GEOLOGY of the W M T E RANGLE POPE COUNTY, ILLINOI

Home , Beech Creek Limestone, Degonia Formation, Golconda Formation, Grove Church Shale, Kinkaid Limestone, Vienna Limestone

GEOLOGY OF THE WmTE RANGLE POPE COUNTY, ILLINOI

C. Pius Weibel .W. John Nelson Lynne B. Oliver .Steven P. Esling

Department of Energy and Natural Resources ILLINOIS STATE GEOLOGICAL SURVEY

BULLETIN 98 1993 Southern Illinois University at Carbondale

BULLETIN 98 1993

ILLINOIS STATE GEOLOGICAL SURVEY Morris W. Leighton, Chief 615 East Peabody Drive Champaign, IL 61820-6964 Cover photo Pounds Sandstone Member of the Caseyvllle Formation southwest of Rock in Pope County (photo by C. Pius Weibel)

Printed by authority of the State of Illinois/1993/1200 ACKNOWLEDGMENTS ABSTRACT 1 INTRODUCTION Location Physiography Geologic Setting Previous Studies Method of Shrdy BEDROCK STRATIGRAPHY Mississippian System Undifferentiated Pope Group Golconda Formation Hardinsburg Sandstone Glen Dean Limestone Tar Springs Sandstone Vienna Limestone Waltersburg Formation Menard Limestone Palestine Sandstone Clore Forma tion Degonia Formation Kinkaid Limestone Mississippian-Pennsylvanian Unconformity Pennsylvanian System Caseyville Formation Wayside" Member Battery Rock Sandstone Member "Drury" Member Pounds Sandstone Member Tradewater Formation Lower shale and sandstone member Middle sandstone member Upper shaley member SURFICIAL GEOLOGY Introduction Methodology Field Methods Laboratory Methods Construction of the Stack-Unit Map Stratigraphy Lithostratigraphic Units: Upland Formations Oak formation Roxana Silt Peoria Silt Peyton Formation Lithostratigraphic Units: Valley Formations Equality Forma tion Cahokia Alluvium Pedostratigraphic Units Sangarnon Soil Farmdale Soil Buncombe Soil Resources Land Use Waste Disposal General Construction Seismic Risk STRUCTURAL GEOLOGY Lusk Creek Fault Zone Raum Fault Zone Hobbs Creek Fault Zone Flick Branch Fault Other Faults History and Origin of Faulting ECONOMIC GEOLOGY Fluorspar Limestone Sandstone Clay Petroleum Coal REFERENCES

FIGURES Cooperative Geological Mapping Program (COGEOMAP), January 1993 Cultural features and drainages of the Waltersburg Quadrangle Map showing major structural features and the Illinois-Kentucky Fluorspar District in the vicinity of the Waltersburg Quadrangle Graphic column of Abner Field No. 1Well Graphic column of U.S. Government No. 1Well Graphic column of Truebger No. 3 Well Graphic column of COGEOMAP W-3 Well Basal chert bed of Degonia Forma tion Graphic column of Goreville Limestone Member of Kinkaid Limestone from an abandoned quarry Graphic column of U.S. Forest Service Eddyville guard station well Field sketch of deformed shale and thin bedded sandstone in "Wayside" member of Caseyville Formation Graphic column of COGEOMAP W-1 Well Graphic column of COGEOMAP W-2 Well Graphic column of "Drury" member of Caseyville Formation Pounds Sandstone Member of Caseyville Formation Graphic columns of measured sections in the Tradewater Formation within the Dixon Springs Graben Stratigraphic classification of the Quaternary deposits in the Waltersburg Quadrangle General locations of borings Vertical distribution of clay minerals and particle sizes for borhgs W2, W7, W3, W16, and W17 Cross section showing the distribution of the Quaternary ~tsin Flat Lick Valley Vertical distribution of clay minerals and particle sizes for borings W10, W12, and W9 Cross sections of Lusk Creek Fault Zone Cross sections of Raum Fault Zone Field sketch of deformed Tradewater strata in a stream bank Interpretive sketch of deformed Pounds Sandstone and Tradewater strata Origin of upthrown and downthrown slices in Lusk Creek Fault Zone Interpretive structural history of the Waltersburg Quadrangle

1 Location of wells used for bedrock study 7 2 Relation between modern soil series and Quaternary map units 23 3 Locations of borings 24 4 Chemical analyses of of channel sample of Tunnel Hill(?) Coal 38

The U.S. Geollogicd Survey (USGS), under the Cooperative Geological Mag- ping Program (COGEOMAP), provided significant support for the research reported in this publication. Annual grants from 1985 through 1991 provided partial funding for the project, Geologic Mapping Along the Southern Clo- sure of the Illinois Basin. The geologic mapping of sixteen 7.5-minute quadrangles and the publication of quadrangle maps (1:24,OUO scale) and the accompanying reports were the objectives of this project. Joseph A. Devera (ISGS) mapped a part of the bedrock in the northwest comer of the quadrangle. Russel Peppers (ISGS) analyzed the palynology of the coals and provided biostratigraphic data. James W. Baxter (ISGS), Russell J. Jacobson OSGS), and Charles M. Rice (USGS) carefully critiqued the geologic map. Heinz H. Damberger, as project leader of COGEOMAP, provided continuous encouragement and advice. Finally, we are grateful to the private landowners who allowed us to enter their property to examine outcrops and especially to those who allowed us to drill the stratigraphic tests.

Bedrock outcrops of the Waltersburg Four northeast-trending parallel the fault zones, occur between these 7.5-Minute Quadrangle in Pope fault zones transect the quadrangle. WOfault planes. County, southeastern Illinois, con- These post-Pennsylvanian faults are The principal mineral. resources sist mainly of upper Mississippian part of a regional northeast-trending in the quadrangle are sandstone for (Chesterian) and lower Pennsyl- fault system in the west part of the construction and limestone for con- vanian (Morrowan to early Atokan) Illinois-Kentucky Fluorspar District. struction and agriculture. Small strata. The Chesterian strata consist The Lusk Creek Fault Zone bounds shallow deposits of fluorspar and as- of fine grained clastic rocks and the northwest side of the Dixon sociated minerals have been mined limestones of the upper Pope Group Springs Graben, and the Hobbs locally, suggesting that unknown and include the Golconda Forma- Creek Fault Zone bounds the south- deeper resources may occur along tion up to the Kinkaid Limestone. east side. The Raum Fault Zone par- faults in the quadrangle. The The Pennsylvanian strata consist of allels the Lusk Creek and Hobbs amount of coal resources is small; the sandstonedominated Caseyville Creek Fault Zones and bisects the coal beds are too thin and discon- and Tradewater Formations. Upper Dixon Springs Graben. The Flick tinuous to exploit economically, al- Valmeyeran limestones occur within Branch Fault (new name) occurs though a few small coal mines have thin fault slices. A petroleum explo- southeast of the Hobbs Creek Fault operated in the past. Three explora- ration well reached the Devonian Zone. The geologic structure of the tion wells for oil and gas have been Lingle Limestone, the oldest known quadrangle is the result of several drilled and all were abandoned. Res- bedrock in the Waltersburg Quad- episodes of deformation. Rifting dur- ervoir characteristics of buried, pre- rangle. The well also drilled through ing the Cambrian Period resulted in upper Mississippian strata are the New Albany Shale, several normal faulting along the Lusk unknown within the quadrangle. lower (Kinderhookian) and middle Creek Fault. Additional normal fault- Laterally extensive aqtlifers and (Valmeyeran)Mississippian forma- ing may have occurred during the economic deposits of sand and tions, and the lowermost Pope Early Pennsylvanian. A post-at oh gravel aggregate are not present Group. compressional episode resulted in re- among the surficial materials. The Extensive Pleistocene (Illinoian verse faulting along the Lusk Creek geology of the area is unsuitable for and Wisconsinan) deposits cover and Raum Fault Zones (which landfills unless measures are taken much of the bedrock. The uplands merge at depth). Final deformation to prevent migration of leachate. are covered by bedrock residuum was an extensional episode, during Properly designed construction pro- (Oak formation) and loess (Roxana which normal faulting occurred jects can be sited throughout most of and Peoria Silts): the slopes by collu- along the same fault planes or along the quadrangle. The study area lies vium (Peyton Formation), and the adjacent fault planes. Narrow slices in a zone of high seismicity; struc- valleys by lacustrine (Equality For- of rock, which are older or younger tures built in valley bottoms are mation) and alluvial deposits (Ca- than the strata on adjacent sides of more at risk than structures having hokia Alluvium). foundations in bedrock.

This study was conducted as part of larly of the Caseyville Formation. and E 1/2 SE, Section 11, T12S, R6E. the ongoing Cooperative Geologic Streams eroding the Pennsylvanian Upland exposures of Mississippian Mapping Program (COGEOMAP), and thick Mississippian sandstones strata are generally above 500 feet which is jointly supported by the have formed narrow valleys or can- rnsl; exposures of Pennsylvanian United States Geological Survey yons, whereas those eroding Missis- strata are generally above 600 feet (USGS) and the Illinois State Geo- sippian limestones, shales, and msl. Bottomlands are generally be- logical Survey (ISGS). This report is thin sandstones have formed broad, tween 350 and 400 feet msl. The low- a companion to the Waltersburg Geo- open valleys. Thicker Mississippian est elevation is less than 320 feet rnsl logic Quadrangle of Weibel et al. limestones are locally characterized in the southeast corner of the quad- (1992) and is one of a series of ISGS by a karst topography and drainage rangle along Eusk Creek. Total relief maps and reports on the geology of system. is 460 feet, although local relief is southern Illinois (fig. 1). This geo- The highest elevations in the typically only 150 to 300 feet. logic mapping will increase our quadrangle are more than 780 feet Lusk Creek, flowing from the understanding of the region and pro- above mean sea level (msl) and are north edge to the southeast comer of vide data useful for land use plan- in the S 1/2 SE, Section 26, TI%, the quadrangle, drains most of the ning, geologic hazard assessment, R6E; SE SW, Section 26, T12S, R6E; quadrangle and joins the Ohio River and mineral resource and groundwater exploration.

P SALINE The Waltersburg 7.5-Minute Quad- rangle is in extreme southeastern Illi- nois between latitudes 37O22'30" and 370301N and longitudes 88'30' and 88"37'3O1'W. Highway access to the area is provided by Illinois route 145 from Eddyville to Glendale in the northwest quarter, Illinois 146 from Dixon Springs to Golconda in the west half along the south edge, and the paved county road from Eddy- ville to Golconda in the east two- thirds of the quadrangle (fig. 2). The B Bloomfield only incorporated village in the CB Cobden quadrangle is Eddyville, which CS Creal Springs straddles the north edge. Only a few buildings are present in the unincor- ED ~dd&ille porated villages of Raum, Rising EQ Equality 1 n GL Glendale Sun, Rock, and Waltersburg. About Goreville two-thirds of the land in the quad- Gorham rangle is privately owned, and most Jonesboro of the rest is part of the Shawnee Na- Published before 1968 Lick Creek tional Forest. Makanda Published after 1985 McClure Y Mapping and compilation completed, Mill Creek The quadrangle is within the under review Rudement Shawnee Hills Section (Leighton et Mapping in progress Shawneetown al. 1948) of the Interior Low Plateaus Stonefort Province (Fenneman 1938), an area Limit of Pennsylvanian System Tamms that contains some of the most rug- Major fault Thebes ged topography in Illinois. The area Waltersburg consists of a dissected plateau, and Ware within the quadrangle, the higher Wolf Lake ridges are generally composed of Pennsylvanian sandstone, particu- 1 Cooperative Geological Mapping Program (COGEOMAP),January 1993. zoic rode were mapped only as undifferentiated Mississippian or Pennsylvanian strata. S. Weller (1920a) described the geology of Hardin County and included detailed descriptions of upper Pvf[ississippian and lower Pennsylvanian strata. His geologic map included a part of Pope County just east of Waltersburg Quadrangle, but only the geology of Hardin County was described. S. Weller (1920b) referred to localities within the Waltersburg Quadrangle in his report on th per Mississippian strata of sou Illinois. Bastin (1931) reported the types and origins of ore deposits and their mineralogical compositions in Hardin and eastern Pope County. He also discussed mining and milling methods. A preliminary geologic map of the Brownfield 15-Minute Quadrangle by S. Weller and Krey (1939) included the Waltersburg Quadrangle. The map was compiled from unpublished manuscripts. Although preliminary, S. Weller and Krey's geologic map was the most detailed of the quadrangle prior to this study The report on the Figure 2 Cultural features and drain- IpJ spar deposits of Illinois by J. ages of the Waltersburg Quadrangle. 0 3 km et al. (1952) is a compilation of surveys undertaken in response to in- at Golconda, Illinois. Abrupt angu- defined by Willman and Frye (1980). creased demand by war-related lar bends in the valley indicate that Unconsolidated material consists of industries. The geologic map was bedrock structure controls the Quaternary alluvium, bedrock resid- largely adapted from S. Weller course of Lusk Creek. A divide east uum, colluvium, lacustrine sedi- (1920a).The bulk of the report de- of the creek extends from the north- ments, loess, and talus. Strata gen- scribed exploration, mining, and east comer of the quadrangle south- erally dip gently to the northwest milling methods, as well as the geol- west to Raum, and thence south- toward the Fairfield Basin part of ogy of the mining districts. southeast to the southeast corner. the Illinois Basin. The quadrangle is As part of a program to remap Streams east of the divide flow into transeded by northeast-trending the Illinois portion of the fluorspar Big Grand Pierre Creek. A divide faults that are part of the Fluorspar mining district, Baxter et al. (1967) west of Lusk Creek separates Lusk Area Fault Complex. mapped and described the areal Creek drainage from Bay Creek geology of two 7.5-minute quadran- drainage. The valley of the Flat Lick gles adjacent to the Waltersburg: Branch of Bay Creek occupies the The first geological reconnaissance the Herod to the northeast and the extreme southwestern part of the of the study area was accomplished Shetlerville to the east. Hook (1974) quadrangle. Hayes Creek, in the by geologists of the Geological Sur- compiled a generalized geologic northwest quarter, is part of the Bay vey of Illinois under the leadership map that included the Waltersburg Creek drainage. All three drainages of Amos Worthen. Engelmann Quadrangle; he also described the flow into the Ohio River east or (1866a) described the areal geology structural geology of the Illinois- southeast of the quadrangle. north of Bay Creek in Pope County. Kentucky Mining District. Pinckney The report remains useful because it (1976) summarized the geologic Geologic Setting contains many outcrop descriptions, setting and mineral deposits of the The quadrangle is in the southem- although a geologic map was not in- Illinois-Kentucky mining district. most part of the Illinois Basin and in cluded and the descriptions of litho- His geologic map included the Wal- the western part of the Illinois-Ken- logic subdivisions were cursory. The tersburg Quadrangle, but it also was tucky Fluorspar District (fig. 3). Out- first systematic areal report on the compiled from previous publica- cropping bedrock formations range stratigraphy structure, ore deposits, tions. Nelson and Lumm (1990a, b) from upper Mississippian (middle and mines of the area included a mapped the geology of the adjacent Chesterian) to lower Pennsylvanian generalized geological map (Bain quadrangles to the north (IEddyville) (Atokan). The quadrangle lies south 1905). The Waltersburg Quadrangle and to the northwest (Stonefort). of the Illinoian glacial boundary as is depicted on this map, but Paleo- The geology was described in SALINE GALLATIN UNION

Figure 3 Map showing major structural features and the Illinois-Kentucky Fluorspar District (light red) in the vicinity of the Waltersburg Quadrangle (gray).

