GEOLOGY OF THE LICK CREEK QUADRANGLE JOHNSON, UNION, AND WILLIAMSON COUNTIES, SOUTHERN ILLINOIS

W. John Nelson and C. Pius Weibel

Department of Natural Resources ILLINOIS STATE GEOLOGICAL SURVEY GEOLOGY OF THE LICK CREEK QUADRANGLE JOHNSON, UNION, AND WILLIAMSON COUNTIE SOUTHERN ILLINOIS

W. John Nelson and C. Pius Weibel

BULLETIN 103 1996

ILLINOIS STATE GEOLOGICAL SURVEY William W. Shilts, Chief 615 East Peabody Drive Champaign, IL 61820-6964 ACKNOWLEDGMENTS Acknowledgments are due to Russel Peppers, who analyzed palynology of coals and provided biostratigraphic data. Jack Masters and Joe Devera care- fully critiqued the geological map. Heinz Damberger, as project leader of COGEOMAP, provided continuous encouragement and advice. Private land- owners in the study area are gratefully acknowledged for permitting access to outcrops on their land. In particular, we thank Sam Michaels, Herman Stokes, and Leonard Jones, who allowed us to drill stratigraphic tests on their land.

Cover Photo Graben created by landslide on north side of Grassy Creek

Printed by authority of the State of Illinois/l996/1200 printed with soybean ink on recycled paper ACKNOWLEDGMENTS ABSTRACT 1 INTRODUCTION Geography and Physiography General Geologic Setting Previous Geologic Studies Methodology STRATIGRAPHY Mississippian System Ste. Genevieve Limestone Pope Group Aux Vases Sandstone Renault Limestone Yankeetown Formation and Downeys Bluff Limestone Bethel Sandstone Ridenhower Shale Cypress Sandstone Golconda Formation Hardinsburg Formation Glen Dean Limestone Tar Springs Formation Vienna Limestone Waltersburg Formation Menard Limestone Palestine Formation Clore Formation Degonia Formation Kinkaid Limestone Mississippian-Pennsylvanian Boundary Pennsylvanian System Raccoon Creek Group Caseyville Formation Tradewater Formation Quaternary System Pre-Illinoian Loess Glasford Formation Younger Loess Alluvium, Colluvium, and Talus DEPOSITIONAL HISTORY Mississippian Femsylvanian Caseyville Formation Tradewater Formation Quaternary Deposits STRUCTURAL GEOLOGY ECONOMIC GEOLOGY Limestone Sandstone Fluorspar and Base Metals Sand and Gravel Clay and Shale Coal Petroleum GEOLOGIC HAZARDS Landslides Karst REFERENCES FIGURES Location map Geologic setting of the study area Generalized stratigraphic column of the Pope Group Graphic column of COGEOMAP borehole L-3 Graphic column of COGEOMAP borehole L-2 Measured sections of Kinkaid Lirnestone from quarries The middle part of the Cave Hill Member in a limestone quarry Laminated lime mudstone from the middle part of the Cave Hill Member Quarry wall shows upper Kinkaid and Caseyville strata Ten measured sections in the lower part of the Caseyville Forma tion Measured section in a roadcut along 1-57 illustrates the reference section of the Wayside Member Pennsylvanian nomenclature used for the Lick Creek area Two measured sections of the Caseyville Formation west of 1-57 Geophysical logs and sample graphic column of Pennsylvanian strata in Monjeb Minerals no. 1 Throgmorton borehole Measured section in a roadcut along 1-57 Tabular-planar crossbedding in the Pounds Sandstone Member Graphic column of COGEOMAP borehole G-1 Sketch of a growth fault in the basal Tradewater Formation in a roadcut along 1-57 Huge tabular-planar crossbedding in the lower Tradewater Formation in a roadcut along 1-57 Map showing distribution of the Glasford Formation, preglacial bedrock channels, and postglacial superimposed drainages Exposure of diamicton of the Glasford Formation Diamicton of the Glasford Formation shows polygonal veins interpreted as dessication cracks A tension fissure caused by a landslide on the north side of Grassy Creek A graben created by a landslide TABLE 1 Boreholes in the study area PLATE Stratigraphic column of rocks exposed at surface The Lick Creek Quadrangle comprises thicker and coarser grained east- cut new channels superimposed into parts of Johnson, Union, and William- ward, and the Caseyville thickens bedrock. Other Quaternary sediments son Counties and lies along the south- eastward from about 180 to 400 feet. in the study area are interpreted as west margin of the Illinois Basin. Subsidence evidently was more alluvium, colluvium, talus, and loess. Outcropping bedrock strata are rapid in the eastern part of the quad- Paleozoic rocks in the quadrangle of Chesterian (late Mississippian) rangle than in the western part dur- dip uniformly northeast at an aver- and Pennsylvanian age. Exposed ing Caseyville time. age of less than lo.The only tectonic Mississippian strata are about 450 The Tradewater Formation (late fault is a southwest-dipping thrust feet thick and consist of alternating Morrowan to early Desmoinesian; fault that has about 10 feet of throw. limestone, shale, and sandstone. Lower and Middle Pennsylvanian) A few normal faults having throws These rocks are assigned to the conformably overlies the Caseyville. of several feet were observed in road- Pope Group and divided into five The Tradewater consists of lithic cuts; they probably are products of formations: Menard Limestone (old- arenite interbedded with shale, silt- soft-sediment deformation. est), Palestine Formation, Clore stone, and thin coal. Maximum thick- Limestone is the only known sig- Formation, Degonia Formation, and ness of the Tradewater is about 300 nificant mineral commodity in the Kinkaid Limestone. Pope Group sedi- feet; its top is eroded. The Caseyville study area. Several quarries have ments were deposited in shallow sub- and Tradewater Formations repre- operated in the Kinkaid Limestone tidal to supratidal environments on a sent shallow marine, estuarine, and in and near the Lick Creek Quad- tectonically stable shelf. Siliciclastic deltaic sediments; they have not rangle. Coal beds are too thin and intervals reflect episodes of deltaic been differentiated in the western lenticular to be of economic interest. progradation. part of the quadrangle. Nine unsuccessful oil and gas explo- The Caseyville Formation (Mor- Quaternary deposits in the study ration holes have been drilled in the rowan; Lower Pennsylvanian) un- area include unlithified clay, silt, and quadrangle. The deepest forma tion conformably overlies the Kinkaid sand and gravel. Diarnicton of the penetrated was the Ste. Genevieve Limestone. The Caseyville is com- Glasford Formation has been map- Limestone (Valmeyeran; middle posed of thick, bluff-forming sand- ped in the northern part of the quad- Mississippian). stone that is interbedded with slope- rangle. The Glasford is interpreted Landslides are a hazard on steep forming intervals of shale, siltstone, as ice-margin and terminal moraine slopes, especially those underlain by and thin, lenticular coal. Caseyville sediment at the extreme southern the Glasford Formation. Sinkholes sandstones are quartz arenites and limit of Illinoian continental glacia- and other karst features occur in commonly contain quartz pebbles. tion. The Glasford filled preglacial some areas underlain by limestone, Individual sandstone units become valleys; streams have subsequently particularly the Kinkaid Limestone.

This report accompanies the Lick has developed in some areas that are Lick Creek and its tributary Buck Creek geologic quadrangle map underlain by thicker Mississippian Branch drain most of the southern weibel and Nelson 1993) and is one limestones. half of the quadrangle. Bradshaw of a series of Illinois State Geological The highest elevation in the quad- Creek drains the southeastern comer. Survey (ISGS) publications on the rangle is more than 860 feet above Both creeks are part of the Cache geology of southern Illinois. This mean sea level, in the S% SW SW of River watershed and are separated study was prepared under the aus- Section 18, TIIS, R2E. Upland Mis- from north-flowing drainages in the pices of the Cooperative Geologic sissippian strata generally are above quadrangle by a major east-west Mapping Program (COGEOMAP) 450 feet, and Pennsylvanian strata divide. The north-flowing streams, and jointly supported by the United generally are above 550 feet. Bottom- including Wolf Creek, Middle Wolf States Geological Survey (USGS) land elevations average about 400 Creek, Little Wolf Creek, Little and the ISGS. COGEOMAP pro- feet. The lowest elevation is less than Grassy Lake, and Devils Kitchen duced maps suitable for (1) under- 390 feet in the southeast corner of Lake, are part of the Big Muddy standing local and regional geologic the quadrangle along Lick Creek. River watershed. history, (2) exploring mineral re- Total relief is 470 feet; local relief is Climate is warm and temperate, sources, (3) assessing geologic haz- as much as 250 feet. with an average annual temperature ards, and (4) planning for land use. Geography and Physiography

The Lick Creek Quadrangle is in JACKSON southernmost Illinois between lati- tudes 37'30' and 37'37'30" N and SALINE GALLATIN WILLIAMSON longitudes 89O00' and 89O07'30" W (fig. 1). Highway access to the area is ------provided by Interstate highway K 57 (1-57) between Marion and Cairo. The Lick Creek and Goreville inter- changes are within the quadrangle. Paved and graveled county roads provide access to most of the study area, except for areas around the Crab Orchard National Wildlife Refuge, where access is by foot trails. Two unincorporated villages, Lick Creek and Wayside, are in the quad- 20 mi rangle, but the latter is a "ghost" 30 km town. Approximately three-fourths of the quadrangle is privately owned, and most of the remainder is in the Shawnee National Forest. The quadrangle is within the Shawnee Hills Section (Leighton M McClure et aL 1948) of the Interior Low ME Mermet B Bloomfield MC Mill Creek PPa teaus Province (Fenneman 1938). CB Cobden MP Mt. Pleasant The area consists of a dissected pla- CS Creal Springs P Pomona teau, whose higher ridges generally Map published D Donqola R Reevesville are composed of Pennsylvanian Map in press or ED ~ddyville RU Rudement sandstone, particularly of the Casey- in preparation EQ Equality S Shawneetown ville Formation. Streams eroding Mapping in progress GL Glendale ST Stonefort the Pennsylvanian sandstones have GV Goreville T Tamms formed narrow valleys and canyons Published before 1968 GR Gorham TH Thebes with high bluffs, whereas those Limit of Pennsylvanian System J Jonesboro W Waltersburg eroding the less resistant Mississip- LC Lick Creek WA Ware Major fault MA Makanda WL Wolf Lake pian limestones, shales, and thin - sandstones have formed broad, Figure 1 Location map shows quadrangles geologically mapped under open valleys. A karst topography COGEOMAP. L -normal fault f anticline --A- reverse fault monocline 14'mi %strike-slip fault o 10 20 30 km

Figure 2 Geologic setting of the study area shows selected structural features.

range of 100°F (3B°C), mean tempera- vegetation is least obstructive. Even gently northeast toward the center ture of 57°F (14"C), mean annual in winter, recently logged areas and of the basin. The study area is a precipitation of 46 inches, and a overgrown pastures can be nearly short distance west of the Illinois- growing season of about 190 days impassible. The only rocks that crop Kentucky Fluorspar District, a com- (Parks 1975).Most ridge slopes and out prominently are massive and plexly faulted area dominated by some ridge tops are wooded, largely well indurated sandstones. Lime- northeast-trending, high-angle nor- in oaks and hickories, along with stones weather deeply by solution mal faults. About 10 miles west of beech, Rtligtree, sugar maple, and and crop out only intermittently on the Lick Creek Quadrangle is the white ash and occasional black wal- south-facing hillsides. Shale, silt- southern terminus of the Ste. Gene- nut, butternut, Ohio buckeye, and stone, thin bedded sandstone, and vieve Fault Zone, which partially basswood (Schwegman et al. 1973). glacial sediment are generally separates the Illinois Basin from Logging is widespread, and tim- exposed only in cutbanks of large the Ozark Dome. A zone of high- bered areas are rapidly overgrown streams, deep gullies, and artificial angle normal and reverse faults, by brambles, brush, and small trees. exposures such as roadcuts. Geo- the Ste. Genevieve has undergone Bottomland forests have largely been logic contacts commonly must be at least two episodes of displace- cleared for agriculture. Many open inferred from float and topography. ment (Nelson and Lumm 1985). ridge tops are abandoned cultivated Descriptions of stratigraphic units The northern part of the Quad- fields converted to pasture. Bottom- are derived in large part from sub- rangle was glaciated during the lands generally are cultivated or con- surface data, particularly from cores Illinoian Age of the Pleistocene verted to pasture by introducing per- drilled specifically for this study. Epoch. The Lick Creek and adjacent ennial grasses, commonly Johnson Goreville Quadrangle contain evi- grass. General Geologic Setting dence of the southernmost advance Bedrock mapping in southern Illi- The Lick Creek Quadrangle is lo- of continental ice sheets in North nois is hampered by deep weathering, cated near the southern margin of America. Glacial sediments and bed- dense vegetation, and the thick blan- the Illinois Basin, east of the Ozark rock throughout the quadrangle are ket of loess. Mapping was conducted Dome, and north of the Mississippi mantled by younger Pleistocene and during the winter, when snakes, ticks, Embayment (fig. 2). Paleozoic bed- Holocene loess, alluvium, colluvium, and biting insects are inactive and rock strata in the quadrangle dip and talus. Table 1 Boreholes in the study area

Operator, farm, ISGS county no. Deepest formation penetrated or lease Location and well type and total depth (ft)

