Illinoian glacial called Peoria Loess, was deposited (the Cahokia Formation) from those boundary) that contains large blocks during the Woodfordian Subage of derived mainly from colluvial proces- of diamicton interstratified with the Wisconsinan Stage by aeolian ses (the Peyton Formation.) The fluvial sand and silt deposits and is processes (McKay 1979); it is the Sugar Creek and Pond Creek trans- clearly of superglacial origin. surficial deposit on the upland of the ects (fig. 27, 28) show the physical study area, overlying the Roxana Silt relationship between the Peyton For-

i Silt The Roxana Silt, in most places. The Peoria Silt is mation, the loess units, and the mainly the result of loess deposition thinner in the study area (0.5 to valley deposits in the study area. during late Altonian time of the 1.3 m) than in locations near major Lithostratigraphic Units: Wisconsinan, originally covered the rivers, where it can be more than 6 landscape. In the study area the meters thick. It is typically altered to Valley Formations Roxana is generally a continuous unit yellowish brown and is lighter in Teneriffe Silt The Teneriffe Silt is that overlies the Oak formation or color than the Roxana. Its physical a term applied in the study area to a the Glasford Formation in stable appearance is dominated by soil laterally continuous, stratified de- upland locations and unweathered characteristics (humic enrichment, posit in the Sugar Creek valley in the bedrock in the more sloping upland soil structure, and biological fea- northwest part of the Creal Springs locations. On a broad lower upland tures) and it is leached of carbonate Quadrangle, just south of the Il- along Pond Creek (fig. 28) the Roxana minerals in all locations examined. linoian Glacial boundary. The de- overlies the Loveland Silt. In some Like the Roxana Silt, the Peoria Silt posit is correlated with the Teneriffe places the Loveland cannot be easily is characterized by consistent vertical Silt on the basis of the presence of differentiated from the Roxana. trends in clay mineralogy and parti- Sangamon Soil in the upper part of Where the distinction is clear, the cle-size distribution. These vertical the unit and its facies relationship Roxana has better developed platy trends show the effect of modern with the adjacent Glasford Forma- structure and is not as red as the pedogenesis; most profiles show a tion. The Illinoian-age Teneriffe Silt Loveland. The Roxana Silt is buried distinct Bt (clay-enriched) horizon of overlies either bedrock or Oak forma- throughout the study area by the a forest-type soil (Alfisol). The Peoria tion and is buried by the Cahokia Peoria Silt. The Farmdale Soil de- Silt contains more silt and less sand Formation (fig. 27). veloped in the Roxana Silt, producing than does the underlying Roxana Silt; No natural exposures of the Tene- the pedologic features (platy and its texture ranges from silty clay loam riffe Silt exist in the study area. granular peds and biological pores) to silt loam. Near ground surface, the Sufficient evidence was found in four that distinguish it from the overlying Peoria contains more illite than ex- borings to subdivide the formation Peoria Silt. The Roxana Silt is thin pandable clay minerals. With depth into two informal members. The (0.3 to 1.8 m) in the study area. In all the percentage of expandable clay lower part of the Teneriffe (member locations observed it is yellowish minerals increases, and kaolinite A) is a poorly stratified silt, typically brown to dark yellowish brown and plus chlorite generally decreases. characterized by a silty clay texture, leached of carbonate minerals. The This vertical trend is probably a although silt loam, silty clay loam, Roxana commonly has a redder hue function of three factors: pedogen- sandy clay loam, sandy loam, loam, than the Peoria Silt. esis, provenance change, and mixing and clay textures are also present. The Roxana Silt generally is a silt with the Roxana Silt. The trends in The upper part of the Teneriffe Silt loam. It contains more sand than the clay mineralogy are typical for the (member B) is characterized by a high overlying Peoria Silt, and its sand southern Illinois region (Graham percentage of sand in silt loam, loam, content generally increases with 1985, Hughes 1987). Figures 26, 30, sandy loam, or clay loam textures. depth, suggesting that it has been 31, and 32 graphically summarize the Member B is brown to yellowish mixed with a more sandy substrate. vertical distribution of clay minerals brown and is leached of carbonates. The clay content decreases with and particle size of typical Peoria Silt Member A may be yellowish brown depth, probably as a function of profiles in the study area. and brown near its top, but becomes

53 bluish gray, greenish gray, or gray, the high percentage of silt and clay) lacustrine deposits. Proper charac- and calcareous with depth. Pedologic suggest that the Teneriffe Silt ac- ter!/, itmn ol thi' important v.iriations development has altered allot mem cumulated in an ice-marginal Q- in these deposits will require further Ihm B and the upper pari ol member linoian lake. Willman and Frye (1980) investigation. \ [he resulting soil, interpreted to discussed the origin oi this ice-margi-

be the Sangamon Soil, formed in the nal lake, which they named I ake Equality Formation Willman and

Teneriffeand is more than J. {meters Sugar, and presented geomorphic Frye (1970) interpreted the Equality thick in one hining (CS24). It has a evidence suggesting that the Il- Formation as Woodfordian agelai as distinct Bt (clay-enriched) horizon, linoian glacier blocked the Sugar trine deposits associated with Wis-

suggesting cumuli< developmenl Creek Valley just to the east ,,'t the consinan glaciation. The type section

overan extended period ol time. 1 hi- townot (.real Springs. Theelevation for this unit occurs in the Saline River high percentage ol fine particle sizes at the top ol the reneriffe Silt in the valley, just to the northeast ol the in member A (clay content up to 66% Maple Branch of Sugar Creek valley study area. The Equality Formation in some beds) suggests that the fene- is below 500 feet. Willman and Frye in the study area is described in two riffe Silt accumulated in a low-en- (1980) believed that the bedrock sur- borings in the Battle Ford Creek ergy, quiet-water environment. In face oi an outlet to Lake Sugar at <\n valley, two borings in the Little Saline

the two borings that penetrated the elevation oi about 520 feet i ontrolled River valley, one boring in the Pond Teneriffe, the unit is 6.9 and 10 meters the maximum elevation of the lake. Creek valley, and one boring in the thick. A silt loam deposit correlated with Grassy Creek valley. Shaw (1915),

The clay mineralogy of the I'ene- the ( ahokia Formation overlies the Frye and others (1972), and Heinrich

riffe in lour borings reveals no consis- reneriffe Silt. I he surfat e oi the ( 1982) developed a conceptual model tent patterns that characterize the reneriffe Silt is an unconformity, for deposition of the Equality Forma- unit. In general, the leneriffe Silt in spanning Sangamonian through tion in the Saline River drainage

the study area contains mainlj illite earlv Wisconsinan time. The Roxana basin. During the Altonian and and kaolinite plus chlorite. The as- and Peoria Silts would have been Woodfordian Subagesof the Wiscon- semblage of clay minerals can be deposited over the reneriffe; how- sinan, the Ohio River carried glacial explained by a mixing ol materials ever, more information is needed to outwash and aggraded faster than its from two principal source areas: adja- distinguish these silt deposits. Sub- tributary valleys having drainage cent diamicton from the Illinoian sequent Wisconsinan and Holocene basins south of the glacial border.

glacier, and older materials I roni the fluvial erosion and deposition has I ligh water levels and sediment watershed of Sugar Creek. Borings made differentiation of the Cahokia dams formed at the mouth of the near tributary streams draining the Formation from the Roxana or Peoria Saline River, impounding water area where the Glasford Formation Silts problematic in the four de- within the drainage basin. Sediment

is present contain high percentages S< i ibid sections containing the carried by flood waters from the Ohio of illite, whereas those located near Teneriffe Silt. River or by streams originating on streams that drain the Oak formation Correlation of this Illinoian silt the adjacent uplands accumulated in have high percentages of kaolinite with the Teneriffe Silt is based on a the lake. In the study area the Equal- plus chlorite. Materials containing precedent established by Lineback ity Formation is mostly a silt loam,

high percentages of kaolinite plus (1979). He applied the term Teneriffe but it may have silty clay loam, sandy chlorite have a high sand content. Silt to silts, clayey silts, sands, and loam, or loam textures. The unit, The Oak formation also contains a clays deposited in basins marginal to almost always unoxidized, can be high percentage of sand and kaoli- the Illinoian glaciers. The Teneriffe gray, dark gray, greenish gray, or dark nite plus chlorite. In three of the four Silt, as mapped by Lineback (1979), greenish gray. The Equality Forma- borings, the percentage of expand- is recognized beyond the margin and tion (except for beds near the top of able clay minerals is greatest near the on top of the Glasford Formation. In the unit within the Battle Ford Creek top of the Teneriffe Silt. Figures 29 its statewide use, the Teneriffe Silt valley) is generally leached of and 33 summarize the vertical dis- may include eolian, glaciofluvial, carbonates. tribution of clay minerals and particle glaciolacustrine, or mass wasted The distribution of clay minerals size in two Teneriffe Silt sections. deposits. Heinrich (1982) applied the within the Equality Formation ap- Three criteria suggest that the unit name Teneriffe Silt to Illinoian-age pears to be a function of location in described in the Sugar Creek valley lacustrine deposits within the Saline the Saline River drainage basin. correlates with the Teneriffe Silt: the River valley just to the northeast of Heinrich (1982) found a high percen- Sangamon-class paleosol in the up- the study area. tage of illite in the Equality Formation per part of the unit; the high percen- It is important to recognize that in the Saline River valley northeast tage of illite (a characteristic of Lineback's definition of the Teneriffe of the study area. These deposits ori- Illinoian-age glacial deposits in the Silt differs from the original defini- ginated partly from the illite-rich region); and a radiocarbon date from tion. Willman and Frye (1970) exclud- sediment eroded from the Glasford a conifer sample found at a depth be- ed the Teneriffe Silt from areas Formation or carried in suspension

tween 1 1 . 91 to 1 1 . 98 meters in boring beyond the Illinoian glacial boun- into the Saline River valley by floods CS20 (figs. 27, 29). This wood sample dary, preferring to draw a vertical on the Ohio River. The deposits in was dated at >40,800 yr BP (ISGS cutoff between the Loveland and the Battle Ford Creek valley, in the 1476). Three factors (the confinement Teneriffe Silts. They interpreted the upper reaches of the Saline River of the deposit within the Sugar Creek Teneriffe Silt to include ourwash, drainage basin, contain high percen- valley in the study area, the proxim- sheetwash, and some eolian depos- tages of kaolinite plus chlorite, re- ity of the Glasford Formation, and its, without mentioning ice-marginal flecting a local bedrock provenance.

54 SECTION CS24 CLAY MINERALOGY (%) PARTICLE SIZE (%) UNIT [SOIL] HORIZON 20 40 60 80 DEPTH 20 40 60 80

Cahokia [Modern]

Teneriffe B [Sangamon] Btb BC

Teneriffe A [Sangamon] BC CB^=

Figure 33 Vertical distribution of clay minerals and particle sizes in boring CS24 (for location, see fig. 26).

In the Grassy Creek, Pond Creek, below 350 feet to a minimum eleva- Willman and Frye (1970) separated and Little Saline River valleys, the tion of 329 feet, but data from this the Equality Formation into the Equality Formation contains a high core are largely inconclusive. The Carmi Member and Dolton Member. percentage of expandable clay miner- Pond Creek and Little Saline River By this classification the deposits in als, suggesting that the sediment was transects (figs. 28, 36) show the the study area correlate with the partly derived from the Roxana Silt distribution of both the Texas City Carmi Member, which includes the that mantled the uplands during the and Cottage members, but the con- predominantly fine-textured de- early Woodfordian. Figures 34 and 35 tact between the members is hypo- posits that accumulated in low- summarize the vertical distribution thetical (the contact is placed at energy environments. The coarser of clay minerals and particle size of Heinrich's (1982) approximate maxi- end of the spectrum is assigned to borings within the Little Saline River mum elevation for the Altonian la- the Dolton Member, typically sandy, Valley. The upper part of the Equality custrine episode. In boring SF26 the which represents higher-energy Formation in this valley is charac- contact between the Cahokia and environments such as beaches. terized by a high percentage of sand. Equality Formations is at an elevation In the study area, no evidence for Heinrich (1982) subdivided the of about 387 feet, which suggests a a paleosol was found in the upper Equality Formation into two informal lake level during the Woodfordian part of the Equality Formation be- members, the Altonian Subage Cot- greater than Heinrich's (1982) esti- neath its contact with the overlying tage member and the Woodfordian mate of 380 feet. The elevation of this Cahokia Formation. A paleosol was Subage Texas City member, which he contact supports the estimate by Frye described below this contact at other differentiated by stratigraphic posi- and others (1972) of about 400 feet locations in southern Illinois tion and composition. He deter- for the maximum level of the lake (Graham 1985; Oliver 1988), suggest- mined that during the Altonian the during the Woodfordian. The Maple ing that in the study area erosion has

Cottage member accumulated in a Branch portion of the Sugar Creek removed it. In boring SF14 (fig. 34) lake (impounded in the Saline River valley in the Creal Springs Quad- and SF26 (fig. 35) the contact be- valley), which reached a maximum rangle does not contain deposits tween the Cahokia and Equality For- elevation of about 350 feet. He belonging to the Equality Formation. mations is placed at a distinct change suggested that the maximum eleva- The contact between the bedrock and in texture. In boring SF14, the contact tion of the lake during the Wood- the valley fill in this valley is probably is placed at the base of a fining-up- fordian was about 380 feet. Deposits at an elevation above the maximum ward sequence. In boring SF26, the of the Equality Formation described lake levels reached during the Wis- contact is placed at the upper contact from borings in the present study consinan. Because only a few borings of a prominent sandy loam unit. In probably correlate with the Texas in the quadrangles encountered the two of the borings in the Battle Ford City member, because deposits of the Equality Formation, no evidence was Creek valley (ED24 and ED25), the Cottage member would not be found found for subunits that could corre- boundary between the Cahokia and in tributary valleys of the Saline River late with the textural and mineralogic Equality Formations is problematic. above an elevation of 350 feet. Only subunits described by Heinrich In boring ED25, the contact is placed one of the borings (ED25) penetrated (1982). at a depth of 8. 4 meters, where both