Nelson et al. (1991). The Glendale completed in the fall of 1989. Out- samples fiom petroleum and min- Quadrangle, which borders on the crop data were recorded in field eral exploration wells. The logs and west of the Waltersburg Quadran- notes and on topographic maps. cores are available for examination gle, was also mapped as part of Field notes were typed and are avail- in the ISGS Geological Records and COGEOMAP (Devera 1991). able for examination in the ISGS Samples Library. The methods used library. Subsurface data consist of for mapping of the surficial geology geophysical logs and cores from are described in the section on surfi- Bedrock mapping for this study three stratigraphic tests drilled as cia1 geology. began in the fall of 1985 and was part of COGEOMAP and logs and The oldest known bedrock stratum thickness of Valrneyeran strata is about 200 feet wide and entirely in the Waltersburg Quadrangle is 1,915 feet. Overlying the Valrney- composed of limestone (Bain 1905). the Devonian Lingle Limestone. The eran is the upper Mississippian The quarry exposes about 50 to 100 youngest bedrock strata belong to (Chesterian)Pope Group, described feet of limestone dipping steeply the Pennsylvanian Tradewater For- in a following section. to the southeast. The exposure is mation. The upper Mississippian extensively faulted, fractured, and Golconda Formation is the oldest mineralized, and the bedding is outcropping formation, except for Undifferentiated Mississippian obscure. On the southeast side of the small outcrops that may include rocks in the Waltersburg Quadran- exposure is a light gray well indu- upper Valmeyeran rocks. gle occur in several small fault rated calcilutite containing nurner- The Austin Roberts No. 1Well slices. These rocks include poorly ous light colored chert nodules. penetrated 462 feet of Lingle Lime- exposed or deformed rocks that lack Northwest of this unit is light to stone (well locations are given in the diagnostic characteristicsused medium gray limestone that weath- table 1). Core descriptions indicate for referral to a specific formation. ers medium to dark gray. It is a fine the Lingle is a tan to light gray, fine This category also includes rocks to medium grained biocalcarenite grained limestone that contains that can be assigned to specific for- with a sparite cement and is locally chert. mations but the map scale precludes oolitic. Macrofossils include pelma- The Lingle is overlain by the New delineation of individual units. tozoan fragments and rugose corals, Albany Shale. The middle to upper A small fault slice along the Lusk which are not age diagnostic. Cono- Devonian Blocher Shale Member of Creek Fault Zone in the SW, Section donts (Cavusgnathus unicornis, the New Albany is 57 feet thick and 30, T12S, R6E, consists of poorly Khdagnathus tenuis, and Larnbhg- consists of a silty, calcareous shale. exposed, steeply dipping limestone. nathusfragilidens) extracted from this The upper Devonian Sweetland The limestone is a gray to dark gray, limestone range from late Valmey- Creek Shale and Grassy Creek Shale coarse grained biocalcarenite that eran to Chesterian Age (Norby, per- Members are 132 and 124 feet thick, contains oolites and rudaceous bio- sonal communication, 1989). This respectively. Both members are char- clasts. The absence of diagnostic lithologic succession does not occur acterized by black shale, but the lithologic characteristics and the in the upper Mississippian Pope older Sweetland Creek also contains small, isolated exposure preclude Group. Several formations in the gray shale. These members are over- referral to a specific unit. The lime- lower part of the group contain light lain by the upper Devonian Saver- stone is probably an Upper Val- colored bioclastic and oolitic lime- ton Shale Member, which is not meyeran to Middle Chester forma- stone, but they are less than 50 feet differentiated from the younger tion. thick or contain shale. The lithologic Hannibal Shale Member on geo- A long faultslice block in the cen- succession is characteristic of the St. physical logs of the Austin Roberts ter of the Lusk Creek Fault Zone Louis Limestone and the overlying No. 1Well. from the east edge of Section 20 to lower part of the Ste. Genevieve. Section 3, TI25 R6E at the north White to light gray, bioclastic, edge of the quadrangle is mapped and oolitic calcarenite also occurs MISSISSIPPIAN SYSTEM as undifferentiated Mississippian. within this fault slice between the The lowermost Mississippian (Kin- Strata within this block range from Clay Diggings Mine and Copperous derhookian) strata in the quadrangle St. Louis(?)Limestone up to Kinkaid Branch. This limestone is strati- is the Hannibal, the uppermost Limestone, but a complete succes- graphically below the Glen Dean member of the New Albany Shale. sion is probably not present. The Limestone and is probably part of The undifferentiated Saverton and best exposure occurs at an aban- the Ste. Genevieve. Hannibal Shales are 11 feet thick. doned quarry at the Clay Diggings Rocks provisionally assigned The Kinderhookian Chouteau Lime- Mine, NW NE SE, Section 16, TI%, to Vienna, Palestine, Menard, and stone, a light gray fine grained lirne- R6E. Bain (1905) briefly described Kinkaid Formations crop out in a stone, is only 6 feet thick in the this locality and considered the lime- northeast-trending ravine in the NW Austin Roberts No. 1Well. The over- stone to be St. Louis. Diffenbach NE, Section 10, T12S, R6E in this lying middle Mississippian (Valmey- (personal communication, 1985), a fault slice. A Vienna-to-Kinkaid eran) strata consist of the following geologist at a fluorspar mining com- sequence is probably not present formations, in ascending order: pany interpreted the limestone to be because of small displacements by Springville Shale, Fort Payne Forma- Ste. Genevieve and/or St. Louis. several faults. The limited extent tion, Ullin Limestone, Salem Lime- Cores of several angled exploratory and intermittent exposures preclude stone, St. Louis Limestone, and Ste. holes drilled through the fault block mapping of individual formations. Genevieve Limestone. The total at the mine indicated the block to be A small area of undifferentiated Mis- sissippian rocks occurs north of the Illinois, just southeast of the Walters- Clay Diggings Mine and adjacent to burg Quadrangle. McFarlan et al. Cliff-forming sandstone that crops the Lusk Creek Fault Zone. These (1955) elevated the Golconda to a out only near the southeast corner of strata colasist of the uppermost group, but herein it is referred to as the quadrangle is referred to as the Clore, Degonia, and lowermost a formation. The formation consists Hardinsburg Sandstone. Brokaw Kinkaid. This sequence probably is of the basal Beech Creek Limestone (1916) first used the name Hardins- compressed as a result of drag fold- Member, the Fraileys Shale Member, burg in a stratigraphic column; the ing along the Lusk Creek Fault Zone. and the Haney Limestone Member. name was based on descriptions Only the Haney is exposed in the and measurements by S. Weller. Waltersburg Quadrangle. Butts (1917) formally introduced the The Pope Group comprises strata name 'Hardinsburg Sandstone" for from the base of the Aux Vases Sand- Haney Limestone exposures near Hardinsburg in stone to the top of the Kinkaid McFarlan et al. (1955) originally Breckinridge County, north-central Formation. The Pope Group is a named the Haney Limestone Mem- Kentucky. lithostratigraphic unit distinct from ber as a formation for exposures The Hardinsburg is predomi- its chronostratigraphic counterpart, along Haney Creek, in Hardin County nantly a fine grained sandstone con- the Chesterian Series. The lower The upper part of the Haney is sisting of subrounded, well sorted boundary of the Chester Series mapped only in the extreme south- quartz grains. Dark minerals and (Swann 1963, Maples and Waters east corner of the quadrangle. Its oc- mica are rare and probably consti- 1987) differs slightly from the Pope currence was extrapolated from the tute less than 1%of the rock. A few Group. The group is about 1,425 feet map of Baxter et d.(1967) because grains have clay coatings. The well thick in the quadrangle, but the low- the bedrock is covered at this local- indurated sandstone is white and ermost Pope formations, from the ity, Baxter et al. described the Haney light gray and weathers orange Aux Vases Sandstone up to the as a 15- to 50-foot-thick limestone brown to gray Low-angle trough Fraileys Shale, do not crop out in the containing interbedded shale and, in crossbeds are prevalent, and ripple Waltersburg Quadrangle. This inter- some places, 10 feet of green gray marks and soft-sediment deforma- val is 384 feet thick in the Austin calcareous shale at the top. The up- tion structures also occur. Bedding Roberts No. 1Well. per contact with the Hardinsburg is planes are generally wavy, and beds not exposed in the quadrangle. Bax- are often lenticular. Beds generally a Fs Butts ter et al. (1967) described the contact range from 0.3 to 1foot thick. (1% 7) named the Golconda Forma- as ranging from transitional to a dis- The lower part of the unit crops tion for exposures near Golconda, conformity. out in ledges 5 to 15 feet high,

Table 1 Location of wells used for bedrock study. Well and Sample base and ISGS county no. and company well type total depth (ft) - Abner Field No. 1 NWc, SE, SE, Core Co. 108 Abner Field Sec. 19, TI3S, R6E Petroleum test TD 777 Austin Roberts No. 1 NW NE SE, SE, Cuttingslgeophysicallogs Co. 244 C. E. Williams Sec. 10, TI3S, R6E Petroleum test TD 3,802 Harold Clanahan No. 1 NW, SW SW Drillers log Co. 182 F. Bolin and N. B. Butler SE, Sec. 25, TI3S, R5E Petroleum test TD 1,100 COGEOMAP W-1 2070 FSL, 1590 FEL, Core Co. 2041 9 ISGS Sec. 14, T12S, R6E Stratigraphy test TD 166 COGEOMAP W-2 2320 FNL, 350 FEL, Core Co. 20420 ISGS Sec. 15, TI2S, R6E Stratigraphy test TD 166 COGEOMAP W-3 15 FWL, 70 FNL, NE, NE, Core Co. 20424 ISGS Sec. 9, T12S, R6E Stratigraphy test TD 280.1 Minton-Baker No. 1 NW NW NE, NE, Core Co. 206 Robert L. Minton Sec. 24, T13S, R5E Petroleum test TD 610 U.S. Government No. 1 250 FWL, 20 FSL, NW, SW, Core Co. 206 Eddleman and McKee Sec. 1, TI3S, R6E Mineral test TD 141.4 Voslow No. 1 NEc, SE, SE, Cuttings log Co. 107 Rodger, Barger, et al. Sec. 18, T13S, R6E Petroleum test TD 1,000 Truebger No. 3 400 FSL, 1600 FEL Core Co. 209 - Sec. 35, TI2S, R6E Mineral test TD 159.5 U.S. Forest Service- 132 FSL, 396 FWL, SE Cuttings log Co. 77 Eddyville Guard Station Sec. 6, T12S, R6E Water well TD 257 Floyd lngram

- --- a NWc: northwest corner; 2070 FSL, 1590 FEL: 2070 feet from the south line and 1590 feet from the east line.