Union County Nation Oil Co. SE NW SE 4 Ste. Genevieve no. 1 Gray Sec. 2, TllS, R1E Petroleum test 1,948 Mitchell NW SW NE 5 Ste. Genevieve no. 1Fly Sec. 9, TllS, R1E Petroleum test 1,728 Skiles Oil Corp. NW NE NW 2 Ste. Genevieve no. 1Brewer Sec. 11, TllS, R1E Petroleum test 1,874 Noella Piacenti 1950' FSL, 2200' FWL, SW 20321 Clore Sec. 16, TllS, R1E Water well 520 Terry Thorn NW SE NW 20500 Pope Group Sec. 16, TIIS, R1E Water well 460 John Shewmaker NW NE SE 20501 Pope Group Sec. 17, TllS, R1E Water well 520 Soil Cons. Service NE NW SE 3 Clore no. 1Parks Sec. 20, TllS, R1E Limestone test 145 Kent Herbert NW NW SW 20502 Pope Group Sec. 21, TllS, R1E Water well 312 Monjeb Minerals NW NW SW 20474 Ste. Genevieve no. 1 Richards Sec. 21, TllS, R1E Petroleum test 1,450 Wayside Farms SW SW NE 20322 Clore Sec. 22, TllS, R1E Water well 390 John R. Beanland NE NW NE 186 Pope Group David Suits Sec. 28, TllS, R1E Water well 740 ISGS NE SW SE 20851 COGEOMAP L-3 Sec. 35, TllS, R1E Stratigraphic test Johnson County Monjeb Minerals SW NE SW 20370 Ste. Genevieve no. 1 Throgmorton Sec. 5, TllS, R2E Petroleum test 2,015 Robert Graves NW SE NW 20273 Kinkaid Sec. 30, TllS, R2E Water well 230 Adams SW NE SE 77 Golconda no. 1 Walker Sec. 31, TllS, R2E Petroleum test 926 ISGS 800' FNL, 2800' FEL 20427 Degonia COGEOMAP L-2 Sec. 31, TllS, R2E Stratigraphic test 264 Williamson County ISGS SW SW SW 23454 Tradewater COGEOMAP G-1 Sec. 28, TlOS, R2E Stratigraphic test 300 Carolyn Oil Co. m SE NW 1097 Ste. Genevieve no. 1 Throgmorton Sec. 29, TlOS, R2E Petroleum test 2,030 Cantine & Hardin SE NW SW 2013 Ste. Genevieve no. 1Jones Bros. Sec. 29, TlOS, R2E Petroleum test 1,991 Hildreth SE NE NE 2290 Ste. Genevieve no. 1Houston Sec. 29, TlOS, R2E Petroleum test 2,109 Previous Geologic Studies rangle, whose southeast quarter Methodology The earliest geological reconnais- includes the Lick Creek 7.5-minute Mapping for this study commenced sance of southern Illinois was per- Quadrangle. Geology of the area im- in the spring of 1987 and was com- formed by the first Geological Survey mediately south of the Lick Creek pleted in the spring of 1988. Outcrop of Illinois, under the direction of Quadrangle was mapped by S. Wel- data were recorded in field notes Amos Worthen. In his reports for ler and Krey (1939) at the scale of and on topographic maps. Field this survey, Engelmann (1866) de- 1:62,500. The Goreville Quadrangle notes were typed and are available scribed the areal geology of Johnson to the east (Jacobson 1991), the for examination in the library of the County and remarked on the topog- Makanda Quadrangle to the west ISGS. Subsurface data employed in raphy near Buck Branch. Worthen (Weibel and Jacobson 1993), and the this study include sample studies described the areal geology of Union Bloomfield Quadrangle to the south- and geophysical logs of oil-test County (1868) and Williamson east (Nelson 1995) have been mapped holes, drillers' logs of water wells, County (1875). These reports estab- at the scale of 1:24,000. The glacial and core descriptions from three lished the stratigraphic and struc- boundary in the Lick Creek Quad- stratigraphic tests drilled by the tural framework of the region and rangle and adjacent areas was mapped ISGS (under COGEOMAP). Logs remain useful because they describe and discussed by Willman and Frye and cores are available for exami- many outcrops. (1980). Our mapping and interpreta- nation in the Geological Records Lamar (1925) mapped and described tion of Quaternary deposits are more and Samples Library of the ISGS. the geology and mineral resources detailed and differ from those of Wells utilized in this study are listed of the Carbondale 15-minute Quad- Willman and Frye. in table 1. The Lick Creek Quadrangle is under- intervals of greenish gray calcareous shale interbedded in the Renault is lain by approximately 14,000 feet of and silty shale occur in the upper variegated red, green, and gray and Paleozoic sedimentary rocks that Ste. Genevieve. occurs in intervals that are thinner overlie Precambrian crystalline base- The deepest penetration below than 5 feet. Eight well records indi- ment rock (Buschbach and Kolata the top of the Ste. Genevieve was cate the Renault is 42 to 70 feet thick. 1991).Only the uppermost 2,600 feet 260 feet in the Monjeb Minerals no. 1 of these strata are exposed at the sur- Richards well (table 1).The company Yankeetown Formation and face or known from well penetra- sample study indicates that approxi- Downeys Bluff Limestone tions within the quadrangle. The mately the lower 35 feet of this inter- Overlying the Renault Limestone is oldest unit reached in drilling is the val was cherty, dolomitic, micritic a complex succession of interbedded Valmeyeran (Middle Mississippian) limestone, a lithology typical of the limestone, sandstone, and shale,. Ste. Genevieve Eimestone, whereas St. Louis Limestone. If this lower- equivalent to the Yankeetown Forma- the oldest outcropping unit is the most rock is St. Louis, the Ste. Gene- tion and Downeys Bluff Limestone Chesterian (Upper Mississippian) vieve is about 225 feet thick in the (fig. 3). This interval cannot be sub- Menard Limestone. The youngest Richards well. divided in the Lick Creek Quadran- bedrock in the study area belongs to gle. Thickness of the interval in the upper Morrowan through lower Pope Group eight wells ranges from 92 to 137 Desmoinesian (?) (Pennsylvanian) The Pope Group (Swam and Willman feet. Tradewater Formation. Plate 1 de- 1961) comprises alternating carbon- In general, sandstone occurs picts a stratigraphic column of ex- ate and siliciclastic formations of late near the base of the Yankeetown- posed strata in the quadrangle. Valmeyeran and Chesterian age. In Downeys Bluff interval, whereas the Lick Creek Quadrangle, the intercalated shale and limestone, Pope includes formations from the along with minor sandstone, occur MISSISSIPPIAN SYSTEM Aux Vases Sandstone at the base to in the upper part. Sandstone is light the Kinkaid Limestone at the top greenish gray to light reddish gray, See. Genevieve Limestone (fig. 3). In wells of the study area, very fine to fine grained, giauconi- Eight wells in the study area have thickness of the group ranges from tic, and calcareous. Shale is varie- reached the Ste. Genevieve Lime- 1,285 to 1,365 feet. Only the upper gated in shades of gray, green, red, stone, and one well (Monjeb Miner- part of the Menard Limestone and purple, and yellow. Much of it is als no. 1 Richards) may have com- younger formations crop out in the calcareous and contains abundant pletely penetrated the formation study area. The lower two-thirds of the marine fossils, largely bryozoans and drilled into the underlying Pope is known from well records and and echinoderm fragments. Lime- St. Louis Limestone (table 1). Geo- exposures in adjacent quadrangles. stone is commonly silty and sandy physical logs and sample studies and varies from oolitic and crinoidal from the eight wells provide data Aux Vases Sandstone Records grainstone to dolomitic lime mud- on the lithology of the Ste. Gene- of eight wells indicate the Aux Vases stone. Pink to red crinoid fragments vieve Limestone. These well re- Sandstone is 21 to 32 feet thick and and abundant chert in limestone cords show the Ste. Genevieve is composed of light greenish gray, near the tog of the interval are char- predominantly limestone, with very fine grained quartzose, glau- acteristic of the Downeys Bluff Lime- thin interbeds and lenses of shale conitic, and calcareous sandstone, stone in southern Illinois. and sandstone (fig. 3). The limestone which grades to sandy limestone. is mostly white to light brownish Fossil fragments and oolites are com- Bethel Sandstone In the kick gray, fine to coarse grained, oolitic mon, and interbeds of greenish gray Creek Quadrangle, the Bethel Sand- and skeletal packstone and grain- calcareous and silty shale also are stone is thin and lenticular and com- stone. Interbeds of darker colored, present. posed of fine to medium grained, micritic, and very fine to finely calcareous sandstone and sandy, crystalline, dolomitic and cherty Renault Limestone Much of the crinoidal limestone with interbeds limestone also are present. Much Renault Limestone is lithologically of dark gray shale. It is absent in of the limestone in the upper part similar to the Ste. Genevieve: light three out of eight wells, less than 5 of the Ste. Genevieve contains quartz colored oolitic and skeletal grain- feet thick in three wells, and 14 feet sand; intervals of sandstone as thick stone and packstone containing thick in one well. as 20 feet are present. Sandstone is quartz sand, and lesser amounts of light greenish gray, very fine to fine darker micritic to finely crystalline, Ridenhower Shale The Riden- grained, quartzose, glauconitic, and dolomitic limestone. Theupper part hower Shale is an interval of shale calcareous. Sandstone units are len- of the Renault is commonly pink or containing thin limestone interbeds ticular and cannot be correlated red, and contains reddish brown, (fig. 3) and is 34 to 83 feet thick. among neighboring wells. Thin hematitic oolites or pellets. Thin Shale is olive gray to dark gray, soft, Member