55 Figure 34 Vertical distribution of clay minerals and particle sizes in boring SF14 (for location, see fig. 26).

SECTION SF26 CLAY MINERALOGY (%) PARTICLE SIZE (%) UNIT [SOIL] 20 40 60 80 20 40 60 80

Cahokia [Modern]

kaolinite and chlorite

CBg

Equality

expandablesj

CBg f

-£-

Figure 35 Vertical distribution of clay minerals and particle sizes in boring SF26 (for location, see fig. 26). : :

the clay content and illite content increase. Organic material retrieved at the base of ED24 is dated at >21,000 yr BP (ISGS 1456). Frye and others (1972) and Heinrich (1982) 500- believed that water was impounded along the Saline River valley during ir f the Woodfordian. Thus, some of the 450- Peyton Formation .<= / material above the base of boring CO / ED24, which has a basal elevation of \S Cahokia Formation SF26 \ about 356 feet, may belong to the SFl4lV

Equality Formation. A tentative IL_ . -V boundary is placed at a depth of 5.4 meters. Below this depth the laminated, calcareous sediment contains 350- x"-V- more clay size material and illite. Equality Formation Xij : • (Texas City Member) \: • Cahokia Formation Willman and 300- interpreted the Cahokia Frye (1970) 500 1000 ft Equality Formation as Holocene-age alluvial Formation (Cottage Member?) 150 300 m deposits. The unit is the surface deposit in all the valleys of the study area except the narrow tributary val- A,AB " C A, Bw Bw c leys in which streams flow on rock. ABb c Bt c Pedologic features, including soil BC c Btb c fabric and evidence of translocated clay, extend throughout the entire CB c CBs thickness of this unit; these features Btb c Btb • CB c are characteristic of a cumulic soil. c: Cahokia Fm CBg c The texture of the Cahokia indicates e: Equality Fm CBg c 0: Oak fm that it originated from the loess or redeposited loess. The Cahokia For- mation may overlie the Oak forma- CBg e tion, the Equality Formation, or the Teneriffe Silt. The thickness of the CBg e Cahokia Formation is highly variable, ranging from to 8.4 meters. CB -0 Most borings terminated before the SF26 base of the unit was penetrated. The SF14 variable thickness of the Cahokia Formation is evidence for cycles of aggradation and degradation in the Figure 36 Cross section showing the distribution of Quaternary units in the Little tributary valleys of the study area Saline River valley (Stonefort 7.5-minute Quadrangle) (for location, see fig. 26). during the Holocene. The Sugar Creek, Pond Creek, and Little Saline River transects (figs. 27, 28, 36) show the Cahokia Formation generally trends with increasing depth. Fig- the physical relationship between the contains a high percentage of kaolin- ures 29, 33, 34, and 35 graphically Cahokia Formation and the other up- ite plus chlorite and illite, in roughly summarize the vertical distribution land and valley stratigraphic units. equal amounts. With few exceptions, of clay minerals and particle size for Near the surface the Cahokia For- expandable clay minerals constitute typical sections in the study area. mation is generally oxidized to vari- less than 20 percent of the total clay Wood recovered at a depth of 5 ous shades of brown and yellowish mineral content; this suggests that meters from boring ED25 was dated brown that grade into unoxidized the Peoria loess provided most of the at 5,500 ± 80 yr BP (ISGS 1457). gray and bluish grays with depth. sediment, but the distribution of clay Pedostratigraphic Units The unit is leached of carbonates in minerals was probably a function of all described geologic sections. The the clay mineralogy of the exposed Yarmouth Soil In the study area, Cahokia Formation is silty; its tex- upland units within a local drainage the Yarmouth Soil developed in the tures are similar to its source mate- basin. The Cahokia Formation does Oak formation and is overlain by the rials, the upland loess deposits and not have distinct vertical trends in Glasford Formation or the Loveland residuum. In general, the unit has a either particle-size distribution or Silt. The Yarmouth is distinguished silt loam texture but may also consist clay mineralogy. However, over short from the other soil-stratigraphic units of loamy sand, sandy loam, silty clay distances, beds within the unit may in the area by its stratigraphic posi- loam, silty clay, and loam. be correlated. For example, borings tion. In other regions the Yarmouth Although its clay mineralogy ED22 and ED23 are separated by is thicker and more weathered than varies from one location to the next, about 4,000 meters and show similar the Sangamon Soil, but in the study

57 area the differences are hard to single-family dwelling, but these a sanitary (municipal) landfill site (1) distinguish. units are generally located only by no waste can be disposed of in stand- chance. The study area does not ing water; (2) no waste can be dis- Sangamon Soil The Sangamon contain economic deposits of sand posed of in areas with a high water Soil in the study area developed in and gravel aggregate within the sur- table unless preventive measures are parts of Glasford Formation, Love- ficial materials. The weathered silt taken to prevent leachate migration;

land Silt, Teneriffe Silt, and Oak deposits that cover the upland have ( J) no Surface runoff should flowinto formation exposed at land surface hitlf commodity value except for or through the operation or com- during Sangamonian time. The construction fill or ceramic products pleted till area; and (4) no disposal Sangamon Soil is distinguished from such as common brick. should take place "unless the subsoil other pedologic units by its stratig- material affords reasonable assur- raphic position and the strength of LAND USE ance that leachate from the landfill its development; in many places it will not contaminate groundwater or has a pronounced Bt horizon and The value of the surficial deposits of surface water." moderate to strong blocky fabric that a region in terms of material and In general, no site within the Creal is commonly called soil structure. space for various land uses is becom- Springs or Stonefort Quadrangles is

The Sangamon Soil is buried by ing increasingly important; it is in suitable for a sanitary landfill unless Wisconsinan-age Roxana Silt on the these near-surface materials that measures are taken to prevent the uplands in the study area. Except in roads, houses, and industrial facil- migration of leachate. The upland the Sugar Creek Valley, the Sanga- ities are built, sewers and pipe lines loess units over the nonglaciated mon Soil preserved in valleys is are laid, crops are raised, and wastes areas of these two quadrangles are developed in the Oak formation are buried, and the value of land, less than 2.5 meters thick, which is and buried by the Wisconsinan-age particularly in developing regions, is too thin for disposal trenches or for Equality Formation; in the Sugar directly related to its suitability for use as a source for trench-cover mate- Creek Valley, the Bt horizon of the such uses. rial. In the glaciated area, the Glas- Sangamon Soil is developed in the In the three quadrangles, impor- ford Formation has a patchy distribu- Teneriffe Silt and is buried by the tant land-use issues (beyond agricul- tion, and the total loess and diamic- Holocene-age Cahokia Formation. tural considerations) include the ton thickness is rarely more than 7 siting of waste disposal (landfill) meters. No major bedrock aquifers Farmdale Soil The Farmdale Soil operations and major construction are located in the study area, but the in the study area formed in the projects. The characteristics and upland units generally overlie sand- Roxana Silt and was buried by the thickness of the surficial deposits are stone that serves as a minor aquifer Peoria Silt. The Farmdale Soil is eas- critical to determining the suitability in the Creal Springs and Stonefort ily identified by its thin to medium of a site for a particular type of land Quadrangles. platy structure, although modern use. Although no large municipali- Suitable waste disposal sites may pedogenesis has obscured some of ties are located in the study area at exist in the Eddyville Quadrangle. In its primary features. Silt coats or present, growth could occur in the this quadrangle, shale, a bedrock masses of clean, white silt grains region in future years. Once a general unit having low hydraulic conductiv- commonly occur along the ped faces. area is selected for any prospective ity, underlies the surficial deposits on Many biological pores appear to be construction or waste disposal use, most upland positions. The Roxana primary features, but the many clay a detailed on-site evaluation must be Silt and Peoria Silt have a combined films, manganese and iron oxide made of the surface deposits before thickness of less than 2 meters in this concretions, and stains along root before the facility can be designed quadrangle, however, providing channels probably reflect overprint- and constructed. This section sum- only a marginal supply of cover ing of the Farmdale Soil by modern marizes the basic characteristics of material. Valley units of all three pedogenesis. surface materials in the quadran- quadrangles are located in regions gles that can affect waste disposal, having poor surface drainage and

construction practices, and seismic high water tables (generally within 1 RESOURCES risk considerations related to such meter of the surface in most bottom- Surficial deposits in the study area projects. lands); therefore, the valleys are not may contain a variety of natural suitable for sanitary landfills. In Waste resources such as groundwater, grav- Disposal places where no other site is avail- el, sand, and clay. Silt and clay-rich Municipal waste includes household able within a reasonable distance of materials in some areas may be suit- refuse and nonsalvageable commer- a community, a sanitary landfill able for ceramic products. cial wastes such as metal and paper. could be located in the study area if No significant groundwater re- This type of refuse is commonly the landfill is lined and leachate is sources have been found in surficial buried in sanitary landfills. The collected and treated. deposits of the study area. The primary consideration in locating a Even more stringent geologic con- upland deposits are generally un- sanitary landfill is minimizing the ditions are required for the safe saturated, and the valleys contain migration of leachate (a solution disposal of hazardous wastes, includ- fine-textured sediments that seldom produced when infiltrating water ing toxic chemical, biological, radio- yield groundwater in economic reacts with the refuse) into ground- active, flammable, and explosive re- quantities. Isolated sand lenses water and surface water. Guidelines fuse. No suitable sites for hazardous within the valley deposits may yield of the Illinois Department of Public waste disposal were found in the sufficient groundwater to supply a Health (1966) require that in selecting study area.

58 in excavating for sewer lines, water nitude, associated with the New Ma- General Construction lines, or septic systems. The glacial drid Fault Zone in eastern Missouri, Most general construction projects, diamicton that underlies the loess in could occur. In the winter of 1811- such as roads, subdivisions, small the northwest part of the Creal 1812, a series of major earthquakes businesses, drainage systems, and Springs Quadrangle has a variable shook the region, and intensities of water and sewage lines, can, if texture, but in most places, this IX or X (on the Modified Mercalli properly designed and built, be sited material has properties comparable Intensity Scale) were probably experi- anywhere in the study area except in to those of the loess. Detailed study enced in the three quadrangles; lowlands prone to flooding or on the of lateral variation in the material earthquakes of this intensity could extremely steep valley slopes. Condi- properties of the diamicton is neces- cause total destruction of weak struc- tions on the uplands are most favor- sary before any construction project tures and major damage to well-built able. Loess, a silty deposit, typically is begun. structures (Nuttli 1973). has a low bearing capacity and is The valley bottoms in the study Structures built in the valley bot- susceptible to frost action if water area are generally not suitable for toms of the area are most at risk; the saturated; however, the loess cover- construction. A high water table (less thick, unconsolidated, and saturated ing the upland areas in the study area than 1 m in places), poor surface deposits found in these areas gener- is unsaturated for most of the year drainage, and silty materials having ally amplify seismic waves and are and probably has a moderate bearing low bearing capacity characterize prone to liquefaction, which causes capacity Sandstone bedrock underly- these areas. Flash flooding is also a a significant loss of bearing capacity. ing the surficial material in many distinct possibility in the narrow Structures having foundations in upland positions has a high bearing valleys. bedrock are at less risk. The founda- capacity and is generally found at tions of critical structures such as shallow depths (less than 2.5 m). The Seismic Risk hospitals, schools, and emergency shallow bedrock may be advantage- The study area lies in a zone of high service centers should be located in ous for projects requiring high seismicity. Historical evidence sug- the bedrock on gently sloping up- bearing capacity, but it is a liability gests that earthquakes of large mag- lands.

APPENDIX A Description of Boring ED8 Description of a core sample collected from a borehole on a narrow upland interfluve located 5 meters north of County Road 23 and 1.1 kilometer east of Illinois State Highway 145 (SE NW NE, Section 29, T11S, R6E, Eddyville 7.5-minute Quadrangle, Pope County). Approximate surface elevation is 845 feet.

Depth Zone Description

Peoria Silt with Modern Soil

0.00-0. 28 A, E A and E horizon of Modern soil, brown (10YR 5/3) silt loam, granular, porous and friable; gradual boundary.

0.28-0.61 Btl Yellowish brown (10YR 5/6) silty clay loam; moderate, fine sub-angular blocky structure; few, fine manganese oxide stains along root channels; abrupt boundary.

0.61-0.99 Bt2 Yellowish brown (10YR 5/6) silty clay loam with common, medium light grayish brown (10YR 6/2) mottles

and common, medium, light gray (10YR 7/1 ) silt coats and common, fine brown ( 10YR 5/3) clay films; moderate fine subangular blocky structure; common, fine to medium, dark yellowish brown (10YR 4/4) iron oxide concretions; large, very dark brown (10YR 2/2) root cast with gray (10YR 5/1 and 7.5YR 6/1) clay films; abrupt boundary.

Roxana Silt with Farmdale Soil

0.99-1.75 2Bt/AEb Yellowish brown (10YR 5/6) silt loam with common, medium dark brown (10YR 4/3) mottles and common thin to moderately thick light brownish gray (10YR 6/2) clay films and common light gray (10YR 7/1) silt coats; strong, thin platy structure; few, fine manganese oxide stains along root channels; diffuse boundary.

1.75-2.28 2Bwbl Yellowish brown (10YR 5/6 and 5/4) silt loam; disturbed sample; common, fine to medium manganese oxide concretions; clear boundary.

2.28-2.39 2Bwb2 Yellowish brown (10YR 5/6 and 5/4) silt loam; strong, fine angular blocky structure; common, medium manganese oxide concretions; abrupt boundary.

Oak formation with Sangamon Soil

2.39-3.05 3Btb Yellowish brown (10YR 5/6) and yellowish red (5YR 5/6) clay with common, medium brown (10YR 5/3) to dark brown (10YR 4/3) clay films; strong fine angular blocky structure; common dark yellowish brown (10YR 4/4), dark reddish brown (5YR 3/3), and yellow (10YR 7/8) sandstone pebbles; gradual boundary; leached residuum.

3.05 3R Bedrock; Pennsylvanian sandstone.