7 whereas the upper part is poorly ex- feet. The core from the Abner Fie1 1 posed. In the adjacent Shetlerville surficial No. Well, just south of the quad- and Herod Quadrangles, Baxter et 1'rangle, contains 52.6 feet of Glen al. (1967) similarly characterized the Dean Limestone (fig. 4). formation as having a lower unit of physical log of the Haro "a prominent ridge-forming sand- No. 1Well, about 1.5 m Tar Springs stone" and an upper unit containing Sandstone the quadrangle, recorded 90 feet of poorly exposed shale. The upper Glen Dean. contact with the overlying Glen Dean Limestone is not exposed in the Waltersburg Quadrangle, but Baxter et al. (1967) described it as an "abrupt change" from gray shale in Glen Dean the uppermost Hardinsburg to lime- Limestone stone of the Glen Dean. The best exposures of the Har- (1857) first referred to outcrops sou dinsburg are in bluffs northeast of of Cloverport in Breckemidge County Eusk Creek and in a southwestward Kentucky, as the "Tar Spring sand- flowing tributary to the creek (SW, stone." The name " Section 13; SE, Section 14; W,Sec- stone" was introduced tion 24, T13S, R6E). In this area, the Hardinsburg (1916) in a description lower part of the sandstone forms Sandstone graphic column; he b the bluff facing Lusk Creek. on descriptions and meas- Wells within the quadrangle were S. Weller. The formation was either drilled through the formation in areas where faulting is prevalent or did not penetrate the entire forma- Haney tion. Baxter et al. (1967) reported a Limestone stone, composed of subangular to thickness of 90 to 115 feet in the adja- subrounded, well sorted, quartz grains. Medium to coarse grains are cent Shetlerville and Herod Quad- Figure 4 Graphic column of up- rangles. About 6 miles north of the per part of core from Abner Field present locally. Siever (1953) petro- quadrangle, the Mary L. Streich No. No. 1Well, located south of Wal- graphically analyzed four samples 1Well drilled through 105 feet of tersburg Quadrangle. of the Tar Springs and determined Hardinsburg Sandstone. that the dominant constituent was because the formation is poorly ex- quartz (80-95%).He also found clay e Lime- posed and generally covered by (1-lo%), carbonate (1-2x1, chert stone succeeding the Hardinsburg vegetation and talus from the over- (1-2%) feldspar (0-2%), and traces Sandstone and overlain by the Tar lying Tar Springs Sandstone. The of heavy minerals. The generally Springs Sandstone is referred to as best of the few exposures are in the well indurated sandstone is white the Glen Dean Limestone. Butts SE, Section 14, T6E, R13S, at the foot to tan and weathers light orange (1917) named the formation for ex- of large talus blocks and high ledges posures along the railroad at Glen on the northeast side of Lusk Creek. Dean in Breckinridge County, north- The limestone is susceptible to disso- es central Kentucky. The Glen Dean, lution by groundwater; thus, sink- from 0.1 to more than 2 feet thick like the Hardinsburg, crops out only holes are common. Sinkhole occur- and is locally lenticular with wavy near the southeast corner of the rences were used as reference points bedding planes. The lower part of quadrangle. to map the unit in the SW, Section the Tar Springs is generally well ex- The Glen Dean Limestone is gray 13, T6E, R13S, where exposures are posed and forms bluffs up to 30 feet to dark gray and weathers gray. It is absent. high. The heights of sandstone bioclastic to locally oolitic limestone The upper contact of the Glen ledges decrease and the percentage and is a moderately sorted, fine to Dean is not exposed in the Walters- of interbedded shale and siltstone very coarse grained biocalcarenite. burg Quadrangle. Baxter et al. (1967) increases upward through the for- Common fossils, often fragmented, described it as an unconfonnity, mation. include pellmatozoans, mgosan cor- with the Tar Springs extending als, Pentremites, bryozoans, and downward in places into the Glen brachiopods, including Composita. Dean. The thickness is estimated to Bedding ranges from 0.2 to 2 feet be about 50 to 60 feet. In the subsur- thick and rarely includes low-angle face, thicknesses are more variable, crossbeds. Baxter et al. (1967) differ- probably because of the nature of silt occurs in beds up to 0.1 foot entiated three ~tswithin the for- the upper contact. The drillers' log thick and, in some places, contains mation: a lower unit of fossiliferous of the Minton-Baker No. 1Well, prevalent mica, carbonaceous plant limestone, a middle calcareous located in Section 24, T13S, R5E, in- fragments, and ripple marks. Baxter shale, and an upper interbedded dicated a thickness of 59 feet. A geo- et al. (1967) characterized the upper limestone and shale. These units physical log of the Austin Roberts part of the formation as shale con- are not differentiated in this study No. 1Well recorded a thickness of 79 taining some carbonaceous beds and rare thin coals in the Shetlervdle poor and typically recognized by the and Herod Quadrangles. A coal near presence of float. The float generally the top of the Tar Springs crops out consists of brown chert and tripoli in a ravine near the NW corner of nodules that contain abundant fossil WE NW, Section 21, T13S, R6E (Bax- fragment molds. The best exposure ter, personal communication, 1991). is in a ravine, just south of Illinois The best exposures of the lower 146, in the NE NW NE NE, Section part of the formation are in Section 20, T13S, R6E. In this area, the lime- 14; S1/2, Section 15; NE, Section 21; stone marks the edge of low pla- and N 1/2 N 1/2, Section 22, T13S, teaus formed on the underlying Tar R6E. The best exposures of the up- Springs Sandstone and is generally Menard per part are a cut bank and an out- slumped. North of Lusk Creek, the Limestone crop adjacent to the road on the Vienna crops out in poor exgosures northwest side of a ravine near the on the dip slope of the Tar Springs southwest corner of Section 12, and is recognized only on the basis T13S, R6E. The upper contact of the of its distinctive float. Tar Springs is not exposed. Baxter et The upper contact is not exposed al. (1967) described the conformable in the quadrangle. The core from contact with the overlying Vienna U.S. Government No. 1Well indi- Limestone as relatively sharp. The cates that the contact is abrupt; how- Tar Springs ranges from 100 to 130 ever, Baxter et al. (1967) described feet thick, an estimate based on out- the upper contact as transitional. An crop study and subsurface data. The incomplete exposure of the lime- drillers' log of Minton-Baker No. 1 stone in the Waltersburg Quadran- Well recorded a thickness of 115 feet. gle is 12 feet thick. Mapping of A geophysical log of the Austin exposures and associated float indi- Roberts No. 1Well recorded 110 feet. cate this limestone is 15 to 25 feet South of the quadrangle, the geo- thick. Subsurface data indicate, Naltersburg Ly-.: physical log of the Harold Clanahan however, that the formation locally Formation - - No. 1Well recorded 100 feet of Tar attains thicknesses of more than 30 Springs Sandstone. feet. The drillers' log from the Vos- low No. 1Well recorded 30 feet of Vi- enna Limestone. The Vienna in the cherty limestone separating the Tar US. Government No. 1Well is 19.6 Springs Sandstone and the Walters- feet thick (fig. 5); however, the well burg Formation is referred to as the was drilled close to a fault. Vienna Limestone. S. Weller (1920b) introduced the name for exposures er Fo of interbedded limestone and shale poorly exposed interval of fine Vienna near Vienna in Johnson County, grained sandstone, siltstone, and Limestone southern Illinois. Swam (1963) re- shale overlying the Vienna Lime- vised the formation, restricting the stone and underlying the Menard unit to include only the middle lime- Limestone is referred to as the Wal- stone part, and assigning the under- tersburg Formation. S. Weller Tar Springs - - - lying and overlying shale to the Tar (1920a) first recognized the 'Walters- Sandstone LyyA Springs and the Waltersburg, resgec- burg sandstone" as one of two for- tively. The outcrop pattern of the mations (Vienna Limestone is the other) that are intercalated between limestone is a thin stripe in the Figure 5 Graphic cohnn of southeast quarter of the quadrangle. the Tar Springs Sandstone and core from U.S. Government No. 1 The Vienna Limestone consists of Menard Limestone. S. Weller re- Well in Section 1, T13S, R6E. generally fine grained limestone; it ferred to exposures at Waltersburg is bioclastic and contains abundant as the type area. S. Weller (1920b) Formation, Shale, or Sandstone, but ap- chert nodules. The gray to gray later described the formation as "a peared to favor Formation. Outcrop brown limestone weathers gray to conspicuous sandstone formation" study and subsurface data indicate light gray and varies locally from in Pope and Johnson Counties and that the lithology is variable and For- calcilutite to coarse grained calcar- specified the type locality as expo- mation is the appropriate descrip- enite. Chert is a diagnostic charac- sures "in the road just north of Wal- tive term in the Waltersburg teristic of the formation. In outcrops, tersburg." Presumably this locality Quadrangle. it occurs as gray to brown, irregular (west edge, NW SW SW, Section 16, Outcrops of the Waltersburg are to lenticular nodules and commonly T13S, R6E) is the abandoned road predominantly light tan to light weathers to tripoli. Pelmatozoan bed west of and parallel to the pre- brown, very fine to fine grained and bryozoan fragments are com- sent road. The outcrop is completely sandstone that weathers gray to mon fossils. Beds range from 0.4 to covered by vegetation. Swann (1963) dark orange brown. The moderately 1.2 feet thick. In this quadrangle, out- listed, without clarification, the de- to well indurated sandstone is com- crops of the Vienna are generally scriptive term of the Waltersburg as posed of subangular to subrounded, moderately sorted, quartz grains, stone beds." He named the lime- to a calcilutite with scatken: and is locally silty. Siever (1953) stones, in ascending order, Walche, petrographically analyzed three Scottsburg, and Allard Limestone samples of the Waltersburg and Members. In the Waltersburg Quad- determined that the dominant con- rangle, poor and only partial expo- stituent is quartz (75-95%). He also sures of these three members pre- found clay (trace to 15%),carbonate vent explicit identification, although (0-5%), chert (trace to 3%), feldspar scattered exposures indicate that all (trace to I%), and traces of heavy three members and the intervening minerals. Low-angle crossbeds and shales are present. The Menard ripple marks are common in some crops out within and adjacent to the places. Bedding is tabular to some- Lusk Creek Fault Zone and in the what lenticular. Beds are from 0.1 to southeast quarter of the quadrangle 3 feet thick, and bedding surfaces north of Waltersburg and along a are wavy or irregular. southwest-trending tributary of The formation is poorly exposed Lusk Creek. overall; sandstone ledges in the up- The lower part of the formation .is per part are less than 5 feet high. dark gray very fine to fine grained The lower part is generally covered calcarenite that weathers gray is and probably consists of shale and locally medium grained, and has siltstone. The best exposures of the scattered, coarse grained bioclasts. upper part are in the SE, Section 30, The limestone is interbedded with T12S, R6E and in the NW, Section very dark gray fissile, calcareous 29, TI%, R6E. Sandstone beds in the shale and is fossiliferous, dominated Waltersburg Formation are discon- by gastropods and pelmatozoans. tinuous (Swann 1963). The core re- Bedding ranges from 0.7 to 2 feet covered from the U.S. Government thick, and bedding surfaces are tact with the Palestine as No. 1Well consists of only siltstone wavy to irregular. Outcrops typi- and shale (fig. 5), but it is possible cally form low ledges 3 to 10 feet that part of the section is absent as a high, and they are often slumped. result of faulting. This lower part is roughly equiva- The upper contad of the forma- lent to the Walche Limestone Mem- tion is not exposed in the Walters- ber. burg Quadrangle. The core from The middle part of the Menard is US. Government No. 1Well indi- dark gray to gray brown limestone cates that the upper contact with the that weathers gray to gray brown. It SW, Section 1, T13S, R6E Menard Limestone is transitional. varies from poorly to moderately Surface mapping indicates that the sorted, very coarse to coarse grained Waltersburg is about 50 feet thick, calcarenite that has scattered to tributary in the NW W SE, kctiom whereas subsurface data indicate a abundant coarse grained bioclasts. 30, TlZS, R6E and along Coppersus range of 40 to 65 feet in the quadran- This unit is commonly interbedded Branch in the NW NE, Section 20, gle. The drillers' log of Minton- with poorly indurated, light gray to TI%, R6E and NW W,section 21, Baker No. 1 recorded a thickness of dark gray fissile, calcareous shale TI%, R6E. 65 feet. A geophysical log of the up to 5 feet thick. The bedding sur- Mapping of exposures indicates Austin Roberts No. 1recorded 64 faces, which are locally argillaceous, that the Menard is 85 to 110 feet feet. The core from the U.S. Govern- and the shale are abundantly fossilif- thick, but lack of exposed contacts ment No. 1Well recovered 40 feet of erous with brachiopods, bryozoans, Waltersburg, but it is possible that pehatozoans, and rugosan corals. the thickness was affected by the The middle part locally contains 4 to nearby Flick Branch Fault. 5 feet of buff, dolomitized limestone. Near the top part, the limestone contains layers of dark brown chert nod- log of the Voslow No. 1 tively thick sequence of limestone ules. Bedding ranges from 0.4 to 2 ed 142 feet. The core of and shale overlying the Waltersburg feet thick, but it is generally 0.5 to 1 ment No. 1Well retriev Sandstone and underlying the Pales- foot thick. Outcrops form rounded 60 feet of the Menard (fig. 5). tine Sandstone is referred to as the ledges that reach heights of up to 15 Menard Limestone. S. Weller (1913) feet. Sinkholes and springs are com- introduced the name "Menard Lirne- mon in some places. This middle stone" for exposures near Menard part is roughly equivalent to the te- (Randolph County), southwestern Scottsburg Limestone Member. Illinois. Swann (1963) described the The upper part of the Menard is referred to as the Palestine Sand- Menard Limestone as "three well- dark gray limestone that weathers stone. It was named for exposures marked limestone units separated gray to buff and is light brown to Palestine Township in Randolph and overlain by units that are brown in some places. It varies from County, southwestern Ilho largely shale but contain thin lime- a fine to medium grained calcarenite Weller 1913). It crops out on northwest side of the Lusk Creek and silty shale grade upward to 0 Fault Zone and in the south-central dark gray shale of the Palestine, surficial which is conformably overlain by ...... , . . part of the quadrangle, southeast of Degonia green gray the Hobbs Creek Fault Zone. olive gray calcareous mudstone in- Formation The Palestine Sandstone consists terbedded with dark gray shaley of the following succession: fine to limestone of the Clore. Baxter et al. medium grahed, thick bedded sand- (1967) also reported a conformable Ford Station stone, and very fine grained, thin upper contact. In the northwest part Member bedded sandstone, siltstone, and of the quadrangle, the uppermost shale. The sandstone is light tan to Palestine and lowermost Clore are gray green to gray and weathers so poorly exposed that the contact gray to olive brown to brown. Grain was not mapped, and the forma- size ranges from very fine to medi- tions are not differentiated on the um. It is composed of well sorted, geologic map (Weibel et al. 1992). In subangular, rarely subrounded, the southeast part, the upper Pales- quartz grains, ranging in size from tine is faulted out of sequence and very fine to medium. Siever (1953) does not crop out. Cora petrographically analyzed six sam- The best exposures of the lower Member ples of the Palestine and detemined Palestine are along Copperous that the predominant constituent is Branch and in the NE, Section 17, quartz (63-97%). Clay (&lo%), car- T13S, R6E, where the sandstone bonate (0-34%), chert (trace to 2%), forms a prominent bluff that faces and traces of feldspars and heavy southeast. The sandstone caps a fault? minerals also are present. Field northwest-dipping cuesta for sev- study indicates that mica and cal- eral miles to the southwest of Cop- careous cement are rare and the perous Branch. The upper part of sandstone is locally silty. The sand- the Palestine generally is poorly stone generally crops out as several exposed, but it also crops out inter- ledges or forms high bluffs in some mittently along this creek. places. The upper part contains in- The thickness of the Palestine, based on outcrop study ranges from tesbedded shale and siltstone. The Figure 6 Graphic column of core from shale is light gray to light brown, fis- 50 to 70 feet. The thickness is ap- Truebger No. 3 Well, Section 35, TlZS, sile, and noncalcareous; it is poorly proximated because the upper con- ME. Thicknesses are corrected to com- indurated and locally silty. The silt- tact is conformable and poorly pensate for angled drilling. stone is gray to dark gray thin bed- exposed. Well data from adjacent ded, and contains oscillation ripple quadrangles indicate the Palestine is east edge of the quadrangle, as well marks and trace fossils. A thin, soft 45 to 70 feet thick. as in a belt southeast of the Hobbs bituminous shale near the top of the Creek Fault Zone. Palestine crops out in a small stream bed in the NW SE SE, Section 17, plex sequence of shale, limestone, Cora Limestone Member T12S, R6E. This shale probably is and sandstone overlying the Pales- Swam (1963) proposed the name equivalent to the thin coals that tine Sandstone and underlying the "Cora Limestone Member" for the locally mark the top of the Palestine Degonia Formation is referred to as lower shale and limestone part of the in western Illinois (Swann 1963). the Clore Formation. S. Weller (1913) Clore exposed near Cora (Jackson Fossils are sparse throughout the named the formation for exposures County), southwestern Illinois. The formation; only rare carbonaceous near Clore School in Randolph member consists of limestone, argil- plant fragments are present. Stig- County, southwestern Illinois. laceous limestone, and shale inter- marian root casts and Planolifes, a Swann (1963) divided the Clore into beds (fig. 6). The limestone is gray to trace fossil, occur in the sandstone three members: the lower Cora dark gray and weathers light gray to below the bituminous shale along Member, consisting of shale and light brown. It is a fine to coarse Copperous Branch (fig. 2). Ripple limestone; the middle Tygett Mem- grained calcarenite or a calcilutite marks and low-angle crossbeds are ber, consisting of sandstone and and has coarse grained bioclasts. Ar- common. Bedding ranges from 0.1 shale; and the upper Ford Station gillaceous limestone beds and shale to 5 feet thick, but it is generally 0.5 Member, consisting of shale and interbeds are common and siltstone to 2 feet thick. Bedding surfaces are limestone. All three members of the beds occur in some places. The shale locally irregular or wavy. Sandstone Clore are recognized in the Walters- shows a variable composition. It is of the lower Palestine generally burg Quadrangle, although they are gray to dark gray fissile, and noncal- forms bluffs 5 to 35 feet high, where- not differentiated on the geologic careous in some places and green as the upper part is poorly exposed. map (Weibel et al. 1992). The Clore gray to olive gray, poorly fissile, and The upper contact of the Pales- crops out in ravines south of Matthis calcareous in others. The shale tine Sandstone and the Clore Forma- Branch, along Copperous Branch, ranges from 1to 6 feet thick. The silt- tion is not exposed, except at one and near the west edge of the quad- stone is brown gray to green gray ar- site in a small northeast-trending ra- rangle. It also crops out along sev- gillaceous, and calcareous. vine in the SW W SE, Section 16, eral streams and in a narrow fault The Cora is moderately to abun- T12S, R6E. At this outcrop, siltstone block in the Raum Fault Zone at the dantly fossiliferous and has abundant brachiopods (Spirifer, Cmposifa, grained, crossbedded sandstone and productids) and pelmatozoans. above it from 3 feet of very fine Gastropods, fenestrate, and ramose grained, thin to medium bedded bryozoans are common, and ru- sandstone below. Stigmarian root gosan corals are rare. Limestone casts occur in the lower sandstone. beds range from 0.3 to 3 feet thick This Tygett limestone bed also oc- and are generally 0.5 to 1.5 feet curs in quadrangles to the west and thick. The limestone forms low sub- northwest of the Waltersburg (Nel- Srove Church tle benches and beds, and common- son et al. 1991, J. Devera, personal Shale Mbr ly weathers to an hourglass shape. communication, 1990). The unit generally is poorly exposed In a fault slice within the Eusk and beds are often slumped. The Creek Fault Zone (NE NW NE, Sec- Goreville Cora ranges from 50 to 60 feet thick tion 5, T13S, R6E), 32 feet of Tygett Ls Mbr and is 57 feet thick in the Truebger Sandstone crop out along Eusk No. 3 Well (fig. 6). Creek. Beds in the upper 20 feet are tabular and thin, ripple marked, and red, green Tygett Sandstone Member crossbedded; in the lower 12 feet, Swam (1963) proposed the name "Ty- beds are thin and interbedded with gett Sandstone Member" for the mid- ripple marked, laminated siltstone. dle clastic part of the Clore Formation exposed near Tygett School in Union Cave Hill County, southern Illinois. The gener- (1963) proposed the name "Ford Sta- Shale Mbr ally well indurated member is domi- tion Member" for the upper carbon- nated by a light gray green to light tan ate part of the Clore Formation sandstone that weathers light brown exposed near Ford Station in Ran- to brown to gray brown. It is com- dolph County, southwestern Illinois. posed of very fine to fine grained The member consists of limestone, quartz that is well sorted and suban- argillaceous limestone, siltstone, Negli Creek gular to subrounded. Dark minerals and shale interbeds; it is lithologi- Ls Mbr are rare, and the sandstone is silty and cally similar to the Cora Member. micaceous in places. Plant molds, silt- The limestone is light gray to dark stone intexbeds, carbonaceous plant gray and weathers gray to orange fragments, trace fossils (Rhiux:malliunz, brown to brown. It varies from calci- Cochlkhnus, and Phycoides-like tubes), lutite to medium grained calcarenite and shale clasts are rare. Ripple marks to a fine grained calcarenite that has and low-angle crossbeds are common. coarse grained bioclasts. Argilla- Bedding ranges from 0.1 to 2 feet ceous limestone beds and shale in- thick, but it is generally less than 0.8 terbeds are common. The poorly Figure 7 Graphic colum of core from foot thick. Bedding planes are planar indurated shale is light gray to dark COGEOMAP W-3 Well in Section 9, and rarely irregular. In the southeast gray, fissile, noncalcareous, and up TlZS, R6E. corner of the quadrangle, the member to 2 feet thick. Moderately indurated is estimated to be more than 60 feet siltstone in the upper part is gray (1967) considered thick, although outcrops form ledges green to Light brown, noncalcareous The basal chert is only 5 to 15 feet high. The member is quartzose, and it has rare carbona- recognized in float or outa only 9 feet thick at the Truebger No. 3 ceous plant fragments and mica used as the mapping Well (fig. 6). flakes. Siltstone exposures are up to the Clore-Degonia co The Tygett is probably present 7 feet thick, and bedding ranges Clore ranges from 95 throughout the area, but it is thinner from laminae to 4 feet thick. The thick, and it is 100 fee in the northcentral and northwest- limestone is fossiliferous and brachi- Tmebger No. 3 Well. em parts of the quadrangle. In these opods and pelmatozoans are abun- areas, it consists of a gray fissile dant; bryozoans are common and shale and a sandstone bed. The 1- rugosan corals are few. Bedding foot-thick sandstone contains abun- ranges from 0.1 to 2.5 feet thick, and dant steinkerns of brachiopods it is generally 1to 1.5 feet thick. The (including Spirifer),pelecypods, and limestone beds are generally pelmatozoan fragments. Near the slumped and often weather to an west edge of the quadrangle, the Ty- hourglass shape. Outcrops of lime- originally designated as gett is thicker, forms small ledges, stone form benches 5 to 15 feet thick. and contains a thin limestone bed 2 The member ranges from 30 to 50 feet thick. The limestone, a calcilu- feet thick and is 32 feet thick in the tite containing abundant pelmato- Tmebger No. 3 Well (fig. 6). zoan fragments, crops out in the The upper contact of the forma- ravine at the north edge of N 1/2 tion is gradational, as indicated by SE, Section 23, TI%, R5E; it sepa- the core of the CQGEOMAP W-3 rates 7 feet of well sorted, fine Well (fig. 7), although Baxter et al. able lithologies of the Degonia For- mation and underlying the cliff- forming sandstones of the Caseyville Formation are referred to as the Kinkaid Limestone. S. Weller (1920b) proposed the name for exposures along Kinkaid Creek in Jack- son County, southwestern Illinois. As originally defined by S. Weller, the Kinkaid included all strata from the top of the Degonia to the base of the Pennsylvanian. Swann (1963) divided the formation into three members: the Negli Creek Limestone Member at the base, the Cave ]Hi19 Shale Member in the middle, and the Goreville Limestone Member at Figure 8 Basal chert bed of Degonia Formation forming a very resistant ledge in Whiteside Branch, near the northwest corner of Section 24, T12S, R5E. Scale is indi- the top' The Grove church Shale cated by geologic hammer in the right center of the photograph. was separated from the Kinkaid For- mation by Swann (1963) but was re- to as the Degonia Formation. It is a sorted quartz grains and is locally vised as the uppermost and fourth relatively thin, nonresistant forma- silty or argillaceous. Siever (1953) member of the Kinkaid by Nelson et tion that underlies gentle slopes in petrographically analyzed seven al. (1991). the center of the area between the samples of Degonia sandstone and The Kinkaid underlies steep Pennsylvanian escarpment and the determined that the predominant slopes below the Pennsylvanian es- Lusk Creek Fault Zone in the north- constituent is quartz (70-92%). He carpment in a narrow west-southwest quarter of the quadrangle. It also found clay (trace to lo%), car- west-trending belt in the northwest also crops out along the Hobbs bonate (0-23%), chert (1-2%), feld- quarter of the quadrangle and in a Creek Fault Zone in the southeast spar (trace to 5%), and traces of wide belt roughly bracketed by the quarter of the quadrangle and in sev- heavy minerals. Bedding ranges Raum Fault Zone and the Hobbs eral ravines at the east edge of the from 0.1 to 0.5 foot thick. The sand- Creek Fault Zone. The forrna tion is quadrangle. The complete succes- stone portion of the formation is 2 to often covered by talus from the over- sion can only be seen in the core of 10 feet thick and has shale interbeds lying Pennsylvanian sandstones. COGEOMAP W-3 Well (fig. 7). and interference ripple marks in The Degonia Formation consists some places. The siltstone is gray Negli Creek Limestone Member of shale, mudstone, siltstone, sand- green and weathers light brown; it is The Negli Creek Limestone Member stone, and chert. At or near the base noncalcareous and well indurated. was originally named a formation of the formation are several promi- Both sandstone and siltstone contain by Malott (1925), a name derived nent, well indurated chert beds. The mica. Beds range from 0.1 to 0.8 foot from strata exposed along Negli chert is gray to gray brown and thick, and ripple marks and trace Creek in Perry County, southern In- weathers white to yellow brown. It fossils are locally present. The shale diana. In the Waltersbwg Quadran- occurs in beds that are 0.3 to 1.5 feet is gray to dark gray and weathers to gle, it is predominantly a gray to thick and contain rare ripple marks. light brown; it is poorly fissile, non- dark gray limestone that weathers The total thickness of the chert is 2 calcareous, and thin bedded (less dark gray to gray brown. It ranges to 5 feet. The chert is generally frac- than 0.5 foot thick). from a calcilutite that contains scat- tured and slumped, but locally it The upper part of the Degonia is tered bioclasts to a coarse grained forms a resistant ledge (fig. 8). The dominated by gray to gray green, biocalcarenite. Poorly exposed shale chert is locally underlain by 0.3 to 2 variegated (blue gray, maroon, and interbeds occur in some places in feet of either (1) gray green to gray red brown) noncalcareous shale and the upper part. The shale is gray to light brown, silty fissile, noncal- claystone that weathers to a varie- green, fissile, noncalcareous to careous shale or (2) gray green, well gated color. The unit is massive, has weakly calcareous, and up to 3 feet sorted, weakly calcareous, quartzose a blocky fracture, and ranges from 2 thick. Argillaceous beds are fossilif- siltstone. In the core of COGEOMAP to 14 feet thick. erous: pelmatozoans (Psztrenzites W-3 Well (fig. 7),the chert is weakly The upper contact is not well ex- and Agizastocrinus), gastropods, and calcareous (and unusually thin), in- posed, but in the core of the COGEO- brachiopods (chonetids and spiri- dicating that the original lithology MAP W-3 Well (fig. 7), the shale at fers) are abundant; bryozoans (Ar- was at least in part composed of the top of the Degonia grades rap- chimedes and trepostomes) are limestone. idly to the overlying Kinkaid Lime- common; and corals and cephalo- Above the basal chert is an inter- stone. Mapping indicates the for- pods are rare. Giroanella oncoids, bel- val of interbedded sandstone, silt- mation is about 25 to 50 feet thick. lerophontid gastropods, and the stone, and shale. The moderately to In the COGEOMAP W-3 core, the coral, Ckaetetelln, are diagnostic of well indurated sandstone is light Degonia is 39 feet thick. the Negli Creek. Trace fossils in- gray green to gray green and weath- clude Chondrites, Zoophycus, and ers to light orange brown. It is com- horizontal burrows. Layers of gray posed of very fine grained, well stone and shale overlying the vari- to dark gray, lenticular chert nodules are common. Low-angle cross- crops out along Ramsey Branch, 40 ft soil beds are rare. Outcrops are generally near the north edge of the quadran- 1 Ill slumped and bedding is locally wavy. gle. The Cave Hill Member is about Bedding thickness varies from 0.1 to 3 80 to 100 feet thick; it is 92 feet thick feet, but it is generally 0.5 to 1.5 feet in the COGEOMAP W-3 Well (fig. 7). thick. The Limestone crops out as rounded ledges that aR generally 10 Gorevi lle Limestone to 25 feet high and are often the site of Swan (1963) named the Goreville springs. The member is generally Limestone Member for exposures about 25 to 30 feet thick; it is 26 feet near Buncombe, south of Goreville thick in the COGEOMAP W-3 Well in Johnson County, southern Illinois. (fig. 7). The member predominantly consists of limestone. It is a gray to dark Cave Hill Shale Member gray fine to coarse grained biocal- Swam (1963) named the Cave Hill carenite (commonly crinoidal) that Shale Member for exposures near weathers light gray to gray brown. Cave Hill in Saline Comty, southern Locally the limestone is argillaceous Illinois. The member generally con- and intercalated with gray to dark sists of a basal shale, middle lime- olive gray callcareous shale. The stone, and upper claystone. diverse fauna includes brachiopods The basal shale is 5 to 10 feet (Chonetes, Spin$?r, Punctospin'fer, pro- thick, dark green gray fissile, and ductids), bryozoms (fenestrates, tre- weakly calcareous. Brachiopods, postomes and rhomboporoids), bryozoans, and pelmatozoan frag- gastropods, Pterotocrinus, Trilophyl- ments are common fossils. Near the lites, Chaetetella, and shark's teeth. top of the basal shale are olive gray Layers of gray chert nodules are calcareous siltstone interbeds 0.1 to locally common in the limestone 0.2 foot thick; the siltstone crops out beds. Bedding ranges from 0.2 to 2 Figure 9 Graphic column of Goreville in a small ravine just east of the feet thick. The limestone crops out Limestone Member of Kinkaid Lime- stone from an abandoned quarry in Sec- Eddyville-Golconda road (SE NE as low ledges that are generally tion 7, TlZS, R6E. Note the intertonguing NW, Section 35, T12S, R6E). slumped and poorly exposed. The of shale and limestone in the lower mid- The middle part of the Cave Hill best exposure is a nearly complete dle part. is 60 to 75 feet thick and consists of section of the Goreville in an aban- limestone containing thin shale inter- doned quarry (fig. 9). The Goreville the geologic map of Weibel et al. beds. The limestone is a well indu- Member is up to 45 feet thick; it is 43 (1992). rated, gray to dark gray calcilutite to feet thick in the COGEOMAP W-3 The Grove Church consists of very coarse grained calcarenite that Well (fig. 7). gray to gray green, fissile shale and weathers light gray to gray brown. is locally silty and calcareous. Sev- A dolomitic limestone bed, which Grove Church Shale eral lenticular limestones, 0.1 to 0.2 weathers to buff, occurs locally. Lay- Swam (1963) designated the upper- foot thick, occur in the upper part. ers of gray to black chert nodules most shale the Grove Church Shale These limestones are light gray and are common in the limestone beds. and separated it from the Kinkaid, weather yellow brown to green gray Argillaceous interbeds are 0.7 to 0.8 based on the study of exposures and they consist of argillaceous calci- foot thick and locally laminated. near Cedar Grove Church in John- lutite and fine grained calcarenite. Brachiopods, bryozoans, and pelma- son County, southern Illinois. Nel- Brachiopods and bryozoans are com- tozoans are common fossils. Lime- son et al. (1991) reduced the rank of mon fo&ils. The ~&tis very poorly stone beds are generally 1 to 2 feet the Grove Church to a member of exposed. The best exposures of the thick. Outcrops are poorly exposed, the Kinkaid Limestone because the Grove Church are in ravines in the and the limestone beds are generally rare exposures of the Grove Church SE SE, Section 4, T12S, R6E. A com- slumped. render it impradicd as a surface plete core of the shale was recovered The upper part of the Cave Hill mapping unit and it is lithologically from COGEOMAP W-3 Well (fig. 7) consists of 10 to 15 feet of variegated related to the Kinkaid in a sequence near those ravines. The Grove (green gray, ocher, and maroon to of alternations sf limestone and Church also crops out near the top red brown) claystone. The claystone shale. Nelson et al. (1991) recog- of small, south-trending ravines in contains thin beds and lenses of bio- nized, however, the member in sev- the N 1/ 2 NE NW, Section 9, T12S, calcirudite that have abundant Ar- eral wells in their study area, a fact R6E, in a small ravine just south of chimdes, Rhom bopora, Cmposita, and that suggests the Grove Church is Illinois 145 in SW SE NE, Section 13, pelmatozoan fragments. useful as a subsurfacemapping TlS, R5E, and in the center of W The best exposures of the Cave unit. The Grove Church is identifi- SE, Section 8, T12S, R6E. The Grove Hill are in and adjacent to small able in the subsurface, if cores and a Church is 24 feet thick in the core. ravines in the SE SE, Section 4 and good set of samples are available. The upper boundary of the NE NE, Section 9, T12S, R6E, and in Geophysical logs alone are not Kinkaid is the Mississivvian-Penn- a short southeast-trendingravine in always sufficient for identification of sylvanian unconformiG The Grove the SE NE SE, Section 34, TlS, R6E. the member. The four members of Church has been eroded in most The upper part of the Cave Hill the Kinkaid are not differentiated on places at the Mississippian-Pennsyl- vanian unconformity; the Goreville tinguishable from Pope Group sand- and Cave Hill Members are eroded stones. Caseyville sandstones lack- ...... I ...... -. . ing pebbles and granules are I...... _.. in some places as well. The Kinkaid ...... fine to generally coarser grained than Pope ...... ::;..I medium ranges from less than 100 feet to at ...... :.:.. ,.., . grained least 186 feet thick. The thickest sec- Group sandstones...... tion in the Waltersburg Quadrangle No complete exposure of the ...... _...... '. ,::. is in the core of COGEOMAP W-3, Caseyville is found in the Walters- .... -_...... :..... which contains all four Kinkaid burg Quadrangle because of erosion Battery :,:...... Rock ...... members. and faulting; thus, the total thick- sandstone 1.'. '. :'.'::,: :. :: is : :'.,:; :'.'. .... ;.'..'... ness estimated from composite Member ...... ississippian-Pen ...... sections. The thickness is variable .: :,. - Unconfodty primarily because the formation was -...... :'..': ... coarse ...... grained In the Waltersburg Quadrangle, the deposited on an uneven surface. A ...... :...... -loo .I-:...... Mississippian-Pennsylvanian con- U.S. Forest Service well near Eddy- ...... - tad is an irregular surface overlying ville started below the top of the , ...... the Kinkaid Formation. The strata Caseyville and drilled through 257 -- -. - . . - . - . - . - . . - . - . - . - micaceous feet of the formation without reach- - . - . - . - . underlying the contact extend from - . - . - . - - . - . - . - . the Grove Church Shale Member ing its base (fig. PO). Core and out- - - - . - . - - - . - - - . - down to the Cave Hill Shale Mem- crop studies near the northeast ...... -. ; -1 50 ber, and perhaps to the Negli Creek corner of the quadrangle indicate ...... :: '...... very fine Limestone Member. The topogra- that the formation attains a thick- :.' ...... : ...... grained .. , .- phic lows on this surface are occu- ness of 375 feet. Nelson et al. (1991) ...... ' . . ' I. .:...... pied by the basal member of the estimated the thickness of Casey- . , , ,. , . . : : :.. fine to Caseyville Formation. ville to range from 200 to 400 feet in "WaysideH': :., -'. ....f.':'.; med. grained --. --. . - Previous studies concur with the the adjacent Eddyville Quadrangle. Member .- . .-...-=carbonaceous interpretation of widespread erosion Since 1960, most geologic map prior to deposition of Pennsylvanian makers in southern Illinois have strata. J. Weller (1939) concluded divided the Caseyville Formation that pre-Pennsylvanian erosion ex- into the 'Wayside" Member (oldest), plained the variable thicknesses of Battery Rock Sandstone Member, the Kinkaid Formation in the Don- "Drury"Member, and Pounds Sand- gola, Vienna, and Brownfield 15- stone Member (Desborough 1961, Minute Quadrangles. Siever (1951), Baxter et al. 1963,1967, Baxter and Wadess (1955), Bristol and Howard Desborough 1965, Nelson and Figure 10 Graphic column of U.S. For- (1971), and Droste and Keller (1989) Lumm 1990a, 1990b, Nelson et al. est Service Eddyville guard station well constructed detailed sub-Pennsylva- 1991).Nelson and Lumm (1987) rec- in Section 6, T12S, R6E. nian paleogeologic maps of the Illi- ognized a basal Lusk Shale Member nois Basin. The maps showed (equivalent to the 'Wayside" Mem- in this text as "Wayside" and "Drury" predominantly southwestward-flow- ber), the Battery Rock Sandstone (a Members because of their question- ing drainage systems of valleys rang- poorly exposed shaley interval), and able status as valid lithostra tigraphic ing from a few feet to more than 300 the Pounds Sandstone. Because units in the Waltersburg Quadrangle. feet deep and up to 20 miles wide. most Pennsylvanian outcrops in the Waltersburg Quadrangle consist of sandstone, only 'Wayside" sand- overlying Mississippian rocks and PE SPSTE stone lentils, the Battery Rock Sand- underlying the massive bluff-form- stone Member, and the Pounds ing Battery Rock Sandstone are re- Sandstone Member were mapped. ferred to as the 'Wayside" Member. The Caseyville Formation comprises The "Wayside" and 'Drury" Mem- Lamar (1925) originally proposed the cliff-forming, quartz-pebble-bear- bers are poorly defined and described the name "Wayside sandstone and ing sandstone and the associated silt- in both their respective type areas shale member" for strata exposed stone, shale, and coal overlying and in the Waltersburg Quadrangle. southeast of Wayside in Union Mississippian strata. Owen (1856), These members consist of a variety County, Illinois. Kosanke et al. named the formation the "Caseyville of intergrading and intertonguing (1960), referred, without explana- Conglomerate," for strata exposed rock types that are dominated by tion, to the unit as the Wayside Sand- along the Ohio River near Casey- fine grained clastics. Both members stone Member. Nelson et al. (1991) ville in western Kentucky. Lee (1916) are poorly exposed and their con- redefined the unit as the Wayside formally defined the CaseyviUe Forrna- tacts are generally concealed by Member. Lamar (1925) described the tion and designated and described talus and surficial sediments. The member as consisting of lithologi- its type section in detail. "Wayside" and 'Drury" cannot be dif- cally variable, lenticular beds that The Caseyville is dominated by ferentiated from each other in areas thicken and thin "with confusing fine to coarse grained, quartzose where the intervening Battery Rock abruptness." He further described sandstone, characteristically contain- Sandstone is absent. Mapping and sandstone beds that ranged from ing subrounded quartz pebbles and correlation of units within the Casey- thin bedded to massive, fine to granules. These pebble- and granule- ville is further complicated by fault- coarse grained, and "pure" to argil- bearing sandstones are readily dis- ing. These members are referred to laceous. According to Lamar, the Wayside contains shales having lentils rest on or occur just above consisting of simple trails and bur- wide textural and compositional Mississippian strata. The sandstone rows are locally common. Plant ranges, and rare, thin beds of argil- is white to gray and weathers light casts are also common. laceous limestone, coal, and con- tan to brown and has rare Liesegang The thin bedded sandstone is in- glomerates of quartz pebbles. In the banding. The grain sizes range from terlayered with siltstone and shde. Waltersburg Quadrangle, sand- fine to coarse, but they are generally The siltstone is gray, quartzose, non- stones within the member are of medium sized and subangular. calcareous, up to 20 feet thick, and variable lithology, some of which The sandstone is a quartz arenite wavy bedded. The shale, less than lithologically resemble the overlying that contains rare dark accessory 10 feet thick, ranges from light gray Battery Rock Sandstone. The 'Way- minerals. The medium to well indu- to dark gray to light brown; it is non- side" Member consists of interlay- rated sandstone contains rare to calcareous, fissile, and poorly to ered sandstone, siltstone, shale, and abundant rounded to subrounded moderately indurated. Locally, it coal. Ledge- and cliff-forming sand- quartz pebbles and shale clasts in contains silty interbeds or is silty stones of the 'Wayside" are deline- some places. The pebbles occur and contains carbonaceous plant ated on the geologic map of Weibel either as scattered clasts or in con- fragments. Conglomeratic sand- et al. (1992). glomeratic lenses that are up to 3 stone lenses occur within this shde. Sandstone lentils of the 'Way- feet thick and contain a ferruginous Clasts in the conglomerate consist side" Member crop out near the cement. The sandstone is poorly to predominantly of quartz pebbles, northwest corner of the quadrangle, well sorted, depending upon the but also include chert, siderite, smd- where they consist predominantly amount of quartz pebbles; generally stone, and shale. Shale clasts aE up of ledge-forming sandstone, and in the sandstone is well sorted. Fossil to 0.3 foot long. The matrix is sand- the southeast half of the Dixon plant casts are locally common, and stone and the cement is gener Springs Graben, primarily between ripple marks and planar crossbeds ferruginous. The conglomerate the Raum and Hobbs Creek Fault are present and locally abundant. lenses are 1to 3 feet thick. A good Zones, where they consist of thick Bedding ranges £rom 0.5 foot thick exposure of a lens is along Beatty bedded sandstone and thin bedded to massive. The sandstone usually Branch in the NW NE SW, Section lithof acies. crops out as a bluff that ranges from 27, T12S, R6E. Black carbonaceous In the northwestern area, the 10 to 40 feet high. In some places, shale occurs in the 'Wayside" along sandstone is light brown to tan and the sandstone is 80 feet high or the stream bed that is parallel to the weathers light brown to gray; it forms two ledges. Raum Fault Zone in Section 13, ranges from very fine to medium Between the Raum and Hobbs TI%, R6E. Soft gray shale contain- grained but is generally fine Creek Fault Zones, thick bedded ing fragmentary impressions grained. This unit is a quartz arenite "Wayside" sandstone containing crops out in a roadcut along Illinois containing rare dark accessory min- quartz pebbles closely resembles 145 in the NE SE SE, Section 14, eral grains. The grains are subangu- the Battery Rock Sandstone. In TI%, R6E. Soft sediment dedorma- lar to subrounded and well sorted. some places, these pebbles are con- tion (slumped bedding) is common The moderately to well indurated centrated within the "Wayside" where the "Wayside" consists of in- sandstone contains rare shale clasts. sandstone; pebbles within the Bat- terbedded shale and sandstone (fig. Bedding ranges from 0.5 foot thick tery Rock are more uniformly dis- 11). The thin bedded "Wayside" htho- to massive, and bedding surfaces tributed throughout the sandstone. facies overlies, underlies, and lakr- are inregular in some places. Ripple These "Wayside" sandstones also ally grades into the thick bedded marks are common and low-angle contain iron-cemented conglom- "Wayside" sandstones. The lateral crossbeds (generally oriented south- eratic lenses, which are character- gradation is exposed near the east southwest) are common in some istically rare in the Battery Rock. edge of the quadrangle be places. The sandstone splits into two The thin bedded lithofacies of the Raum and Hobbs Creek or more tongues, or lentils, that are 'Wayside" Member is poorly to mod- The 'Wayside" Membe separated by mostly covered inter- erately exposed and composed of northwestern part of the quadrangle vals and form ledges 5 to 40 feet sandstone, siltstone, shale, and cod. is up to 120 feet thick where it fib a thick. Intervals of poorly exposed The sandstone is white to light gray pre-Pennsylvanian paleovalley The shale 5 to 10 feet thick are interca- and weathers light tan to brown. It outcrop pattern of the sandstone lated with sandstone. The shale is is very fine to fine grained, well in- beds indicates the paleovalley gray to dark gray and weathers light durated, and generally well sorted, trends northeastsouthwest, nearly gray to brown; it is moderately fis- except where quartz pebbles are pre- parallel to Illinois 145. In the east- sile and noncalcareous. In some sent. The sandstone is a quartz central part of the quadrangle places, it contains abundant carbona- arenite that contains rare accessory member is more than 120 feet ceous plant fossils. dark minerals and mica. Bedding The best exposures of the thick bed- Lentils of thick bedded 'Wayside" generally is tabular and less than 0.5 ded 'Wayside" in this area are along sandstone crop out in the southeast foot thick, but occasional lenticular Beatty Branch and in ravines along half of the Dixon Springs Graben, beds are up to 3 feet thick. Low- the east edge of the map area, par- primarily between the Raum and angle crossbeds occur in some ticularly in the area around the SW Hobbs Creek Fault Zones. These len- places. Ripple marks are common to Section 24, T12S, R6E. tils generally overlie thin bedded abundant; their crest orientations Structural movements in the "Wayside" sandstones; however, at are locally divergent. Small load Dixon Springs Graben may have in- scattered localities along Beatty casts, flute casts, and tool marks are fluenced deposition of the thin bed- Branch and along Lusk Creek, the locally abundant and trace fossils ded 'Wayside" lithofacies, which is , approximately 5 ft ,