Casey- Glen vile Dean

iardins. burg

Kinkaid Haney Cave *LF! Hill

Negli Creek &..L-. - .. y

Ford Station

Clore

---I------Cora Riden- hower

Bethel Uc = a 2 K m 2 % 5 g Menard 9 3 SE

qenault

Walters. Aux burg Vases

Vienna Q) - .!? Q) > Ta r 3j g Springs 8

Figure 3 Generalized stratigraphic column of the Pope Group (Mississippian) and enclosing strata. partly silty, calcareous, and very Cypress Sandstone The Cypress 10 to 50 feet of the Cypress is com- fossiliferous; in the lower Riden- Sandstone, penetrated in eight wells, posed mostly of dark gray silty hower, it tends to be dark and is 106 to 165 feet thick. The lower shale containing carbonaceous sideritic. Ridenhower shale has two-thirds of the Cypress is almost debris and thin coal (fig. 3). lower electrical resistivity than most entirely sandstone: white to light other shales of the Pope Group. gray, fine to medium grained quartz Golconda Formation The Gol- Limestone is largely brownish gray, arenite. Some sandstone is calcare- conda Formation is a 133- to 204- argillaceous, crinoidal and oolitic ous and contains marine fossil frag- foot-thick interval of limestone and grainstone. The thickest limestone ments. Thin interbeds of olive gray shale, penetrated by nine wells. beds (up to 15 feet) are at or near the to reddish gray, calcareous shale Three members can be recognized: top of the Ridenhower. occur in some wells. The uppermost (1) the thin basal Beech Creek Lime- stone Member at the bottom, (2) the stone is 17 to 41 feet thick and litho- corner of the quadrangle. Exposures Fraileys Shale Member, and (3) the logically resembles the lower lime- consist of isolated ledges of lime- Haney Limestone Member at the top stone. It is largely coarse crinoidal stone, many of which have been dis- (fig. 3). and oolitic grainstone and packstone, placed downslope by slumping or The Beech Creek is 2 to 10 feet but wackestone and dolomitic lime soil creep. Springs and small sink- thick in eight out of nine wells and mudstone also are present. holes are common in the area of consists of dark brownish gray, fine Menard outcrops. Most information grained, argillaceous, dolomitic, cri- Tar Springs Formation The Tar on the lithology of the Menard has noidal wackestone and packstone. Springs is 70 to 99 feet thick and been taken from well records, which In the Monjeb no. 1 Richards well, composed of 80% to 100% interlami- indicate the Menard is 132 to 147 the Beech Creek is unusually thick nated shale and siltstone (fig. 3). For feet thick, and approximately the (33 feet) and consists of light brown, this reason, the name Tar Springs upper 50 to 60 feet crops out within micritic to fossiliferous limestone Formation is used instead of Tar the quadrangle. that is sandy at the base. Springs Sandstone. Shale and silt- Limestone, the dominant lithol- The Fraileys is 65 to 140 feet thick stone are medium to dark gray and ogy is medium to dark gray and shale with occasional interbeds of olive gray, fissile, and noncalcar- generally weathers to smooth, light limestone. Most of the shale is me- eous. In several wells, black carbona- gray surfaces. Most of it is fossilifer- dium. to dark gray, sideritic, calcare- ceous shale and thin coal occur near ous lime mudstone and fine to coarse ous, and fossiliferous. Near the top the top of the Tar Springs. Sand- grained skeletal wackestone that of the member is an interval of varie- stone, where present, is near the top contains abundant pelmatozoan gated greenish gray and red clay- of the formation and thinner than 20 fragments. Other fossils include stone. Limestone beds in the Fraileys feet. Like other sandstone of the bryozoans, brachiopods, and a few are mostly thinner than 5 feet and Pope Group, this is white to light pelecypods (razor clams). Bedding are argillaceous crinoidal wackestone gray, very fine to fine grained quartz at outcrops ranges from about ?hto 2 and grainstone. arenite. feet thick. Bedding surfaces are The Haney Limestone is 13 to 60 wavy or hummocky and are sepa- feet thick and varies from light Vienna Limestone The Vienna rated by argillaceous partings. The brownish gray, oolitic grainstone Limestone is 7 to 33 feet thick and is limestone contains interbeds of me- and crinoidal-bryozoan wackestone mostly medium to dark brownish dium gray or olive gray to black, and packstone to dark brownish gray, argillaceous, and silty lime slightly to highly fissile shale that is gray, argillaceous and cherty dolomi- mudstone containing scattered bio- partly calcareous and fossiliferous. tic lime mudstone. Laminae and in- clasts and much chert. Lighter colored, Shale interbeds range from a frac- terbeds of gray, calcareous, fossilif- sandy skeletal, and oolitic packstone tion of an inch to about 15 feet thick. erous shale less than 5 feet thick are and grainstone occur in the upper The uppermost part of the present. part of the Vienna in some wells. Menard is composed largely of shale with thin interbeds of limestone. In Hardinsburg Formation The Waltersburg Formation The the core from COGEOMAP borehole Hardinsburg Formation is a silici- Waltersburg Formation is 38 to 60 L-3, the uppermost 25 feet of the clastic unit 22 to 70 feet thick. Sand- feet thick and composed dominantly Menard is largely medium dark stone, siltstone, and shale occur in of medium to dark gray, olive gray, gray to black, fissile, calcareous clay varying proportions. Sandstone is and greenish gray clay shale and shale (fig. 4). The shale contains ar- white to light gray, very fine to fine silty shale. Shale contains laminae or gillaceous limestone lenses and is grained quartz arenite. Siltstone and thin interbeds of siltstone and very moderately to abundantly fossilifer- shale are medium to dark gray and fine grained, dark gray, argillaceous ous (brachiopods, bryozoans, pelma- greenish gray, laminated, and gener- sandstone. Flakes of carbonaceous tozoans). Limestone interbeds are ally noncalcareous. The Hardinsburg plant remains occur in the shale, and medium to dark gray, argillaceous, is almost entirely sandstone in the coal was reported near the top of the fossiliferous (brachiopods and pel- Adams no. 1Walker well; but in Waltersburg in one sample log. The matozoans) lime mudstone. The other wells in the quadrangle, 50% shale also contains marine fossils, thickest limestone bed in the core is to 100% of the formation is shale including echinoderm and bryozoan about 3 feet thick. and siltstone. fragments. Contact with the overlying Pales- tine Formation was mapped at the Glen Dean Limestone The Glen Menard Limestone The oldest highest exposure of limestone below Dean Limestone is an interval of bedrock unit exposed in the quad- sandstone float from the Palestine. limestone and shale 60 to 95 feet rangle is the Menard Limestone, an Well records indicate this contact is thick, as shown by the logs of nine interval of interbedded limestone sharp or rapidly gradational. The wells. A thin lower limestone, a me- and shale (fig. 3). The Menard was contact is sharp and probably dis- dial shale, and a moderately thick named by S. Weller (1913) for expo- conformable in the core from CO- upper limestone are consistently pres- sures at the quarry of the Menard GEOMAP borehole L-3. ent. The lower limestone (4 to 15 feet Correctional Center at Chester, Ran- thick) is brownish gray, dolomitic, dolph County, southwestern Illinois. Palestine Formation The silici- oolitic, and crinoidal packstone. The Swann (1963) divided the Menard in clastic unit overlying the Menard medial shale is 24 to 49 feet thick southern Illinois into three members Limestone in southern Illinois was and is olive gray, greenish gray, and (Walche, Scottsburg, and Allard), but originally named the Palestine Sand- dark gray soft, calcareous clay shale these members are not distinguish- stone for exposures in Palestine containing abundant bryozoans. able in the Lick Creek Quadrangle. Township, Randolph County, south- Red shale was reported in the sam- The Menard crops out along western Illinois (S. Weller 1913). ple log of one well. The upper lime- Bradshaw Creek at the southwest This report uses the term formation supplement observations from the Clore Formation The succession meager outcrops. of interbedded shale, limestone, and Sandstone of the Palestine is sandstone overlying the Palestine olive gray to light brown and dark Formation is called the Clore Forma- gray green and weathers light yellow- tion. The Clore was named by ish brown, to orange brown or S. Weller (1913) for exposures near brown. It is fine grained (rarely me- Clore School, Randolph CounvF dium grained) and composed of sub- southwestern Illinois. Swann (1963) rounded, well sorted quartz sand divided the Clore into three mem- with a few percent mica, feldspar, bers: (1)the lower Cora Member of and dark grains. Carbonized plant shale with thin limestone beds, (2) Ford fragments are locally abundant, rip- the Tygett Sandstone Member of Station Member ple marks are common, and bedding sandstone, siltstone, shale, and thin ranges from 0.1 to 1 foot thick. At limestone beds, and (3) the upper the top of the formation is greenish Ford Station Member of interbedded gray to brownish gray calcareous limestone and shale. All three mem- siltstone that contains abundant car- bers of the Clore are present in the Tygett bonaceous plant fragments and inter- Lick Creek Quadrangle. For this sur- Sandstone beds of fissile, gray noncalcareous vey, the Cora was mapped sepa- Member shale. rately; the Tygett and Ford Station Siever (1953) reported that quartz Members were combined as one is the dominant constituent of sand- unit because the contact between the stone from the Palestine, with sub- members was not easily mappable. ordinate clay, carbonate, and chert A limestone bed in the Tygett Mem- and traces of feldspars and heavy ber is shown on the geologic map Cora Member minerals. Such composition is typi- (Weibel and Nelson 1993). cal for sandstone of the Pope Group The Clore crops out in the south- (Potter 1963). These sandstones are eastern and south-central part of the quartz arenites and sublitharenites. quadrangle, from Bradshaw Creek Well records indicate that the Pales- eastward. The formation is 110 to tine is lithologically variable. In some 138 feet thick, as measured on the wells, the formation is entirely shale logs of six wells. and siltstone; but in others a sand- Palestine stone up to 20 feet thick occurs near Cora Member Swann (1963) pro- Sandstone the base. posed the name "Cora Limestone In the core from COGEOMAP Member" for the lowest part of the borehole L-3 (fig. 4), the Palestine is Clore Formation, as exposed near 60.8 feet thick and consists of inter- Cora, Jackson County southwestern bedded and interlaminated sand- Illinois. The member is largely lime- stone and shale. Sandstone in the stone in its type area; but in the Lick core is light gray very fine grained, Creek Quadrangle, the Cora consists !- - -L 1.- 1 Limestone partly calcareous quartz arenite; of approximately two-thirds shale shale is dark gray, well indurated, and one-third limestone. Thus, we silty, and noncalcareous. Ripple lami- refer to the unit as the Cora Member. Figure 4 Graphic column of COGEO- nations, horizontal shale lamina- Shale of the Cora is medium olive MAP borehole L-3. This core contains tions, small load casts, and slump to greenish gray to dark gray calcare- the reference section of the Tygett structures are common throughout ous to noncalcareous, and generally Sandstone Member of the Clore For- the core, and several burrowed inter- fissile. It is mostly clay shale, but mation. vals are present. Near the middle of some silty shale and a little siltstone the formation is a thin, dull, argil- are present. Siltstone is greenish rather than sandstone because shale laceous coal, which overlies a silt- gray to medium gray, laminated to and siltstone are major constituents stone containing plant fossils and thinly bedded, and partly calcare- in the Lick Creek Quadrangle. plant rootlets. Overlying the coal is ous. Silty beds occur mostly in the In the quadrangle, the Palestine is mudstone that contains limestone lower part of the member. 40 to 67 feet thick and crops out in a nodules and plant fossils. A layer of Limestones of the Cora are argil- narrow belt northeast of Bradshaw fragmented pelecypods occurs laceous and medium gray to dark Creek near the southwest corner of about 20 feet below the top of the gray, weather light olive gray to the quadrangle, and also along a Palestine. light brown, and tend to spa11 into south-flowing tributary of Bradshaw Contact between the Palestine thin, irregular layers as they weather Creek in the SE, Section 3, T12S, and the overlying Clore Formation and to break into small, flat chips R1E. Most Palestine outcrops consist is not exposed in the quadrangle. when hammered. Limestones con- of sandstone that forms small, dis- Contact was mapped in the field at sist of fossiliferous lime mudstone continuous ledges. Shale and silt- the lowest exposure of limestone or and fine to medium grained skeletal stone of the Palestine are exposed calcareous shale typical of the Clore. wackestone, containing numerous only locally in the banks of streams. Well records, including the core from whole fossils. Fossils of the Cora Well records, particularly the core COGEOMAP borehole L-3, indicate include brachiopods (compositids, from COGEOMAP borehole L-3, a sharp but conformable contact. spiriferids, derbyids, and produc- tids), bryozoans, gastropods, pelma- The type section is near Tygett Tygett are very fine to fine grained, tozoans, and rare orthoconic cepha- School on the south side of Brad- argillaceous quartz arenites; gener- lopods. Fossils from the Clore listed shaw Creek in the Makanda Quad- ally they are light gray to light by Lamar (1925) are mostly, if not rangle, about 2 miles west of the brownish gray and weather yel- entirely, from the Cora Member. Lick Creek Quadrangle (near center, lowish brown. Quartz grains are The larger proportion of shale, NE NW, Sec. 24, TllS, RlW, Union well sorted and subrounded, and more argillaceous limestones, and County). Previous geologists dark mineral grains are present. greater abundance of whole fossils mapped the Tygett in formations Tygett sandstones are largely thinly distinguish the Cora from the other than the Clore. Lamar (1925) bedded, but thick bedded sand- Menard Limestone. Limestone beds mapped the Tygett as part of the De- stones occur locally in the upper in the Cora rarely exceed 3 feet, gonia Formation in most of the Lick parts of both sandstones. Current whereas those of the Menard com- Creek Quadrangle, but southeast of and interference ripple marks, along monly are 10 feet or more thick. Lick Creek village he mapped some with vertical and horizontal bur- Limestone beds of the Cora crop out Tygett as part of the Palestine. South rows and trails, are common in the only in deep ravines and stream of the Lick Creek Quadrangle, thin bedded sandstone. The trace banks, and limestone blocks on hill- S. Weller and Krey (1939) mapped fossil Rhizocorallium occurs near the sides generally have been displaced the Tygett in the Degonia Formation. top of the lower Tygett sandstone. by slumping and soil creep. The Tygett Member logically Stigmarian root casts are present at In the core from COGEOMAP should include all sandstone in the the tops of both sandstones. borehole L-3, the Cora is dominated middle part of the Clore Formation. A middle limestone in the Tygett by ?4- to 7-foot-thick intervals of Swann (1963), however, designated was previously recognized south- shale that contain interbedded lime- only the lower of the two sandstones east of the Lick Creek Quadrangle, stone (fig. 4). The shale is mostly as the Tygett at the type section, and in the Waltersburg Quadrangle greenish gray to medium dark and placed the upper sandstone, about (Weibel et al. 1991), the Glendale dark gray, laminated, calcareous, 5 feet thick, in the Ford Station Mem- Quadrangle (Devera 1991), and the and fossiliferous.Some shale is ber. As the upper sandstone is traced Bloomfield Quadrangle (Nelson black and noncalcareous and con- eastward, it becomes thicker in places 1993). In the Lick Creek Quadrangle, tains laminae of micaceous siltstone, than the lower sandstone. In the the middle limestone interval of the horizontal burrows, and siderite lay- Lick Creek Quadrangle, the upper Tygett is 2 to 10 feet thick and con- ers. Brachiopods, bryozoans, and and lower sandstones both are 20 to sists of a single limestone bed or two echinoderm fragments are common. 40 feet thick, separated by 10 feet or or three limestone beds separated by The numerous thin interbeds of lime- less of shale and limestone. layers of medium to dark brownish stone that range from several inches The Tygett Sandstone Member is gray, fissile clay shale. Tygett lime- to more than 4 feet thick are medium therefore revised to include both up- stone resembles limestone of the gray to dark gray, argillaceous lime per and lower sandstones, along Cora Member: argillaceous lime mudstone with fossil fragments and with the thin intervening shale and mudstone and skeletal wackestone shale laminae. Whole and fragmen- limestone. The Ford Station Member with abundant pelmatozoan and tary brachiopods, fenestrate and is restricted to limestone and shale brachiopod fragments. Coal frag- ramose bryozoans, gastropods, and overlying sandstone of the Tygett. ments less than 0.5 inch in diameter pelmatozoans are common; several Sandstone does not occur in the Ford occur in the limestone. Good expo- coquina beds are present. Station at its type section (Swann sures of the medial Tygett lime- In the Lick Creek Quadrangle, the 1963, p. 42). stones occur in ravines in the NE, Cora is 55 to 75 feet thick in outcrops A subsurface reference section for Section 32, and the NW, Section 33, and 38 to 60 feet thick in wells. the Tygett is hereby designated in TllS, RlE, and in Sections 1,2, and Thickness was measured from the the interval from 88.3 to 141.5 feet in 3 of T12S, R1E. highest occurrence of limestone or the core from COGEOMAP borehole In the Lick Creek Quadrangle, calcareous shale to the lowest. Vari- L-3 (fig. 4). The core is stored in the the Tygett is 28 to 80 feet thick. Well ance between surface and subsur- samples library of the ISGS under records indicate that the Tygett thins face data may reflect imprecise sample number C-13460. to the north and that the middle placement of member contacts be- In outcrops in the Lick Creek limestone unit is absent in the north- cause of poor exposures. Some shale Quadrangle, the Tygett is about 70 ern part of the quadrangle. Contact of the uppermost Palestine Forma- to 80 feet thick and consists of two with the overlying Ford Station tion or lowermost Tygett Sandstone relatively thick, upward-coarsening Member is sharp and possibly dis- Member may have been included siliciclastic units separated by a thin conformable. Fossil root casts at the with the Cora on the geologic map interval of intercalated limestone top of the Tygett are evidence for (Weibel and Nelson 1993). and shale. The siliciclastic intervals subaerial exposure. Contact of the Cora with the over- both grade upward from clay shale lying Tygett is conformable and or silty shale at the base to sand- Ford Station Member The name either sharp or gradational through stone at the top. Basal shales are "Ford Station Limestone Member" a few inches, from limestone of the medium gray, olive gray, brownish was proposed by Swann (1963) for the uppermost Cora Po clay shale and gray, fissile, and noncalcareous. upper part of the Clore exposed near silty shale of the Tygett. Laminae and thin interbeds of light Ford Station in Randolph County, gray siltstone to very fine sandstone southwestern Illinois. Because the Tygett Sandstone Member The become thicker and more numerous unit contains roughly equal propor- Tygett Sandstone Member, as named upward. Fine grained siliciclastic tions of shale and limestone, the by Swann (1963), is the middle clas- rocks are planar laminated and rip- name is shortened to "Ford Station tic portion of the Clore Formation. ple laminated. Sandstones in the Member" in this report. 0 ft stones to wackestones that contain near the bottom and top, with finer , ,s., .(7 -$. 5.- . . . 1 . loess, residuum fine to coarse grained pelmatozoan grained strata between. , . :.'I. . -. and brachiopod fragments. Some of The lower 41.5 feet of the Dego- the limestone beds are dolomitic and nia was cored in COGEOMAP bore- argillaceous, containing interbeds hole L-3 (fig. 4). The basal 20 feet and inclusions of shale. Shale is of consists of dark gray noncalcareous Wayside Member two types: a partly calcareous and shale with fine grained sandstone fossiliferous, poorly indurated, dark laminae and burrow fillings. The greenish gray to dark olive gray to overlying 4.5 feet of strata are gray black, poorly to moderately fissile to brown, carbonaceous claystone. clay shale; and a partly noncalcare- The upper 17 feet of the Degonia 3rove Church Shale Member ous, micaceous, moderately indu- in the core consists of very fine 22.5 ft rated, dark gray and fissile clay shale grained, yellow brown, quartzose to finely silty shale. sandstone. The Ford Station is 32 feet thick Variegated mudstone 10 to 15 feet Goreville in COGEOMAP borehole L-3 and 20 thick occurs at the top of the Dego- Limestone to 45 feet in other boreholes in the nia in the study area and elsewhere. Member quadrangle. Contact with the overly- Typically, medium to dark gray 42.4 ft ing Degonia Formation is sharp (as poorly laminated, silty shale at the shown in a core from COGEOMAP base grades upward to multi-hued borehole L-3) and apparently discon- (yellow, gray, and maroon) noncal- formable in the few places where it careous, blocky claystone. This mud- is visible. A good exposure occurs stone was cored in COGEOMAP along a small ravine between borehole L-2 (fig. 5). Variegated Drapers Bluff and Lick Creek (SW claystone of the upper Degonia is SE SE, Sec. 36, TllS, RlE). persistent throughout southern Illi- Cave Hill nois (Swann 1963). Member Degonia Formation This silici- 92.4 ft The Degonia Formation abruptly clastic unit overlying the Clore For- thickens westward and changes fa- mation was originally named the cie~near the west edge of the Lick "Degonia Sandstone" by S. Weller Creek Quadrangle. Here, along Brad- (1920) for outcrops in Degonia Town- shaw Creek, in the SE, Section 29, ship, Jackson County, southwestern TllS, RlE, is the easternmost occur- Illinois. Swann (1963) called the unit rence of thick bluff-forming sand- the Degonia "Sandstone" or "Shale." stone in the Degonia outcrop belt in In the Lick Creek Quadrangle, it Illinois. To the west, similar thick Negli Creek consists of various lithologies and sandstones are common in the Dego- Limestone therefore is named the Degonia For- nia. In the quadrangle, the sand- Member mation. stone is white to light gray and 30.2 ft The Degonia consists of interbed- brown, very fine to fine grained, ded shale, siltstone, and sandstone. well sorted quartz arenite. Bedding YV Degonia Formation Shale is mostly gray to brownish is mostly 0.2 to 0.5 foot thick, but - ..... , ..-. . . .. - . .- . . .-.. . . gray, weathers brown, and is fissile, several beds are 2 feet thick. Low- noncalcareous, and poorly indu- angle crosslamination is common, Figure 5 Graphic column of COGEO- rated. Siltstone is medium gray to and foreset laminae dip south-south- MAP borehole L-2. greenish gray noncalcareous, and east to southwest. The sandstone moderately indurated. Sandstone thickens from less than 10 feet to A massive 5-to-16-foot-thick lime- is argillaceous, very fine to fine more than 40 feet within a lateral stone bed occurs at or near the base grained, and light gray light brown, distance of about % mile. of the Ford Station Member in this or greenish gray weathering orange The Degonia thickens westward quadrangle and appears to be con- brown to gray brown. The sand is on the outcrop from about 40 feet to tinuous across several adjacent quad- mostly subrounded, well sorted 80 feet. Data from six wells indicate rangles. The limestone is light to quartz grains, with a few percent of the Degonia is 48 feet to 78 feet in dark gray, slightly dolomitic lime dark minerals. Locally the sandstone the northwest quarter of the quad- mudstone to skeletal wackestone, contains scattered shale clasts. Beds rangle. containing fine to coarse echinoderm are irregular and 0.1 to 1foot thick. The contact with the overlying and brachiopod shell fragments. Ripple marks and horizontal lamina- Kinkaid Limestone is sharp and un- Good exposures of this limestone tions are present; burrows are common. dulatory and may be disconform- occur along Bradshaw Creek at the Plant fossils and a thin carbonaceous able. In most places, the limestone west edge of the quadrangle (SW SE, shale (almost a coal) occur in a gully overlies variegated claystone, but Sec. 29, and MW NE, Sec. 32, TIIS, in the NE SE, Section 35, TllS, RlE. locally the claystone is absent NE). Probable root impressions occur in (eroded ?), and the Negli Creek The upper part of the Ford Sta- the claystone below this shale. In Limestone Member directly overlies tion consists of alternating beds outcrops in the SE, Section 36, TllS, sandstone or siltstone of the Degonia. from limestone and shale, as in the RlE, shale coarsens upward to silt- core from COGEOMAP borehole L-3 stone. Along the drainage that trends Kinkaid Limestone The upper- (fig. 4). Limestones are light gray to east from the center of Section 35, most Mississippian formation in dark gray to brownish gray mud- the Degonia consists of sandstone southern Illinois is the Kinkaid Limestone, named by S. Weller Lick Creek in the NW, Section 36, rangle is in a quarry in the NE, Sec- (1920) for exposures along Kinkaid T11S. RlE, and in an abandoned tion 29, TllS, R1E. Good exposures Creek in Jackson County, southwest- quarry in the SE, Section 20, TllS, occur along the large ravine in the ern Illinois. As originally defined, RlE. NW, Section 31, TllS, R2E. Com- the Kinkaid included all strata from The Negli Creek is a limestone plete or nearly complete exposures the top of the Degonia Formation to unit containing a few partings and are present in quarries just southeast the base of the Pennsylvanian Sys- thin interbeds of shale. The lime- of the study area in the Goreville tem. Swam (1963) redefined the stone is medium to dark gray and and Vienna Quadrangles (fig. 6). Kinkaid as containing three mem- mostly weathers gray to brownish These exposures and data from bers: (1)the Negli Creek Limestone gray Locally, dolomitic layers seven wells indicate that the Cave Member at the base, (2) the Cave weather yellowish orange. Textur- Hill is 83 to 92 feet thick in the re- Hill Shale Member, and (3) the Gore- ally the limestone ranges from fos- port area. ville Limestone Member at the top. siliferous lime mudstone to coarse At the base of the Cave Hill is an Shale overlying the Goreville was as- grained skeletal packstone and interval of 12 to 16 feet of greenish signed by Swam to a new formation, grainstone, but it is mostly lime gray to bluish gray and dark gray the Grove Church Shale. However, mudstone and wackestone. Beds clay shale to silty shale. The calcare- Nelson et al. (1991) revised the range from 0.2 to 3 feet thick and are ous, soft, and fissile shale contains Grove Church back to a member of hummocky. Wavy shale partings numerous fenestrate bryozoans, the Kinkaid Formation because the and interbeds occur throughout the brachiopods, pelecypods, pelmato- Grove Church is too thin and discon- member but are most common near zoans, gastropods, and pelmatozoan tinuous to be mapped as a separate the base. The thickest shale interval fragments. In the core from COGEO- formation at scales of 1:24,000 or observed was about 2 feet thick; MAP borehole L-2 (fig. 5), the upper smaller. Since the Grove Church is most are much thinner. Shale is non- part of this shale is silty and con- present but unmappable in the Lick calcareous, dark gray, and blocky tains both plant fossils and marine Creek Quadrangle, this report also to fissile. Irregularly shaped, gray to invertebrates. groups it in the Kinkaid. black chert layers and nodules are The middle part of the Cave Hill In southern Illinois, the upper common in the limestone beds. is largely limestone with a few shale part of the Kinkaid was eroded ex- Fossils are found throughout the interbeds and is 55 to 60 feet thick tensively prior to deposition of Pem- Negli Creek and include brachio- (figs. 3,5, 6, and 7). The core from sylvanian sediments. Consequently, pods, bryozoans, solitary rugose COGEOMAP borehole L-2 (fig. 5) the Grove Church Member is absent corals, ostracodes, endothyrid fora- and sections measured in quarries in much of the Lick Creek Quadran- minifera, and pelmatozoan frag- indicate that the detailed strati- gle, and locally the Goreville Mem- ments. Large bellerophontid gastro- graphic succession in the middle ber is also missing. The Kinkaid pods and Girvanella oncoids, when Cave Hill is consistent throughout ranges in thickness from about 110 found together, are diagnostic for the quadrangle. At the bottom is me- feet near the center of Section 25, the lower part of the Negli Creek. dium to dark gray lime mudstone to TllS, RlE, to 187.5 feet in COGEO- Light colored, fine to coarse grained fine grained skeletal wackestone MAP borehole L-2 (fig. 5). crinoidal or skeletal packstone and and packstone in beds 0.2 to 3 feet The Kinkaid underlies steep grainstone occur in places at the top thick. Thin interbeds of dark gray, slopes below the Pennsylvanian of the member. Glauconite grains, calcareous shale are numerous. This escarpment from the southeast cor- small dolomite rhombs, and oolitic limestone intertongues with the ner to the central west edge of the limestone occur in the core from underlying shale at the Southern quadrangle. West and northwest of COGEOMAP borehole L-2 (fig. 5). Illinois Stone Company's quarry in Lick Creek village, the Kinkaid sur- Pelmatozoan fragments, brachio- the Vienna Quadrangle (fig. 6, col- rounds several outliers of Pennsylva- pods, bryozoans (fenestrate, ramose, umn C). Above the base, the middle nian strata but is commonly covered and fistuliporid), foraminifera, and Cave Hill is mostly dense lime mud- by talus from overlying sandstones. trilobites occur in the upper Negli stone that breaks with conchoidal The extensive talus prevents accu- Creek. fractures and contains numerous lay- rate placement on the geologic map Data from seven boreholes indi- ers and lenses of dark gray to black of contacts between members of the cate that the Negli Creek is 30 to 32 chert. At the Southern Illinois Stone Kinkaid. feet thick. Complete outcrop expo- Company's quarry, some of this lime- sures of the member were not found stone contains fine horizontal to NegBi Creek Limestone Member in the study area. Contact with the slightly undulating laminations Malott (1925) proposed the name overlying Cave Hill Member is (fig. 8). Petrographic study indicates "Negli Creek Limestone" as a forma- sharp but probably conformable. that the laminations are graded and tion for limestone exposed along the micrite is partially dolomitized. Negli Creek, Perry County, southern Cave Hill Member Swann (1963) The middle Cave Hill also contains Indiana. Swann (1963) revised the defined the Cave Hill Shale Member dysmicrite-a lime mudstone con- Negli Creek to a member. The Negli based on exposures in a quarry on taining spar-filled veins and cavities Creek is one of the most reliable Cave Hill in Saline County southern that probably reflect shrinkage of marker units in the Pope Group be- Illinois, where the unit is largely the sediment. The upper part of the cause it is highly consistent in thick- shale. In the Lick Creek Quadrangle, middle Cave Hill consists of lime- ness and lithology throughout south- the Cave Hill consists largely of lime- stone that varies from lime mud- ern Illinois (except where eroded be- stone, with shale/claystone intervals stone to medium grained skeletal neath Pennsylvanian rocks). In the at the base and the top. Thus "shale" grainstone. Crossbedded grainstone Lick Creek Quadrangle, the Negli is dropped from the name of the occurs in the quarry in Section 29, Creek is readily recognized. Good member in this report. The best ex- TIIS, R1E (fig. 6, column A). At the exposures occur on the east side of posure of the Cave Hill in the quad- top of the middle Cave Hill is 5 to 10 C Southern Illinois Stone Co. NW1/4 Sec. 11, T12S, R2E A SE SW Vienna Quadrangle NE SE NE Sec. 4. TI 2s. R2E Goreville Limestone Sec. 29, TI 1 S, R1 E Member type section Lick Creek Quadrangle