STRUCTURAL GEOLOGY AND MINERAL DEPOSITS W. John Nelson

The three quadrangles of interest lie intersects the Lusk Creek Fault Zone faults forming a zone 500 to 1,500 feet along the southern margin of the Illi- near the eastern edge of the Eddy- wide. The faults strike about N40°E, nois Basin (fig. 2). The strata dip ville Quadrangle in Section 25, T11S, and their overall displacement is regionally northward toward the R6E (fig. 37). down to the southeast. Rocks of the structural center of the basin, which The only part of the Shawneetown Abbott Formation southeast of the is located about 60 miles north of the Fault Zone within the study area is fault zone are juxtaposed with Casey- study area. The average dip is rough- a pair of faults forming a narrow ville and uppermost Chesterian ly 1 in 50 (1°) in the Eddyville and graben that strikes slightly east of strata northwest of the zone. The Stonefort Quadrangles and slightly north in Wl/2, Section 24, and NW, downthrown block has been called less in the Creal Springs Quadrangle. Section 25, T11S, R6E. Faulting is the Dixon Springs Graben (Weller Regional dip direction is slightly west indicated by steeply dipping, shat- and Krey 1939); its southeastern of north in the Eddyville Quadran- tered, and slickensided rock and by margin is formed by faults that lie gle, due north in the Stonefort Quad- juxtaposition of pebbly Caseyville outside the study area. rangle, and slightly east of north in sandstone with brown, micaceous The Caseyville Formation and up- the Creal Springs Quadrangle. sandstone believed to belong to the permost Chesterian rocks northwest The structural pattern is strongly Abbott Formation. The faults appar- of the Lusk Creek Fault Zone are hori- modified by four important zones of ently converge and die out toward zontal or dip gently within a few deformation that cross the study area the south. Northward, they extend hundred feet of the fault zone. Close (fig. 37): the Shawneetown Fault out of the quadrangle and merge to the fault, they are sharply tilted Zone, which grazes the eastern edge with the main part of the Shawnee- toward the southeast and dip as of the Eddyville Quadrangle; the town Fault Zone, as mapped by steeply as 55° adjacent to the fault Lusk Creek Fault Zone, which cros- Baxter et al. (1967) in the Herod zone. A narrow hogback ridge of Ca- ses the southeastern corner of the Quadrangle. The faults apparently seyville sandstone and conglomerate same quadrangle; the McCormick are high angle, but their direction of follows the northwest edge of the Anticline, which curves westward dip is unknown. The dips of rocks ad- fault zone, extending southwest from the east-central part of the jacent to the faults are not consistent from the center of Section 35, T11S, Eddyville Quandrangle to the south- from place to place. The strata on R6E. A deeply dissected plateau westernmost part of the Stonefort both sides of the faults dip west in capped by sandstone of the middle Quadrangle; and the New Burnside the north part of Section 24, but far- part of the Abbott Formation occurs Anticline, which runs westward a- ther south they dip eastward. The re- southeast of the fault zone in the cross the northern part of the Eddy- versed dips suggest the possibility of Dixon Springs Graben. The strata in ville and Stonefort Quadrangles and more than one episode of movement. the graben dip gently northwest, turns southwest through the Creal with an average inclination of about Springs Quadrangle. The newly Lusk Creek Fault Zone 5° in the Eddyville and adjacent named Battle Ford Syncline is be- The Lusk Creek Fault Zone was Waltersburg Quadrangles. Close to tween the McCormick and New named for Lusk Creek by Weller et the fault zone, the dip gradually Burnside Anticlines, and the newly al. (1952). It trends southwest from flattens out, then abruptly reverses. named Bay Creek Syncline is south the western terminus of the Shawnee- Abbott sandstone dips as steeply as of the McCormick Anticline. The town Fault Zone and crosses the 65°SE adjacent to the faults. The rocks Little Cache Fault Zone, also newly southeastern corner of the Eddyville in the graben are only slightly frac- named, is in the southwestern corner Quadrangle. From there, the fault tured, except immediately southeast of the study area. zone extends 25 miles southwest of the fault zone where they are across bedrock uplands (Weller 1940) moderately fractured. STRUCTURAL FEATURES and continues farther beneath the Within the fault zone is a central sediments of the Mississippi Embay- slice of highly fractured to shattered Shawneetown Fault Zone ment (Kolata et al. 1981). A northeast- and mineralized Caseyville and un- The Shawneetown Fault Zone is ern extension of the zone is called differentiated Chesterian strata. part of the Rough Creek-Shawnee- the Herod Fault Zone. The Lusk These rocks strike subparallel to the town Fault System, which runs about Creek Fault Zone is part of the fault zone and dip 25° to 55°SE. The 125 miles east-west across southeast- Fluorspar Area Fault Complex and central slice is internally faulted, ern Illinois and western Kentucky contains the northwesternmost limit although few details can be mapped and has maximum vertical displace- of known commercial fluorspar from available exposures. ment of at least 3,500 feet (Nelson deposits. The faults dip steeply southeast. and Lumm 1984). Near its western As mapped in the Eddyville Quad- Attitudes of mineralized fault planes end, the Shawneetown Fault Zone rangle, the Lusk Creek Fault Zone is in three fluorspar mines were listed curves sharply to the southwest and composed of two to three parallel by Weller et al. (1952, table 4):

61 NW Caseyville

J L :fc rf -L ^— i ^ ^^~-^- i_" T_iJ- -_i_ Kinkaid ='T i -~T^ : -^ Abbott Chesterian (undifferentiated)

-^~l"- a 1 i 1- "-J rL"^-~ "-^"^-~L : "Kinkaid~ - --i-

V\ Chesterian

Figure 38 Profile oi I usk( rtvk hiult/oni-inSntion V. I IIS. KM- (si'i- tig. 37 lor line of section). Outcrop of Caseyville

Formation is repeated in two faull slices ["he middle faull is a reverse fault ils if places basal Caseyville above upper ( aseyville. fne other faults, and the nel displacement are normal

,""N -T-r---^casevville --^ _^^

Abbott Chesterian (undifferentiated)

Caseyville •

\ Chesterian

Figure 39 Profile of Lusk Creek Fault Zone in SW, Section 35, Tl 1 S, R6E (see fig. 37 for line of section). The fault zone contains two slices. The southeastern slice, containing Chesterian and Caseyville strata, is upthrown relative to rocks on either side. The northwestern slice of Abbott Formation is downdropped relative to rocks on both sides. Net displacement and final motion was normal, down to the southeast.

Little Lusk Creek. alluvium

Figure 40 Profile of Lusk Creek Fault Zone just southwest of Lost 40 Mine (see fig. 37 for line of section) . Wedge-shaped slice of Chesterian undifferentiated at mine is upthrown, relative to rocks on both sides. Northwest of the mine a low-angle normal fault separates Caseyville (above) from Kinkaid (below). This fault apparently follows bedding planes near the northwest brow of the hill, then cuts across bedding as the bedding steepens toward the southeast. !

Lost 40 Mine dips 50°SE. Directly above near the a NE NE SE, 3-12S-6E, Eddyville Reelfoot Rift top of the bluff, Caseyville sandstone Attitude: N20°E/38-73°SE NW SE lies at nearly the same attitude. Shat- Rock Candy Mountain Mine sea tered, slickensided, and mineralized NE SE SW, 25-11S-6E, Herod sandstone and limestone float were Attitude: N40°E/85°SE Simpn.Ss".:;-. found about midway on the hillside Clay Diggings Mine °- between the two outcrops. North- -Mt.°Sirnon NE SE, 16-12S-6E, Waltersburg Precambrian ward on the hillside, Pennsylvanian Attitude: N15°E/85°SE sandstone directly overlies Kinkaid The fault at the Rock Candy Moun- Limestone and both dip about 20°SE. tain is in an open cut. fault that parallel to Mine exposed A becomes bed- b Lusk Creek Raum Steep southeast dips of faults are ding northward is believed to separ- Fault Zone Fault Zone confirmed by proprietary test drilling ate Caseyville from Kinkaid at this Pennsylvanian near the Lost 40 and Clay Diggings site (fig. 40). Mississippian-r-1 Mines and by a proprietary seismic profile a few miles south of the Geophysical findings A seismic Devonian- Eddyville Quadrangle. Dominantly reflection profile across the Lusk Ordovician dipslip motion is indicated by striae Creek Fault Zone indicates that the \/ and corrugations on fault surfaces fault zone penetrates Precambrian

' '• exposed at the Rock Candy Mountain crystalline basement (fig. 3). The • • •.' G o .' and Clay Diggings Mines. Attitudes section between the base of the Knox %>. of drag folds and jointing also indi- Group (upper Cambrian) and the in- cate dip slip. Drag-fold axes are ferred top of Precambrian is thicker horizontal or nearly so and strike southeast of the fault zone than to parallel to the faults; the dominant the northwest, indicating that the joint set is parallel to the faults and fault zone underwent normal move- the secondary set is perpendicular. ment during late Precambrian to The Lusk Creek Fault Zone con- middle Cambrian time. The south- tains normal and reverse faults in and east side dropped downward, allow- near the Eddyville Quadrangle. The ing thicker sediments to accumulate southeasternmost fault, which juxta- there. poses Abbott Formation in the Dixon The Lusk Creek Fault Zone lines Springs Graben with older rocks in up with the northwest margin of the the central slice, is a normal fault Reelfoot Rift (Ervin and McGinnis throughout its length. The fault 1975), which strikes northeast and northwest of the slice of undifferen- underlies the Mississippi Embay- is reverse tiated Chesterian rock a ment from northeastern Arkansas to Figure 41 Interpreted history of Lusk fault; the central slice is raised rela- southernmost Illinois. The rift has Creek Fault Zone, (a) Reelfoot Rift forms tive to Pennsylvanian rocks on either been defined by reflection and refrac- in late Precambrian to early Cambrian side. In NE, Section 35, T11S, R6E, tion seismic studies, gravity and mag- time; Lusk Creek fault develops as a listric the central of three faults is reverse, netic surveys, and limited deep normal fault down to the southeast. Rift- and the Caseyville Formation is re- drilling. It is bounded by large nor- fill sediment is deposited on the downthrown block. In late Cambrian time, the peated in two fault slices (fig. 38). mal faults that penetrate crystalline sea transgresses the region and Mt. Upraised central slices also exist at basement. Pre-Knox layered rocks Simon Sandstone is deposited on both the Rock Candy Mountain Mine (Bax- thicken dramatically on the down- sides of the fault, (b) In late Paleozoic ter et al. 1967) at the Clay Dig- thrown sides of faults, indicating that and time, compression from the southeast gings Mine in the Waltersburg Quad- faulting was active during pre-Knox reactivates the Lusk Creek Fault Zone as rangle (Weibel et al., in preparation). sedimentation (McKeown and a reverse fault. Raum Fault Zone develops At the latter site, the central slice Pakisar 1982, Gori and Hays 1984, as an antithetic reverse fault, and the contains Ste. Genevieve Limestone, Howe and Thompson 1984). block between the two fault zones is upthrown 800 to 1,500 feet relative to The seismic profile (fig. 3) further raised, (c) During the Mesozoic Era, rocks outside the fault zone. shows that the southeastern bound- extension takes place, allowing normal movement along Lusk Creek and Raum A narrow sliver of Abbott Forma- ary of the Dixon Springs Graben, the fault zones; the downdipped block tion is downfaulted between Casey- Raum Fault Zone, dips northwest between is the Dixon Springs graben. ville Formation and Chesterian strata and intersects the Lusk Creek Fault Note drag along both fault zones and about 1/2 mile northeast of the Lost at about the base of the Knox. Zone narrow slices of rock left high within the 40 Mine (fig. 39). The Abbott out- Thus, the Raum Fault Zone is an anti- fault zones. crops consist of iron-rich micaceous thetic fault zone, whereas the Lusk sandstone, carbonaceous shale, and Creek Fault Zone is the master sion that produced the Reelfoot Rift coal, all steeply dipping. structure. (fig. 41a). Slippage probably ended Southwest of the Lost 40 Mine, a by late Cambrian time, since Knox low-angle normal fault apparently is Interpretation The Lusk Creek and younger strata do not appreci- present on the northwest side of the Fault Zone evidently originated as a ably change thickness across the fault fault zone. Kinkaid Limestone in the normal fault during latest Precam- zone. The faults that currently dis- bank of Lusk Creek strikes N35°E and brian-early Cambrian crustal exten- place bedrock at the surface in the

63 .