Figure 11 Field sketch of deformed shale and thin bedded sandstone in "Wayside" member of Caseyville Formation, NW NE SE, Section 27, T12S, R6E. Horizontal movement along shale layers produced a small recumbent fold. Strata apparently were deformed before lithification. thicker in the graben than in the area other Caseyville members; Battery of the formation in the adjacent Ed- northwest of the graben, except in Rock strata lacking pebbles are rare. dyville and Stonefort Quadrangles the paleovalley. Thin beds of con- Dark accessory minerals are rare (Nelson and Lumm 1990a, b). glomerate, particularly those con- and mica is absent. Fossil plant 11 ember The interval taining cobble-sized clasts, suggest casts, including lycopods and cala- local periodic uplifts that either sup- mitids, and tabular crossbeds, both of fine grained, thin bedded strata plied clasts directly or diverted large and small scale, are common. between the Battery Rock and drainages; both actions accelerated Most crossbeds are oriented to the Pounds Sandstone Members is re- downcutting. Paleoslumped beds southwest, but along Frieze Branch, ferred to as the "Drury"Member. outcropping along Beatty Branch a few are oriented to the northwest. Lamar (1925) originally proposed may have been caused by penecon- Bedding ranges from 0.5 foot thick the name, Drury Shale and Sand- temporaneous tectonism. An alterna- to massive. The sandstone forms stone Member, for strata cropping tive explanation is that the slumped ledges and bluffs 5 to 40 feet high. out along Drury Creek in Jackson bedding is the result of sediment In the few places where it is ex- County, southern Illinois. Lamar de- loading on top of unstable, water- posed, the lower contact of the Bat- fined the member as "the unit of in- saturated deposits. tery Rock is generally sharp and lies terbedded shale and sandstone at the base of the massive pebble- lying above the Lick Creek and be- bearing sandstone. The upper con- low the next persistent, thick, mas- The lower of two rela- tact is not exposed in any outcrop; it sive sandstone above, the Makan- tively widespread bluff-forming, was mapped at the highest exposure da." The Lick Creek and the thick, quartz-pebble-bearing sandstones in of sandstone containing abundant massive Makanda sandstone were the Caseyville Formation is referred pebbles, generally at the top of a considered to be equivalent or near- to as the Battery Rock Sandstone ledge or bluff. In the core of COGEO- ly equivalent to the Battery Rock Member. Cox (1875) named the MAP W-1 Well (fig. 12), the upper and the Pounds Sandstones (Wan- member for Battery Rock, a massive contact is gradational. In Sections 13 sandstone bluff along the Ohio and 14, T13S, R5E (Pine Hollow and River in Hardin County southern Avery Hollow), the Pounds Sand- I surficial I Illinois. It crops out extensively in stone lies directly on top of the Bat- the vicinity of Eddyville; smaller tery Rock, and the two members exposures are in Pine Hollow and cannot be readily differentiated. The along Beatty Branch near the Ram Battery Rock Sandstone is generally Creek Fault Zone, as well as in a 30 to 60 feet thick; it is more than 110 large ravine northeast of Raum. feet thick near Eddyville (fig. 10). The Battery Rock is a white to Through most of the quadrangle, light gray to light brown sandstone the Battery Rock Sandstone consists that weathers gray brown to brown. of isolated tongues and lenses of It is fine to very coarse grained, but thick bedded to massive conglom- generally coarse grained, and con- eratic sandstone, generally enclosed tains abundant quartz pebbles. by the "Drury" and "Wayside"Mem- Grains in this quartz arenite are sub- bers. Southwest of Eddyville, along angular and poorly to moderately Hayes Creek, the Battery Rock con- F-T-Z;&~ p1 ants sorted. The quartz pebbles are gray sists of several cliff-forming inter- - to white, rounded to subrounded, vals, separated by bench-forming and up to 0.1 foot in diameter. The intervals of poorly exposed strata. pebbles occur in conglomeratic The Battery Rock has been identified lenses, often aligned along bedding in a few small areas southeast of the and crossbedding surfaces, or scat- Lusk Creek Fault Zone. The lenticu- tered throughout the rock. The Bat- lar nature of the Battery Rock in this Figure 12 Graphic column of core tery Rock generally contains more quadrangle contrasts with the nearly from COGEOMAP W-1 Well in Section quartz pebbles and granules than continuous, more tabular character 14, T12S1 R6E. less 1939, J. Weller 1940, Desborough 0 1960). Mapping now in progress I surficial I Pounds indicates that the Battery Rock and Ss Mbr Pounds Sandstone Members cannot --- be readily identified and differenti- rare marine ated in the "Drury" type area in the Makanda Quadrangle. The status of the "Drury" as a valid member is questionable because of its uncer- tain definition. In addition, the Drury and the 'Wayside" Members cannot be differentiated where the Battery Rock Sandstone is absent. covered The "Drury" Member is poorly exposed in the Waltersburg Quad- rangle and was not mapped as a separate unit. The "Drury" has been generally faulted out of sequence and crops out only in a large ravine northeast of Raum and in a small "Drury" area along the Raum Fault Zone in Member Avery Hollow. The unit generally forms a gentle slope beneath the Figure 13 Graphic column of core Pounds Sandstone and is often cov- from COGEOMAP W-2 Well in Section ered by talus from the Pounds. A 15, T12S, R6E. complete top-to-bottom core of the "Drury" was recovered from the CO- The "Drury" in the COGEOMAP GEOMAP W-1 Well (fig. 12) and a W-1 core (fig. 12) consists of more partial core was recovered from the than 120 feet of interbedded silt- COGEOMAP W-2 Well (fig. 13). stone, shale, thin conglomerate, and The outcrop sequence of the two thin coals. The lower contact "Druryt'in the large ravine northeast of with the underlying Battery Rock lycopod and Raum (SW, Section 12, and W,See- Sandstone Member is transitional. tion 13, SE, Section 14, TI%, R6E) is The thick, dark gray shale at the top about 70 feet thick and displays vari- contains scattered mollusks, includ- able lithologies (fig. 14). The lower coal ing a small orthoconic cephalopod. Gentry (?) is aq$laceous and probably equiva- The shale may correlate with a goni- Coal Bed lent to the Gentry Coal Bed that was atite-bearing shale in the Eddyville Quadrangle (Devera et al. 1987). iattery Roc mapped to the east (Baxter et al. 1963, Ss Mbr Baxter and Desborough 1965, Baxter et The middle and upper parts of al. 1967) and to the north (Nelson and the "Drury" were recovered from the Figure 14 Graphic column of "Drury" Lumm 1990a). A stream bed exposure lowermost 37 feet in the core of CO- member of Caseyville Formation, from (NE NW NW, Section 13, TI%, R6E) of GEOMAP W-2 Well (fig. 13) where it measured section in a ravine in E1/2 SW, the coal contains lycopod leaves and is dominated by shale. The contact Section 12, T12S, R6E. pteridosperm axes (W. A. DiMichele, with the overlying Pounds Sand- peranal communication, 1986).The stone Member is gradational. We11 (fig. 13) and the upper part dark gray to black shale above this from COGEOMAP W-1 Well (fig. 12). coal contains abundant c&onaceous Pounds Sandstone Member The Pounds consists chiefly of plant impmiom. In the middle, the The upper of the two sandstones in quartz arenite that is white to light "Druty"contains an argillaceous coal the Caseyville Formation is referred gray and weathers tan to light bed 05 to 0.7 foot thick. to as the Pounds Sandstone Mem- brown; it is medium to coarse A lenticular body of siltstone, ber. The sandstone is widesp~ad, grained and very coarse grained in about 10 feet thick, in a ravine in the forms bluffs, and bears abundant some places. The quartz grains are center E 1/2 E 1/2 SE, Section 12, quartz pebbles. J. Weller (1940) subangular to subrounded; dark T13S, R5E is tentatively included in named the member for strata in minerals and mica are rare, as are the "Drury" Member. The siltstone is Pounds Hollow (Gallatin County), Liesegang banding and iron oxide gray micaceous, argillaceous, and southern Illinois. The Pounds crops grain coatings. Sorting ranges from contains plant fragments. The silt- out south-southwest of Rock (figs. 2, poor to medium, depending upon stone is overlain and underlain by a 15), in a narrow northeast-trending the amount of quartz granules and massive sandstone that bears quartz belt on the northwest side of the pebbles present. Quartz granules pebbles and is either Battery Rock or Raum Fault Zone, and just west of and pebbles are rare to abundant. Pounds. Alternatively, the siltstone Eddyville. A nearly complete top-to- They are white to gray white, sub- may occur entirely within the bottom core of the Pounds was re- rounded to rounded and generally Pounds and not as part of the covered from COGEOMAP W-2 scattered; they are aligned along "Drury." bedding planes in some places. Pla- Figure 15 Pounds Sandstone Member of Caseyville Formation forming picturesque bluffs southwest of Rock, in SW SW SE SE, Section 2, T13S, R5E. The bluffs are typical in their massive appearance, rounded ledges, and honeycomb weathering. These strata dig about 4"NE. nar crossbeds and ripple marks are the base of the Sebree Sandstone in bearing quartz arenites of the Casey- common in the moderately to well western Kentucky, The upper bom- %rilleFormation, but it is difficult to indurated sandstone. Bedding dary of the formation has been distinguish from the underlying ranges from 0.5 foot thick to mas- revised several times (Glenn 1912b, Tradewater sandstone. sive. The member generally forms Lee 1916, Glenn 1922, Wanless 1939, The petrologic change between bluffs 10 to 40 feet thick. The mem- Kehn 1963), but the lower boundary the Caseyville and younger Pennsyl- ber contains a few interbeds of shale has not. Kosanke et al. (1960) aban- vanian rocks is gradational. Potter and siltstone and a local, unnamed doned the name Tradewater in favor and Glass (1958) classified Pennsyl- coal. The coal crops out in the NE SE of the Abbott and Spoon Forma- vanian sandstones of the Illinois Ba- SE SE, Section 32, TI%, R6E; it is up tions. Jacobson (1991), citing prob- sin into three groups: an ortho- to 0.5 foot thick, lenticular, and argil- lems with differentiating the latter quartzitic group (Caseyville Forma- laceous. formations on a regional basis, resur- tion), a transitional group (lower half In general, the Pounds is lithologi- rected the name Tradewater Forma- of Tradewater Formation), and a sub- cally similar to the Battery Rock tion. In the Waltersbwg Quadrangle, graywacke group (upper half of Sandstone except that quartz peb- the Tradewater forms a wide north- Tradewater Formation and younger bles are smaller and less numerous east-southwest outcrop belt com- Pennsylvanian sandstones). They de- in the Pounds. Most pebbles are less prising most of the bedrock in the scribed the Caseyville sandstones as than 0.1 foot in diameter, and they northwest half of the Dixon Springs consisting primarily of quartz (95% are scattered throughout the sand- Graben. detrital component). Carbonate is a stone. The Tradewater Formation is secondary component, and feldspar, The Pounds ranges from 20 to 75 composed of sandstone, siltstone, lithic fragments, matrix clay and feet thick. The lower contact is not shale, and thin coal beds. Sandstone, mica are rare. The transitional sand- exposed but is sharp in the core of roughly 1/2 to 2/3 of the total inter- stones consist of quartz (83% detrital COGEOMAP W-2 Well. The upper val, is very fine to coarse grained component) and secondary carbon- contact is poorly exposed; the con- and contains local shale clasts and ate (dominated by siderite).They tact was mapped at the highest expo- quartz granules; quartz pebbles are also have slightly more feldspar, sure of sandstone bearing quartz absent. Tradewater sandstones are lithic fragments, matrix clay and pebbles. The contact is often at the mineralogically less mature than mica than does the Caseyville. Potter top of a massive bluff; however, the those of the Caseyville, and contain and Glass (1958) characterized the contact was slightly above a ledge or more mica, feldspar, lithic grains, transition group as being "somewhat bluff in some areas. and interstitial clay. Weathering of less well sorted" and having more an- these accessory grains produced gular grains than the Caseyville. Tradewater Formation iron oxide grain coatings; Tradewa- The Tradewater Formation in this Strata dominated by subgraywacke ter sandstones thus generally quadrangle generally consists of a sandstones and fine grained clastics weather to a darker color than composite sequence of three infor- overlying the Caseyville Formation Caseyville sandstones. Tradewater mal lithologic members: lower shale are referred to as the Tradewater For- sandstones appear progressively and sandstone member, middle mation. The name, Tradewater For- less mineralogically mature up- sandstone member, and upper mation, was proposed by Glenn ward through the formation. The shaley member. The boundaries of (19121) for the interval between the youngest Tradewater sandstone is these members are poorly exposed top of the Caseyville Formation and distinguishable from the pebble- and poorly defined, and their lateral extent is not well known. The mem- 1977,1978) and underlain by soft to fine grained, and contains suban- bers, therefo~,were not mapped in- claystone and overlain by up to 1 gular quartz grains and some mica dividually for this report, although foot of claystone, friable sandstone, and dark minerals. It is formed in the tops of prominent ledge-forrning or a conglomerate of shale clasts and beds 0.3 to 0.7 foot thick, is resistant, sandstone are shown on the geo- coal particles in a sandstone matrix. and contains shale clasts. The silt- logic map of Weibel et al. (1992). The lower shale and sandstone stone is well sorted quartzose and member of the Tradewater contains cont aim abundant carbonaceous ne lenticular sandstone bodies, gener- plant fragments. It is well indurated r of ally in the middle part but also near and has planar bedding less than 0.2 the Tradewater Formation consists the base. These basal Tradewater foot thick. The shale is gray to dark of a poorly exposed sequence that sandstones may directly overlie the gray, noncakareous, and fissile. It oc- ranges from 50 to 85 feet thick. It is Caseyville. The previously described curs in units up to 0.4 foot thick. dominated by shale and contains basal interval in Section 28 is suc- The upper part of the lower shale lenticular sandstones and thin dis- ceeded by a thick lenticular sand- and sandstone member is lithologi- continuous coals. stone. The sandstone generally cally variable (fig. 16) and consists The lower contact and base of the forms one or two thin ledges that of shale, siltstone, and thin coal. The formation is not exposed; however, overlie the basal shale sequence. This shale is dark gray fissile, carbona- it is present in the core of COGEO- sandstone is approximately equiva- ceous, and commonly contains plant MAP W-2 Well (fig. 13) where the lent to the Grindstaff Sandstone fossils. Coal crops out in the SE SE, top of the Caseyville Formation Member, Abbott Formation, of Bax- Section 29, T12S, R6E, and in the cen- grades upward into a claystone con- ter and Desborough (1965) and Bax- ter NE, Section 32, T12S, R6E. The taining root casts. The claystone is ter et al. (1967). Nelson et al. (1991) coal is 2 to 2.5 feet thick, contains a succeeded by a thin argillaceous mapped lower Abbott sandstone len- 0.2-foot clay parting, and overlies a coal and a dark gray abundantly tils at about the same stratigraphic light gray claystone with root casts. bioturbated siltstone. A similar suc- position in adjacent quadrangles to At the site in Section 29, the upper 1 cession is exposed in the large the north and northwest. foot of the coal is argillaceous and ravine east of the COGEOMAP well The sandstone of the lower shale underlies about 7 feet of dark gray in the SW NW, Section 14, TlS, and sandstone member of the Trade- shale that contains abundant plant R6E, as described by H. Wanless water is white to light gray and compressions (unpublished ISGS (1934, unpublished ISGS field weathers buff to pink to brown; it is field notes by M. Hopkins and R. notes). The interval, at an aban- generally fine to medium grained Peppers, 1967, and R. Peppers and doned mine site, is an upward suc- and rarely very fine or coarse R. Jacobson, 1974). The coal at the cession of soft claystone, coal, dark grained and well indurated. The site in Section 32 is partially exposed gray shale containing plant fossils, grains are well sorted, subangular, and 1foot thick. It is pdynologically micaceous shale, very fine grained dominated by quartz and have vari- similar to the Smith coal bed of the sandstone with root casts, claystone able amounts of accessory dark min- lower Tradewater Formation in west- with root casts, and dark gray to er& and mica, and rare clay ern Kentucky (R. Peppers, written black shale. Coal that crops out in a coatings. Liesegang banding is communication, 1974). The fossil small northeast-trending ravine, just locally common. Shale laminae and flora axe dominated by lycopods, east of the Eddyville-Golconda road interbeds are rare. Bedding ranges including stems of Lepidodmdron (NW SE, Section 22, T12S, R6E), is from thin (less than 1ft) to massive. acukatum, foliage, cones, and stig- also probably equivalent to the coal Ripple marks are rare to common, marian root impressions (James Jen- described by Wanless. At this site, particularly in the thinner beds. The nings, personal communication, the coal is overlain by gray silty sandstone crops out as either one or 1989). This coal overlies gray mas- shale. In the center of Section 28, two ledges that have a total thick- sive claystone and underlies poorly T12S, R6E, the basal Tradewater in- ness ranging from 5 to 30 feet. The indurated, silty, very fine grained terval consists of light gray to gray sandstone is similar to the Pounds sandstone that has shale interbeds shale and siltstone with scattered Sandstone, except that quartz peb- (2 to 3 feet thick). Above the shale is thin sandstone beds. In the south- bles are absent and slightly more ac- a sandstone; it is orange brown to west quarter of the quadrangle, the cessory minerals are present. A unit brown, medium grained, moder- basal part locally contains a coal that of fine grained sandstone and silt- ately indurated and sorted, and was mined in the center of the S 1/2 stone lies between the sandstone locally cemented with dark brown S 1/2, Section 12, T13S, R5E. The and the upper part of the member. iron oxide. Bedding is 0.1 to 0.5 foot coal is interpreted, on the basis of The best exposures of these lenticu- thick. The section is capped by a palynological analysis (Peppers, un- lar sandstones are in the large ravine coarse grained sandstone of the mid- published ISGS data, 1970), to be in the NE SW, Section 28, T1 S, R6E, dle sandstone member. younger than the Reynoldsburg and along Lusk Creek in the center, Coal Bed, older than the Manley Section 32, T12S, R6E. The core of Coal Bed, and possibly equivalent to COGEOMAP W-2 Well includes 24 The middle sandstone member of the Tunnel Kill Coal Bed (Nelson et feet of this sandstone (fig. 13). the Tradewater Formation forms al. 1991) and the Bell Coal Bed of Laterally equivalent to the len- ledges and cliffs along Eusk Creek western Kentucky. The coal mined ticular sandstone is a succession of in the northern part of the Dixon in Section 12 reportedly was as interbedded, thin bedded sand- Springs Graben and along Quarrel much as 3.5 feet thick (Wanless, un- stone, siltstone, and shale. The sand- Creek in the southern part of the gra- published ISGS field notes, 1934, stone, up to 1foot thick, is very fine ben. This sandstone is lithologically NW NE NW NW, 22 sw 36-1 1S-6E center W and NE NE and NE NE Eddyville Quad. 1 1-12s-6E 15-12s-6E 21 -1 2s-6E