-. :. :. -'. .. . .- -..- I .. :,...... - .I - .._ .* ------CASEWILLE .- .._. - - . . - , . - . . FORMATION ._. . _.

---- concealed concealed I I------I- Figure 6 Measured sections of Kinkaid Limestone from quarries. feet of light gray, nodular-bedded has several thin interbeds of shale; it of Auchinzedes), and rugose corals. lime mudstone containing numer- is as thick as 50 feet in the study area Limestone beds 0.5 to 3 feet thick are ous streaks and inclusions of green but is absent locally because of pre- separated by shale partings, which clay. Pennsylvanian erosion (for example, commonly are stylolitic. The upper part of the Cave Hill near the center of Sec. 25, TIIS, RlE). The Goreville crops out in ledges Member consists of a 13- to 18-foot- The limestone is light to medium 10 to 20 feet high, and karst topog- thick interval of claystone, shale, gray and brownish gray, locally dark raphy is common in areas underlain and thin limestone beds (figs. 3,5, gray, and generally weathers light by this unit. Contact with the over- 6, and 9). The mottled and varie- gray. It is dominantly a medium to lying Grove Church Member is dis- gated claystone is greenish gray, coarse grained crinoidal packstone conformable (Weibel and Norby 1992). brick red, and ochre. Irregular and grainstone but ranges from very masses of yellowish gray limestone fine to very coarse grained. The Grove Church Shale Member or dolomite are common in the lower Goreville is skeletal packstone This uppermost Mississippian unit claystone. The claystone is overlain to wackestone that contains pellets was named by Swann (1963) for by dark gray, calcareous, well lami- and, locally, irregularly shaped tri- Cedar Grove Church in the Lick nated shale that is interbedded with politic chert nodules, while the upper Creek Quadrangle. The type section dark gray, argillaceous lime m~~d- Goreville includes oolitic crinoidal is in a ravine just west of an unpaved stone, in which myalinid gelecypods packstone and grainstone. Fora- road and in the ditch east of the and plant fragments are abundant. minifera, brachiopods, bryozoans, road north of Cedar Grove Church molluscs, ostracods, and trilobites in the NE NW, Section 31, TIIS, R2E. Goreville Limestone Member are common bioclasts, and oncoids Nelson et al. (1991) reduced the The Goreville Limestone Member are present. The lower part of the Grove Church to a member of the was named by Swann (1963) for ex- member is generally darker, finer Kinkaid Limestone. The member is posures in the Southern Illinois grained, and more argillaceous than thin, exposed in only several places Stone Company quarry south of the upper part. The lower Goreville in the quadrangle, and crops out at Goreville, just southeast of the Lick is abundantly fossiliferous, contain- three places in Section 31, TIIS, R2E, Creek Quadrangle (fig. 6, column C; ing pelmatozoans, bryozoans (in- Johnson County: (1)the type sec- and fig. 9). The limestone member cluding unusually large specimens tion, (2) just north of the road east of ST. covered 1 -- poorly

exposed

------covered covered I

Gorevi, Limestc Membr

-1 -1 Cave Hill Member

Figure 10 Ten measured sections in the southeastern part of study area illustrate the Mississippian-Pennsylvanian un- conformity and lithologic variation in the lower part of the Caseyville Formation. Datum is the base of the Goreville Lime- stone Member. Base map (inset) shows locations: (A) roadcut on 1-57, (B) ravine west of Chimney Rock, (C) southwest face of Drapers Bluff, (D) Grove Church type locality in ravine and roadside, (E) ravine on the south side of Cedar Bluff, (F) ravine and hillside near Gurley Cemetery (G) ravine and pond spillway near Ferne Clyffe State Park, (H) east fork of Buck Branch, (I) north-trending ravine and hillside, and (J) north-trending ravine in SW NE, Section 4, T12S, R2E, Goreville Quadrangle.

Cedar Grove Church, and (3) the GEOMAP borehole L-2 (fig. 5). The careous shale and limestone. Lime- ravine trending east-northeast just basal 6 feet of the member consists stone occurs as nodules and poorly south of Cedar Bluff. The member of greenish gray weakly calcareous defined beds. Petrographically, the also crops out in a southwest-trend- mudstone that contains siderite nod- limestone ranges from skeletal ing ravine near the center of the SW ules, common but poorly preserved wackestone to grainstone. Bioclasts NE NE, Section 27, TIE, RllS, Union casts of brachiopods and fenestrate are largely pelmatozoan fragments, County At these exposures, the bryozoans, and rare, flattened pro- but brachiopods, bryozoans, fora- Grove Church consists of gray to ductid brachiopods. This shale minifera, fish debris, ostracodes, ru- olive gray and light brown, soft, non- grades upward to gray, noncalcar- gose corals, and trilobites are present. calcareous to calcareous shale or eous mudstone about 11 feet thick, Flora and fauna from the type local- claystone that contains limestone which in turn is overlain by 0.85 foot ity were listed by Jennings and beds 0.3 to 1foot thick. The limestone of dark gray weakly calcareous silty Fraunfelter (1986). Conodonts from is gray, fine grained, argillaceous shale that contains coal laminae and the member have been documented and fossiliferous skeletal packstone carbonaceous plant impressions. by Rexroad and Merrill(1985), Man- and wackestone. The uppermost unit of the Grove ger and Sutherland (1987), and The best record of the Grove Church in the core is 4-foot-thick, Weibel and Norby (1992). Church is from the core from CO- interbedded, highly fossiliferous cal- ...... :...... : .....o'...: ...... 0 ."' ..o:...... , ...... '..O'...... ' , . . :. 0 ...... :..... Battery Rock . . : ...... -: :.. : . Sandstone .. O'.. .' ...a : :. : Member ..'...... :. ... 0.;...... '. .O'. ' *.',O,'..'. " ...... Ca-, .....:.. .:. .:. . .',O . . ' . ". .;.; .' ;...... '. : 1 float ... 0...... : .o" . . O.'O.' .. O.'O.. 0 . 0' 0.'0.'0 / covered (

L ~~~~.AP-+Limestone Goreville Limestone Member Member

-ave Hill Member

The Grove Church is 22.2 feet a system of paleovalleys that are as Formation. Everywhere it has been thick in COGEOMAP borehole L-2 deep as 400 feet and trend south- observed, the actual contact is sharp (fig. 5). Swann (1963) measured 16 west across the sub-Pe~sy]lvanian and marked by an abrupt change in feet at the type section. Less than 10 surface. The Mississippian-Pennsy1- lithology. feet of strata is exposed at other out- vanian boundary is the Kaskaskia- A series of measured sections in crops in the study area. Absaroka sequence boundary of the southeast quarter of the Lick Sloss (1963) and is attributed to a Creek Quadrangle illustrates the un- Mississippian- global eustatic event by Ross and conformity (fig. 10). Near 1-57 the Pennsylvanian Boundary Ross (1985) and Saunders and Caseyville Formation overlies the Most geologists consider the Missis- Ramsbottom (1986). Goreville Member of the Kinkaid sippian-Pennsylvanian boundary in In the Lick Creek Quadrangle, (fig. 10, collurnn A). Only 0.5 ride east the Illinois Basin to be a regional un- the Mississippian-Pennsylvanian of the highway, the Goreville is en- conformity. Siever (1951), Wanless boundary is notably disconformable. tirely missing, and basal Caseyville (1955), and Bristol and Howard Basal Pennsylvanian strata (Casey- strata rest on the Cave Hill (fig. 10, (1971,1974) described the boundary ville Formation) variably overlie column B). The basal bed of the in southern Illinois, mapped the sub- the Grove Church, Goreville, or Caseyville at this site is a conglomer- Pennsylvanian surface, and mapped Cave Hill Members of the Kinkaid ate composed of limestone and chert clasts as large as 0.2 foot, along with low the Carbondale Formation in stone. West of 1-57, the Caseyville quartz granules and crinoid colum- west-central Indiana. In southern Illi- thins to 180 feet in outcrops in the nals in a matrix of calcareous sand- nois, the Raccoon Creek Group com- NW, Section 22, TIIS, R2E, and to stone. Farther southeast, the contact prises two formations: the Caseyville 220 feet in the Mitchell no. 1 Fly well rises stratigraphically so that the (older) and the Tradewater. The Rac- in Section 9, TIIS, R1E. West of 1-57, Goreville and Grove Church Mem- coon Creek is composed almost sandstones in the Caseyville are less bers of the Kinkaid are preserved entirely of siliciclastic rocks, in con- than 50 feet thick and lack quartz (fig. 10, columns D and E). Still far- trast to the underlying Pope Group, pebbles. These sandstones are dis- ther east, the Caseyville again cuts where limestone and siliciclastic continuously exposed near the west down into the Goreville, as shown in intervals alternate. edge of the quadrangle, so that the sections from the ravine near Gurley The Caseyville and Tradewater Caseyville-Tradewater contact can- Cemetery (fig. 10, column F) and the Formations were differentiated in not be accurately located. spillway of a farm pond near Ferne most of the Lick Creek Quadrangle. Clyffe State Park (fig. 10, column G). Near the west edge of the study Wayside Member The Wayside Logs of wells east of the study area, however, these formations Member was named by Lamar area indicate that the Grove Church were not differentiated, and the Rac- (1925) for the settlement of Wayside reaches a maximum thickness of coon Creek Group is shown as a sin- in the center of the Lick Creek Quad- about 70 feet. Where the Grove gle unit on the geologic map. rangle. Lamar defined the Wayside Church is thickest, the lower 40 to 50 as the interval of intercalated sand- feet is largely shale, and the upper Caseyville Formation The name stone and shale underlying the Lick part is largely limestone. Before ero- "Caseyville" was first used by Owen Creek (now Battery Rock) Sandstone sion, the upper Grove Church lime- (1856),but Lee (1916) was the first to at the base of the Pottsville (now stone probably was a widespread, describe the Formation in detail. The Caseyville) Formation. Lamar did fairly uniform unit, like other lime- type section is on the west bluff of not designate a type section for the stone units within the Kinkaid. This the Ohio River in eastern Hardin Wayside. Wanless (1956) stated that upper Grove Church limestone rep- County, Illinois, opposite the village the Wayside type section occurs in resents erosional remnants of the of Caseyville, Kentucky (Lee 1916). ravines in the N% of Section 30 and youngest preserved Mississippian Approximately 500 feet of interbed- the NE NW, Section 31, TIIS, R2E; unit in the Illinois Basin. ded conglomeratic sandstone, shale, but he did not publish a description Rexroad and Merrill(1985) chal- and thin coal and limestone layers of the section. The exposures cited lenged the hypothesis of a wide- constitute the type section. by Wanless are poorly suited as a spread sub-Pennsylvanian discon- Geologists differ about defining type or reference section because formity in the Illinois Basin. Report- the Caseyville, but we distinguish they contain numerous gaps and do ing similar conodont faunas in the the Caseyville from the overlying not show contacts with adjacent type Grove Church and in the over- Tradewater Formation in southern units. A far superior exposure of the lying Wayside Member of the Illinois by the character of the sand- Wayside is the large roadcut along Caseyville Formation, these authors stones. Caseyville sandstones are 1-57 about 1.5 miles northeast of the concluded that no significant hia- quartz arenites that commonly con- Lick Creek interchange (NW NW! tus exists between the two units. tain quartz granules and small peb- Sec. 25 and S?h SW, Sec. 24, TIIS, Rexroad and Merrill further argued bles. In contrast, Tradewater sand- RlE). We hereby designate this road- that sedimentation may have been stones are lithic arenites that rarely cut as the principal reference section continuous across the Mississippian- contain quartz granules but contain of the Wayside Member (fig. 11; fig. 10, Pennsylvanian boundary in the substantial amounts of feldspar, column A ). The member is approxi- Grove Church type area. However, lithic fragments, mica, and clay ma- mately 140 feet in this section, and Jennings and Fraunfelter (1986) ex- trix. Also, Caseyville sandstones are all but the basal 15 feet is continu- amined macrofossils from the Grove generally thicker, more massive, and ously exposed. The roadcut displays Church and Wayside type areas, better indurated than Tradewater diverse sedimentary features of the found evidence for a "major hiatus" sandstones (Nelson 1989).Shales, Wayside and has been featured in between the Grove Church and the siltstones, and minor rock types of published field guides (Ethridge et ai. Wayside, and further suggested that the Caseyville generally are not dis- 1973, Palmer and Dutcher 1979). Wayside conodonts examined by tinguishable from their counterparts The Wayside is composed largely Rexroad and Merrill(1985) were re- in the Tradewater. The top of the of slope-forming, interbedded, and worked from older strata. Weibel Caseyville in the Lick Creek Quad- interlaminated (heterolithic) shale, and Norby (1992) re-studied cono- rangle was mapped at the highest siltstone, and fine grained, thinly donts and lithostratigraphy of the occurrence of quartz arenite that con- bedded sandstone. Lenticular bodies Mississippian-Pennsylvanian tains granules and pebbles. The of bluff-forming, crossbedded, and boundary interval and concluded Caseyville-Tradewater contact is massive sandstone also occur in the that a relatively short hiatus is pres- mappable on the outcrops and in member. In addition to the Buck ent between the type Grove Church subsurface cores and well cuttings. Branch and Keller sandstone lentils and Wayside Members. The Caseyville thins and becomes (fig. lo), other, smaller sandstone finer grained westward. East of 1-57, lenses near the base of the Wayside outcropping Caseyville is 300 to 350 have been mapped but not named. PENNSYLVANIAN SYSTEM feet thick and contains bluff-forming, The Wayside is readily mappable conglomeratic sandstones more than in the eastern two-thirds of the Lick Raccoon Creek Group 100 feet thick. Wells in the,northeast Creek Quadrangle, where the over- The name "Raccoon Creek Group" corner of the quadrangle indicate lying Battery Rock Sandstone -Mem- was first used by Wier and Gray the Caseyville is 350 to 400 feet thick ber is present. In the western third (1961) for Pennsylvanian strata be- and contains as much as 90% sand- of the quadrangle, the Battery Rock occurs as lenses less than 3 feet thick within heterolithic strata. Clasts of shale, siltstone, ironstone, and small Battery Rock quartz pebbles float in a matrix of Sandstone Member sandstone that is cemented by cal- cite or iron oxide. Fragments of lime- stone, chert, and silicified fossils reworked from the Kinkaid Lime- stone were also observed in several places at the base of the Wayside. Common sedimentary structures 0 / of thin bedded strata in the Wayside / / include interference ripples, current / Keller ripples, small load casts, tool marks, sandstone ball-and-pillow structures, and I, I, lentil slumped bedding. All of these struc- \ \ tures are present in the reference sec- -., tion along 1-57 (fig. 11). Interference . ripples and load casts are found at practically all outcrops of hetero- lithic Wayside. Most laminae and Wayside beds are a fraction of an inch to 3-4 Member inches thick, although occasional lenses of sandstone up to several feet thick are present. Thicker sand- stone beds generally have sharp upper and lower contacts.