Eddyville Quadrangle resulted from tilted and downthrown slices along north of McCormick and exiting at post-Atokan (Abbot! Formation) re- the northwestern side of the fault the southwestern corner of the quad- activation of the original Cambrian zone (figs. 38 to 40) are entirely rangle. It continues across the Bloom- fault zone. products of the extensional episode. field Quadrangle, gradually turning

The presence of parallel high-angle I he normal faults probably are of more southward and dying out in reverse and normal movements in early Mesozoic age. Numerous gra- southern Johnson County, east of the same fault zone seems to require bens developed in the eastern United Vienna (Weller 1940, Nelson in prep.). two episodes of movement/ compres- States during the Triassic Period; the sion and extension. The sharp drag Atlantic Ocean began to open during Structure The McCormick Anti- and tilting of strata down to the the furassic. Subsidence of the Mis- cline is an asymmetrical fold, with a southeast throughout the fault zone sissippi Embayment began in the steep and narrow northwest limb indicate that the last important move- Cretaceous Period. The Lusk Creek and a broad and gentle southeast ment was normal faulting, with the Fault Zone apparently does not de- limb. Dips on the northwest flank southeast side dropped down. The form upper Cretaceous strata ol the range from 12° to 45° and typically episode of reverse faulting there Embayment in southernmost Illinois are 20° to 35°. The southeast limb dips fore must have occurred earlier, (Kolata etal. 1981). less than 10° in most places, but suggesting that the region was first This scenario of reverse faulting locally is steeper, especially near subjected to compression from the followed by normal faulting is the faults. Structural relief from the southeast, which reactivated the same as that proposed for the Rough anticlinal crest to the trough of the buried rift-boundary fault as a re- Creek-Shawneetown Fault System Battle Ford Syncline, northwest of verse fault with its southeast side (Smith and Palmer 1981, Nelson and the anticline, is at least 500 feet in upthrown (fig. 41b). Lumm 1984, Kolata and Nelson, in most places and reaches a maximum Displacement along the Lusk press). The Rough Creek-Shawnee- of about 800 feet in the eastern part Creek Fault Zone during compres- town, like the Lusk Creek, contains of the Stonefort Quadrangle. The sion was probably a few hundred feet parallel high-angle normal and relief is considerably less, 200 to 300 in the Eddyville Quadrangle and at reverse faults that outline narrow feet, from the anticline to the Bay least 800 feet at the Clay Diggings slices of older rock apparently Creek Syncline on the southeast. Mine. The Raum Fault Zone may sheared off the hanging wall (south Superimposed upon the larger fold have formed as a backthrust. The or southeast block) during normal are several smaller anticlines (see fig. compression episode was probably movements. Both fault systems are 37 and structure-contour lines on induced by the Alleghenian Orogeny reactivated late Precambrian-early geologic maps). Three of these in the in late Pennsylvanian through Per- Cambrian rift-boundary faults. They Eddyville Quadrangle have curved mian time. Later, southeastern form a continuous shear zone and axes. The eastern ends of the minor Illinois underwent northwest-south- are products of the same stresses. anticlinal axes strike east-west, east extension, which created the parallel to the larger structure; west- numerous northeast-trending nor- McCormick Anticline ward they curve toward the south- mal faults of the Fluorspar Area Fault Name and extent Brokaw (1916) west. Thus, they form a right-handed Complex. The hanging wall of the mapped an anticline in northwestern en echelon pattern. Subordinate

Lusk Creek Fault Zone collapsed, Pope County, Illinois, and named it anticlines in the Stonefort Quad- forming the Dixon Springs Graben the McCormick Anticline after the rangle have slightly sinuous axes (fig. 41c). Some backslippage may village of McCormick in the Stonefort nearly parallel with the larger fold, have taken place along reverse faults, Quadrangle. Jacobson and Trask and form a relay rather than an en but most normal movement occurred (1983), on the basis of preliminary echelon pattern. on a newly formed fault, which pre- mapping, thought that faulting In profile, the folds vary from sently forms the southeast margin of dominated over folding and sug- smoothly arched, to boxlike, to sharp the Lusk Creek Fault Zone. This nor- gested changing the name to McCor- crested. Smooth-crested folds are mal fault is believed to intersect the mick Fault Zone. Continued map- exemplified near Burden Falls in the reverse fault at depth (figs. 38 to 40) ping reveals an anticline with sub- Stonefort Quadrangle (Sections 10, Displacement during extension ordinate monoclines, synclines, and 11, and 15, T11S, R5E) and north of was substantially greater than that faults. The name McCormick Anti- Pleasant Ridge Church (Sections 6 during compression, since the net cline is retained for the sake of and 7, T11S, R6E) in the Eddyville throw of the Lusk Creek Fault Zone simplicity; the structure could be Quadrangle. A box fold with a slight- presently is down to the southeast. called an anticlinorium, a faulted ly tilted crest roughly 1/2 mile wide The total normal displacement in- anticline, or an anticline and fault occurs in the eastern part of the creases southwestward from roughly zone. Eddyville Quadrangle (fig. 42). 300 feet at the eastern edge of the The McCormick Anticline begins Sharp anticlines, faulted along their Eddyville Quadrangle to 1,500 feet at just east of the Eddyville Quadran- crests, are found southwest of Clay Diggings; these are minimum gle, at the western edge of the McCormick in the Stonefort Quad- figures, since the central slices may Shawneetown Fault Zone, and ex- rangle. The transition from steeply have been higher before normal fault- tends westward across the north- dipping beds on the northwest limb ing. Drag during normal movement central part of the Eddyville Quad- to gently dipping beds farther north- rotated bedding within and near the rangle, gradually curving toward the west is abrupt in most places. The fault zone, so that it dips southeast. southwest (figs. 2 and 37). In the dip changes from 45° to less than 10° Any drag folds formed during re- Stonefort Quadrangle, it turns to a in a few yards near the southwest verse faulting were obliterated. The heading of about S50°W, passing just corner of the Stonefort Quadrangle.

64 Figure 42 Cross section of McCormick structure and Winkleman Fault in the northeastern part of the Eddyville Quadrangle (see figure 37 for line of section). The McCormick structure is an asymmetrical box-fold. Sharp flexures here and on the south side of Cochran Hollow may be faulted at depth. Winkleman Fault apparently is a normal fault dipping steeply southeast; it represents the eastern terminus of the New Burnside structure.

Faults have been mapped along attitudes of adjacent rocks indicate to the southeast; yet the stratigraphic most of the length of the McCormick steep dips. displacement is down to the north- Anticline (fig. 37). Some faults pierce The few slickensides that have west. Two other cases are shown the crests of sharp anticlines. Others been noted indicate dominantly (figs. 44 and 45) in which two nearly diagonally cross the southeast flank dip-slip displacement, as do the parallel faults outline a steeply tilted of the structure. Both categories of orientations of drag-fold axes, nearly central slice of Caseyville sandstone. faults in map view are rotated slightly horizontal and parallel to faults. In the examples in figures 44 and 45 counterclockwise to the trend of the On some faults, the direction of and elsewhere, the last movement larger structure, so they describe a last movement deduced from drag was evidently normal and down to right-handed en echelon pattern. folds and tilt of strata is opposite to the southeast, partially or completely This right-handed arrangement is the the stratigraphic displacement. One canceling an earlier movement in same as that noted for the three small example from the southwestern part which the southeast block was anticlines in the Eddyville Quad- of the Stonefort Quadrangle is illus- raised. The geometry is nearly identi- rangle. Few faults have been mapped trated in figure 43. Strata dip steeply cal to that of the Lusk Creek Fault on the northwest flank of the struc- southeast along both sides of this System and implies the same se- ture, where dips are steepest and fault, suggesting a large downthrow quence of structural events. abrupt changes in dip are common. Most of the faults that have been "^center, section 36 observed are normal faults that dip NW SE 60° or steeper. A normal fault dipping 45°NW with about 25 feet of throw -750 ft Battery Battery Battery is well exposed along the ravine ^Rock Ss -200 m Rock Ss______Rock Ss north of Pleasant Ridge Church, near the center of NVi, Section 7, T11S, Wayside NNaysic^*^^- Mbr -500 ft R6E (Eddyville field stations 287 and 288). Smaller normal faults that dip Mississippian Mississippia" -100 m 45° to 80° are exposed along an -250 ft adjacent cliff of Pounds Sandstone. \| A fault exposed in a stream bed in SE NW SE, Section 36, T11S, R5E 300 m \ 600 m sea (Stonefort field station 357) strikes - level N20°E and dips 70°SE. Two high- 1000 ft 2000 ft angle reverse faults and several Figure 43 Cross section through a fault on the McCormick Anticline southwest of steeply dipping normal faults are the Zion Church, Stonefort Quadrangle (section runs S45°E from center of Section exposed along Ogden Branch in SW 36, T11S, R4E; see fig. 37 for line of section). The fault strikes approximately N20°E NE SW, Section 16, T11S, R5E (Stone- and dips 70° southeast, as exposed in stream bed near line of section. The stratigraphic fort field station 656). displacement is down to the west; however, the strata on both sides of the fault dip On other faults not completely southeast, indicating that the last movement on the fault was down to the southeast exposed, nearly straight mapped (normal) following an earlier episode of reverse faulting in which the southeast side traces across rugged terrain and was raised.

65 v

ous, enough measurements NW SE were taken to expose some definite trends. slickensides ^slickensides Along the McCormick Anticline in ^-^-gTv^-N. and breccia A Pounds Ss ^ v the Eddyville Quadrangle (fig. 46a), .\\.-:;-'S!t — — the joini directions cluster in two U'l'V'tfA * \ well-defined maxima. The stronger is N50°-60°E, which is parallel to the main direction of faults. The secondary maximum is N5()"-60"W, nearly approx. 100 ft (30 m) i TV perpendicular to the first set. Joints are most numerous and closely

Figure 44 Field sketch of' relationships in NWSESW, Section 5, T11S,R6E, Eddyville spaced near faults. Well-developed Quadrangle (see fig. ^7 tor line oi section), steeply tilted, conglomeratic sandstone joints also are common along the is found between two outcrops of Pounds Sandstone, with indications of faults on crests and steep north flanks of the both sides. Assuming tli.it the faults dip steeply southeast (as suggested by the tilt folds. Joint data from the Stonefort of the strata), we have an upthrow n ientr.il slue but almost no displacement across Quadrangle (fig. 46b) show consider- the fault zone. Drag folding of sandstone southeast of the fault zone indicates that ably more scatter and represent fewer the last movemenl was down to the southeast. This configuration is nearly idenlu .il to that of the Lusk Creek Fault Zone. readings than in the Eddyville Quad- rangles. Northeast and east-west trends of joints seem to be preferred. fractured and brecciated Northeast-trending joints seem to Caseyville Fm dominate northeast of McCormick village, whereas east-west joints are most common southwest of McCor- mick. The rose diagram for joints south of the McCormick Anticline in the eastern part of the Eddyville Quadrangle (fig. 46c) displays two strong, nearly equal maxima, one at N10°-15°E and the other at N80°- 90°W. The first set is parallel to the Figure 45 Cross sectional sketch, not to scale, of field relationships near head of Shawneetown Fault Zone, and the ravine just west of McCormick, NE SE NE, Section 20, T11S, R5E (see fig. 37 for line of section). Outcrops of steeply dipping to vertical, fractured, and brecciated Caseyville second set is perpendicular to the sandstone are found between gently dipping Abbott sandstone on the northwest. Shawneetown and parallel to the This configuration suggests two periods of movement, in which the Caseyville strata McCormick Anticline. Farther south southeast of the fault zone were first raised and then lowered. The southeasterly tilt (not shown in the rose diagram), the and the drag folds were imparted during the second movement, which involved joint orientation changes to NE-SW normal faulting. and NW-SE, parallel and normal to the Lusk Creek Fault Zone. Small trace-slip faults have been this type of fault is on Pounds Joints are rare and poorly devel- observed in several places along the Sandstone just east of the north- oped south of the McCormick Anti- north or northwest flank of the trending stream 600 feet from the cline in the Stonefort Quadrangle McCormick Anticline. (As defined by south line, 2,100 feet from the east and western half of the Eddyville Beckwith (1941), a trace-slip fault is line of Section 6, T11S, R6E (Eddy- Quadrangle. Jointing also is incon- perpendicular or oblique to bedding ville field station 285). spicuous in the Battle Ford Syncline, and underwent slip parallel to bed- north of the McCormick Anticline. ding, so that no offset of bedding is Joints Sets of parallel planar frac- Measurements were recorded at only apparent. A strike-slip fault in hori- tures, normal or very steeply inclined 15 field stations within the syncline. zontal strata is one example of a to bedding, are conspicuous in many At these localities, a preferred orien- trace-slip fault.) The strike of these outcrops along and near the McCor- tation of N45°-60°E was observed. faults varies from N15°E to N70°W, mick structure. Such joints are seen making them oblique or nearly per- in many lithologies, being best devel- New Bumside Anticline pendicular to the large mapped oped in well-indurated, thin-bed- Name and extent The New Burn- faults. The dip is normal to bedding, ded, quartzose sandstones and silt- side Anticline was first described and the faults bear prominent stones. In these rocks, joints com- and named by Brokaw (1916). Weller grooves and striations parallel to the monly are spaced a few inches apart (1940) renamed the eastern part of trace of bedding (thus the term trace- and locally are a fraction of an inch the structure the Stonefort Anticline, slip fault). In no case could the apart. Massive sandstones typically which he considered to be separate direction or amount of offset be contain very large planar fractures from the New Burnside. Jacobson determined. Because all observed spaced several feet to tens of feet and Trask (1983) thought the struc- trace-slip faults are confined to single apart, but near faults the sandstones ture was dominated by faulting and outcrops and contain no noticeable are closely jointed. Orientations of proposed the name New Burnside gouge or breccia, their extent and joints are summarized in the form of Fault Zone. Mapping for this report displacement are believed to be rose diagrams (fig. 46). Although the shows that the New Burnside and small. One of the best places to see sampling was not statistically rigor- Stonefort segments are intimately