oal

tykj ...... Oft " ." ' . Figure 16 Graphic columns of measured sections in the Tradewater Formation within the Dixon Springs Graben demonstrating cokplex lithofaAes changes. Datum is the top of the sections and is approximate.

and stratigraphically similar to the The sandstone is interbedded in sandstone overlying the middle Finnie Sandstone Member of the places with very dark gray noncal- sandstone member of the Trade- Abbott Formation of Baxter et al. careous, fissile shale or very dark water. These rock are roughly (1967) and the middle Abbott sand- gray to brown, well indurated, non- equivalent to the middle-upper Ab- stone of Nelson et al. (1% 1). calcareous, laminated siltstone. bott Formation of Baxter and Desbor- The middle sandstone member Along Lusk Creek in Sections 21,29, ough (1965) and Baxter et al. (1967), is light gray to buff and weathers 31, and 32, T12S, R6E, the entire in- and to the olive shale of Nelson et brown gray to dark brown; it is me- terval becomes shaley and thin to al. (1991). dium grained, rarely fine or coarse medium bedded, and it is not easily The member is predominantly grained, and moderately to well indu- distinguished from adjacent units. composed of light gray to buff, very rated. The grains are subangular, The middle sandstone member fine to fine grained sandstone that moderately to well sorted, and ranges from about 25 to 135 feet weathers yellow brown to orange dominated by quartz. Mica and dark thick. It is thinner to the southeast brown. The sandstone is dominated minerals are rare to common; lithic where it is finer grained and grades by quartz and contains mica. Bed- fragments and clay grain coatings are into underlying strata. The sand- ding is generally less than 1foot rare. This sandstone contains more stone is thickest adjacent to and thick and bedding planes are irregu- nonquartz components than does southeast of the Lusk Creek Fault lar. Ripple marks and shale dasts Caseyville sandstone. Lieseg ang band- Zone. The lower contact is generally and partings are common. The sand- ing is common, and the unit locally covered; where it is exposed, it cuts stone is generally interbedded with contains scattered quartz granules down into the underlying shale and very dark gray to black, fissile shale, and shale clasts. Bedding ranges from sandstone member. The upper con- gray to dark gray laminated silty 0.25 to 1.25 feet thick and is generally tact of the member is shown on the shale, and gray to brown quartzose planar; it is locally wavy to irregular. geologic map (Weibel et al. 1992). siltstone. The member is poorly Low-angle crossbeds and ripple exposed and occurs only in the syn- marks are common in some places. The clinal area of the Dixon Springs Gra- The sandstone forms ledges 5 to 35 youngest bedrock strata in the ben adjacent to Lusk Creek. The feet high. Waltersburg Quadrangle consist of thickest section exposed is about 100 interbedded shale, siltstone, and feet. SURFICIAL GEOLOGY