.Fossils A diverse marine fauna has been collected from thin bedded sandstone of the lower part of the

/ -. Wayside Member. Rexroad and Mer- /unnamed rill (1985) and Jennings and Fraun- 1 sandstone felter (1986) together listed more \ ,lentil than 40 species of marine inverte- - - - brates, including conodonts, coelen- terates, brachiopods, pelecypods, gastropods, cephalopods, an arthro- pod, and crinoid columnals. Collec- tions for both studies were made along the north-flowing tributary of covered I Buck Branch in the W?h NE, Section Goreville 30, TIIS, R2E. We also found fossils Limestone in the streambed in the SE SE NE, Member below road level 15 Section 30 and in the sandstone over- lying the type Grove Church Shale Figure 11 Measured section in a roadcut along 1-57 illustrates the in the streambed and roadcut in the reference section of the Wayside Member (SE SW, Section 24, and NE NW, Section 31. Most fossils are NW NW, Section 25, TIIS, R~E). poorly preserved molds and casts in sandstone and are not easy to find. Trace fossils are common in hetero- is absent, and the Wayside cannot be the remainder of the rock. Some lithic rocks of the Wayside through- distinguished from overlying strata sandstones have calcite cement, out the study area. Most traces con- of the upper part of the Caseyville whereas others have silica cement sist of simple, unbranched cylindri- Formation. and sutured or pressure-welded cal burrows and poorly preserved Among the heterolithic rocks that grains. Siltstone in the Wayside is trails not assignable to specific ichno- constitute the bulk of the Wayside, light to medium gray and quartzose, genera. Diverse trace fossils occur sandstone is the prevalent lithology. containing a higher proportion of mica in the 1-57 roadcut. In addition to un- This sandstone is white to light gray and clay minerals than do the sand- identified trails and burrows, the very fine to fine grained, well indu- stones. Shale is medium to dark gray trace fossils include numerous rep- rated quartz arenite. Grains are 95% rarely black, well laminated, and ichnia, Lockeia, and Conostichus or more monocrystalline, well sorted, moderately to highly fissile. Most of (Joseph A. Devera, written communi- and well rounded to subangular the shale is silty, but thin intervals of cation 1993). The trace fossil Cono- quartz. Polycrystalline quartz, mus- clay shale and blocky claystone are stichus is interpreted as the resting covite, feldspar, lithic fragments present. place of a burrowing sea anemone (largely argillite), and stable heavy Conglomerate, a minor lithology and indicates a marine environ- minerals such as zircon make up in the lower part of the Wayside, ment of deposition (Devera 1989). Plant fossils, which are fairly com- feet above the base of the Caseyville. a sharp contact by carbonaceous mon in siltstone and thin bedded The sandstone is dominantly fine to shale and claystone. sandstone of the Wayside, are medium grained and well sorted, mostly carbonized compressions or but sparse quartz granules and peb- Batte y Rock Sandstone Member casts and molds of stem and bark bles occur at the base. In places, the Cox (1875) named this member for a fragments. Other plant fossils can be sandstone has well developed pla- bluff called Battery Rock along the found with a diligent search. Among nar crossbedding that dips south or Ohio River in Hardin County Illi- the 33 varieties of plant remains col- southeast, while in other places the nois. The type section is part of the lected from the Wayside by Jennings rock appears massive or shows faint Caseyville type section. The Battery and Fraunfelter (1986) are lycopods, undulating and contorted lamina- Rock crops out extensively in south- sphenophytes, ferns, seed ferns, cor- tions that suggest slumping or de- ern Illinois and parts of western Ken- daiteans, seeds, and ovules. We watering of the sand prior to lithi- tucky and is nearly continuous in found well preserved plant fossils fication. The Buck Branch thins the fluorspar district (Baxter et al. along the large streambed in the SE toward the south and grades into 1963, Baxter and Desborough 1965, NE NE, Section 29, TllS, R2E. They heterolithic strata (fig. 10, columns F Baxter et al. 1967) and westward in consist of compressions of leaves and G). In the SW NW, Section 29, a the Eddyville (Nelson and Lumm and stems and sand-filled stig- thin conglomerate of ironstone clasts 1990a), Stonefort (Nelson and marian root casts, both found in in a matrix of iron-rich sandstone Lumm 1990b), Creal Springs (Trask gray shale that underlies a 2-foot- occurs in the Buck Branch (fig. 10, and Jacobson 1990), and Goreville thick bed of black shale. Carbona- column I). The Buck Branch is gener- (Jacobson1991) Quadrangles. The ceous shale that contains abundant ally overlain conformably by hetero- Battery Rock is the lower part of the plant compressions also occurs just lithic rocks, but near the center of Lick Creek Sandstone Member outside the study area along a north- Section 29, the Buck Branch is eroded mapped by Lamar (1925) in the Car- flowing stream in the SW NE, Sec- at the base of the Battery Rock Sand- bondale 15-minute Quadrangle (fig. tion 4, T12S, R2E, Goreville Quad- stone. Lower contact of the Buck 12).Lamar's Lick Creek Sandstone rangle (fig. 10, column J). Branch is erosional and is well ex- also includes younger strata up to posed at the northwest corner of Sec- the top of the Pounds Sandstone .Sandstone lentils Mappable tion 30 and in the E% NE, Section 29 Member of the Caseyville. bodies of bluff-forming sandstone (fig. 10, column H). At these sites, The Battery Rock is a coarse occur at or near the base of the Way- the lower contact of the Buck Branch grained, pebbly to conglomeratic side in several areas. One such len- undulates strongly and truncates sandstone that forms cliffs as high til is exposed in the 1-57 roadcut slumped bedding of underlying silt- as 140 feet in the southeast quarter and extends about 1 mile east of the stones. A lag deposit of small quartz of the quadrangle. Westward, the highway (fig. 10, columns A and B). pebbles, shale and coal clasts, and sandstone thins, loses its quartz peb- This lentil is about 30 feet above the fossil wood fragments is at the base bles, and becomes finer grained. It base of the Caseyville Formation of the Buck Branch in these outcrops. pinches out entirely in the SE, Sec- sandstone and is 14 feet thick in the The Buck Branch lentil may be tion 15, TllS, R1E. roadcut, thickening locally to 25 equivalent to the Omar sandstone In the southeast, the Battery Rock feet. The sandstone is dominantly lentil of Jacobson (1991) in the Gore- is poorly sorted, coarse quartz fine grained, but a basal conglomer- ville Quadrangle. arenite containing abundant, white, ate contains quartz, chert, and shale The Keller sandstone lentil (infor- well rounded quartz pebbles up to pebbles up to 2 inches in diameter. mal name) crops out near Keller about 1 inch in diameter. Pebbles oc- Trough and planar crossbedding are Cemetery in the western part of Sec- cur as conglomeratic lenses and as prominent, along with asymmetrical tion 28, TIIS, R1E. The Keller thick- laminae and stringers on foreset and current ripples and contorted bed- ens from a feather-edge east of 1-57 bottomset beds of crossbedding; ding (slumping or dewatering to about 80 feet thick in the NE, Sec- they are also scattered throughout structures). tion 20, TIIS, R1E. The base of the the sandstone. Planar and trough Other basal Wayside sandstone Keller lies 20 to 100 feet above the crossbedding occur in bedsets 1 to 5 lenses occur in Sections 29 and 32, base of the Caseyville Formation. feet thick. Crossbedding is generally TIIS, R2E (fig. 10, columns F and G). The Buck Branch and Keller sand- unidirectional, dipping south or These sandstones are well sorted, stones are lithologically similar and southwest. Other sedimentary struc- very fine to fine grained quartz occur at about the same stratigraphic tures are scour or cut-and-fill fea- arenites that contain few or no position. Where the Keller is thick, it tures with pebble lags, and slumped quartz pebbles. Planar crossbedding generally becomes coarser grained or contorted laminations. The lower and contorted bedding are common. and contains quartz pebbles, particu- contact of the Battery Rock Sand- The sandstones are up to 20 feet thick larly near the base. The lower con- stone in the southeastern area is and 0 to 20 feet above the base of the tact, where observed, is erosional erosional. The Buck Branch sand- Caseyville. The pinch-out of one of (fig. 10, column A, and fig. 11).A stone is entirely cut out near the cen- these sandstones can be seen along basal! lag conglomerate of shale ter of Section 29, TllS, R2E, and the road and hillside near the center cIasts was seen in several places. partially cut out near the northwest of the EX, Section 31, TIIS, R2E. Near the west edge of the quad- corner of the same section. The up- The Buck Branch sandstone rangle the Keller crops out as two per contact of the Battery Rock Sand- lentil (informal name) forms cliffs iedge-forming sandstones separated stone in this area is poorly exposed and ledges along Buck Branch in Sec- by a covered (presumably shaley) in- but probably conformable. tions 19,20,29, and 30, TIIS, R2E. terval. The upper part of the Keller is North and west of Buck Branch, The Buck Branch sandstone is up to fine grained, crossbedded, and bur- the Battery Rock becomes domi- 40 feet thick, and its base is 50 to 60 rowed sandstone that is overlain with nantIy fine grained, and quartz peb- Lamar 1925 Kosanke et al. 1960 This report grained laminated or thinly bedded sandstone occur in gullies and streambeds. No meaningful compos- ite section can be assembled from these spotty exposures. The uppermost 10 feet of the un- named member is exposed at the Makanda southwest end of a large roadcut sandstone member along 1-57 in the NE SE NE, Section 24, TIIS, R1E. Exposed strata consist of planar-laminated, gray silty shale and siltstone with lenticular inter- beds of very fine grained quartz arenite (fig. 15).The contact to the Drury shale and overlying Pounds Sandstone is sandstone member sharp and appears to be erosional. East of the highway in the SE, Sec- Pound Pound tion 19, TIIS, R2E, a sandstone up to Sandstone Member Sandstone Member 20 feet thick that crops out above the unnamed member is fine grained Lick Creek Drury Shale Member unnamed quartz arenite with few pebbles. It is sandstone Member both overlain and underlain by Battery Rock Battery Rock poorly exposed, gray shale, silt- Sandstone Member Sandstone Member stone, and thin bedded sandstone. The sandstone may be either an iso- Wayside sandstone Wayside Wayside Member lated lentil or a westward-thinning and shale member Sandstone Member tongue of the upper Battery Rock Sandstone. Figure 12 Pennsylvanian nomenclature used for the Lick Creek area. Two well exposed sections of the unnamed interval are in deep ra- bles are rare. Abrupt thickness and sandstones are "stacked" in the vines west of 1-57 (fig. 13). In one facies changes take place north of Throgmorton well. Wells in the west- exposure (fig. 13, column A), the in- the branch in Sections 19 and 29, ern half of the study area indicate no terval is about 90 feet thick. Flaggy where the sandstone varies from 50 thick sandstones in the Caseyville. bedded, very fine quartz arenite at to 100 feet thick and intertongues the base contains interference ripples with thin bedded, shaley sandstone Unnamed member A slope-form- and horizontal and vertical burrows. and siltstone. Along 1-57! the Battery ing interval of heterolithic shale, silt- Above this base is gray silty shale, Rock is about 30 feet thick and com- stone, and thin bedded sandstone then intensively burrowed sandy posed of fine grained crossbedded overlies the Battery Rock Member. siltstone. Just below the overlying sandstone containing scattered The name "Drury Member" was for- Pounds Sandstone is sandstone quartz pebbles; the lower contact is merly applied to this interval containing stigmarian root casts, erosional (figs. 10 and 11). (Kosanke et al. 1960, Baxter et al. overlain by shale and siltstone con- West of 1-57, the Battery Rock is 1967, Nelson et al. 1991, Jacobson taining plant stem and leaf fragments. fine to medium grained, generally 1991); but the interval does not corre- In the other exposure (fig. 13, col- well sorted quartz arenite containing spond to the Drury Sandstone and umn B) about 45 feet of fine grained few or no quartz granules. It is me- Shale Member as mapped by Lamar strata is exposed. Shale at the base dium to thick bedded and generally (1925). Mapping in the Lick Creek grades upward to thin bedded, bur- crossbedded. The lower contact is and Makanda Quadrangles (Jacob- rowed sandstone, which in turn still erosional, whereas the upper son and Weibel1993) demonstrates grades to siltstone and then to dark contact is gradational to thin bedded that Lamar's Drury Member is gray sideritic shale. Hence, this is a sandstone and siltstone (fig. 13). largely in the lower part of the Trade- coarsening-upward cycle overlain Near the northeast corner of the water Formation, although in some by a fining-upward cycle. Contact to quadrangle (Sec. 29, TlOS, RlE), logs areas the Drury includes uppermost the Pounds Sandstone is concealed. and samples of three oil-test holes Caseyville strata (fig. 12). To avoid indicate the Battery Rock is nearly further confusion, we are abandon- Pounds Sandstone Member The massive, fine to coarse grained sand- ing the name "Drury Member" and Pounds Sandstone Member was stone 90 to 100 feet thick. leaving the member unnamed in named by J.M. Weller (1940) for Southward, the Monjeb no. 31 this report. East of 1-57, the un- Pounds Hollow in Gallatin County Throgmorton well in Section 5, TllS, named member is 20 to 90 feet thick Illinois. The Pounds crops out exten- R2E1 penetrated 295 feet of Casey- and forms a gently sloping or rolling sively in southeastern Illinois and ville Formation, of which all but the bench or steeper slopes that are lit- has been mapped westward from basal 45 feet is sandstone (fig. 14). tered with talus from the overlying the type locality to the Lick Creek The Caseyville sandstone is fine Pounds Sandstone. Exposures of the Quadrangle (Baxter et al. 1963, Bax- grained at the tog, becoming coarse unnamed member are fragmentary. ter and Desborough 1965, Baxter grained with quartz granules in the Small outcrops of medium to dark et al. 1967, Nelson and Lumm 1990a lower part. The Pounds, Battery gray clay shale and silty shale, gray and b, Trask and Jacobson 1990, Rock, and possibly Buck Branch laminated siltstone, and very fine Jacobson 1991). These authors char- acterize the Pounds as a bluff-forming, massive or crossbedded, quartzose Pounds ...... sandstone in which quartz pebbles --.-.* ...... are common but generally smaller ...... Member and less abundant than in the Bat- ...... covered tery Rock Member. In most areas, ---- the Pounds is the youngest sand- stone having typical Caseyville lith- ology, and the top of the Caseyville is generally mapped at the top of the Pounds. In the eastern half of the Lick Figure 13 Two measured sec- Creek Quadrangle, the Pounds is 30 tions of the Caseyville Forma- to 80 feet thick and forms rounded, tion west of 1-57: (A) ravine in south-facing cliffs. West of 1-57, the E?h SW and SE NW, Section 14, Pounds becomes discontinuous and TIIS, RlE, and (B) ravine in SW disappears near the west edge of the NW SE, Section 15, TllS, RlE. quadrangle. The Pounds is composed domi- nantly of white to light gray, fine In three wells in Section 29, TIOS, grained, well sorted quartz arenite. R2E, the upper Caseyville consists Quartz granules and small pebbles of 165 to 220 feet of fine to coarse are less common in the quadrangle grained, partly pebbly sandstone than they are farther east. Current with few or no shaley interbeds. In ripples, interference ripples, and the Monjeb no. I Throgmorton we11 crossbedding are present, but much (Section 5, TIIS, R2E), the upper of the sandstone is nearly massive Caseyville contains 250 feet of mas- and displays faint, contorted, and sive sandstone, grading from very slumped laminations. No trace fos- coarse at the base to fine grained at sils or body fossils have been the top (fig. 14). Evidently, the observed. Pounds and Battery Rock Sand- The roadcut along 1-57 (fig. 15) stones are superimposed in these shows the sharp and apparently wells. These four wells in the quad- erosional lower contact of the rangle have the only reliable logs of Pounds, as well as the gradational the upper Caseyville. upper contact, lateral intertonguing of sandstone, and overlying silty Tradewater Formation The shale of the basal Tradewater Forma- Tradewater Formation was named tion. The gradational upper contact covered for the Tradewater River in western is also visible in ravines east of the Kentucky by Glenn (1912).The type highway in Section 19 and the NW, I section was described by Lee (1916), Section 20, TIIS, R2E. In these ravines, and the formation has been mapped thick bedded, clean quartz sand- widely in western Kentucky and stone of the Pounds grades upward southern Illinois. Kosanke et al. through a 10- to 30-foot-thick inter- (1960) divided the Tradewa ter into val to micaceous, brown weathering the Abbott (older) and Spoon Forma- lithic arenites of the Tradewater Keller tions in Illinois, but subsequent map- Formation. The Caseyville-Trade- sandstone ping shows that the Abbott and water contact was mapped at the lentil Spoon are distinguishable only in highest occurrence of quartz arenite. small areas (Nelson et al. 1991, Jacob- West of 1-57, as the Pounds thins, son 1991). Accordingly, this report its bedding generally becomes thin- reintroduces the Tradewater Forma- ner, and shale and siltstone interbeds tion in southern Illinois. become more numerous. Interfer- The Tradewater is an interval of ence and oscillatory ripple marks, intercalated sandstone, siltstone, small-scale crossbedding and cross- rangle, including Grassy Creek and shale, and thin, lenticular coal and lamination, and burrows and other the large stream west of Grassy Creek limestone. It can be distinguished unidentified trace fossils are common. (flowing to Devils Kitchen Lake). from the Caseyville by the character Crossbedding mostly dips south- Here the sandstone is very fine to fine of the sandstones. Caseyville sand- west. As elsewhere in the quad- grained quartz arenite with rare stones are dominantly quartz are- rangle, lower contact is sharp, and granules. Tabular-planar and wedge- nites, whereas Tradewater sand- upper contact is gradational. The planar crossbedding occurs in sets stones are lithic arenites (subgray- sandstone generally is coarsest at the as thick as 6 feet and dips southeast, wackes) that contain conspicuous base and becomes finer grained and east, and north (fig. 16). Current and amounts of lithic fragments, feld- more thinly bedded upward (fig. 13). interference ripples having diverse spar, mica, and interstitial clay. The Founds crops out along sev- orientations also were noted, along Quartz granules and small pebbles eral north-flowing streams in the with unidentified burrows and occur in lower Tradewater sand- northern half of the Lick Creek Quad- poorly preserved plant remains. stones but are uncommon. Sample S.P. Log Member Fn The upper part of the Tradewater has been eroded throughout the Lick Creek Quadrangle; its maximum thickness, in wells in Section 29, TlOS, R2E, is about 300 feet. Exposures of the Tradewater gen- erally are poor. The formation mainly upper underlies a dip slope that is mantled sandstone with loess and, toward the north, with glacial drift. Most sandstones are weakly indurated and do not form long, continuous bluffs as do Caseyville sandstones. Outcrops of the fine grained strata are mostly fragmentary. The best Tradewater ex- posure is a roadcut along 1-57 (NE, Sec. 24, TIIS, RlE), which shows the basal 80 feet of the formation. The lithologic succession of the Tradewater is known largely from well records, particularly from CO- GEOMAP borehole G-1, in which the Tradewater was continuously cored (fig. 17). The succession varies, but four informal members can be recognized in most of the quadrangle: (1)basal shaley member, (2) lower sandstone member, (3) middle shaley member, and (4) upper sand- stone member. Boundaries of these units are too poorly exposed to map in most areas. On the geologic map, we show ledge-forming sandstones, designated as lower Tradewater (Its) and other Tradewater sandstones (ts).