66 related, although separated by a saddle, and that faulting is subordinate to folding. We refer to both by the older name, New Burnside Anti- cline. The New Burnside Anticline is north of and trends roughly parallel to the McCormick Anticline (figs. 2 and 37). The axis of the New Burn- side extends westward across the northern edge of the Eddyville Quadrangle and curves to trend Figure 46 Rose diagrams of joint orientations along and south of McCormick west-southwest across the Stonefort Anticline. Average readings from (a) 43 sites along the McCormick Anticline in the Quadrangle. In the Creal Springs Eddyville Quadrangle; (b) 23 sites along the McCormick Anticline along the Stonefort Quadrangle, it turns southwest- Quadrangle; and (c) 23 sites south of the McCormick Anticline in the Eddyville ward, passing just south of New Quadrangle. Burnside and Parker. Beyond Parker the structure gradually broadens and places, the elevation of the top of the which is a sharp but apparently un- flattens; it dies out northwest of Abbott Formation drops 400 feet in faulted hinge (fig. 47). Roadcuts on Tunnel Hill. A series of northeast- 1/2 to 3/4 mile north and 200 to 250 Route 145, a short distance west of trending normal faults associated feet in 1 mile south of the anticlinal Blackman Creek, show a sharply with the New Burnside extends into crest. The relief is only about 130 feet hinged box fold with the south limb the southern parts of the Harrisburg in the structural and topographic faulted. Farther west, along Battle and Rudement Quadrangles north saddle at Oldtown, Stonefort Quad- Ford Creek, two parallel cuspate and northeast of the current study rangle. Railroad cuts expose the anticlines, separated by a shallow area. The New Burnside and McCor- structure well and show it to be a syncline, have been mapped (fig. 48). mick Anticlines both are arcuate in slightly faulted monocline (fig. 19). The anticline near Murray Bluff is map view, with the convex side The anticline plunges abruptly at sharp crested; the southern limb is facing northwest. its east end in NE NE, Section 34, cut off by a fault that strikes parallel T10S, R6E, Eddyville Quadrangle. A (N50°E) to the fold axis (fig. 49). The Structure The New Burnside northeast-facing monocline of low fold and fault terminate abruptly Anticline is geometrically similar to relief and a southeast-dipping fault near Bill Hill Hollow, and another the McCormick Anticline, but has branch off the east end of the anti- anticline arises 2,000 feet north near less relief and is less faulted (fig. 37 cline. At its southwestern end, the Stonefort Bluff. The sudden offset of and geologic maps). The steeper New Burnside Anticline merges al- the fold axis and the linear trend of north flank dips 10° to 25° in most most imperceptibly into a region of Bill Hill Hollow suggest a tear fault places and locally is as steep as 60°. homoclinal northerly dip. along the hollow. Such a fault, if it Dips on the southeast flank generally East of Oldtown, the New Burn- exists, is entirely concealed by al- are less than 10°. Both flanks flatten side consists of a series of anticlines, luvium. West of Stonefort Bluff, the as the anticline plunges southwest- arranged in subparallel relay or right- axis of the New Burnside Anticline ward in the Creal Springs Quad- handed en echelon pattern. Near the is sinuous and possesses saddles and rangle. The three areas of maximum eastern end of the structure, some of elongate domes, but it is a continu- relief are near the northwest corner the anticlines are cuspate in profile. ous fold. In profile, it is smoothly of the Eddyville Quadrangle, north This is best seen on the steep west arched, not cuspate or boxlike. of Sand Hill in the Stonefort Quad- bluff of Blackman Creek in SE SW Faulting along the New Burnside rangle (Section 4, T11S, R5E), and SE, Section 27, T10S, R6E (Eddyville Anticline is most pronounced in the near the border of the Stonefort and field station 85). Dips on both flanks Eddyville Quadrangle. The trace of Creal Springs Quadrangles. In these of the fold steepen toward the crest, the Winkleman Fault (Cady 1926)

N S

Murray Bluff Ss '== 8x v. •:'.•.'. — — ^r~~~'^^. h sa^o '<': :: \ Abbot^J^^l^-^ ^^.•./...j olive shale middle vaNey f , oor

r 50m "150 ft \ 300 ft '

100 m

Figure 47 Profile of New Burnside structure on the west side of Blackman Creek (see fig. 37 for line of section). Note sharp-crested anticline; dips increase toward crest on both flanks. N S

s'"---

Ifault Ifault (-250 ft 50 m 100 m

500 ft

Figure 48 Profile of New Bumside structure where it crosses Battle Ford Creek, in the north-central part of the Eddyville Quadrangle (see fig, X] lor line ol section). TWo sharp-crested anticlines, separated by a shallow syncline, are present. The northern anticline changes into .i fault eastward, whereas the southern anticline changes into a fault eastward and dies out westward.

Figure 49 Profile of a hillside east of a ravine, near center E 1/2, Section 25, T10S, R5E, Eddyville Quadrangle (field station 29). Note sharp fold hinge in Murray Bluff Sandstone; dip changes within a few feet from 10°N to 35°-40°S. Many fractures but no offsets are visible in the hinge; small normal faults are exposed on ledges north of the hinge. East of the fold hinge a concealed fault juxtaposes sandstone of lower Spoon Formation with Murray Bluff. trends N60°E and extends from the area and in the adjacent Harrisburg have been mapped along the anti- northeast corner of the quadrangle Quadrangle, a series of northeast- cline in the western parts of the to the eastern end of the New Burn- trending faults outlines a graben. Stonefort and Creal Springs Quad- side Anticline, where it curves west Several of these faults are exposed in rangles. All of them dip steeply and and parallels the fold for about 1/2 highwalls in the Brown Brothers have throws of a few tens of feet. mile. Then it again bends sharply to Company No. 1 Mine and were ex- They extend farther south than north the southwest and connects with a posed before reclamation in the No. of the fold axis; several faults nearly complex zone of faults along the 2 Mine farther north. All are normal reach the trough of the Battle Ford McCormick Anticline. The Winkle- faults that dip 70° or steeper and bear Syncline. The four eastern faults man Fault is a high-angle normal vertical striae and corrugations probably are simple normal faults. fault with a maximum throw of about indicative of pure dip-slip displace- The westernmost fault has drag 100 feet. ment (fig. 50). Displacements of inconsistent with stratigraphic offset. An east-west trending fault in Sl/2, faults exposed in the coal mines A sandstone bed appears to be Section 29, T10S, R6E, is exposed at range from a few feet to 150 feet. downthrown about 20 feet to the several places in a stream bed and Faults along the anticline in the northwest, but rocks dip steeply appears to dip almost vertically. It Stonefort and Creal Springs Quad- southeast on both sides of the fault passes laterally at both ends to rangles are more widely spaced and plane in SW NW NW, Section 25, unfaulted sharp-crested anticlines. have smaller displacements than T11S, R3E. This suggests that the In the northwestern part of the those in the Eddyville Quadrangle. southeast block was first raised and Eddyville Quadrangle near Murray The railroad cut south of Oldtown then lowered, as on the Lusk Creek Bluff is a large high-angle fault that reveals numerous high-angle normal Fault Zone and several faults in the strikes N50°E; its southeast side is faults and a few high-angle reverse western part of the McCormick downthrown as much as 200 feet. faults that strike N75°W to N65°E, Anticline. The fault lies a few tens of feet and have displacements ranging A high-angle reverse fault that southeast of a sharp-crested anti- from a few inches to 10 feet. Five strikes N65°W was observed in a cline. At the north edge of the map northeast-trending en echelon faults stream cut north of the anticline in

68 Figure 50 (a) Fault surface exposed by mining in reclaimed Brown Brothers Excavating No. 2 Mine just north of the Eddyville Quadrangle. The fault plane dips steeply, exhibiting vertical slickensides, normal movement, and little folding of strata, (b) Sandstone breccia on fault surface on highwall of the abandoned Brown Brothers No. 1 Mine just north of the Eddyville Quadrangle (SE NW, Section 20, T10S, R6E, Harrisburg Quadrangle).

Nl/2 NE NW, Section 6, T11S, R5E 50°E in the Stonefort and Creal (Stonefort field station 747). The atti- Springs Quadrangles. Thus, joints tude and location of this fault are are generally subparallel with nearby anomalous for faults along the New normal faults along the anticline. A Burnside Anticline. secondary northwest-trending set of Trace-slip faults similar to those joints, indicated on the rose dia- described along the McCormick grams, is much weaker than the Anticline exist along the New northeast-trending set. Burnside also. Several prominent A rose diagram (fig. 52e) of 37 joint ones (fig. 51) were observed on a measurements northwest of the New sandstone ledge in SW SE NW, Burnside structure in the Creal Section 35, T10S, R5E (Stonefort field Springs Quadrangle reveals no de- station 558). The site is on the north- finite preferred orientation. A dia- west flank of the anticline where gram (fig. 52d) for the area southeast bedding dips 25° to 30° northwest. of the structure, representing 66 The faults are nearly perpendicular stations, shows a strong peak at to the anticline and dip vertically. N10°-20°E and a secondary peak at Other trace-slip faults can be seen in N50°-60°E. the railroad cut about 1,000 feet south of the grade crossing at Oldtown and Battle Fbrd Syncline in a railroad cut south of Parker in The Battle Ford Syncline, named in the Creal Springs Quadrangle in NE this report, lies between the McCor- SWNW, Section 17, T11S, R4E. These mick and New Burnside Anticlines. faults also strike northwesterly. Its name is taken from Battle Ford Creek, which follows the synclinal Joints Rose diagrams of joints axis for a short distance in the north- along the New Burnside Anticline central Eddyville Quadrangle. The Figure 51 Trace-slip fault near center (fig. 52) represent average readings syncline extends about 18 miles from of W 1/2, Section 35, T10S, R5E, Stonefort at a total of 103 sites in all three quad- Wl/2, Section 34, T10S, R6E, Eddy- Quadrangle. This vertical fault strikes rangles. A preferred northeasterly ville Quadrangle, to the headwaters N45°W. Striae and corrugations on the orientation of joints is all Section T11S, evident in of Sugar Creek in 35, fault surface plunge about 30° northwest, three quadrangles. More precisely, R3E, Creal Springs Quadrangle (fig. parallel to the trace of the bedding on the the principal trend is N50°-60°E in 37). The Battle Ford Syncline is a fault surface. The staff is graduated in feet the Eddyville Quadrangle and N40°- topographic depression as well as a and inches.

69 structural one. The upper reaches of Battle Ford Creek, the Little Saline River, and Sugar Creek all follow the Structural trough. Upland surfaces within the syncline are largely dip slopes on the Murray Bluff Sand- stone Member of the Abbott Forma- tion. The Battle Ford Syncline is broad and asymmetrical. Its width increases from a little over 1 mile on the east to about 4 miles on the west. The trough or axis is sinuous and lies generally within 1 mile of the crest of the New Burnside Anticline. Relief from synclinal trough to New Burn- side crest varies from less than 50 feet to about 300 feet. The south flank of the syncline dips at an average rate of less than 1° until close to the McCormiek Anticline, where the inclination abruptly steepens. Struc- tural relief between the trough of the syncline to the crest of the McCor- mick Anticline ranges from 400 feet to more than 750 feet (see structure Figure 52 Rose diagrams of joint orientations on and near New Burnside Anticline contours on geologic maps) in the Eddyville Quadrangle. Average readings from (a) 27 sites along the New Burnside Anticline, Eddyville Quadrangle; (b) 23 sites along At its western end, the Battle lord the New Burnside Anticline, Stonefort Quadrangle; (c) 53 sites along the New Burnside Anticline, Creal Syncline loses its identity where the Springs Quadrangle; (d) 66 sites southeast of the New Burnside Anticline, Creal New Burnside Anticline fades away. Springs Quadrangle; (e) 37 sites northwest of the New Burnside Anticline, Creal At the eastern end, the syncline is Springs Quadrangle; and (f) 33 sites along Little Cache Fault Zone and vicinity, Creal tightly closed off by a west-facing Springs Quadrangle. flexure, roughly parallel to Blackman Hollow. East of this point, the strata Smith Springs. The syncline extends published and preliminary gravity slope steadily northward, inter- about 12 miles southwest from the and magnetic surveys of the Stone- rupted only by the Winkleman Fault. east-central part of the Eddyville fort and Creal Springs Quadrangles, The eastern end of the syncline is cut Quadrangle, through Watkins Ford, and two proprietary seismic reflec- by the Winkleman Fault, which dia- to the center of the southern border tion profiles. gonally links the McCormiek and of the Stonefort Quadrangle, where Regional maps of the gravity field

New Burnside Anticlines. Displace- it leaves the study area. in southern Illinois include those of ment on this fault is approximately The trough of the Bay Creek Syn- McGinnis et al. (1976) and Hilden- 125 feet down to the southeast. The cline lies roughly 2 miles southeast brandetal. (1977). Regional magnetic downdropped block southeast of the of the McCormiek Anticline and maps were made by McGinnis and Winkleman Fault contains the struc- strikes parallel to the latter. The dips Heigold (1961), Lidiak and Zietz tural lowest point (structurally) in the on both flanks average 1.5° and are (1976), and Johnson etal. (1980). All Battle Ford Syncline. This roughly quite regular. The northwest flank, were based on control points spaced triangular basin is bordered by the in common with the southeast flank 1 mile or more apart. They show re- fault, the McCormiek Anticline, and of the McCormiek Anticline, curves gional trends but do not indicate the eastern closure of the syncline. from northeast to east. Structural anomalies that can be related to The drainage in this little basin contour lines on the south flank specific structures mapped in the gathers inward from three directions, trend slightly north of due east. The study area. flowing down sandstone dip slopes trough of the syncline is 300 to 400 A ground magnetic survey by Hei- and merging at the fault to a single feet lower in elevation than the crest gold and Robare (1978) covered most northwest-flowing stream deeply of the anticline (see structure con- of the present study area, including incised in Murray Bluff Sandstone tours on geologic maps). The eastern all of Johnson County, southwestern northwest of the fault. closure of the Bay Creek Syncline is Saline, and northwestern Pope gradual; the western closure has not County. Three detailed profiles were Bay Creek Syncline been mapped. made; the only one in our study area The name Bay Creek Syncline is ap- crossed the McCormiek Anticline plied in this publication to an en- Geophysical Expression along the Illinois Central Railroad in closed structural depression that lies of Anticlines the Stonefort Quadrangle. This pro- southeast of the McCormiek Anti- Geophysical data available for the file was considered inconclusive by cline. It is named for Bay Creek, study area include several regional its authors. Heigold and Robare's which approximately follows the axis magnetic and gravity surveys, one map of residual magnetic intensity of the syncline from its source to Bell published local magnetic survey, un- (fig. 53) indicates an overall magnetic

70 gradient rising toward the northwest across the study area. The contour lines dI magnetic intensity form a slightly arcuate pattern roughly paralleling the McCormickand New Burnside Anticlines. Considering that sedimentary rocks generally have very low magnetic susceptibil- ity, Heigold and Robare believed tin- magnetic gradient to reflect configuration of the Precambrian surface. They regarded the McCormick and New Burnside Anticlines as products of compression from the southeast. Although they saw no indication that the McCormick and New Burnside Anticlines affect basement, Heigold -30,000 and Robare speculated that the arcuate form of these structures may ha\ e Figure 54 Cross section in western Maryland and West Virginia, from Kulander been controlled by the configuration and Dean (1986). Narrow, steep-flanked anticlines and broad, intervening synclines of the basement surface. northwest of the Allegheny structural front are related to imbricate thrust faults above A suite of gravity and magnetic major detachment surfaces in Lower Cambrian and Upper Ordovician shales. maps of the Creal Springs Quad- rangle was prepared by Lawrence gravity map shows a strong and and appeared to be offset by one or Malinconico of Southern Illinois sinuous gravity gradient down to the more faults that apparently flatten University, Carbondale. Malinconico north, just south of the New Burn- with depth. The Creal Springs profile and Steven Brennecke also produced side Antii line. This suggests possible was of poor quality, and reflectors a map of the first-order residual duplication by thrusting of the rela- could not be correlated with strati- magnetic field in the Creal Springs tively dense Valmeyeran carbonate graphic units. The other seismic pro- Quadrangle. These maps, like section on the south limb of the fold file (fig. 3), of much higher quality, Heigold and Robare's map, show (Malinconico, personal communica- ran north-south through the Eddy- magnetic field increasing toward the tion, 1988). However, no correspond- ville Quadrangle, crossing the northwest. Several oval to irregular ing gravity and magnetic features are McCormick and New Burnside Anti- shaped magnetic highs and lows, 1/2 associated with the McCormick Anti- clines and the Lusk Creek Fault Zone. to 2 miles across at the long axis, also cline. Gravity and magnetic data are This profile showed strong arching are shown on the maps. Several pro- inconclusive on the nature of the of reflectors near the surface on both nounced lows are present just south anticlines at depth. anticlines and also indicated two or of the crest of the New Burnside Two proprietary seismic reflection three south-dipping listric faults, Anticline. Malinconico (personal profiles from the study area were stacked one above another beneath communication, 1988) suggested that viewed by the authors of this report. the crest of the McCormick Anticline. these could reflect thickened A north-south profile in the Creal The New Burnside Anticline appa- sedimentary section, possibly due to Springs Quadrangle crossed the rently was cut by three fairly high- overthrusting beneath the south western end of the New Burnside angle planar faults, of which two flank of the anticline. The Bouger Anticline. The anticline was evident dipped south and one dipped north.