glycolatd, and analyzed for diffrac- The surficial geology of the Walters- tion spectra of the common clay and burg Quadrangle was studied as Field Methods nonclay minerals. In this method, part of a cooperative project be- Because exposed Quaternary sec- the instrument records peaks in the tween the Department of Geology tions are rare in southern Illinois, region of 17 A as expandable cay Southern Illinois University at Car- samples of the surficial materials minerals, 10 A as ilLite, and 7 A as bondale (SIUC), and the ISGS. The were collected with a hydraulic soil kaolinite and chlorite. surficial materials studied include probe (Giddings Machine Com- Graham's (1985) method is modi- all the relatively soft, nonlithified pany), which recovers core and fied from Hallberg et al. (1978) and sediments that cover the Paleozoic auger samples 6 to 15 meters (20-50 is based on a routine method used bedrock of the region. The deposits ft) deep. Samples were generally col- by the ISGS to scan large numbers of formed during the Quaternary lected with a slotted tube that samples for stratigraphic and classi- Period, the most recent geologic yielded cores approximately 7.6 cm fication purposes. This method time period. The Quaternary depos- (0.25 ft) or 5 crn (0.16 ft) in diameter. yields useful clay mineralogy data its cover a major unconforrnity, a Samples were also collected with a for characterizing Quaternary sedi- break in the geologic record that rep- flight auger 5 an (0.16 ft) in diame- ments; however, many factors other resents almost 300 million years be- ter. DriJl sites were selected not only than clay mineralogy may affect tween the Paleozoic and Quaternary on the basis of landscape position peak height, and the accuracy of the Periods. In the study area the surfi- and accessibility, but also on the method is not well documented. cial deposits consist of loess, allu- basis of prospects for obtaining the Therefore, conclusions made on the vium, colluvium, lacustrine most complete successions of uncon- basis of comparisons between clay deposits, and weathered residual solidated surficial materials. mineralogy data from this report material derived from the bedrock. Cores were described in detail and clay mineralogy data deter- Surficial geologic materials may under field moisture conditions. mined by similar methods using dif- contain natural resources, such as Munsell color, mottles, soil struc- ferent instruments should be used groundwater or sand and gravel ture, texture, presence or absence of with caution. aggregates. Their composition, thick- carbonate minerals, manganese ox- ness, and physical characteristics de- ide, iron oxide concretions, and Construction of the termine the suitability of a site for other features were described. Tex- specific land uses, such as a munici- ture was determined following the The distribution of surficial deposits pal landfill or industrial complex. U.S. Department of Agriculture tex- (lithostratigraphic units) is a func- The characteristics of the surficial de- tural classification. The weathering tion of the depositional conditions posits also affect drainage, ground- zone (soil horizons) terminology and the postdepositional erosional water recharge, and the impact of used is that of Soil Survey Staff history of each unit. These two fac- certain environmental hazards, such (1975), with modifications by Foll- tors cause complex relationships as flooding and earthquakes on the mer et al. (1985), and Soil Survey among the stratigraphic units in the region. Staff (1992). Geologic samples were study area, A stack-unit map (Kemp- This investigation included collected from the cores for labora- ton 1981) illustrates the areal and (1) characterizing the surficial mate- tory analyses. vertical distribution of geologic ma- rials in terms of particle size terials to a given depth below the distribution, clay mineralogy and ratory Methods surface. A generalized stack-unit thickness; (2) summarizing the strati- The particle size distribution of the map was prepared by combining in- graphy of the surficial deposits samples was determined at the formation obtained from 20 bo~gs within the Waltersburg Quadrangle; SIUC Department of Geology. A pi- made in the area, field observations, (3) preparing a detailed stack-unit pette method described by Graham and hand augering. Additional infor- map of the surficial deposits (Oliver (1985) was used. Particle size classes mation on the distribution and 1988); (4) assessing the resource po- include clay (less than 0.002 mm), nature of the near-surface materials tential of the Quaternary deposits, fine silt (0.002-0.02 mm), coarse silt came from the county soil survey including shallow groundwater and (0.02-0.62 mm), and sand (0.62-2 report (Parks 1975). Soil reports pro- aggregate; and (5) evaluating the mm). vided information on the distri- suitability of the surficial materials Clay mineralogy of the samples bution and nature of near-surface for specific land uses. was determined at SIUC by X-ray materials. Maps included in the soil analysis of oriented slides of the less report show the distribution of par- than 0.002-mm fraction. The clay frac- ticular soil series in the study area tion was placed on glass slides, dried, and are useful in distinguishing ma- Table 2 Relation between modem reasons: (1) the soil maps and the 7.5- controlled to a large extent by the soil series and Quaternary map units. geomorphic processes of erosion eolian deposition. This explains Upland soils distinction between the Grantsburg (generally slopes sequence of surficial deposits in the less than 12%) present upland and lowland posi- Robbs tions. Zanesville (generally slopes The nature and origin of the less than 12%) upland and valley lithostratigraphic Sideslopes md pedostratigraphic units obser- Beasely 5 feet below ground surface has Pit- ved in the Waltersburg Quadrangle Muskingum-Berks tle effect on the type sf soil series at (fig. 17) are described in this section. Wellston a site. The upland deposits consist of loess Wellston-Berks A detailed stack-unit map of the overlying residuum on flat to moder- Zanesville (generally slopes ately sloping surfaces that have not more than 12%) been substantially reworked by dlu- Lowland (Cahokia) vial and colllluvial processes. The val- Belknap ley deposits overlie bedrock in the Ginat tiond and used bottodands and consist of lacus- Sharon evaluations of the surficial geologic trine strata or alluvial material or Weinbach materials. The maps do not provide both. sufficient data for site-specific inter- Lowland (CahokiaIEquality) Belknap pretations. A copy of the map is Bonnie available for inspection in the ISGS Library. Rock Outcrop 0 This is an infor- Sandstone Rock Land mal unit (Nelson et al. 1991) used for classifying the unconsolidated Stratigraphic studies facilitate under- material, primarily in stable upland jor landscape anc4 geologic bounda- standing of the origin of the units areas in the Waltersburg Quadran- ries. The surficial lithostratigraphic and provide a framework for corre- gle' resting on bedrock and below lo- units were interp~tedfrom the soil lating and predicting their character ess. It is a sandstone residuum with map units (table 2). and occurrence. The relationships of abundant sandstone pebbles within The preparation of a stack-unit the surficial deposits is classified as a yellowish brown to brownish yel- map requires some subjective deci- (1) chronostratigraphic (time rela- low matrix of clay sandy clay or sions; in some cases, boundaries can- tionships), (2) lithostra tigraphic clay loam. The Oak is oxidized and not be drawn with certainty because (lithologic or compositional rela- leached of carbonate material of insufficient data. The vertical se- tionships), and (3) pedostratigraphic throughout its thickness, which quence of deposits from a borehole (soil development history or relation- ranges from 0.05 to 0.8 meter. The is first related to the soil series and ships of pedogenic attributes). clay content of the unit (1545%) landscape position; topographic fea- Most of the stratigraphic units in often increases with depth at the ex- tures are then used as a guide to the area correlate with units de- pense of the silt fraction in thicker drawing map-unit boundaries. A scribed by Willman and Frye (1970) sections (more than 0.5 m) (figs. 18, boundary between geologic units and Lineback (1979). The distribu- 19a, b). In thinner sections, the sand crosses a soil-map boundary for two tion of the lithostratigraphic units is content (10-45%) increases with

CHRONOSTRATIGRAPHY Uplands LITHOSTRATIGRAPHY valleys

I Holocene Stage I I 1 Modern Soil - a, Valderan-Greatlakean 0) Peyton Fm Cahokia Fm +a Substage Twocreekan Substage Peoria Silt Equality Fm Buncombe soil $ Farmdalian substage 1 Farmdale Soil Altonian Substage Roxana Silt Equality Fm I Sangamonian Stage Sangamon Soil lllinoian Stage Oak formation Pre-lllinoian

Figure 19 Stratigraphic classification of the Quaternary deposits in the Waltersburg Quadrangle. depth at the expense of the silt frac- Table 3 Locations of borings. tion (figs. 19c-e).The kaolinite plus chlorite content increases with Well Location Elev. (ft) depth, which shows the influence of the bedrock as a source of sediment for the residual material. Nelson et al. (1991) suggested that most of the Oak formation consists of material that is older than pre-Illinoian (300,000 to 2 million years) because of its stratigraphic position below correlated Illinsian units (Loveland Silt, Glasford For- mation, and Teneriffe Silt) in the Eddyville, Stonefort, and Creal Springs Quadrangles. In the Walters- burg Quadrangle, the Oak formation was found below the Roxana Silt of Wisconsinan age. The Oak for- Figure 18 General locations of borings mation contains pedogenic features; (see table 3 for specific information). where overlain by the Roxana Silt, this paleosol is correlated with the deposit on the stable upland posi- Sangamon Soil. tions. The Peoria Silt is oxidized to a yellowish brown matrix with light Roxana Silt The Roxana Silt gray mottles, and leached of carbon- overlies the Oak formation and is ate minerals. Its physical appear- ana Silts are typical for the southern the result of loess deposition during ance is dominated by features Illinois region (Graham 1985, late Altonian time of the Wisconsi- associated with modem pedogene- Hughes 1987, Nelson et al. 1991). nan. This unit is generally a silt sis. In the study area, the Peoria Silt loam that ranges from 0.2 to 1.35 me- ranges from 0.90 to 1.75 meters Peyton Formation The Pey- ters (0.664.43 ft) thick. It has a yel- (2.95-5.74 ft) thick; it is thicker than ton Formation includes all sediment lowish brown to dark yellowish previously reported for locations far- deposited at the base of slopes by brown matrix and light brownish ther north (Nelson et al. 1991).This mass wasting and slope wash that gray mottles. The Roxana is oxi- increased thickness is a result of the has accumulated from the end of the dized and leached of carbonate min- proximity of the Waltersburg Quad- Wisconsinan to the present. The Pey- erals in all sections described in the rangle to the ancient Ohio River ton consists of reworked loess, resid- study area. Clay content remains channel (Cache River, Bay Creek). uum, and bedrock clasts. The ~t, fairly constant (20-30%) with depth Nelson et al. (1989) suggested that generally thin, displays textural and and any elevated clay content near the valley now containing the Cache mineralogic characteristics of the the top of the Roxana probably re- River and Bay Creek was used by source material. In larger valleys the sulted from clay elluviated from the the ancient Ohio River between Peyton colluvial material grades lat- Peoria Loess during modem pedo- 25,000 and 12,500 years ago. erally into alluvium that is stratified genesis. The expandable clay miner- The texture of the Peoria Silt and better sorted. An arbitrary verti- als that dominate the upper Roxana ranges from silty clay loam to silt cal line separates deposits that origi- Silt (figs. 19a-e) indicate a north- loam and has a relatively uniform nated mostly from fluvial processes western source for the loess (Frye et sand content. The clay content (Cahokia Formation) from those de- al. 1962).The kaolinite plus chlorite ranges from 15% to 40% and greater rived mainly from colluvial proc- fraction and the sand content in- values are found in the lower part esses (Peyton Formation). The Flat crease toward the base of some sec- (Bt horizon) of the modem soil (fig. Lick transect (fig. 20) shows the tions (figs. 19a-d) and may indicate 19).Near the ground surface, the physical relationship between the mixing of the Roxana with the un- Peoria contains more illite than ex- Peyton Formation, the loess units, derlying Oak forma tion. The Farm- pandable clay minerals. The percent- and the valley deposits in the study dale Soil developed in the Roxana age of expandable clay minerals area. Silt has a distinct platy structure and increases with depth and the a slightly different color and particle kaolinite plus chlorite decreases. tratigraphic Units: size distribution that differentiates This vertical trend is probably a func- Formations the Roxana from the overlying Peo- tion of pedogenesis, provenance ria Silt. change, and mixing with the Roxana uality Formation Willrnan Silt. The elevated ilJite content (figs. and Frye (1970) interpreted the Peoria Silt The Peoria Silt, also 19b-e, 20) indicates that at least a Equality Formation as Wisconsinan- caUed the Peoria Loess, overlies the portion of the loess originated from age lacustrine deposits. Shaw (1915), Roxana Silt and was deposited dur- a northeastern source (Wabash and Frye et al. (1972), and Heinrich (1982) ing Woodfordian Substage of the Ohio River valleys) (Frye et al. 1962). developed a conceptual model for Wisconsinan Stage by eolian proc- The vertical trends in clay mineralogy deposition of the Equality Forrna- esses (McKay 1979). It is the surficial and texture for the Peoria and Rox- tion in the Saline River drainage Roxana [Farmdale]

Vertical distribution of clay minerals and particle sizes for borings (a) W2, (b) W7, (c) W3, (d) W16, and (e) cations see fig. 18 and table 3). Peyton Formation

Peyton Formation Peyton Formation

lower Equality Formation \ upper Equality Formation

A P\ E Bw Bt

CBSI -

BtbI

D Ab p: Peoria Silt r: Roxana Silt o: Oak fm D c: Cahokia Fm e: Equality Fm zb: Buncombe soil zf: Farmdale Soil W12 zs:Sangamon Soil

Figure 20 Cross section showing the distribution of the Quaternary units in Flat Lick Valley (for location see fig. 18). Letters to the left of columns are soil horizon designations. basin northeast of the Waltersburg herein referred to as the upper and graphic unit (Graham 1985) devel- Quadrangle. During the Altonian lower members (fig. 20). Both mem- oped in the top of the upper mem- and Woodfordian Subages of the bers have an unoxidized dark gray ber beneath its contact with the Wisconsinan, the Ohio River carried color. Textures range from silty clay Cahokia Alluvium. glacial outwash and aggraded faster loam to clay with clay content as Heinrich (1982) divided the than tributary valleys south of the high as 80%. The matrix contains pri- Equality Formation in the Saline glacial border. High water levels mary carbonate minerals and shell River Valley into two informal units: and sediment dams formed at the fragments in all described sections. the Altonian Subage Cottage mem- mouth of the Saline River, impound- Illite was the dominant clay mineral ber and the Woodfordian Subage ing water within the drainage basin. in both members, although the per- Texas City member. He differenti- Sediment carried by floodwaters centage of expandable clays in- ated them on the basis of strati- from the Ohio River and sediment creased upward through the upper graphic position and composition. from the watershed accumulated in member (figs. 21a, b). The larger con- Each member was further divided the lake. A similar sequence of tent of expandable clay could have on the basis of color, presence or ab- events explains lacustrine deposits originated from erosion of Roxana sence of carbonate minerals, day discovered in two borings in the Flat Silt from the surrounding uplands mineralogy, and texture. The upper Lick Valley in the southwest corner during deposition of the upper part of the Cottage member (Hein- of the Waltersburg Quadrangle. member. Organic carbon from the rich's unit b) is equivalent to the The Equality Formation in the Farrndale Soil developed in the top lower part of the Equality Forma- Waltersburg Quadrangle can be of the lower member dated at 22,650 tion. His entire Texas City member divided into two informal lithostrati- k440 years BP (ISGS 1604). The Bun- is equivalent to the upper part of the graphic members (Oliver 1988), combe soil, an informal pedostrati- Equality. These suggested correla- I I CLAY MINERALOGY ('lo) DEPTH PARTICLE SIZE (%)