Basal shaley member The basal 30 to 60 feet of the Tradewater For- mation in the study area is mainly silty shale and siltstone, containing Pounds thin, lenticular coalbeds. This basal and shaley member is equivalent to the Battery Rod Ferne Clyffe member (informal) of Sandstone Jacobson (1991) in the adjacent Gore- Members ville Quadrangle. The basal shaley member is fully exposed in the roadcut along 1-57 in the SW NW NW, Section 19, TIIS, R2E. Here, the member is 30 to 40 feet thick and consists of dark gray fissile shale interlaminated with light gray siltstone to very fine grained sand- stone (fig. 15). Sandstone interbeds become thinner and less numerous upward. Planar lamination, flaser bedding, current and interference ripples, and crosslamination (in silt- stone) are prevalent. Small-scale growth faults (fig. 18), slumped bed- ding, and ball-and-pillow structures occur in the roadcut. Trace fossils are Goreville locally abundant and include forms Ls Member having marine affinities. Fossils con- ,,, , Cave Hill sist of Lockeia, the regichnia Uchirites ,,, Member and Koupichniurn, Cruziana, and vari- Figure 14 Geophysical logs and sample log (graphic) column ous cubichia, repichia, and domich- of Pennsylvanian strata in Monjeb Minerals no. 1 Throg- nia, as well as resting-traces of an morton borehole, SW NE SW, Section 5, TllS, WE, Johnson unidentified shrimplike organism County, ISGS County no. 20370. (Devera 1989). The basal shaley mem- ber intertongues with the under- lying Pounds Sandstone and is overlain with erosional contact by sandstone. I covered 1 Borehole data and outcrops in the northeast quarter of the Lick Creek Quadrangle indicate thin coal or lower highly carbonaceous shale in the sandstone basal Tradewater. In COGEOMAP borehole G-1, a 1.1-foot-thick bed of bright-banded coal, which overlies claystone containing s tigmarian root- lets, was cored (fig. 16). Coal occurs near the same position in samples from two oil-test holes close to CO- GEOMAP borehole G-1. In the first sample, a 2-inch-thick coal bed over- lies rooted claystone and is overlain by dark gray clay shale in a stream- bed in the SW SW NW, Section 1, TllS, R1E. This coal is very close to the base of the Tradewater. In the sec- ond sample, coal laminae occur in sandstone along the streambed north of Little Grassy Lake near the Pounds center of the NE NW, Section 4, Sandstone TllS, R1E. These scattered occur- Member rences probably represent more than one coal bed. Palynological study by Russel A. Peppers (written commu- nications 1988) indicates basal Trade- water coals in the Lick Creek Quadrangle are equivalent to the Figure 15 Measured section in a Reynoldsburg Coal Bed or the roadcut along 1-57 south of the Gore- slightly younger Bell Coal Bed. Both ville interchGge (Secs. 18 and 19, - ,- SF, ,-, of these coals are present in quadran- .-.. -..-..\ TllS, R2E, and Sec. 24, TIIS, RlE). gles east of Lick Creek, although they are lenticular. Sandstone occurs at the base of the Tradewater east of 1-57 in the northern parts of Sections 19 and 20, TllS, R2E. This sandstone is a slightly micaceous, argillaceous, lithic arenite that grades downward to quartz arenite of the Caseyville Forma tion.

Lower sandstone member The lower sandstone member of the Tradewater Formation is 30 to 90 feet thick. This member crops out discontinuously near the crest of the south-facing drainage divide in the central Lick Creek Quadrangle and along several streams that flow north from that divide. We mapped the sandstone where it is well ex- posed and did not attempt to project it through covered areas (Weibel and Nelson 1993). Generally the lower sandstone is friable and weathers deeply forming outcrops only on steep hillsides. This member is composed of Figure 16 Tabular-planar crossbedding in Pounds Sandstone, west side of brown-weathering, micaceous, lithic Grassy Creek, SW NW, Section 7, TllS, R1E. Foreset beds dip east. Staff is 5 feet arenite that generally is poorly long. can be divided into three separate that is 40 to 65 feet thick, as deter- sandstone bodies above one another, mined by subsurface data. This unit each separated by erosional contacts. is poorly known in the Lick Creek A basal, lenticular unit of coarse, Quadrangle because outcrops and conglomeratic sandstone is 1 to 15 borehole records are few. feet thick and displays large-scale The middle shaley member was trough crossbedding and small-scale cored continuously in COGEOMAP ripple lamination. A lag conglomer- borehole G-1, where the member is ate of shale, ironstone, and quartz about 40 feet thick and consists of pebbles overlies the erosional lower siltstone to fine grained sandstone contact. The middle unit is 7 to 12 that contains laminae of gray shale feet of fine to coarse grained sand- (fig. 17). Vertical and horizontal bur- stone that has huge, planar, south- rows occur throughout the unit; por- west-dipping foreset beds (fig. 19). tions of the core are so intensively Current ripple marks superimposed burrowed that lamination is obliter- on the foreset beds show northerly ated. The core also contains several paleocurrent; hence, the middle sand - zones of intraformational conglom- stone represents bidirectional cur- erate that contain clasts of coal, rents. Foreset laminae are arranged shale, and siderite. The burrowed in thin-thick couplets that are consis- unit directly overlies coal (palyno- Murray Bluff tent with neap-spring tidal cycles Sandstone logically equivalent to the Smith Member (?) (Kvale and Uhlir 1988, Kvale and coal bed) and is sharply overlain by Archer 1991). The upper unit is fine crossbedded upper Tradewater grained, lithic arenite with siltstone sandstone. and shale interbeds, ripple marks, The middle shaley member is and small-scale trough crossbedding. about 65 feet thick in the Monjeb The lower sandstone member in no. 1 Throgmorton well (Sec. 5, the core of COGEOMAP borehole TIIS, R2E) and composed of me- G-1 (fig. 17) is a fine grained, shaley dium to dark gray silty, carbona- sandstone 60 to 100 feet above the ceous shale and siltstone, grading approximate base of the Tradewater. It is thor- at the base to very fine grained sand- equivalent of oughly burrowed, and part of it is a stone. Near the top of the interval is Smith coal strongly calcareous interval and con- black, highly carbonaceous shale bed (W. KY) tains crinoid and brachiopod frag- that contains pyrite crystals and ments. Stigmarian root casts occur coarse plant remains. lower above and below the calcareous On the outcrop, the middle sandstone marine zone. At the top, the sand- shaley member is interlaminated unit stone grades to rooted claystone with siltstone, with occasional and a bright banded, pyritic coal lenses and interbeds of sandstone. bed 1.1 feet thick. The shale is medium to dark gray, The lower sandstone member is fissile, and noncalcareous, and con- basal equivalent to, if not continuous shaley tains siderite nodules. Siltstone is unit with, the Cedar Creek sandstone len- light gray to brown and quartzose; til, mapped by Jacobson (1991) in the sandstone is very fine grained, silty, Goreville Quadrangle and by Trask and laminated to thinly bedded. and Jacobson (1990) in the Creal Shale rip-up clasts, fragmentary Springs Quzdrangle, east of the plant remains, burrows, and other Reynoldsburg study area. Palynological study indi- unidentified trace fossils are com- Coal Bed cates that the coal that directly over- mon in the member. lies the lower sandstone in COGEO- The middle shaley member litho- Figure 17 Graphic column of CO- MAP borehole G-1 correlates with the logically resembles and occupies the GEOMAP borehole G-1. Smith coal bed in western Kentucky same stratigraphic position as the (Russel A. Peppers, written commu- Lake of Egypt member in the Gore- nication 1989).The Smith coal occurs ville Quadrangle (Jacobson 1992) sorted and fine to coarse grained. slightly below the middle of the and the olive shale member in the Quartz granules and small pebbles Tradewatex Formation in Kentucky, Creal Springs, Stonefort, and Eddy- locally occur at or near the base. Bed- overlying the Finnie Sandstone ville Quadrangles (Nelson et al. ding varies but generally is thick, Member and underlying the Lead 1991). Palynology of associated and crossbedding is well developed. Creek Limestone Member (Peppers coals suggests the middle shaley Most of the observed foreset beds 1988). Thus, the lower sandstone is member may be equivalent to the dip south or southeast, but several approximately equivalent to the Lead Creek Limestone Member in dip north. Finnie Sandstone and to the Grind- western Kentucky (Peppers 1988). The lower sandstone member is staff Sandstone in the fluorspar well exposed in the roadcut along district. Upper sandstone member The 1-57 just southwest of the Goreville youngest part of the Tradewater For- interchange, where the member is 50 Middle shaley member Overlying mation in the quadrangle consists of to 60 feet thick, with the upper con- the lower sandstone member of the sandstone with local interbeds of tact covered (fig. 15). The member Tradewater is an interval of shale siltstone and shale. Thickness of this Figure 18 Sketch of a small growth fault in the interlaminated shale and sandstone of the basal Tradewater Forma- tion in a roadcut along 1-57. cocation is given in figure 15. current ripples indicating westerly paleocurrents were observed along Little Wolf Creek near the north edge of the quadrangle. Nearly mas- sive sandstone bearing faint, slumped, and contorted laminae is exposed along Wolf and Middle Wolf Creeks at the north edge of the quadrangle. Although the upper sandstone is predominantly lithic arenite, clean quartzose sandstone that approaches quartz arenite occurs in several places. Clean sandstone on the north- east side of Devils Kitchen Lake in the SW SW, Section 26, TlOS, RlE, appears to grade westward to lithic arenite. Clean quartz sandstone is in- terbedded with lithic arenite just north of the study area on the west shore of Herrin Lake, NW SW, Sec- tion 20, TlOS, R2E, Crab Orchard Lake Quadrangle. These sandstones, Figure 19 Huge tabular-planar crossbedding in sandstone of the lower Trade- 200 to 300 feet above the base of the water Formation in a roadcut along 1-57. Foreset beds dip southwest, The alter- Tradewater, resemble those of the nating thin and thick foreset laminations, most clearly visible at the left side of Caseyville Formation except for the the photo, have been interpreted as reflecting tidal ebb and flow cycles (Kvale absence of quartz granules. and Archer 1991). The upper sandstone of the Trade- water in the core of COGEOMAP upper sandstone member has not posed of subrounded to subangular borehole G-1 (fig. 17) consists of 150 been determined adequately but quartz sand along with considerable feet of sandstone with interbeds of may be as much as 150 feet. Sand- amounts of lithic fragments, mica, medium to dark gray silty shale. stones shown with the symbol ts on feldspar, and clay matrix. Fresh rock The sandstone is fine to coarse the geologic map (Weibel and Nel- is light gray or yellowish gray grained and crossbedded, and con- son 1993) belong to this member. whereas weathered surfaces are gen- tains rip-up clasts of shale, siderite, The upper sandstone member erally brown and encrusted with and coal. This sandstone is coarser crops out discontinuously along iron oxides. Bedding varies from grained than that observed on north-flowing drainages in the thin to massive;but most of the out- nearby o~tcrops.~ northern half of the quadrangle. The cropping sandstone has irregular, The upper sandstone is at least rock is locally well indurated, but in thick bedding. Tabular-planar cross- partly continuous with the Murray most places, it is weakly cemented bedding occurs in sets as thick as 5 Bluff Sandstone Member, mapped in and erodes easily. Locally, the upper feet; foreset beds generally dip quadrangles to the east. The upper sandstone forms cliffs as high as 60 southward. Crossbed orientations sandstone in the Lick Creek Quad- feet. are diverse near the spillway of a rangle, however, probably also in- The upper sandstone generally is pond in the NE NE, Section 26, cludes strata younger than the very fine to fine grained and com- TlOS, RlE. Shallow troughs bearing Murray Bluff. QUATERNARY SYSTEM by thick loess. Good exposures of oxidized wood, which are radio- Bedrock geology was the principal the Glasford were observed in cut- carbon-dated as older than 40,000 focus of this study and most Quater- banks of Wolf Creek in the NE, Sec- years, a finding consistent with 11114- nary deposits were not mapped or tion 32, TlOS, R2E; in cutbanks and noian age (Follmer, written commu- examined in detail. The Glasford landslide scarps on the north side of nication). Formation was mapped because it Grassy Creek in the S%, Section 25, Thickness of the Glasford Forma- shows interesting relationships to TlOS, R2E; in the spillway of a lake tion in the study area is difficult to geomorphology at the southern mar- in the SW NE, Section 29, TlOS, R2E; assess because the sediment was de- gin of Pleistocene continental glacia- and in an east-trending ravine near posited on an uneven bedrock sur- tion. the northwest corner of the NE SW, face and few well records are avail- Section 27, TIOS, R1E. Because the able. A test hole on the floodplain of Pre-Illinoian Loess Glasford is not lithified, most expo- Grassy Creek in the SW SW SE, Lamar (1925) described "pre-Illi- sures are short lived. Section 25, TlOS, RlE, penetrated noian loess" in an exposure along Glasford sediments in the study 55 feet of Glasford sediments with- the road "a few hundred feet south area are mostly diamicton that is out reaching bedrock (Steven Esling, of the center of the north line" in composed of silty clay with minor personal communication 1988). Section 36, TlOS, R1E. A roadcut on amounts of sand and gravel and Immediately north of the drill site, the east side of the road at this loca- occasional cobbles and boulders the Glasford extends 60 feet up the tion reveals yellow brown to orange (figs. 21 and 22). The silty clay is hillside, implying a minimum thick- brown loess that contains sub- light gray to medium brownish or ness of 115 feet. The Glasford may angular sandstone clasts. This de- bluish gray and weathers yellowish be thicker than 120 feet along the di- posit probably is the Loveland Silt, a gray Sand and pebbles are scattered vide between Wolf and Middle Wolf windblown deposit of Illinoian age throughout the diamicton and also Creeks at the north edge of the quad- that occurs in unglaciated areas of occur as small, discrete lenses and rangle. In the valleys of all the large Illinois (Willman and Frye 1970, stringers. Sand grains are light gray streams in the northeast quarter of Frye and Willman 1975). The Love- to orange brown and composed the quadrangle, the Glasford prob- land is probably widespread in the mainly of rounded to subrounded ably underlies Holocene alluvium. area, but it is generally covered by quartz and chert. Angular or only Judging by borehole data and the younger deposits, so drilling would slightly abraded sandstone clasts profiles of streams in unglaciated be needed to determine its extent. As derived from the Tradewater Forma- areas, the preglacial profiles of these shown on the stratigraphic column tion or younger Pennsylvanian creeks probably were V-shaped. of the geologic map (Weibel and strata are common and range in size Along several north-trending Nelson 1993), the Petersburg Silt from granules to slabs about 1 foot valleys, Glasford sediments form may underlie the Glasford Forma- in maximum dimension. Erratics of terraces, which may occur along one tion in the northern part of the quad- granite and phaneritic, mafic igne- or both sides of a valley and have rangle. The Petersburg and Loveland ous rock, basalt, and yellowish gray steep slopes and nearly level tops. are equivalent units; the name dolomite are common in places. Elevations of terraces are consistent "Petersburg" is used where the They are mostly well rounded and within a valley but may differ among Glasford overlies the silt (Willman range from small pebbles to boul- valleys. Terraces are at about 570 feet and Frye 1970). ders 4 feet in diameter. Erratics are elevation along Wolf Creek, 550 feet largest and most numerous near along Middle Wolf Creek, 560 feet Glasford Formation Devils Kitchen Lake, whereas only along Little Wolf Creek, and 620 feet Unlithified diamicton containing occasional small, igneous pebbles along Grassy Creek. Many land- lenses of sand and gravel in the occur along Wolf and Middle Wolf slides are evident in terrace deposits northern part of the Lick Creek Creeks. along the steep valley walls, particu- Quadrangle is mapped as the Glasford deposits generally lack larly on the north side of Grassy Glasford Formation (Weibel and sorting, grading, or stratification Creek. Nelson 1993).The Glasford was (figs. 21 and 22). The only stratified Superimposed drainage devel- named for a town in Peoria County, sediments are thin, discontinuous oped along several creeks near the Illinois, and is interpreted as glacial layers of sand and sandstone clasts. north edge of the quadrangle. Super- till with intercalated outwash depos- Sand lenses vary from horizontal to imposed stream segments occupy its and overlying accretion-gley de- steeply tilted; some are contorted, narrow, sinuous to meandering posits (Willman and Frye 1970). which suggests slumping and defor- gorges cut into Pennsylvanian sand- Lamar (1925) used the term "Illi- mation while in a viscous state. stone. Wolf Creek and Middle Wolf noian glacial drift" for the deposits Along Grassy Creek in the S% Creek enter sandstone gorges at or assigned in this report to the Glasford SW SE, Section 25, TlOS, RlE, Glas- just north of the north boundary of Formation. ford diamicton contains prominent the quadrangle (fig. 20). The sand- The Glasford occurs mostly along polygonal joints that are lined with stone floor of Wolf Creek is at an ele- valleys in the northeastern corner of iron oxides (fig. 22). Leon Follmer vation of 480 feet, and the floor of the quadrangle (fig. 20). It probably (written communication 1989) inter- Middle Wolf Creek is at 505 feet. also occurs to the northwest, but is preted the joints as dessication Midway between Wolf and Middle largely submerged beneath Devils cracks filled with secondary weath- Wolf Creeks, the Glasford is exposed Kitchen and Little Grassy Lakes. ering products and representing a along a north-trending ravine down Near the north edge of the quad- mature weathering profile in the to an elevation of 475 feet-lower rangle, the Glasford partly extends "C" horizon of the Sangamon Soil. than bedrock exposures in Wolf and across upland divides, where it is Embedded in the diamicton at the Middle Wolf Creeks. Hence, the difficult to map because it is mantled same site are fragments of partially creeks must have joined south of