-4000 ft

-2000 m

1 2 3 km

Figure 55 Profile in the Ruhr coal basin, West Germany, showing deformation of Upper Carboniferous strata as a result of the

Variscan orogeny (late Paleozoic) . Profiles are based on borehole records and surveys in multiple-seam underground coal mines. Upright boxlike and sharp-crested anticlines contain imbricate reverse faults, mostly high-angle, on crests and flanks. Regional direction of thrusting was south (right) to north. Seismic reflection surveys in northeastern France indicate that the Variscan thrust faults flatten at depth into decollements in Devonian strata. (Raoult and Meilliez 1987; Drozdzewski et al. 1980)

72 GARRETT HAMPSHIRE CO..MD CO..WV Georges Allegheny NITTANY ANTICLINORIUM structural Creek Wills Mountain Bedford front Syncline Syncline

Normal and reverse faults were 1963). The Deer Park and Accident direct analogues to the present case. interpreted. A strong deep reflector Anticlines (fig. 54) are relatively Petersen (1983) cited several exam- on this profile, probably at the base narrow and have steep flanks, espe- ples of detached thrust folds that are of the Knox Group (upper Cambrian- cially on the northwest; the adjacent related to nearby high-angle base- lower Ordovician) showed neither Berlin and Georges Creek Synclines ment-rooted reverse faults. An exam- folding nor faulting in the area of the are broad and nearly flat bottomed. ple from the Anadarko Basin is McCormick and New Burnside The crest of the Deer Park Anticline shown (fig. 56). Petersen described Anticlines. Thus, this profile indi- is smoothly arcuate, whereas that of and illustrated comparable structures cates that the McCormick and New the Accident Anticline is boxlike. from the Sweetwater Uplift and Big- Burnside Anticlines are not rooted in Both anticlines contain imbricate horn Basin in Wyoming. These anti- basement, but are detached within (overlapping) southeast-dipping clines occur singly or in small parallel the sedimentary column. thrust faults that do not reach the or en echelon groups, generally sev- surface; both also have northwest- eral miles basinward from the parent Origin of McCormick and dipping backthrusts. A paired fore- high-angle basement-rooted faults. New Burnside Anticlines thrust and backthrust can produce a I personally have mapped a well- The structural geometry of the box fold. Note that some faults in exposed segment of such an anti- McCormick and New Burnside Anti- figure 54 are entirely detached (not cline, the Beaver Creek Anticline in clines, as mapped at the surface, is connected to decollements). Such the eastern part of the Bighorn Basin. consistent with the conclusion from faults can result from "crowding" of The anticline is about 5 miles long, seismic evidence that the anticlines strata on the limbs of a fold. Note averages 1/4 mile wide, and has 200 are products of detached thrusting that two sets of faults, emanating to 300 feet of structural relief. The from the southeast. from two decollements, are stacked fold hinge varies within short dis- Detached thrust folding typically in the Deer Park Anticline. Similar tances, from smoothly curved to box- yields sets of elongate, parallel, stacking of faults was observed on like to hingelike. In map view, the arcuate anticlines and synclines, the McCormick-New Burnside seis- fold axis is slightly to sharply sinuous with the steeper limbs facing away mic profile. and is arcuate overall, the convex from the direction of tectonic trans- An example from the Ruhr coal side facing the basin (westward). port. Most of the world's folded basin of West Germany (fig. 55) illu- Thrust faults, with dips ranging from mountain belts exhibit such a pat- strates boxlike and sharp-crested horizontal to nearly vertical, cut the tern. The McCormick and New Burn- anticlines in a thrust-fold belt. The crest and limbs of the anticline. side Anticlines fit the same pattern, Ruhr area has undergone a greater Except for the prominence of thrust- with obvious differences in scale and degree of horizontal shortening than ing, this structure closely resembles tectonic setting. has the McCormick-New Burnside the McCormick and New Burnside Striking similarities are seen in area, so folds are sharper and more Anticlines in both scale and geome- profile between the McCormick and tightly crowded in the former than try. Noggle (1986), who mapped a New Burnside Anticlines and parts in the latter. Nevertheless, similari- larger area, interpreted the Beaver of the moderately compressed sec- ties in fold geometry are apparent. Creek Anticline as a detached thrust- tion of the Allegheny Plateau, north- The present study area is located fold connected with major basement- west of the Allegheny structural front within the North American craton, seated thrust faults at the west flank in West Virginia and western Mary- more than 200 miles from the Alle- of the Bighorn Uplift, 2 to 3 miles land (fig. 54). In the Allegheny ghenian and Ouachita fold-thrust distant. example, anticlines formed where belts at the late Paleozoic continental The McCormick and New Burn- northwest-verging thrust faults margin. It is highly improbable that side Anticlines, by analogy to the ramped upward from decollements decollements traversed such a dis- examples above, are here interpreted located within the incompetent tance from these orogenic belts to as thrust-folds linked by decolle- Martinsburg Shale (upper Ordovi- southern Illinois. However, thrust- ments to the basement-seated Lusk cian) and in basal Cambrian shales fold structures have been document- Creek Fault Zone (fig. 57). Reverse (Kulander and Dean 1986, Rodgers ed in cratonic settings and provide faulting on the Lusk Creek and fold-

73 CARTER-KNOX FIELD

Figure 56 Example of foreland detachment structure in the Anadarko Basin, Grady and Stephens Counties, Oklahoma. This thrust/fold structure developed in response to basement uplift of the Wichita Mountains (near the end of the Pennsylvanian Period) on the southwest flank of the Anadarko Basin, along a high-angle reverse fault. Basement uplift along Lusk Creek Fault Zone induced detached thrusting along the McCormick and New Burnside Anticlines. (From Petersen 1983) ing of the anticlines took place during have propagated upward from thrust quent extension connected with the same compression episode, pre- faults at depth or developed in pre- Triassic-Jurassic rifting created nor- sumably late Pennsylvanian and viously unfaulted areas where fold- mal faults. Events on the detached Permian. Stacking of thrust faults on ing and jointing had weakened the anticlines and on the basement- seismic profiles indicates at least rocks. The en echelon arrangement rooted Lusk Creek and Rough Creek- three decollement horizons. Likely of many faults suggests that the Shawneetown Fault Zones are inti- units include Chesterian shales, the extension stress was not quite normal mately related. New Albany Shale (mainly upper to the anticline, but rotated slightly No evidence exists for pre-Pennsyl- Devonian), the Maquoketa Shale counterclockwise. Alternatively, a vanian structural movements. Wide- (upper Ordovician), and a shaly component of left-lateral wrenching spread deformation elsewhere in the interval at or near the base of the may have been involved. Illinois Basin during the time period Knox Group, possibly correlative The trace-slip faults, which are represented by the Mississippian- with the Davis Shale (upper Cam- mostly normal or highly oblique to Pennsylvanian hiatus (Kolata and brian) of southeastern Missouri. the fold axes, probably originated Nelson, in press) did not affect the Most of the faults at the surface during compression as either small present study area. Evidence consists along the anticlines are normal faults tear faults or conjugate strike-slip of boreholes and outcrops that show that probably developed during the faults. Most likely, they formed while Goreville and Grove Church Mem- later (early Mesozoic) episode of ex- bedding was still nearly horizontal, bers of the Kinkaid at or near the tension, which caused normal fault- and subsequently rotated as the crests of the anticlines. If any uplift ing along the Lusk Creek and Rough rocks were tilted. had taken place during the pre- Creek-Shawneetown Fault Zones Pennsylvanian hiatus, these units and in the Fluorspar Area Fault Time of Deformation would have been eroded. Complex. Several faults along the of Anticlines Initial uplift of the McCormick

McCormick Anticline and one near I believe the major deformation on Anticline during Caseyville sedimen- the western end of the New Burnside the McCormick and New Burnside tation is suggested by observations evidently originated as reverse faults Anticlines was post-Desmoinesian that the Caseyville is thinner on the during compression, and later under- (Spoon Formation). A compressional anticline than in adjacent synclines. went normal movement. Most thrust event, probably related to the late The Drury and Wayside Members in faults, however, probably did not Pennsylvanian-Permian Alleghenian particular appear to be thinner on the reach the surface. Normal faults may orogeny, folded the strata. Subse- anticline than elsewhere. Lithofacies

74 New Burnside NW Anticline

Dna New Albany Figure 5 7 Hypothetical origin of McCormick and UmIS Middle, Lower New Burnside Anticlines and associated faults . (a) Devonian; Silurian In late Paleozoic time, reverse movement occurs Om Maquoketa along the Lusk Creek Fault Zone. Horizontal Oqp Galena-Platteville thrusts (decollements) propagate toward the Osp St. Peter northwest and ramp upward; imbricate thrusting -Gd Davis Shale produces anticlines. Likely decollement zones include (1) upper Cambrian Davis Shale, (2) upper Ordovician Maquoketa Shale, and (3) Upper Devonian New Albany Shale. (b) Mesozoic extension allows normal, down-to-the-southeast movement on imbricate faults beneath anticlines, in some cases canceling early reverse displacements.

and thickness data are too sparse to nearly parallel to the dominant support further speculation. paleocurrent direction of lower Little Cache Fault Zone A series of imbricate thrust faults Pennsylvanian strata, the case for Two faults along Little Cache Creek is exposed in Wayside strata near the contemporaneous tectonism is not in the southwestern corner of the south portal of the Illinois Central particularly strong. The basal unit of Creal Springs Quadrangle are part of Railroad tunnel in NE, Section 31, the Abbott exposed at the north a zone of north-trending faults first T11S, R5E (Stonefort field station portal of the Illinois Central Railroad mapped by Weller and Krey (1939). 187). The faults ramp upward toward tunnel (see p. 25-26) was described The name Little Cache Fault Zone, the south and are truncated at the as a "breccia" and attributed to sub- introduced in this report, is from the base of the Battery Rock Sandstone aqueous gravity slides off the flank creek whose course is largely control- (fig. 58). Therefore, the faults formed of the anticline (Potter 1957). This de- led by the fault zone. after deposition of the Wayside and posit is not clearly a gravity slide; if The two faults form a graben about before deposition of the Battery it is a slide, movement might have 1,800 feet wide and trend slightly east Rock. Potter (1957) described this been triggered by nontectonic causes. of north (fig. 37). The western fault exposure and attributed thrusting to No similar rocks have been described has 200 to 250 feet of throw where it gravitational slides off the flank of a elsewhere in the Illinois Basin. exits in the study area. Eroded fault- rising McCormick Anticline. A pos- No evidence was found for contem- line scarps on Caseyville sandstone sible angular unconformity between poraneous structural movements are present in several places and indi- Wayside and Battery Rock Members during deposition of the Spoon and cate that the fault plane dips steeply was observed near the crest of the Carbondale Formations or for any east or is vertical. The fault plane was McCormick Anticline along a tribut- deformation on the New Burnside observed in a small draw west of Lit- ary of Caney Branch, SW SW NE, Anticline during Pennsylvanian tle Cache Creek in NE SW SW, Sec- Section 11, T11S, R5E (Eddyville field sedimentation. tion 27, T11S, R3E (Nelson's field station 402). Paleoslumps that create In summary, although initial uplift station 91). Here, the fault strikes angular unconformity may be trig- of the McCormick Anticline in Morro- N5°E and dips 80° to 85°E. Clay gouge gered by nontectonic causes, yet no wan and Atokan time may have and breccia are present; drag is con- such features have been found in the influenced sedimentation patterns fined to a narrow zone. The eastern Caseyville in our study area away and triggered gravitational slides, fault is poorly exposed. Its throw from the anticline. such movements, if they occurred, increases southward to roughly 150 Possible influence of the McCor- were much smaller than post-Atokan feet at the southern edge of the mick Anticline on distribution of movements. Uplift of only a few feet, quadrangle. Available evidence indi- sandstone in the Abbott Formation however, could divert the course of cates that the eastern fault, like the was mentioned in the discussion of a deltaic distributary as accompany- western, is a steep normal fault.

environments of deposition of the ing earth tremors triggered slumping I have traced the Little Cache Fault Abbott. Inasmuch as the anticline is of water-saturated sediments. Zone several miles south of the pre-

75 sen! study area and have observed only high-angle normal faults. Another fault that may be part of the Little Cache Fault Zone was mapped along Larkin Creek in Sec-