igure 21 Vertical distribution of clay minerals and particle sizes for borings (a) W10, (b) W12, and (c) W9 (for locations see fig. 18 and table 3). nantly fine textured deposits that ac- the lacustrine sediments discussed cumulated in low energy envhn- ments. The coarser end of the spectrum is assigned to the Dolton Member, which is typically sandy ~lpresentshigher energy envhn- study area correlate with the Carmi ments such as beaches, and is not Member, which includes the predomi- pentin the study area. e 8 willman served in the valleys, the Farmdale ing increasingly important; it is in and Frye (1970) interpreted the Ca- Soil developed in the lower Equality these near-surface materials that hokia to consist of Holocene alluvial Formation and is buried by the up- roads, houses, and industrial facili- deposits. The unit is the surface de- per Equality Formation. ties are built, sewers and pipelines posit in all the valleys of the study The Farmdale is recognized by its are laid, crops are raised, and wastes area, excluding the narrow tributary distinctive platy structure, although are buried. The value of the land, valleys in which streams flow on modem pedogenesis has obscured particularly in developing regions, rock. The texture of the Cahokia in- some of its primary features on the is often directly related to its suita- dicates that it originated from loess uplands of the study area. Common bility for such uses. or redeposited loess. The unit over- root traces may be primary features, In the Waltersburg Quadrangle, lies the Equality Formation in the but the presence of many clay films, important land use issues (beyond Flat Lick Valley and ranges from 2.0 manganese and iron oxide concre- agricultural considerations) include to 4.5 meters (6.G14.8 ft) thick in the tions, and stains along root channels the siting of waste disposal (landfill) described sections. In other broad probably reflects overprinting of the operations and major construction valleys within the Waltersburg Farrndale Soil by modem pedogene- projects. The characteristics and Quadrangle, the Cahokia Alluvium sis. In one valley section (fig. 21b), thickness of surficial deposits are may overlie bedrock or the Oak for- the A horizon of the Farmdale soil critical to determining the suitability mation. The Cahokia generally is was presewed. of a site for a particular type of land oxidized to yellowish brown with use. Although no large municipali- light brownish gray and gray beds The Buncombe ties are now located in the study and is leached of carbonate miner- soil, an informal term, developed in area, growth could occur in the re- als. Elevated clay content typically the upper Equality Formation and is gion in future years. Once a general characterizes the gray beds. buried by the Cahokia Formation. area is selected for any prospective The alluvium in the valley bot- Graham (1985) defined the soil us- construction or waste disposal use, a toms may grade into the colluvium ing borehole sections observed detailed site evaluation must be of the Peyton Formation near steep along the upper Cache River valley made of the surface deposits before slopes along valley walls. The ma- h the study area the Buncombe soil the facility can be designed and con- trix of the Cahokia Alluvium is silty; shows evidence of translocated clay structed. This section summarizes its textures are similar to the source fine root traces, and manganese and the basic characteristics of surface materials, the upland loess deposits, iron oxide concretions, and stains. materials in the quadrangle that can and residuum. Typical textures in- affect waste disposal, construction clude silt loam, silty clay loam, and practices, and seismic risk considera- silty clay. tions related to such projects. A change in clay mineralogy dis- In many areas, unconsolidated surfi- tinguishes the Cahokia Alluvium cia1 deposits contain a variety of from the underlying Equality For- natural resources such as groundwa- Municipal wastes includes house- mation in the Flat Lick Valley. The ter, gravel, sand and day; however, hold refuse and nonsalvageable expandable clay content of the Caho- no significant resources have been commercial wastes such as metal kia generally increases with depth, found in the thin surficial deposits and paper. This type of waste is com- whereas the expandable clay con- of the study area. The unconsoli- monly buried in sanitary landfills. tent of the upper member of the dated units do not include any later- The primary consideration in locat- Equality formations generally de- ally extensive aquifers. The upland ing a sanitary landfill is minimizing creases with depth (figs. 21a-c). The loess and residuum are generally un- the migration of leachate (a solution top of the Buncombe soil marks the saturated and the valleys contain produced when infiltrating water re- contact between the two units. fine textured sediments that seldom acts with the refuse) into groundwa- yield groundwater in economic ter and surface water. Guidelines of quantities. Isolated sand lenses the Illinois Department of Public within the valley deposits may yield Health (1466) require that in select- Sangatlaon So The Sangamon sufficient groundwater to supply a ing a sanitary (municipal) landfill Soil developed in the Oak formation single-family dwelling, but these site (1) no waste can be disposed in before deposition of the Roxana Silt lenses are generally found by standing water, (2) no waste can be on the uplands of the Waltersburg chance. The study area does not con- disposed in areas with a high water Quadrangle. The Sangamon Soil is tain economic deposits of sand and table unless preventative measures distinguished from other pedologic gravel aggregate within the surficial are taken to prevent leachate migra- units by its stratigraphic position and materials. The weathered silt depos- tion, (3) no surface runoff should strength of development; in described its that cover the upland have little flow into or through the operation sections, it has a pronounced Bt hori- commodity value except for con- or completed fill area, and (4) no dis- zon and a moderate to strong blocky struction fdl or clay pr6duas such posal should take place "unless sub- fabric that is co~monlycalled soil as brick. soil material affords reasonable strum. assurance that leachate from the landfill will not contaminate ground F USE or surface water." Soil developed in the Roxana Silt on The value of surficial deposits of a In general, no site within the Wal- the uplands of the study area and is region in terms of material and tersburg Quadrangle is suitable for a buried by the Peoria Silt. Where pre- space for various land uses is becom- sanitary landfill ~mlessmeasures are taken to prevent the migration of steep slopes. Conditions on the up- face drainage, and silty materials leachate. The upland loess units lands are most favorable. Loess, a having low bearing capacity. Flash throughout the study area are less flooding is also a distinct possibility than 3 meters (9.8 M) thick, too thin for disposal trenches or for use as a source for trenchcover material. Fre- quent flooding and high water s in a zone of high tables (generally within I m of the cal evidence indi- surface) eliminates the valley areas probably has a moderate bearing ca- cates that earthquakes of large mag- for consideration as sanitary landfill p acity. nitude, associated with the New sites. No major bedrock aquifers are Oliver (1988) estimated the soil Madrid Fault Zone in eastern Mis- located in the study area, but the up- cohesion by determining the uncon- souri, could impact the area. In the land units generally overlie sand- fined compressive strength of the winter of 1811-1812, a series of ma- stone that serves as a minor aquifer. Peoria Silt and the Roxana Silt in the jor earthquakes shook the region If no other site is available within a and intensities of IX or X on the reasonable distance of a community, modified Mercalli Intensity Scale a sanitary landfill could be located were probably experienced in the in the study area if the landfill is area of the Waltersburg Quadrangle. lined and leachate is collected and Earthquakes of this intensity could treated. cause total destruction of weak struc- Even more stringent geologic con- be attributed to its higher percent- res and major damage to well ditions are required for the safe dis- age of clay-sized materials and its built structures (Nuttli 1973). posal of hazardous waste, including lower percentage of expandable clay Structures built in the valley bot- toxic chemical, biologic, radioactive, rninerals relative to the Roxana Silt. toms of the shdy area are most at flammable, and explosive refuse. No Sandstone bedrock underlying risk; the thick, unconsolidated, and suitable sites for hazardous waste the surficial material in many up- saturated deposits found in these disposal were found in the study land positions has a high bearing areas generally amplify seismic area. capacity and is generally found at waves and are prone to liquefaction, depths less than 3.0 meters (9.8 ft). which causes a significant loss of The shallow bedrock may be advan- bearing capacity. Structures having Most general construction projects tageous for projects requiring high foundations in bedrock are at less such as subdivisions, small busi- bearing capacity, risk. The foundations of critical nesses, roads, drainage systems, and in excavating for sewer lines, water structures, such as hospitals, water and sewage ]lines can be sited, lines, or septic system. The valley schools, and emergency service ten- if properly designed and built, bottoms are generally not suitable ters should be constructed in the nearly everywhere in the study area. for construction. These areas are bedrock on gently sloping uplands. exceptions are valleys prone to characterized by a high water table flooding or those with ext~mely (less than 1m in places), poor sur- The Waltersburg Quadrangle is situ- Within the study area, the Lusk sures are marked by outcrops and ated near the south margin of the Creek Fault Zone has an average float of fractured, silicified sand- Illinois Basin. Paleozoic strata re- trend of N45"E and varies in width stone and brecciated limestone. Frac- gionally dip northward at an aver- from a few yards to about 1,400 feet. tures and crevices are filled with age rate of a few degrees toward the Numerous deep ravines cross the white calcite, and quartz, as well as center of the basin. Only a few miles northern part of the fault zone and minor amounts of fluorite and metal- south of the quadrangle, Cretaceous afford excellent exposures of its lic sulfides. Numerous prospect pits and Tertiary sediments overlap structure. Near the west edge of the and a few small abandoned mines Paleozoic rocks at the north edge of quadrangle, the zone is not well ex- occur along the faults. Angled bor- the Mississippi Embayment. The posed. Information from outcrops is ings in the fault zone in the northern Waltersburg Quadrangle is domi- supplemented by proprietary well part of the study area indicate that nated by northeast-trending fault data and seismic reflection data. the major faults dip 60" to 70°SE zones (fig. 3), which are part of the The net displacement of the Lusk (Robert Diffenbach, personal com- Fluorspar Area Fault Complex. Creek Fault Zone is 600 to 900 feet munication, 1985).Interpretation of Three previously named fault down to the southeast. Mississip- a proprietary seismic profile and zones-the Lusk Creek, Raum, and pian rocks northwest of the fault interpretations by Bertagne and Hobbs Creek--cross the quadrangle. zone are juxtaposed with Pennsylva- Leising (1991) indicate that the Lusk The newly named Flick Branch nian rocks southeast of the zone. Creek Fault Zone dips steeply to the Fault is southeast of the Hobbs The downdropped block southeast southeast from the surface down to Creek Fault Zone. of the Lusk Creek is the Dixon the Precambrian crystalline base- The structural pattern mapped Springs Graben (J. Weller 1939).The ment. here differs from that shown by S. graben is bounded on the southeast An unusual feature of the Lusk Weller and Krey (1939) primarily in by the Hobbs Creek Fault Zone and Creek Fault Zone is the presence of detail, but several faults they bisected by the Raum Fault Zone. narrow slices of upthrown rock mapped were not substantiated by Pennsylvanian beds immediately within the fault zone. Slices of rock this study. Minor discrepancies in southeast of the fault zone dip south- older than that on either side of the fault mapping exist between the pre- east away from the zone, at angles zone occur at several places in the sent map (Weibel et al. 1992) and the as steep as 70". Dips rapidly dimin- study area (fig. 22). The best exam- geologic map of the adjacent ish southeastward, toward the axis ple is at the Clay Diggings Mine, Shetlerville Quadrangle (Baxter et of a syncline, which lies 1/4 to 1/2 where a quarry highwall exposes al. 1967).The discrepancies involve mile southeast of the Lusk Creek the Ste. Genevieve Limestone and faults of small displacement in areas Fault Zone. Between the syncline St. Louis(?) Limestone. Angled cores of poor exposure. and the Raum Fault Zone, bedding drilled through the fault zone also dips 4" to 12"NW. Two northwest- encountered these limestones at dipping, high-angle, normal faults shallow depths in the fault zone The Lusk Creek Fadt Zone (J. Wel- of small displacement are near the (Diffenbach, personal communica- ler et al. 1952) is the northwestern- synclinal axis close to the north edge tion, 1985). These formations are up- most of thenamed fault zones in of the quadrangle. thrown 800 to 1,500 feet relative to the study area, and it delimits the Northwest of the Lusk Creek their positions on either side of the northwest margin of the Fluorspar Fault Zone, bedding distal to the fault zone(fig .22b). Upthrown slices Area Fault Complex. The Lusk zone dips northwest at an average containing the Vienna and Menard Creek is exposed for about 28 miles, of about 3", but proximal to the Limestones occur northeast of the of which 7.5 miles lie within the zone, bedding generally dips 10" to Clay Diggings Mine along the north- study area. The Lusk Creek merges 30°SE (toward the faults). In parts of east-trending ravine in the NW NE, with the Shawneetown and Herod Sections 29 and 30, T12S, R6E, strata Section 10, T12S, R6E. Outcrops and Fault Zones northeast of the Walters- near the northwest side of the fault float of Ste. Genevieve(?)also occur burg Quadrangle, and it is buried by zone dip northwest as steeply as 41 ". along the fault zone between the Cretaceous strata in the Mississippi Thus, bedding is upturned toward mine and Copperous Branch. Embayment southwest of the quad- the fault zone on both sides, as Similar examples of upthrown rangle (fig. 3). Kolata et al. (1981) shown in the cross section attached slices in the Lusk Creek Fault Zone mapped a subsurface continuation to the geologic map (Weibel et al. are documented both north of the of the Lusk Creek Fault Zone in 1992). study area in the Eddyville Quad- Paleozoic bedrock beneath the Em- The Lusk Creek Fault Zone is rangle (Nelson et al. 1991) and west bayrnent. composed of high-angle faults, most of the area in the Glendale Quadran- of which dip southeast. Fault expo- gle (Devera 1991). Downthrown fault slices are p~s- bounded by reverse and normal bayment (S. Weller and Krey 1939, ent in the form of narrow wedges of faults. In all cases, bedding within Ross 1963, Gause 1966). conglomeratic sandstone of the slices dips steeply southeast, com- In the Waltersburg Quadrangle, Caseyville Formation, faulted monly subparallel to the fault dips. the Raum Fault Zone is 7,500 to against Mississippian rocks on both Interpretation of the unusual struc- 12,000 feet southeast of the Lusk sides (fig. 22). The downthrown ture of the Lusk Creek Fault Zone Creek Fault Zone. The Ram is Caseyville slices, in most cases, will be discussed at the end of this mapped as a single fault or as a zone occur northwest of the upthrown section. of faults generally less than 300 feet slices of Mississippian rocks de- wide. At the surface, the Caseyville scribed above. A wedge of rock con- Formation and upper Pope Group taining Caseyville and Tradewater The Raum Fault Zone (Baxter et al. are displaced with net throw down strata is faulted between two slices 1967) is a narrow zone of faults that to the northwest. The net throw in- of Mississippian rock at the mid- lies southeast of, and forms a graben creases from less than 100 feet near point of the boundary between Sec- with, the Lusk Creek Fault Zone the northeast comer of the quadran- tions 20 and 21, T12S, R6E (fig. 22c). (fig. 3). The RamFault Zone ex- gle to 200 to 300 feet near the south- The Lusk Creek Fault Zone con- tends southwestward from a com- west corner. tains both normal and reverse faults plexly faulted area on the west flank Strata on both sides of the Raum (fig. 22). The southeasternmost fault, of Hicks Dome in the Shetlerville Fault Zone generally dip less than a normal fault that borders the Quadrangle (Baxter et al. 1967), 5"W.The dips steepen up to Dixon Springs Graben, exhibits the crosses the Waltersburg Quadrangle, 85"W close to and within the fault drag folding typical of a normal and continues beneath the Creta- zone. The dips are consistent with fault. Upthrown and downthrown ceous overlap in the Mississippi Em- the displacement and are probably slices within the fault zone are the result of drag. In some places,

Figure 22 Cross sections of Lusk Creek Fault Zone. (a) Ora Scott Mine, S1/2 SE NW, Section 10, T12S, R6E. The central upthrown slice of Chester Group strata is flanked by downthrown slices of Caseyville. (b) Clay Diggings Mine, SW NE SE, Section 16, TlZS, R6E. The fault zone contains an upthrown slice of St. Louis(?) and Ste. Genevieve Limestones and a downthrown wedge of Caseyville. (c) SE NE, Section 20, T12S, R6E, and NW SW, Section 21, T12S, R6E. The downdropped block of Pennsylvanian strata is between two upthrown slices of Mississippian rock. drag folding is absent, for example, near Sulphur Springs Church in Sec- tions 20 and 27, T12S, R6E, and northwest of Rising Sun in Sections 5,6, and 7, T13Sf R6E. Outcrops, well records, and a proprietary seismic profile indicate that the major faults dip steeply northwest. A major fault, exposed in a gully just northeast of the stream in the SW NW,, Section 13, T12S, R6E, strikes N45"E and dips 60" to 80°NW,. The fault is marked by a zone of fractured and brecciated rock. Angled core holes in the vicinity of Raum penetrated as many as four high-angle, northwestdipping fault planes in the Raum Fault Zone (Diffenbach, personal communication, 1985).The seismic profile shows that the Raum is an antithetic branch of the Lusk Creek Fault Zone, intersecting the latter in Up- per Cambrian or Lower Ordovician strata. Figure 23 Cross sections of Raum Fault Zone. (a) Center NW, Section 13, T12S, R6E. Similar to the Lusk Creek, the Displacement across fault zone is small, but the central slice of Chesterian rock is up- Raum Fault Zone contains slices of thrown several hundred feet relative to Pennsylvanian rocks on both sides. (b) Bank rock that are upthrown relative to of Lusk Creek, N1/2 NE, Section 5, T13S, R6E. Net displacement is down to north- both bordering blocks. A slice of Mis- west; slices of Chester Group strata are upthrown and tilted southeast. sissippian rock occurs between Pennsylvanian rocks near the east edge of the quadrangle in Sections Along most of its length in the crop. The straight trends of the 13 and 14, TI%, R6E (fig. 23a). The Waltersburg Quadrangle, the Hobbs faults across rugged topography in- upthrown slice is bounded by a nor- Creek Fault Zone is composed of the dicate steep dips. In the Shetlerville mal fault on the northwest and a two faults that form a graben 800 to Quadrangle, the Shelby Fault (part reverse fault on the southeast. Rocks 4,000 feet wide. The southeastern of the Hobbs Creek Fault Zone) is a within and bordering the upthrown fault is downthrown to the north- normal fault that dips 60" (J. Weller slice dip steeply northwest and are west and is the larger of the two. Ver- et al. 1952).The general absence of strongly sheared and fractured; how- tical separation on this fault is more drag structures and wide, fractured ever, little displacement has occurred than 250 feet near Waltersburg, and brecciated zones is also sugges- across the fault zone. where the Caseyville Formation is tive of normal faulting. Strata adja- Another upthrown slice in a cut juxtaposed against the Menard cent to and within the Hobbs Creek bank of Lusk Creek in the N1/2 NE, Limestone and Palestine Sandstone. Fault Zone generally dip northwest Section 5, T13S, R6E (fig. 23b) ex- The displacement decreases toward a few degrees, in contrast to the poses Degonia and Clore strata, the northeast and is only about 20 steep dips along the Lusk Creek and faulted against Caseyville on the feet near the east border of the quad- Raum Fault Zones. northwest and against Degonia on rangle. The northwestern fault has a A triangular fault slice, obliquely the southeast. Bedding of the up- maximum throw of 70 feet, but crossing the Hobbs Creek Fault thrown slice dips 38" to 44"SE, con- along most of its length the displace- Zone, occurs near the common cor- trary to the generally prevailing ment is less than 40 feet. This fault ner of Sections 3,4,9, and 10, T13S, northwest dips in the Raum Fault may die out to the northeast, where R6E. The slice contains Kinkaid Zone. it lines up with a fault mapped in Limestone and is upthrown relative the Shetlerville Quadrangle by Bax- to adjacent rocks within the fault Hobbs Creek Fault Zone ter et al. (1967). zone. It is in an intermediate struc- The Hobbs Creek Fault Zone (Baxter Faults of the Hobbs Creek Zone tural position relative to the lower et al. 1967), southeast of the Raum are high angle or nearly vertical. The rocks southeast of the fault zone and Fault Zone, extends from the west best exposure of a fault plane is on the higher rocks northwest of the side of Hicks Dome to the edge of an outcrop of the Caseyville Forma- zone. Thus, this slice differs from the Mississippi Embayrnent (fig. 3). tion in the NE SE NE NE, Section 9, slices in the Raum and Lusk Creek It is a zone of normal faults having T13S, R6E, where the fault plane is Fault Zones, in which slices are overall downward displacement to juxtaposed with the Degonia Forma- structurally above the adjacent the northwest; the zone delimits the tion. A surface that is parallel to the strata. The slice in the Hobbs Creek southeast margin of the Dixon fault trace and contains vertical (dip- Zone is a small horst, bounded by Springs Graben. slip) slickensides occurs on the normal faults, within a graben. The southeast side of the sandstone out- large northwest-dipping fault, on Figure 24 Field sketch of deformed Tradewater strata exposed in stream bank, NW SW W,Section 14, T12S, R6E (see fig. 25). Folding, bw-angle faulting, and a sandstone dike are visible. A-White, fine grained, massive, quartz sandstone; B-brown gray, very fine grained, micaceous, argillaceous, thin bedded sandstone; C-dark gray, silty, carbonaceous shale; D-dark gray, bioturbated, carbonaceous siltstone; E-black, fissile, carbonaceous shale; and F-sandstone dike associated with listric fault. the southwest side of the Hobbs Lusk Creek Fault Zone may have Creek Fault Zone, is the master fault been active during deposition of the of the system; other faults probably 12, the Tar Springs Sandstone dips Pennsylvanian Caseyville and Trade- intersect it at depth (see cross sec- about 20°SE Oames Baxter, personal water Formations. The basal "Way- tion on geologic map (Weibel et al. communication, 1990).The fault side" member of the Caseyville 1992)). probably is a normal fault having thickens abruptly from about 20 feet downward displacement of 10 to 20 northwest of the fault zone to 140 Fa feet to the southeast. feet or more southeast of the zone. The Flick Branch Fault is southeast Paleo- slump structures, such as the of the Hobbs Creek Fault Zone and one illustrated in figure 18, are com- extends N55"E from Waltersburg to mon in the "Wayside" southeast of the east edge of the quadrangle, tucky Fluorspar Dis- the fault zone. These slumps may where it connects with a fault trict is among the most complexly have been triggered by seismic activ- mapped by Baxter et al. (1967) in the deformed areas of fie North Ameri- ity during deposition of the "Way- Shetlerville Quadrangle. The fault can midcontinent, and it has a long side." Coarse conglomerates passes near the mouth of Flick history of faulting. Previous workers containing large clasts of sedimen- Branch and takes its name from that who have discussed regional rela- tary rocks are interbedded with fine stream. The Flick Branch probably is tionships and timing of events in- grained strata of the "Wayside" a high-angle normal fault. The north- within the Dixon Springs Graben. west side is downthrown about 65 The clasts may have been derived feet at the east border of the quad- Sutton (1951), Hey1 and Brock from nearby bordering fault scarps. rangle, and about 100 feet in the (1961), Hey1 et al. (1965), Hook Deformed bedding in the Trade- vicinity of Waltersburg. Mississip- (1974), Trace (1974), Trace and Amos water Formation (fig. 24) is common pian formations from the Clore to (1984), and Nelson and Lumm along the axis of the synche that the Tar Springs are displaced. Strata (1987).These workers outlined a va- lies just southeast of the Lusk Creek on both sides of the Flick Branch riety of scenarios, but all recognized Fault Zone. In one area, deformed Fault dip northwest at an average of recurrent events of faulting, doming, lower Tradewater and upper Casey- about 5". Dips as steep as 35"NW igneous intrusion, and mineraliza- ville strata (Pounds Sandstone) occur close to the fault plane and are tion, extending from late Paleozoic contain large rotational slump attributed to drag. Along part of its into Cenozoic time. blocks that are outlined by listric length, the Flick Branch Fault splits Evidence within the Waltersburg normal faults (fig. 25). The beds are into two faults that outline a graben. Quadrangle supports at least three, folded and penetrated by sandstone and possibly four, episodes of fault- dikes. These structures indicate ex- ing, which in some cases involved tensive failure of sediments prior to A fault having a trend of N20°E is in- reversals in the direction of slip lithification, perhaps in response to terpreted to be in Sections 9 and 16, along the same fracture surfaces. tectonic activity. This activity is con- T13S, R6E. This fault diagonally A proprietary seismic profile sup- sistent with the downward move- links the Flick Branch Fault with the ports Bretagne and Leising's (1991) ment of the Dixon Springs Graben Hobbs Creek Fault Zone. The fault is interpretation that Cambrian strata during the Morrowan and Atokan indicated by juxtaposition of Clore are thicker on the southeastern, Epochs. In addition, the middle Limestone against Menard and downthrown side of the Lusk Creek sandstone unit of the Tradewater Palestine Formations. It has a down- Fault Zone than they are on the thins and grades laterally into shale ward displacement of 50 to 100 feet northwestern, upthrown side. This southeast of the syncline in the SW, to the east. thickness pattern is the result of nor- Section 15, T12S, R6E. This facies A fault striking N45"E in Section mal movement of the fault zone dur- change possibly indicates the influ- 12, T13S, R6E, was extrapolated into ing Cambrian sedimentation. ence of local structural movement this quadrangle from the Shetlerville Thickness patterns and paleo- during deposition. Quadrangle, where it is more clearly slump features indicate that the Figure 25 Interpretive sketch (not to scale) of deformed Pounds Sandstone and Tradewater strata discontinuousPy exposed along a large ravine in the SW NW, Section 14, T12S, R6E and SE NE, Section 15, T12S, R6E. Listric normal faulting (rotational slumping) occurred during deposition of carbonaceous shale. Slumping may have been triggered by tectonic movements along the Lusk Creek Fadt Zone, about 1mile northwest of this site.