their present intersection prior to unstratified clayey silt or silt overlies mixture of loess and rock fragments) deposition of the Glasford (fig. 20). diamicton of the Glasford Formation. mantles most hillslopes in the auad- After Glasford deposition, Wolf and rangle. Because bediock geology Middle Wolf Creeks cut new chan- Alluvium, Collluvium, was the primary emphasis of this nels through the Glasford into bed- and Talus survey, colluvium was not mapped. rock. Neither creek has cut its new Alluvium (stream sediment) was Talus (broken rock debris on steep channel as deeply as the preglacial mapped where it forms distinct slopes) was mapped only where it channels that are now filled with floodplains in valleys. Alluvium produces significant landforms and Glasford sediments. overlies the Glasford Formation in conceals bedrock. Mapped talus is The superimposed segment of valleys in the northern part of the mostly at the base of sandstone cliffs Grassy Creek (partially flooded by quadrangle. Cutbank exposures and in the Caseyville Formation, where Devils Kitchen Lake) begins at the borehole records indicate that allu- sandstone boulders up to the size of bridge near the center of Section 26, vium generally is only several feet a house are randomly intermixed TlOS, RlE. Here the stream flows on thick. A thin layer of colluvium (a with smaller fragments. sandstone at an elevation of 505 feet (fig. 20). One mile upstream, a test hole was drilled in Glasford diamic- ton down to an elevation of 485 feet without reaching bedrock (Steven Esling, personal communication 1988). Hence, the pre-Glasford streambed of Grassy Creek at the well site was at least 20 feet lower in elevation than the present bedrock- floored streambed at the head of the narrows. The pre-Glasford course of Grassy Creek probably ran north or northwest of the bridge, where no bedrock crops out (fig. 20). Younger Loess Windblown silt or loess overlies the Glasford Formation as well as Paleo- zoic bedrock throughout the Lick Creek Quadrangle, but these were not mapped or studied in detail. Clean exposures of loess are not common because of vegetation and slumping. Loess is commonly 3 to 5 Figure 21 Exposure of diamicton of the Glasford Formation on the north side of feet thick in the study area, and lo- Grassy Creek in SW SW SE, Section 25, TlOS, R1E. Staff is 5 feet long. cally is thicker than 10 feet. Three stratigraphically distinct loesses are reported in southern Illi- nois (Willman and Frye 1980). The oldest of these, the Loveland Silt, was described above. The Roxana Silt and the overlying Peoria Silt are Wisconsinan and widespread in southern Illinois. Most loess at or near the surface in the Lick Creek Quadrangle is yellowish brown, light brown, or brownish gray, and probably is Peoria Silt rather than Roxana Silt, which tends to be pink- ish gray One of the few clean expo- sures of loess in the quadrangle is in the spillway of a lake in the SW NE, Section 29, TlOS, R2E. At this site, brownish gray to yellowish brown

Figure 20 Map showing distribution of Glasford Formation, preglacial bed- rock channels, and postglacial super- imposed drainages, in the northern Lick Figure 22 Diamicton of the Glasford Formation in a bed of G Creek and southern Crab Orchard polygonal veins interpreted as dessication cracks formed in Lake Quadrangles (facing page). profile of the Sangamon Soil (Leon Follmer, personal commu DEPOSITIONAL HISTO

ISSISSIPPLAN Reduced clastic input allowed study area. Thus, this interval repre- Body fossils, trace fossils, sedimen- deposition of carbonate rocks in the sents clastics that prograded from tary structures, and sedimentary se- overlying Ford Station Member. the northeast (Randall 1970, Nelson quences indicate that Pope Group Dolomite, laminated lime mudstone et al. 1991). The middle Cave Hill (Chesterian) strata in the study area and "bird's-eye" structures in the ba- contains a variety of carbonate are of shallow marine and marginal sal Ford Station limestone were inter- rocks, which represent a variety of marine origin. Lateral continuity preted by Abegg (1986) as tidal flat environments. Much of the middle and uniformity of thin units, particu- sediments (shallow subtidal to inter- Cave Hill consists of lime mudstone, larly in the Menard, Clore, and tidal and possibly supratidal). some of it finely laminated, indicat- Kinkaid Formations, point to tec- The Degonia Formation is litho- ing very low depositional energy. tonic stability in the study area. logically similar to the Palestine and Hardgrounds occur in the Southern The Menard Formation contains probably represents similar deposi- Illinois Stone Company's quarry just an abundant fauna that indicates tional conditions. Carbonaceous outside the quadrangle (Joseph A. deposition in marine water of nor- shales and rooted zones are evi- Devera, personal communication mal salinity and oxygen content. dence of subaerial exposure and ter- 1988). The variegated claystone near The prevalence of lime mudstone restrial swamps. The regionally the top of the Cave Hill contains fea- and wackestone implies gentle widespread red and green varie- tures typical of paleosols formed in waves and currents. Sources of ter- gated claystone at the top of the arid or semiarid conditions, includ- rigenous clastics were distant from Degonia is similar to other Chester- ing blocky texture and carbonate the study area. The Menard may ian strata interpreted as upper tidal glaebules. An alternative deposi- have been deposited in relatively flat to marsh deposits (Weimer et al. tional setting is upper tidal flat to deep water or in a shallow but pro- 1982).The thick sandstone of the marsh (Weimer et al. 1982). tected setting, such as a broad bay. Degonia near the west edge of the The Goreville Limestone Menz- The Palestine Formation is a quadrangle is part of a system of ber, largely crinoidal grainstone, is siliciclastic unit that represents pro- southwest-tyending sand bodies that a high-energy, shallow marine de- grading deltas or shoreline. Ripple exhibit paleocurrents toward the posit. A regression at the end of marks, crossbedding, and abundant southwest (Potter 1963).West of the Goreville sedimentation is marked by burrows indicate moderate agitation study area in the Cobden Quadrangle, a paleosol (Weibel and Norby 1992). in shallow water. Common plant re- bidirectional (herringbone) crossbed- The Grove Church Shale Member mains and thin coal overlying a ding and coupled crossbedding at its type locality records an initial rooted zone are evidence of prox- occur in sandstone of the Degonia transgression and deposition of imity to the shore and local subaerial and indicate tidal influence (Devera prodeltaic mudstone, followed by re- exposure. and Nelson 1995). Thick Degonia gression and soil formation. Another Like the Menard, the Cora Mem- sand bodies may have been depos- transgression and deposition then ber of the Clore Formation contains ited in estuaries or as shallow, off- occurred in a low-energy, near-shore abundant marine fossils throughout. shore, tidally constructed sand marine environment (Weibel and The fauna and the micritic nature of ridges (Off 1963). Norby 1992).Judging by strata pre- the limestones indicate water of nor- The Negli Creek Member of the served in nearby areas (Nelson et al. mal salinity and low to moderate tur- Kinkaid Formation grades upward 1991), at least another 50 feet of sedi- bulence and turbidity probably on from lime mudstone and wacke- ment, including a thick limestone. an open marine shelf (Abegg 1986). stone in the lower part to packstone was deposited before the major re- The Tygett Member of the Clore and grainstone in the upper part. gression that marks the end of the contains two siliciclastic intervals Similar trends were observed in the Mississippian Period. that coarsen upward and are capped Negli Creek east of the study area by rooted zones. The trace fossil Rhi- (Nelson et al. 19%).The trend im- zocorallium, found just below the plies upward shoaling and increase rooted zone of the lower sandstone, in depositional energy. Buchanan has strong marine affinities (Devera (1985) attributed micritic limestones Caseyville Formation 1989).We concur with Abegg (1986) of the lower Negli Creek to a pro- In three important aspects, Casey- that most of the Tygett Member ex- tected marine shelf and upper Negli ville strata contrast with Pope cept the roofed zones represents sub- Creek packstone and grainstone to a Group strata: (1)near-total absence tidal sedimentation. The Tygett more 3pen shelf. of carbonate rocks, (2) a marked in- records two episodes of prograda- The Cave Hill Member contains crease in grain size, and (3) pro- tion, separated by a return to open three depositionally distinct sub- nounced lenticularity of rock bodies. marine conditions similar to those of members. The lower siliciclastic in- Pebbly quartz arenites lithologically Cora sedimentation. terval coarsens upward and becomes and temporally equivalent to the coarser and thicker northeast of the Caseyville occur throughout large regions of the eastern United States. represent marsh or swamp deposits in the lower member in the 1-57 Sedimentologic patterns point to and are the only Caseyville rocks roadcut are typical of brackish- sources in an active orogenic belt in clearly not of marine origin. water environments (Devera 1989), the northeastern United States and The Buck Branch, Keller, Battery and the sedimentary structures sug- southeastern Canada (Nelson 1989). Rock, and Pounds sandstones have gest tidal action. However, thin coal Uplift in the source area, perhaps erosional lower contacts and basal beds in the lower member in the sub- coupled with climatic changes, sent conglomerates, as do basal Wayside surface are evidence of terrestrial a greatly increased sediment load sandstone lenses along 1-57 and east- swamp conditions. The lower sand- throughout the Illinois Basin. This in- ward (fig. 10). These sandstones evi- stone member in the 1-57 roadcut flux of coarse clastics choked off car- dently are channel deposits. Uni- contains tidal channel deposits bonate sedimentation. Lenticular directional, south- or southwest- (Kvale and Uhlir 1988, Kvale and rock bodies and rapid facies changes dipping crossbedding in many Archer 1991). Marine fossils in a reflect the irregular sub-Pennsylva- exposures supports Ethridge and drill core and intensely burrowed nian surface along with concurrent Jacobson's views that these are flu- siltstone and sandstone in this mem- tectonism, uneven compaction, load- vial or distributary channel sands. ber are further indicators of marine ing, and shifting sediment transport However, bidirectional or multi- conditions. The overlying middle routes. Despite these effects, eustatic directional paleocurrents are indi- shaley member likewise contains changes are still evident in the rock cated in places, particularly near the burrows and other trace fossils. The record. tops of sandstones and in areas equivalent olive shale in nearby Previous geologists interpreted where the sandstones are thin. For quadrangles contains a distinctly the Caseyville in and near the Lick example, alternating thin-thick fore- marine assemblage of trace fossils Creek Quadrangle as largely deltaic set laminae and interference ripple (Devera 1989). The middle shaley sediments. Ethridge et al. (1973) sug- marks occur in the Pounds Sand- member, however, also contains gested that two progradational del- stone along I57 and suggest tidal coaly shale with terrestrial plant fos- taic sequences are represented in the influence (Erik Kvale, personal com- sils. The upper sandstone member lower Caseyville exposed along 1-57, munication 1988). Also, the lack of in the Lick Creek Quadrangle lacks They interpreted upper Caseyville clay matrix and good sorting of some features diagnostic of particular de- and lower Tradewater strata along of the sandstones suggest winnow- positional environments, although 1-57 as deposits of distributary chan- ing and reworking by tidal currents. local bidirectional crossbedding and nels, interdistributary bays, and re- An alternative view of the big well winnowed quartz sands sug- lated environments. In the same Caseyville sandstones is that they gest estuarine or tidal settings for roadcuts, Koeninger and Mansfield are estuarine sediments. The ero- part of the member. (1979) identified a variety of deltaic sional surfaces on which they lie environments, including channels, may have developed during regres- Quaternary Deposits point bars, bays, floodplains, and sions. As sea level rose again, in- The Glasford Formation was prob- marshes. Caseyville strata exposed cised valleys were drowned and ably deposited by and from glaciers along 1-24 in the Goreville Quad- became estuaries. The dominant cur- that entered north-trending valleys, rangle were similarly interpreted as rents in the estuaries were fluvial as suggested by Lamar (1925).The distributary-channel, interdistribu- and down regional dip (toward the dip-slope of Pennsylvanian sand- tary, and overbank facies of river- Ouachita trough); but bidirectional stones in the Lick Creek Quadrangle dominated or high-constructive tidal currents also were active, espe- presented the final barrier to south- deltas (Jacobson 1987). cially in late stages of valley filling. ward advance of Pleistocene ice Some evidence, however, does The Caseyville Formation is sheets. The Glasford probably in- not agree with fluvial-deltaic mod- much thicker and contains thicker cludes sediment deposited in lakes els. Heterolithic strata that constitute and coarser sandstones in the east- that formed as the glaciers melted the bulk of the Wayside Member con- ern half of the quadrangle. This and dammed north-trending valleys tain locally abundant marine fossils, thick Caseyville rests on some of the (Willman and Frye 1980). along with sedimentary structures youngest preserved Mississippian Superimposed drainage devel- suggesting tidal flats: interference rocks in the Illinois Basin. Hence, the oped where Glasford sediments ripples, rill marks, and small load thickness change probably reflects filled preglacial valleys. After the ice casts. In the 1-57 roadcut, millimeter- more rapid subsidence in the eastern receded,, north-flowing creeks mean- scale ripples, "wrinkle marks," and part of the quadrangle. Structural dered across the gently sloping Glas- possible mudcracks in thin bedded mapping of the Kinkaid Limestone ford surface htwere unable to re- Wayside strata suggest very shallow (Weibel and Nelson 1993) reveals no occupy their former channels. water, perhaps intertidal (Erik Kvale, faults or sharp flexures. Thus, re- Cutting downward, the creeks en- personal communication 1988). gional downwarg or tilting of the countered bedrock in places. Unable Coals, carbonaceous shales, and crust apparently was involved. to migrate laterally, they eroded deep, rooted zones occur above and below sinuous, and meandering gorges the Buck Branch and Keller sand- Tradewater Formation into sandstone. Upstream from super- stones and in the interval between Sedimentation patterns similar to imposed segments, the creeks ag- the Battery Rock and Pounds Sand- those of the Caseyville continued graded, forming floodplains. Thick stones. Coals and rooted zones occur during deposition of the Tradewater deposits of Glasford Formation in the same stratigraphic positions Formation. The lower shaley mem- along the sides of pregPacial valleys in quadrangles to the east, but all of ber was deposited at least partly in remain as terraces. These terraces are these coals are %enticular(Jacobson shallow subtidal to intertidal set- gradually disappearing through gul- 1991, Nelson et al. 11991). These strata tings not far from shore. Trace fossils lying, creeping soil, and landsliding GEOLOGY