. Battery Rock Sandstone tion 15, T11S, R3E, Creal Springs Quadrangle. The fault strikes about N10°E and has the east side downthrown about 45 feet. In an exposure south of Larkin Creek in NE SW SE, Section 15, the fault plane dips about 80°E and bears vertical striatums, indicating dip-slip faulting. Shale dipping 60° to 80°E is juxtaposed with sandstone. About 30 feet north is another fault with a strike of N30°W and vertical dip and nearly horizontal slickensides. Sandstone adjacent to this fault dips northwest and is upthrown 5 to 6 feet on the south Figure 58 Sketch of the east side of the west. The offset was right lateral railroad mi immediately south of the tun- (assuming horizontal movement), nel portal in SE NW NE, Section 31, I I IS, R5E, Stonefort Quadrangle, showing a The strike-slip fault has an orienta- series ol imbricate north-dipping thrust faults within the Wayside Member of the tion compatible with a conjugate ( aseyville Formation. The faults steepen upward and are truncated at the base of the dextral fault produced in a stress field overlying Battery Rock Sandstone Member, indicating that faulting took place shortly with maximum stress N10°E, after deposition of Wayside strata and before deposition of the Battery Rock. minimum stress N80°W, and inter- mediate stress verticil. Normal t.iults rock is dark green to nearly black, L. G. Henbest (ISGS, unpublished that strike N10°E would form under finely crystalline to porphyrinic, and field notes, 1926) reported an igneous the same stress conditions. contains numerous inclusions of sed- dike containing fragments of "gran- The Little Cache Fault Zone prob- imentary rocks. It was weathered to ite, dolerite and gneiss" in a ravine ably is a product of the episode of ocher-colored clay as deeply as 30 feet in El/2 SE SW, Section 4, T11S, R6E. extensional tectonics that caused below top of sedimentary rock. On We found no igneous rock at this normal faulting elsewhere in the the basis of petrographic study, the location (Eddyville field station 121); study area. rock is an alnoite, composed of al- however, a rough-textured coarse tered olivine phenocrysts in a ground breccia of sedimentary rock frag- Other Structures mass of melilite, spinel, mica, pero- ments in a matrix of bright orange- Faults in northeastern Creal vskite, and carbonate. The rock has red material was found along a fault Springs Quadrangle Two small a globular segregationary (or frag- that strikes northwest and dips faults apparently unrelated to other mental) texture (D. G. Fullerton, vertically. The outcrop could be a structures in the area have been Exmin Corporation, written com- diatreme or explosion breccia similar mapped in the northeastern part of munication, 1988). Similar composi- to those around Hicks Dome (Baxter the Creal Springs Quadrangle: one tions are reported for other intrusive and Desborough 1965, Baxter et al. in Nl/2, Section 4, T11S, R4E, and rocks in the region (Clegg and Brad- 1967). If Henbest's descriptions of the other in Section 28, T10S, R4E. bury 1956, Hook 1974, Trace 1974). inclusions are accurate, fragments of These faults are mapped on the basis One dike observed at the strip mine Precambrian rock have been blasted of vertical offset of coals and other and not studied petrographically ap- upward no less than 15,000 feet. marker beds in the Spoon Formation. peared to be dominantly carbonate. Both strike north-northwest and Contact zones several inches wide on MINERAL DEPOSITS have the northeast side downthrown the small dikes and up to 5 feet wide approximately 25 feet. The type of on the large dike consist of coked coal Coal fault could not be determined but and baked, fractured, and mineral- Small-scale commercial and local coal probably is normal. ized shale and siltstone. mining has taken place within the Ground magnetometer surveys by study area from the early 20th cen- Igneous dikes Ultramafic dikes Richard Lewis (personal communica- tury (and probably before) through were uncovered late in 1984 during tion, 1985) suggest that the large dike the mid-1970s. Several coal seams in surface mining for coal at Peabody extends southeastward into the the Abbott and Spoon Formations Coal Company's Will Scarlet Mine, Eddyville Quadrangle. Lewis also locally reach a thickness of 3 to 4 feet just north of the Eddyville Quad- predicted a sill or laccolith in Val- and occur close enough to the surface rangle in Sections 13 and 14, T10S, meyeran carbonate rocks in Section for strip mining or shallow under- R5E, Saline County. The largest dike 25, T10S, R5E. Heigold and Robare's ground mining. These coals have was 10 to 23 feet wide and had a (1978) map shows a magnetic high among the highest heating values of strike of N30°W and vertical dip. here. Two oil-test holes in Section 25 any in the Illinois Basin (Damberger Several parallel dikes a few inches to bottomed in Chesterian strata with- 1971) and some of them are low in 3 feet wide were nearby. The igneous out encountering igneous rock. sulfur. The main deterrent to mining

76 is the sporadic distribution of the Tunnel Hill Coal Bed The Tunnel Delwood Coal Bed The Delwood coal. The seams are largely lenticular Hill Coal is known only from a strip Coal Bed probably offers the best and grade laterally into clastic rocks. mine in NW NW, Section 6, T12S, prospects for mining of any coal seam Faults and folds further segment the R4E, and from test holes C-3 and C-5 in the study area. It is present in all

deposits into small tracts. With exten- (table 1), all in the southern part of three quadrangles and is 3 to 4 feet sive thick coals of the Carbondale the Creal Springs Quadrangle. Col- thick over much of its extent. The Formation available just to the north, lapsed drift mines and test pits sug- largest known deposit lies in the tri- the study area is not attractive for gest wider distribution of the coal, angular structural depression that in- large-scale mining under current eco- but the coal itself was not seen. In cludes the type locality in Sections nomic conditions. However, oppor- the boreholes and strip mine, the 33 and 34, T10S, R6E, and Sections 3 tunities exist for small surface mines Tunnel Hill varied from 12 to 28 and 4, T11S, R6E. It also occurs near and possibly drift or slope mines in inches thick. Two weathered samples the northern edge of the quadrangle several parts of the report area. of coal from the mine were analyzed in parts of Sections 27 and 28, T10S, and showed about 5 percent ash, 0.6 R6E. These two areas together com- Coals of Caseyville Formation percent sulfur, and 10,400 Btu/lb; the prise about 525 acres. Within them The Gentry Coal Bed, near the base heating value and probably the sul- the coal ranges from about 24 to 47 of the Drury Member, crops out in fur content were lowered by oxida- inches thick. Assuming an average the southwestern part of the Stone- tion. Coal from the two drill cores thickness of 36 inches, we estimate a fort Quadrangle. The Gentry and a was not analyzed because it was thin total resource of approximately 2.8 slightly younger coal in the Drury and contained many shale partings. million tons of coal, all within 75 feet Member are known from drilling and The Tunnel Hill Coal must be re- of the ground surface. A drawback outcrops along the McCormick Anti- garded as a marginal mining pros- to mining this coal is the common cline between Burden Falls and Del- pect. It might present a worthwhile presence of a clay parting several wood, but no coal thicker than 24 target if found together with minable inches thick near the middle of the inches has been found. The Gentry Reynoldsburg Coal. However, the seam. No analyses of the Delwood Coal commonly contains a few inches Tunnel Hill appears to be thin or Coal in the Eddyville Quadrangle are of clean coal near the top, but the absent where the Reynoldsburg is available. rest is thinly interlaminated shale well developed. The Delwood Coal is known in the and coal. A few caved-in adits or Stonefort Quadrangle only from the prospect pits in this coal have been Oldtown Coal Bed The Oldtown core of hole S-2. In this hole, the coal seen; no commercial mining has been Coal Bed has been mapped in the was 42 inches thick, with a 2-inch attempted or appears feasible. Stonefort Quadrangle, mainly along claystone parting near the middle; its the northern edge of T11S, and ex- depth was 23 feet. Most of the shal- Reynoldsburg Coal Bed The Rey- tends a short distance into the adja- low reserves probably underlie the noldsburg Coal was mined for local cent Eddyville and Creal Springs marshy bottomlands of Pond Creek. use in the southeastern Creal Springs Quadrangles. The coal was surface Northwest of Pond Creek, the coal is and southwesternmost Stonefort mined just west of the railroad tracks far below drainage. The Delwood Quadrangles. West of Reynoldburg, near Oldtown and was taken from Coal lies approximately 110 feet in Sections 31 and 32, T11S, R4E, the small drifts or "dogholes" elsewhere. below the Mt. Rorah Coal, the out- coal varies from 15 to 36 inches thick, It is 30 to 36 inches thick in the surface crop of which is plotted on the but rapid changes in thickness there mine and railroad cut; Smith (1957) geologic map. Results of chemical render reserve estimates and mine reported 42 inches at Frank Durfee's analyses for the Delwood Coal from planning difficult. However, the coal strip mine at the western edge of the the Stonefort Quadrangle (hole S-2) is, at least locally, of superior quality. Eddyville Quadrangle. Only a few are given in table 5. Among the first eight samples listed inches of coal were found in test The Delwood Coal is widespread in table 5, the average ash content holes S-2 and S-3 (table 1) and in test in the northern part of the Creal was 4.3 percent, average sulfur 1.27 holes drilled a short distance west of Springs Quadrangle. Its outcrop has percent, and average heating value Durfee's mine. The "golden sand- been traced for several miles in the 13,750 Btu/lb. This compares with stone" generally directly overlies or area north and west of New Burnside typical values of 8 to 12 percent ash, occurs within a few feet of the top of village, and the coal probably occurs 2 to 5 percent sulfur, and 11,800 to the Oldtown Coal; the coal probably in the subsurface farther north and 12,700 Btu/lb for coals of the Carbon- is eroded in many places. west. The thickness of the coal varies dale Formation in southern Illinois. Analytical results of the Oldtown from 24 to 72 inches, and a claystone The character and quality of the Coal from the E. and L. Coal Com- parting up to 18 inches thick is com- Reynoldsburg Coal vary laterally, as pany strip mine (table 5) indicate monly present. The Delwood Coal does the thickness. For example, the moderate ash and low sulfur content. probably lies at strippable depth over Reynoldsburg becomes canneloid Analysis of the coal from test hole several square miles, but no attempt and was tested for use as an oil shale S-3, where the seam was only 0.4 feet has been made to calculate its ton- along Ozark Creek, in Section 27, thick, probably is not representative nage because of the paucity of control T11S, R4E (Barrett 1922). Also, the of the coal where it reaches minable points. No chemical analyses are split Reynoldsburg Coal in borehole thickness. Like coals mentioned available for the Delwood Coal in the S-4 has high ash and extremely high above, the Oldtown Coal may be Creal Springs Quadrangle. sulfur content (table 5). At best, the locally recoverable by surface min- Reynoldsburg presents opportuni- ing. New Burnside Coal Bed The New ties for small-scale strip mining. Burnside Coal underlies most of Sec- tion 7 and parts of Sections 4, 5, 6, (No. 4)) Coal Members. A small area tions 2 and 15, T10S, R6E, contains and 8, T11S, R4E, Creal Springs of Carbondale Formation is mapped three oil wells and one shut-in gas Quadrangle. The New Burnside Coal northwest of the abandoned Brown well. Cumulative oil production

is largely coextensive with the under- Brothers Excavating Company No. 1 through 1983 was about 27,000 bar- lying Delwood Coal and has been Mine in Section 30, T10S, R6E, rels. One well each produces oil from

surface mined with it. The thickness Eddyville Quadrangle. The Brown the Degonia, Waltersburg, and Cyp- varies from a few inches to 54 inches. brothers mined the Davis, Dekoven, ress Sandstones (Chesterian); the gas Exposures inb strip mines (fig. 20) and Houchin Creek Coals and well was completed in the Walters- indicate that rapid lateral thickness explored the remaining reserves burg. Outside the Mitchellsville area, changes, splitting, and local erosion northwest of the mine. The nature of only small and widely scattered hy- are common with this seam. There- the deposits is inadequately defined drocarbon deposits have been found fore, closely spaced test drilling is because of complex faulting and poor south of the Cottage Grove Fault Sys- needed to characterize its reserves exposure. tem in Saline and Williamson Coun- and extent. Chemical analysis (table ties. Most wells had initial produc- Oil and Gas 5) indicates moderate ash and sulfur tions of 20 to 80 BOPD and quickly content and a heating value of nearly A total of 29 oil and gas test wells are declined to less than 10 BOPD. 13,000 Btu/lb. known to have been drilled: 9 each That exploratory success has been in the Eddyi ille and Stonefort Quad- so limited is difficult to explain. Some

Murphysboro Coal Member Coa I rangles and 11 in the Creal Springs operators have noted the lack of por- believed to be the Murphysboro Coal Quadrangle (table 3). Slight shows of osity in reservoir rocks and suggested occurs in a small part of El/2, Section oil or gas were noted in several wells, that pore space was lost because of 8, T11S, R4E, Creal Springs Quad- but none are known to have yielded mineralization or recrystallization. rangle. The seam is not currently commercial quantities of hydrocar- Petrographic studies are required to exposed, but several collapsed mine bons, and all were abandoned. test this idea. As for why the big adits suggest that it is at least a couple All except three of these wells anticlines have not yielded oil, per- of feet thick. The Murphysboro oc- reached total depth in Mississippian haps the many faults and fractures curs 20 to 30 feet above the New rocks (table 3). Most of those drilled allowed it to escape from shallow Burnside Coal, and the two coals before 1950 were drilled with cable reservoirs. Seismic exploration is probably could be strip mined to- tools and finished in strata between needed to evaluate internal structure gether. Elsewhere in the study area, the Palestine Sandstone and the Ste. of these folds, which may not resem- outcrops and borehole data show the Genevieve Limestone. Wells after ble surface structure. Murphysboro to be thin or absent. 1950 were drilled with rotary rigs; most reached the Valmeyeran Ste. Fluorspar and Related Mt. Rorah and Wise Ridge Coals Genevieve or St. Louis Limestones. Minerals