The Lusk Creek Fault Zone dis- Zones indicate that the last major fault slices of the Raum Fault Zone places the Tradewater Formation, displacements in both zones were (fig. 23b), and upthrown slices also indicating that most faulting is normal. Bedding along both fault may be remnants of reverse drag. post-Atokan. Other faults in the zones dips predominantly toward The upthrown slices are fragments study area are parallel to the Lusk the downthrown block (footwall). of the hanging wall and were up- Creek and exhibit similar geometry, Hence, reverse movements must lifted during reverse faulting. In indicating a similar history of move- have occurred earlier than the nor- some places, the earlier reverse ment. Most of the faults in the quad- mal movements. Drag from the later faulting and later normal faulting rangle are high-angle normal faults, normal movement may have obliter- occurred along different fault planes indicating a stress field with north- ated drag structures that had (figs. 23/24), and slices of rock west-southeast extension. formed during the earlier reverse between the two faults were left Reverse faults and upthrown faulting. Possible remnants of the re- behind when the hanging wall fault slices in the Lusk Creek and verse drag occur in a few places. subsided during normal faulting Raum Fault Zone cannot be ex- Along the Lusk Creek Fault Zone, in (fig. 26). plained by extension. An episode of the line of the cross section on the Downthrown slices in the Lusk compression is required to induce re- geologic map (Weibel et al. 1992), Creek Fault Zone probably formed verse faulting. Bedding attitudes in beds dip away from the fault on during the later phase of normal and near the Raum and Lusk Creek both sides. The southeastdipping faulting. These slices are wedge- shaped fragments of the footwall that were rotated and dragged downward (fig. 26). Although several studies have indicated strike-slip movement on northeast-trending faults in the fluorspar district (Hey1 and Brock 1961, Hook 1974, Trace and Amos 1984), no evidence for horizontal movement was found in this study. The nearly vertical plunge of slickensides, parallelism of faults and drag folds, and absence of en echelon or pinnate structures point to predomi-, nantly dip-slip movement. In summary the following sequence of structural events is pro- Figure 26 Origin of upthrown and downthrown slices in Lusk Creek Fault Zone. posed (fig. 27). (a) Reverse faulting occurs along fault B, southeast black uplifted. Faults A and C are (1) Rifting occurred during the incipient. (b) Later normal faulting occurs, southeast block downdropped. Most dis- Cambrian Period; the Lusk Creek placement occurs along faults A and C. An "upthrown"wedge of rock is caught be- Fault Zone developed as a normal tween faults B and C, whereas a slice of rock is downdropped between faults A and B. fault (southeast side down). 1 Lusk Creek Raum 1

Lusk Creek

Lusk Creek d

L> rV 7r 7 vrv

Figure 27 Interpretive structural history of the Waltersburg Quadrangle. (a)Cambrian rifting. (b) Possible Morrowan-Atokan normal faulting. (c) Post-Pennsylvanian reverse faulting. (d) Final episode of normal faulting.

(2) Additional normal faulting on brian normal displacement @owe The presence of the McCorrnick the Lusk Creek Fault Zone may and Thompson 1984). These faults and New Burnside Anticlines (fig. 3) have occurred during the Morrowan define the northwest margin of the northwest of the Lusk Creek Fault and Atokan Epochs, influencing Reelfoot Rift (Ervin and McGinnis Zone indicates that the northwest thickness and facies patterns and in- 1975), a failed intracratonic rift. At boundary of the reactivated Reelfoot ducing slumping of Caseyville and its northeast end, the Lusk Creek Rift may have shifted northwest- Tradewater sediments prior to lithifi- Fault Zone merges with the Rough ward during the late Paleozoic. Seis- cation. Creek-Shawneetown Fault System mic data indicate that the faults (3) Post-Atokan reverse faulting (fig. 3), which is the north boundary associated with these anticlines do along the Lusk Creek and Raum of the east-trending Rough Creek not extend to the basement. These Fault Zones (which merge at depth) Graben (Soderberg and Keller 1981, faults are probably listric faults that uplifted the intervening block. Bretagne and Leising 1991).Seismic parallel bedding planes and prob- (4) The final episode of faulting profiles across the Rough Creek- ably merge with the Lusk Creek was extensional and induced nor- Shawneetown Fault System indicate Fault Zone at depth. The anticlines mal displacements on faults in the normal displacement (down to the are the product of post-Pennsylva- study area. south) occurred during the Cam- nian compressional reactivation of This sequence of events is similar brian Period (Bretagne and Leising the rift faults. to that inferred for the Rough Creek- 1991).Thus, during the Cambrian A recent study by Hildenbrand et Shawneetown Fault System (Nelson and perhaps later, in the Rough al. (1992) suggests that correlative and Lumm 1987, Bretagne and Creek-Shawneetown, Lusk Creek, magnetic and gravity anomalies Leising 1991, Kolata and Nelson 1991). and the Reelfoot Rift northwest- about 80 kilometers (50 mi) north- The Lusk Creek Fault Zone is bounding faults in southeastern west of the Lusk Creek Fault Zone nearly aligned with faults in south- Missouri and northeastern Arkansas (Johnson County) may be indicative eastern Missouri and northeastern were an interconnected rift-bound- of a mafic intrusion along the north- Arkansas, where seismic profiles in- ary fault system. west boundary of the rift structure. dicate more than 10,000 feet of Cam- The age of this pluton is not known. The principal geologic resources in either the McClellan Mine or the Sandstone (Grogan and Bradbury the Waltersburg Quadrangle are Luella Mine is probably the same as 1968). Throughout the quadrangle, limestone for construction and agri- the Ora Scott Mine, but absence of these formations occur at depth, and cultural purposes, and sandstone for precise locations precludes accurate in most cases, below the level of construction purposes. Fluorspar identification. past mining and prospecting. In the and base metals have been mined Prospect pits and waste piles Lusk Creek Fault Zone, the wallrock along fault zones in the past; addi- near the head of a small ravine for ore is mainly the uppermost Mis- tional resources may exist in the sub- about 1,000 feet north of the Ora sissippian and the lower Pennsylva- surface. Resources of coal are small; Scott Mine indicate possible pre- nian. The Clay Diggings Mine is the coal beds are too thin and discon- vious exploration or small scale min- only place in the quadrangle where tinuous to be exploited economi- ing. J. Weller 's (1943a) map indicates mineralization occurs at the surface. cally. Few exploration wells for an abandoned shaft surrounded by Thus, the potential for shallow re- petroleum have been drilled, and several prospect pits in this area. sources is low. Unknown deeper re- much of the quadrangle has yet to Other small abandoned mines sources may be present, particularly be tested. The resource potential and prospect pits occur along the in the interval from the St. Louis to (e.g., groundwater, sand and gravel) fault zone, but they are not shown the Cypress, along the Lusk Creek of the surficial geologic materials of on the geologic map (Weibel et al. Fault Zone and other faults in the the quadrangle have been pre- 1992).J. Weller (194310) reported that Waltersburg Quadrangle. The ongo- viously assessed in the section on although this area had character- ing Conterminous U.S. Mineral As- surficial stratigraphy. istics similar to both the Ora Scott sessment Program (CUSMAP) is and Clay Diggings Mines, minerali- attempting to determine the likeli- zation had not been reported. The hood of finding additional mineral Fluorspar and associated minerals Ozark-Mahoning Company drilled resources in the area. have been produced from vein de- angled core holes for prospects posits in the quadrangle, which lies along the Raurn Fault Zone (Robert estone on the west margin of the Illinois- Diffenb ach, personal cornrnunica- The Kinkaid and Menard Lirne- Kentucky Fluorspar District. Several tion, 1985). stones offer the best prospects for abandoned fluorspar mines and The mineral deposits in the Illi- small or moderate quarry opera- prospect pits occur along the Lusk nois-Kentucky Fluorspar District tions in the Waltersburg Quadran- Creek Fault Zone. The Clay Dig- occur as vein deposits in breccia gle. Limestone resources of gings Mine, also known as the zones and fissures dong faults, bed- southernmost Illinois, including the Pittsburg Mine, consisted of at least ded replacement deposits in the Waltersburg Quadrangle, were five shafts between 70 and 85 feet wall rocks of the faults, and residual evaluated in a regional study by deep. The shafts followed narrow deposits (J. Weller et al. 1952). In the Lamar (1959).His report is the pri- veins and breccia containing fluo- Waltersburg Quadrangle, known mary source for the following evalu- rite, galena, and sphalerite (Bain mineral deposits occur only as vein ations. The Kinkaid Limestone has 1905, J. Weller 1944, J. Weller et al. deposits. The chief minerals in vein the thickest limestone beds and the 1952).Very little is known about the deposits in the district are fluorite best potential in the quadrangle for early production history of this and calcite, but sphalerite, galena, limestone production for Portland mine; it produced fluorspar from and barite are locally abundant (Bax- cement, agricultural limestone, and 1939 to 1941 and possibly in 1942. ter and Bradbury 1989). Most eco- crushed rock; however, the Kinkaid, The Ora Scott Mine, in the S 1/2 nomic vein deposits of fluorspar locally contains shale beds and chert SE NW, Section 10, T12S, R6E, pro- have occurred along faults of moder- nodules that are deleterious to com- duced a small amount of fluorspar ate displacement (J. Weller et al. mercial production. The Goreville from small veins within brecciated 1952).These ore bodies are associ- Limestone Member of the Kinkaid limestone and quartz sandstone (J. ated with faults of 25 to 500 feet dis- was quarried about 1mile south- Welier et al. 1952). According to J. placement. These faults apparently southeast of Eddyville (SE NE SE, Weller (1943a), mining was initiated provided the optimum avenues and Section 17, T12S, R6E). J. Weller et al. around 1900, and in the following 40 open fissures for fluid circulation (1952) also reported that the Kinkaid or 50 years, a total of more than and mineral deposition (Baxter and Limestone was quarried during the 1,000 tons of fluorspar was extracted Bradbury 1989). 1930s by the Civilian Conservation on an intermittent basis from several Vein deposits in the Illinois-Ken- Corp at the Clay Diggings Mine, adits and shafts. The last known tucky Fluorspar District are concen- along Lusk Creek in the SE, Section year of production was 1952. Of the trated in the interval from the St. 16, T12S, R6E. Examination of the two mines described by Bain (1905), Louis Formation up to the Cypress site indicates that the Ste. Genevieve Limestone and possibly other lime- at a depth of 1,000 feet. The wells and Tradewater Formations at sev- stones were quarried. The Glen presumably were drilled for oil in eral sites in the quadrangle, particu- Dean and Cora Limestones gener- fault-bounded structural traps. No larly from the lower Tradewater. The ally contain shale beds and are too oil shows were reported in any of mines consisted of shallow drift and thin to be quarried. The Menard the wells. small strip mines; all are now aban- Limestone contains shale beds and The predominant source rocks for doned. The remaining coals occur in chert nodules, but may have lirne- oil produced in the Illinois Basin are thin or lenticular beds that have stone beds thick enough in some organic-rich shales of the Devonian- poor potential for commercial exploi- places to be used for agricultural Mississippian New Albany Group tation. limestone and crushed rock. The (Barrows and Cluff 1984). In the Wal- Coals in the Caseyville Formation Vienna Limestone is thin and con- tersburg area, studies of source consist only of small, isolated pods. tains abundant chert nodules, pre- rocks indicate the New Albany is an Near the center, S1/2 NE SE, Section cluding it as a limestone resource. excellent source rock and is within 8, T13S, R6E, about 1.3 feet of shaley the oil maturation window (Barrows coal crops out in a small ravine in Sandstone and Cluff 1984).Older and deeper which a small amount of coal was Thin bedded sandstone in the 'Way- Ordovician and Cambrian source mined, apparently for local use. side" Member of the Caseyville For- rocks may be present in the area, but Palynological and biostratigraphic mation is quarried in the NE corner, the distribution and quality of these analyses (Peppers, personal commu- Section 27, T12S, R6E for use as flag- sediments is not established. The nication, 1987) indicate the coal is in stone and facing stone (The geologic presence of Early Cambrian (pre-Mt. the lower Caseyville Formation. map of Weibel et al. [I9921 does not Simon Sandstone) rift-fill shale sedi- H. R. Wanless (unpublished ISGS have a quarry symbol.) Similar rock ments within the Reelfoot Rift/ field notes, 1934) reported 2.2 feet of crops out along the Beatty Branch Rough Creek Graben has been sug- "shaley"coal cropp& out near an and in Flick Branch valley. gested by Wester (1983) and Kolata abandoned mine drift in the ravine and Nelson (1991). Verification of (near center SW, Section 5, T13S, Clay these sediments in this region and R6E) north of Rising Sun. Wanless Clay was mined from a shaft at the their analysis for a potential source referred to the coal as the "Wayside" Clay Diggings Mine from about rock await the drilling of a well coal, but this designation was made I866 to 1907 (Lamar 1942). The clay through the Paleozoic sediments to on the basis of stratigraphic relation- deposit, about 15 feet wide, was lo- the Precambrian basement. ships and without the aid of palynol- cated along the major fault of the Complex regional faulting, ogy. Neither the outcrop nor the Lusk Creek Fault Zone (Engelmann sparseness of drill hole data, and drift opening could be located dur- 1866b, Purdy and DeWolf 1907) and lack of seismic data further limit the ing this study. This coal is probably on the northwest side of the narrow evaluation of possible hydrocarbon younger than the lower Caseyville Ste. Genevieve fault block. Lamar traps. Structural closures may exist coal described above, although it is (1942) analyzed samples of the clay along faults in the quadrangle, but it possible that the coals are the same from waste piles and identified the is not known whether faults in this age. A small, lenticular coal bed in clay as halloysite. The quantity of area are barriers to hydrocarbon mi- the Pounds Sandstone crops out clay is unknown. gration. Most of the quadrangle, in- along Lusk Creek in the SW SW SE, cluding areas adjacent to faults, has Section 32, T12S, R6E. The bed is not been tested. Upper Mississip- less than 0.5 feet thick, and the Three unsuccessful oil and gas ex- pian and Pennsylvanian rocks, lower part is argillaceous. Several ploration wells have been drilled in which are the most prolific and prospect pits surround the exposure, the quadrangle. The wells were widely distributed reservoirs in Illi- but it appears that very little coal ranked as wildcats because they are nois, are exposed at the surface (or was mined. more than 1.5 miles from established eroded) and flushed of hydrocar- The Tunnel Hill(?) Coal Bed in commercial operations. The quad- bons. Reservoir characteristics of the lower shale and sandstone mem- rangle lies about 10 miles south of buried, pre-upper Mississippian ber of the Tradewater Formation the Mitchellsville Oil Field, the strata are unknown within the quad- cropped out south of the Mount southernmost oil field in Illinois rangle, although the potential for Zion Church in the center S 1/2 S (located in TlOS, R6E). The Minton- the occurrence of hydrocarbon accu- 1/2, Section 12, T13S, R5E. It was in- Baker No. 1Well was drilled in the mulations associated with Silurian termittently mined by several com- horst between the Raum and Hobbs pinnacle reefs in the area has been panies from the 1930s to the late Creek Fault Zones to the Mississip- postulated by Whitaker (1988). The 1970s. Production figures are not pian Haney Limestone Member of inferred reversals of displacement available, but the mine reportedly the Golconda Formation at a depth along the Lusk Creek and Raum produced 5,955 tons in 1970. The of 610 feet. The Austin Roberts No. 1 Fault Zones could diminish the go- coal contained several clay partings Well was drilled between the Hobbs tential for petroleum occurrences be- and varied in thickness from about Creek Fault Zone and the Flick cause hydrocarbons may have been 2.5 to 3.5 feet, but thinned laterally Branch Fault to the Devonian Lingle flushed prior to this last major epi- to the north and northeast. The mine Limestone at a depth of 3,802 feet. sode of deformation. was abandoned because of the clay The Rodger, Barger et al. No. 1Well partings, the difficulty of removing was drilled in the graben within the overlying sandstone, and the deple- Hobbs Creek Fault Zone to the Mis- For local use, local supplies of coal tion of coal. sissippian Ste. Genevieve Limestone have been mined in the Caseyville Table 4 Chemical analyses of channel sample of Tunnel Hill (?) Coal. the last operating mine in the quadrangle, extracted this coal in the Basis W1/2, SE, SE, SE, Section 29, T12S, As received Moisture and ash-free R6E. The operation was abandoned in 1974. R. B. Nance and G. J. All- Moisture gaier (unpublished ISGS field notes, Volatile matter 1975) measured a lower 0.6 foot coal Fixed carbon and an upper 1.0 foot coal which Ash contained a pyritic layer. The coals Total sulfur were separated by 0.10 foot of argil- Heating value (Btuhb) laceous coal. The coal crops out in a stream bed just south of the mine site; it is about 2 feet thick, overlies a The mine site has recently been Creek. Palynological and biostrati- rooted underclay and grades up to reclaimed. The chemical analysis in graphic analyses of the coal (Pep- black carbonaceous shale. Northeast table 4 is taken from a channel sam- pers, personal cornrnunication, 1989) of the strip mine, about 1.3 feet of ple of the coal, excluding shale part- indicate the coal approximately cor- the coal crops out in a small ravine ings. The sulfur content of this relates to the Smith coal bed in the just east of the Eddyville-Golconda sample is relatively low for coal lower Tradewater Formation of west- road (NW SE, Section 22, T12S, from the Illinois Basin, but the ash em Kentucky. The coal is discontinu- R6E). The same coal was mined content is high. ous, has a maximum thickness prior to 1934 from several pits in the The most widespread coal in the ranging from 2 to more than 3 feet, SW NW, Section 14, T12S, R6E. H. B. quadrangle is in the Tradewater For- and locally has a clay parting of 0.1 Stonehouse (unpublished ISGS field mation. It crops out intermittently to 0.3 foot. 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