The structure of the Lick Creek abandoned sandstone quarry south- the downthrown block (reverse Quadrangle is simple. Paleozoic east of 1-57 in the NE SW NW, Sec- drag), and thickening of strata on strata dip gently toward the north- tion 25, TllS, RlE. The fault strikes the downthrown block (small-scale east, as shown by structure contour N60°W, dips about 25" to the south- growth faulting). Such features are lines on the geologic map (Weibel west, and displaces strata of the typical of faults that developed dur- and Nelson 1993).The average dip Wayside Member of the Caseyville ing or shortly following deposition of the Kinkaid Limestone decreases Formation. Throw is about 10 feet, of the sediments. from about 100 feet per mile (1.9%) and net slip (assuming only dip-slip Joints are common in sandstone in the southwestern part of the quad- motion) is about 24 feet. Shale beds outcrops in the study area and are rangle to about 80 feet per mile (1.5%) are folded and contorted in a man- shown on the geologic map. That in the northeastern part. These dips ner consistent with reverse faulting. most joint observations are in the are less than lo.The strike of bed- A thin zone of brecciated sandstone western half of the quadrangle re- ding changes from northwest to marks the fault plane. Rocks adja- flects differing propensities of the southeast in the southwest to west- cent to the fault plane are moder- authors to record joint observations northwest to east-southeast in the ately fractured and stained salmon in the field, more than an actual northeast. This gentle northeast dip pink. Slickensides and mineraliza- westward increase in frequency and is basically regional dip from the tion are absent. intensity of joints (although joints east flank of the Ozark Dome into The nearest major fault zone is do appear to be more frequent to the the Illinois Basin (fig. 2). the Ste. Genevieve Fault Zone, west). Most joints are discontinuous, J.M. Weller (1940, p. 12) mapped which is about 13 miles southwest spaced several inches to several feet a feature called the Goreville anti- of the thrust fault (fig. 2). The Ste. apart, and not mineralized. At no clinal nose, extending from Section Genevieve strikes northwest and is place in the quadrangle is jointing 32, TllS, R2E, northeastward into composed of high-angle reverse intense and pervasive. The most the Goreville Quadrangle. Weller faults whose southwest side is up- common orientations of joints are based the anticline on elevation thrown (Nelson and Lumm 1985). northeast to east-northeast and north- changes of lower Pennsylvanian The trend and sense of movement of south to slightly west of north, but sandstones. Our mapping and that the small thrust fault are similar to joints having other trends appear of Jacobson (1991) shows that the those of the Ste. Genevieve Fault sporadically. The relationship of Goreville anticline does not exist at Zone, implying that the small fault joints to other structures is unclear, the level of the Kinkaid Limestone, may have developed under the and no regional synthesis of jointing which has a northeast homoclinal same stress field as did the Ste. has been attempted. Joints in the dip. The structure of Pennsylvanian Genevieve. study area probably resulted from strata is difficult to map because A small fault, mapped by Lamar more than one tectonic episode. sandstones are lenticular, bedding (1925) as striking northeast across To summarize, bedrock strata surfaces are not planar, and marker Grassy Creek in Section 1, TllS, in the Lick Creek Quadrangle dip beds are absent. Because sandstones RlE, and Section 6, TllS, R2E, appar- regionally northeast at an average in the Caseyville Formation thicken ently does not exist. Sandstone beds rate of less than lo.No significant near Goreville, the tops of these in this area dip gently northeast, but folds or faults were mapped. A small, sandstones tend to rise because of do not appear to be offset. northeast-verging thrust fault, known differential compaction and produce Several faults too small to indi- from a single exposure, may be asso- the appearance of an anticlinal nose. cate on the geologic mag occur in ciated with the Ste. Genevieve Fault J.M. Weller (1940) suggested that the the study area. The best exposed ex- Zone. Other minor structures in the Goreville anticline might be a prod- amples are in the basal shale mem- quadrangle probably formed during uct of "unequal original deposition" ber of the Tradewater Formation in deposition and compaction of the rather than tectonic deformation. the roadcut along 1-57 (fig. 18). sediments. Jointing is common, but The only fault large enough to These faults display listric surfaces nowhere intense, and its relation- map in the Lick Creek Quadrangle is that merge with bedding planes, ship to regional structure is obscure. a small thrust fault exposed in an downward rotation of layering in The principal geologic resource in rangle, particularly in the Caseyville The absence of traces of minesali- the Lick Creek Quadrangle is lime- Formation. Thick intervals of nearly zation and of the type of structures stone for construction and agricul- pure quartz sandstone occur in the associated with ores in the Illinois- tural purposes. Slight potential Caseyville in the southeast quarter Kentucky district imply that the exists for mining fluorspar, base of the quadrangle. Although degree Lick Creek Quadrangle is not a metals, or coal. Nine unsuccessful of cementation varies widely, Casey- promising area for commercial de- petroleum-test holes have been ville sandstones tend to be more re- posits. However, Eidel and Baxter drilled to upper Mississippian tar- sistant to weathering and abrasion (1989) postulated on the basis of gets; deeper prospects remain un- than sandstones of the Pope Group trace element studies that fluorite tested. or Tradewater Formation. mineralization may occur in an area Lamar (1925) reported that sand- of southwestern Illinois that in- Limestone stone from the Lick Creek area was cludes this quadrangle, and small Kinkaid Limestone has been quar- formerly used for building stone, fluorite-containing veins and vugs ried in the Lick Creek Quadrangle culverts, retaining walls, and water- have been observed in the Ste. Gene- and used for aggregate, road rock, well linings. Concrete and other ma- vieve Limestone at a quarry near Portland cement, agricultural lime, terials have largely supplanted Anna, about 6 mi%essouthwest of and bituminous pavement (Lamar these uses of sandstone, and current the Lick Creek Quadrangle. 1959). The Southern Illinois Stone demand for sandstone as a quarry Company operates a large quarry product is small. The only recently- Sand and Gravel just southeast of the study area and active sandstone quarry in southern Prospects for commercial sand and quarries from the Goreville, Cave Illinois is a small operation in the gravel operations in this quadrangle Hill, and Negli Creek Members of Waltersburg Quadrangle (Weibel are poor. Locally, material suitable the Kinkaid. In the Lick Creek Quad- et al. 1991) that produces flagstone for fill can be obtained from some of rangle, quarries formerly operated for walkways and decorative siding. the larger creek beds in the area. in the Cave Hill Member in the SM An abandoned sandstone quarry Some medium to coarse grained, NESE, Section 21, near the center of was observed during mapping just relatively uncemented quartz sand- EM NE, Section 29, and NW SE, Sec- east of 1-57 in the W?4 NW, Section stone of the Caseyville Formation tion 20, all in TllS, R1E. A small 25, TIIS, RlE, Thick bedded sand- has potential as a source of silica for quarry in the Goreville Member was stone from the lower Wayside Mem- manufacturing amber glass bottles in the NW SW NW, Section 25, of the ber of the Caseyville, is exposed in and as molding and sand-blasting same township. the pit. The operator, dates of opera- sand (John M. Masters, written com- The thickness and lithologic suc- tion, and uses of the stone are un- munication 19%). cession of the Kinkaid appear to be known. Proximity to 1-57 suggests consistent throughout the quad- that rock from this quarry was used rangle, but undesirable components as fill during highway construction Shale and claystone units in the include shale interbeds and chert in the 1960s. Caseyville and Tradewater Forma- nodules. The thick intervals of shale tions are a potential source of clay at the top and base of the Cave Hill Fluorspar and Base Metals resources, most likely for manufac- Member can be handled by quarry- The Lick Creek Quadrangle lies ture of red-burning fired clay prod- ing the rock in benches, as is done at northwest of the Illinois-Kentucky ucts such as common brick. Some the Southern Illinois Stone Company Fluorspar District (fig. 2). Within claystone may be valuable as liners quarry Thus, given favorable eco- the district, fluorspar occurs as vein and covers for waste disposal. If fire- nomic factors, there is good poten- deposits along faults and as bedded- clay-type underclays occur in min- tial for quarry development in the replacement deposits associated able thicknesses, they would be Kinkaid Limestone in the Lick Creek with small faults or fracture zones. usable as low-grade, high-plasticity Quadrangle. Although vein deposits occur refractory clay (Randall E. Hughes, Other limestones of the Pope along faults with upper Chesterian written communication 1994). Group, such as the Menard Limestone and Pennsylvanian wall rocks, eco- and the Cora Limestone Member of nomically minable deposits of both Coal the Clore Formation, are too thin or types are mostly confined to the Coal in the Lick Creek Quadrangle contain too many shale interbeds to interval from the St. Louis Lime- has negligible potential for commer- be of likely commercial interest. stone through the Cypress Sand- cial exploitation. No record was stone (Grogan and Bradbury 1968). found of any coal mining in the Sandstone In the Lick Creek Quadrangle, these quadrangle, nor was any evidence Large amounts of sandstone are rocks occur at depths of 400 feet or of past mining observed during available in the Lick Creek Quad- greater. mapping. The thickest coal observed in the study area is 1.1 feet thick, remaining tests in the quadrangle be present. A number of formations which is well below the minimum reached the Ste. Genevieve; the Adams below the Ste. Genevieve that have thickness for economic mining. no. 1 Walker well terminated in the yielded hydrocarbons elsewhere in Chesterian Golconda Formation. the Illinois Basin are probably pres- Petroleum The nearest oilfields are the ent here. They include the St. Louis, Nine oil- and gas-test holes have Energy and Marion fields, which Salem, and Ullin Limestones (Missis- been drilled in the quadrangle; all are about 10 miles north of the quad- sippian), Dutch Creek Sandstone were dry and abandoned (table 1). rangle in T9N, R2E, Williamson (Middle Devonian), Clear Creek A show of oil was reported in the County. Formation (Lower Devonian), and Ste. Genevieve Limestone at 1,980 to Evaluating petroleum resources Galena (Trenton)Group (Middle 1,981 feet in the Monjeb Minerals no. 1 of the Lick Creek Quadrangle is diffi- Ordovician). The New Albany Shale Throgmorton hole in Section 5, TllS, cult. No structural features that (Devonian-Mississippian), which R2E. The deepest hole drilled to date could provide traps are known, but is 50 to 100 feet thick in this area, is is the Hildreth no. 1 Houston, which deep buried structures and strati- an excellent source rock when reached a depth of 2,109 feet in the graphic traps created by up-dip within the oil maturation window Ste. Genevieve. Seven of the eight pinchouts of reservoir rocks might (Barrows and Cluff 1984). Bedrock and surficial materials of the karstification because it is soluble in springs, and fractures widened by quadrangle generally provide stable even slightly acidic water. Typical solution, occur in the Menard, Clore, conditions for construction projects. karst features are enclosed depres- and Kinkaid Formations. In the thin- A few areas, however, are known to sions (sinkholes or dolines), caves, ner limestones of the Clore, only sev- be unstable. Landslides have occur- numerous large springs, and fluted eral small sinkholes were observed, red along steep slopes underlain by rock outcrops (Ford and Williams but widened joints are common. The the Glasford Formation, and some 1989). Surface drainage is commonly largest sinkholes are found in the areas of limestone bedrock have devel- disrupted and may be subordinate Menard and Kinkaid Limestones, oped karst features. to underground drainage. Solution which contain the thickest intervals generally occurs along joints, which of limestone. Some sinkholes in the Landslides are common in southern Illinois. Kinkaid outcrop belt cover several Numerous recent landslides have Water flowing along joints dissolves acres and are more than 20 feet occurred along steep valley walls in the rock and gradually widens the deep. In several cases, younger the northern part of the report area, joint. Karstification begins in the sub- basal Pennsylvanian rocks exhibit particularly along the north side of surface and is not always evident at karst features where they have col- Grassy Creek in the S%, Section 25, the surface. Sinkholes appear only lapsed into caves that developed in TlOS, R1E. These landslides involve when the roofs of subterranean pas- the underlying Kinkaid Limestone. unlithified sediment of the Glasford sageways begin to collapse. Aquifers in karstified bedrock Formation. In the Lick Creek Quadrangle, are easily susceptible to contamina- During mapping, a house nar- karst features, including sinkholes, tion from the surface because the rowly escaped destruction in a land- slide. The house was built on Glas- ford sediments near the top of a steep slope on the north side of Grassy Creek, about 50 feet above stream level. The stream undercut the foot of the slope, triggering the landslide. The hillside below the house failed in a series of rotational slump blocks, forcing Grassy Creek to cut a new channel farther south. Gaping fissures appeared next to the foundation of the house (fig. 23), while uphill (north) of the house a graben 50 to 60 feet long and 10 to 12 feet wide was formed, damaging the driveway (fig. 24). An artificial pond just east of the house lost its water; this water possibly lubricated shear planes at the base of the land- slide, thereby assisting the slide. Numerous older landslides (possibly 10 to 50 years old) were observed in this area. Evidence for landslides includes hummocky top0 g- raphy, tilted trees, and scarps near the tops of steep slopes. Slides are most likely to occur when a creek undercuts the foot of a steep slope, especially when groundwater levels are high, the creek is high, and the toe of the slide is saturated. Karst Karst topography is created by chemi- Figure 23 Tension fissure caused by a landslide on the cal dissolution of rocks by water. north side of Grassy Creek. The creek is to the south Limestone is especially prone to (right) of the house. Figure 24 A graben created by a landslide on the north side of Grassy Creek. The view is to the east; the house to the right is the same house shown in figure 23. The scarp on the uphill side (left) apparently is the major glide plane of the landslide, whereas the scarp to the right represents an antithetic fault. The hazards of building on steep slopes underlain by the Glasford Formation are evident in this photo. bedrock is so honeycombed by large irregular bedrock surface, (2) infiltra- ping; but in nearby areas, farm passageways and karst aquifers tend tion of surface water and soil piping, ponds constructed on karst have Post to recharge more rapidly than other and (3) collapse of solution cavities their water, and sinkholes appeared types of aquifers. Rapid recharge al- (White 1988).In places, plugged in a schoolyard at Dongola (Union lows little time for physical, biologi- sinkholes have caused flooding County) in 1993 (Panno et al. 1994). cal, and chemical breakdown of problems when structures were built Solutions to karst-related construc- water-borne contaminants. below surface outflow elevations. tion problems are available, but gen- Karst areas may be unstable for No specific karst-related construc- erally are expensive (Knight 1971, construction because of (1)differen- tion problems were observed in the Sowers 1984, Wilson and Beck 1988, tial compaction of soil overlying an Lick Creek Quadrangle during map- Destephen and Wargo 1992). Abegg, F.E., 1986, Carbonate petrol- Buschbach, T.C., and D.R. Kolata, sippian Sequences of Southern ogy paleoecology and deposi- 1991, Regional setting of Illinois Illinois: Thirty-Seventh Annual tional environments of the Clore Basin, in M.W. Leighton, D.R. 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