The Mt. Rorah Coal Member under- The Jenkins No. 1 Mohler (well 21, Fluorspar was mined at the Lost lies several square miles in the north- table 3) bottomed in lower Devonian 40 Mine in the Eddyville Quadrangle eastern part of the Creal Springs Clear Creek Chert at a total depth of and at several properties along the Quadrangle and northwestern part 4,250 feet. Two wells drilled by the Lusk Creek Fault Zone adjacent to of the Stonefort Quadrangles and has Texas Pacific Company in the north- the study area. Small amounts of been exploited in numerous small eastern part of the Eddyville Quad- galena, sphalerite, and barite are surface and underground mines. The rangle penetrated sub-Devonian found along with fluorspar (Weller et thickness in this area appears to be strata. The John Wells et al. No. 1 al. 1952). The Lost 40 and other mines consistently about 3 feet. Its gentle (well 2, table 3) bottomed in Silurian were small, shallow operations that dip and topographic position should carbonate at 6,200 feet, and the Mary exploited ore in Pennsylvanian and allow widespread contour and area Streich No. 1 Well (well 7, table 3) upper Chesterian wall rocks. Else- surface mining, but the quality of the finished in upper Cambrian Mt. where in the Illinois-Kentucky fluor- coal is poor. Claystone and shale Simon Sandstone at 14,942 feet. To spar district, the richest vein deposits partings are common, numerous date, this well is the deepest drilled are generally found in lower Ches- claystone dikes were observed in Mt. in Illinois. terian units and in the upper part of Rorah Coal near Brushy Creek, and Most exploration focused on obvi- the Ste. Genevieve Limestone. Thus, the sulfur content is high (table 5). ous structural targets: the McCor- prospects appear good for fluorspar As with all coals of the study area, mick and New Burnside Anticlines. along the Lusk Creek Fault Zone additional drilling and sampling will One or more wells have been placed below the depths currently explored. be required to assess the minability on all large areas of closure on both Lesser possibilities exist for fluor- of the Mt. Rorah Coal. The Wise anticlines. Other wells were drilled spar and related minerals along the Ridge Coal Bed occurs a short dis- on anticlinal flanks, presumably in a McCormick and New Burnside Anti- tance above the Mt. Rorah in most of search for combination stratigraphic/ clines. Normal faults in the McCor- the study area, but has not been structural traps. A few wells are in mick and New Burnside Anticlines observed thicker than 12 inches. synclines. Only two have been apparently have common origin with drilled south of the McCormick mineralized faults in the fluorspar Coals of Carbondale Formation Anticline. district to the southeast. The critical The Carbondale Formation in the Minor production of oil and gas question is whether faults on the study area includes the Davis, Deko- has been achieved north of the study McCormick and New Burnside struc- ven, Colchester (No. 2), Survant, and area. The Mitchellsville field, north tures were accessible to the same Houchin Creek (formerly Summum of the Eddyville Quadrangle in Sec- mineralizing fluids. If these are reac-

78 tivated detached thrust faults, as we The Cave Hill Member probably con- Sandstone occurs throughout the believe, they would connect with tains too much shale to be worth three quadrangles, but similar sand- ore-solution pathways only via a quarrying in the study area. The stone is abundant throughout south- series of decollements in ductile Goreville Limestone Member reaches ern Illinois. In the study area, the shales. Movement of mineralizing 45 feet thick and is less shaly and only likely use for sandstone is as fill fluids along such decollements cherty than the rest of the Kinkaid. for construction projects on location. seems unlikely. It has been quarried in the Walters- Sand and gravel deposits are small, burg Quadrangle less than 1 mile thin, and sporadic. Stream deposits Stone, Sand, and Gravel south of the study area. Nearly the are largely silt and clay, with inter- Stone, sand, and gravel occur within entire thickness of the Kinkaid Lime- mixed sand and rock fragments. the study area, but distance to market stone is quarried on a large scale near Local deposits of sand from weath- and lack of transportation facilities Buncombe in Johnson County, about ered sandstone occur at such sites as render commercial development un- 6 miles southwest of the Creal Sand Hill in the northern part of the likely. However, some of these mate- Springs Quadrangle. The Kinkaid is Stonefort Quadrangle. These sands rials are suitable for local use. less shaly at Buncombe than in the might be usable in small amounts as The Kinkaid Formation contains study area. The Buncombe quarry fill on location. Much better sand and limestone that may be suitable for fill also has the advantage of being gravel deposits, convenient to trans- material, road gravel, riprap, or located along a railroad. The small portation, are being exploited in the agricultural use. The basal Negli deposits of Kinkaid Limestone with- Mississippi Embayment south of the Creek Member, which averages in the study area are remote from study area and in the region of glacial about 30 feet thick, is mostly lime- railroads or good roads. drift to the north. stone, but is argillaceous and cherty.

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Kempton, J. P., 1981, Three-dimen- ical Survey, Bulletin 48, 172 p. quake Region: U.S. Geological sional geologic mapping for Lannon, M. S., 1989, The Quaternary Survey Professional Paper 1236, environmental studies in Illinois: history and surficial geology of the 201 p. Illinois State Geological Survey, Stonefort 7.5-Minute Quadrangle, Miles, C, and B. Weiss, 1978, Soil sur- Environmental Geology Notes southern Illinois: M.S. thesis, vey of Saline County, Illinois: Uni- 100, 43 p. Southern Illinois University, Car- versity of Illinois at Urbana-Cham- King, Philip B. and Helen M. Beik- bondale, 192 p. paign, Agricultural Experiment man, compilers, 1974, Geologic Lannon, M. S., in prep., Geologic Station, Soil Report 102, 94 p. map of the United States: U.S. map of the Quaternary geology of Miller, M. E, 1984, Distribution of Geological Survey, (scale the Stonefort 7.5-Minute Quad- biogenic structures in Paleozoic 1:2,500,000). rangle, Illinois. nonmarine and marine-margin se-

Klasner, J. S., 1982, Geologic map of Lee, W , 1916, Geology of the Shaw- quences: an actualistic model: the Lusk Creek roadless area, neetown Quadrangle in Ken- Journal of Paleontology, v. 58, no. Pope County, Illinois: U.S. Geolog- tucky: Kentucky Geological Sur- 2, p. 550-570.

ical Survey Miscellaneous Field vey, Series 4, v. 4, part 2, 73 p. Nelson, W J., in preparation, Geo-

Studies Map MF-1405-A. Leighton, M. M., and J. A. Brophy, logic map of the Bloomfield Quad-

Klasner, J. S., 1983, Geologic map of 1961, Illinoisan glaciation in Il- rangle, Johnson County, Illinois: Burden Falls roadless area, Pope linois: Journal of Geology, v. 69, Illinois State Geological Survey,

County, Illinois: U.S. Geological no. 1, p. 1-31. map and report.

Survey Miscellaneous Field Stud- Leighton, M. M., G. E. Ekblaw, and Nelson, W J., and H.-F Krausse, ies Map MF-1565-A. L. Horborg, 1948, Physiographic 1981, The Cottage Grove Fault Koeninger, C. A., and C. F. Mans- divisions of Illinois: Journal of System in southern Illinois: Il-

field, 1979, Earliest Pennsylvanian Geology, v. 56, no. 1, p. 16-53; linois State Geological Survey, depositional environments in cen- Illinois State Geological Survey, Circular 522, 65 p.

tral southern Illinois, in J. E. Report of Investigations 129. Nelson, W J., and D. K. Lumm, 1984, Palmer and R. R. Dutcher, editors, Lidiak, E. G., and I. Zietz, 1976, Structural geology of southeastern Depostional and Structural His- Interpretation of aeromagnetic Illinois and vicinity: Illinois State tory of the Illinois Basin, Part 2, anomalies between latitudes 37°N Geological Survey, Contract/Grant Invited Papers: Ninth Interna- and 38°N in the eastern and Report 1984-2, 127 p.

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Survey, Guidebook 15a, p. 76-80. Lineback, J. A., 1979, Quaternary Geological Survey, Contract/Grant

Kolata, D. R., and W. J. Nelson, in deposits of Illinois: Illinois State Report 1985-3, 94 p.

press, Tectonic history of Illinois Geological Survey, map (scale, Nelson, W J., and D. K. Lumm, Basin, in M. W. Leighton, D. R. 1:500,000). 1986a, Geologic map of the Shaw- .

neetown Quadrangle, Gallatin Illinois: University of Illinois at 1958, Chester cross-bedding and County, Illinois: Illinois State Urbana-Champaign, Agricultural sandstone trends in Illinois Basin: Geological Survey, Illinois Experiment Station, Soil Reporl American Association ot Petro-

Geologic Quadrangle Map Series 94, 126 p. leum Geologists Bulletin, v. 42, 1 (1:24,000). Peppers, R. A., 1988, Palynological no. 5, May 1958, p. 1013-1046.

Nelson, W. J., and D. K. Lumm, correlation of major Pennsylva Potter, P. I-., and R. Siever, 1956, 1986b, Geologic map of the Equal- nian (upper Carboniferous) time- Sources Of basal Pennsylvanian ity Quadrangle, Gallatin and Sa- stratigraphic boundaries in tin- sediment in the Eastern Interior

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2(1:24,000). Abstracts with Programs, v. 20, Randall, J. W., 1970, Environment of

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1986c, Geologic map of the Rude- Peppers, R. A., andJ.T Popp, 1979, the Cave I lill Member, Kinkaid ment Quadrangle, Saline C lounty, Stratigraphy of the lower part ol Formation (upper Mississippian) Illinois: Illinois State Geological the Pennsylvania!! System in in southern Illinois: M.S. thesis, Survey, Illinois Geologic Quad- southeastern Illinois and adjacent Southern Illinois University, rangle Map Scries 3 (1:24,000). portions of Indiana and Kentu< ky, Carbondale, 150 p.

Nelson, W. J. and D. K. Lumm, 1987, mil. PalmerandR. R. Dutcher, Raoult, J. F, and F. Meillie/., 1987, Structural geology of southeastern editors, Deposition.il ami Struc- The Variscan Front and the Midi

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Nelson, W. J. and D. K. Lumm, boniferous Stratigraphy and 473-480. L990a, Geologic map of the Ed- Geology, Field Trip 9, Illinois State Rexroad, C. B., and G. K. Merrill, dyville Quadrangle, Illinois: Geological Survey, Guidebook 1985, Conodont biostratigraphy Illinois State Geological Survey 15a, p. 65-72. and paleoecology of middle Car-

IGQ-5, (1:24,000). Petersen, F. A., 1983, Foreland de- boniferous rocks in southern Illi-

Nelson, W. J. and D. K. Lumm, tachment structures, in J. D. nois: C ourier Forschung Institut 1990b, Geologic map of the Lowell and R. Gries, editors, Senckenberg, v. 74, p. 35-64. Stonefort Quadrangle, Illinois: Rocky Mountain Foreland Basins Riggs, M. H., 1990, The surficial Illinois State Geological Survey, and Uplifts: Rocky Mountain As- geologic mappping and Quater- IGQ-6, (1:24,000). sociation of Geologists, Denver, nary history of the Creal Springs Noggle, K. S., 1986, Stratigraphy and Colorado, p. 65-78. Quadrangle, Southern Illinois: structure of the Leavitt Reservoir Pfefferkorn, H. W., 1971, Note on M.S. thesis, Southern Illinois Quadrangle, Bighorn County, Conostichus broadheadi Lesquereux University, Carbondale, 172 p. Wyoming: M.S. thesis, Iowa State (trace fossil: Pennsylvanian): Riggs, M. FL, in prep., Geologic map University, Ames, 97 p. Journal of Paleontology, v. 45, no. of the Quaternary geology of the North American Stratigraphic Code, 5, p. 888-892. Creal Springs 7.5-Minute Quad- 1983, The North American Com- Phillips, T. L., and R. A. Peppers, rangle, Illinois.

mission on Stratigraphic Nomen- 1984, Changing patterns of Rodgers, J., 1963, Mechanics of Ap- clature: American Association of Pennsylvanian coal-swamp vege- palachian foreland folding in Petroleum Geologists Bulletin, v. tation and implications of climatic Pennsylvania and West Virginia: 67, no. 5, p. 41-875. control on coal occurrence: Inter- American Association of Pet- Nuttli, O. W., 1973, The Mississippi national Journal of Coal Geology, roleum Geologists Bulletin, v. 47, Valley earthquakes of 1811-12: v. 3, p. 205-255. no. 8, p. 1527-1536. intensities, ground motion and Potter, P. E., 1957, Breccia and small- Rust, B. R., M. R. Gibling, M. A.

magnitudes: Bulletin of the Seis- scale Lower Pennsylvanian over- Best, S. J. Dilles, and A. G. Mas- mological Society of America, v. thrusting in southern Illinois: son, 1987, A sedimentological 63, no. 1, p. 227-248. American Association of Petro- overview of the coal-forming Oliver, L., 1988, The stack unit leum Geologists Bulletin, v. 41, no. Morien Group (Pennsylvanian), mapping, Quaternary stratig- 12, December 1957, p. 2695-2709, Sydney Basin, Nova Scotia, raphy, and engineering properties 12 figures. Canada: Canadian Journal of of the surficial geology of the Potter, P. E., 1963, Late Paleozoic Earth Sciences, v. 24, p. 1869-1885. Waltersburg 7.5-Minute Quad- sandstones of the Illinois Basin: Schwalb, H. R., 1982, Paleozoic rangle, Pope County, Illinois: M.S. Illinois State Geological Survey, geology of the New Madrid area: thesis, Southern Illinois Univer- Report of Investigations 217, 92 p U.S. Nuclear Regulatory Commis- sity, Carbondale, 149 p. Potter, P. E., and H. D. Glass, 1958, sion, NUREG CR-2909, 61 p. Owen, D. D., 1856, Report on the Petrology and sedimentation of Shaver, R. FL, and others, 1986, geological survey in Kentucky the Pennsylvanian sediment in Compendium of Paleozoic rock- made during the years 1854 and southern Illinois: a vertical profile: unit stratigraphy in Indiana - a 1855: Kentucky Geological Survey Illinois State Geological Survey, revision: Indiana Geological Bulletin, Series I, v. 1, 416 p. Report of Investigations 204, 60 p. Survey Bulletin 59, 203 p. Parks, W, 1975, Soil Survey of Pope, Potter, P. E., E. Nosow, N. M. Smith, Shaw, E. W, 1915, Newly discovered Hardin, and Massac Counties, D. H. Swann, and F. H. Walker, beds of extinct lakes in southern

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Murray Bluff Sandstone Member, upper Abbott Formation, just east of the type locality. Strata dip northwest (left) on flank of New Burnside Anticline.