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APPLICATION OF HIGH RESOLUTION SEQUENCE STRATIGRAPHY TO TIDALLY INFLUENCED UPPER MISSISSIPPIAN CARBONATES ILLINOIS BASIN

LANGHORNE B SMITH JR

Miami 4600 Rickenbacker Causeway Miami Florida 33149 Comparative Sedimelllology Laboratory University of AND

J FRED READ

24061 Department ofGeological Sciences Virginia Tech Blacksburg Virginia

Genevieve and Paoli Formations of the Illinois basin are composed of five carbonate and ABSTRACT The Upper Mississippian Chesterian Ste sections based on detailed measured sections of 57 mixed carbonate siliciclastic fourth order 100500 k y sequences Interpretive cross closely carbonate and siliciclastic horizonsand distinctive marker beds can be correlated spaced outcrops and cores show that sequence bounding paleosol of as as nine parasequences basin wide within the available biostratigraphic framework Each sequence is composed many regionally developed ooid tidal and skeletal bank carbonate eolianites at the base overlain discontinuous ridge Carbonate parasequences have patchy updip by laterally siliciclastic of skeletal limestone fos facies and laterally extensive muddy carbonate caps Mixed carbonate parasequences are composed capped by siliferous shale Carbonate tidal flat facies are rare in the succession

sea whereas the were fourth order 500 k eustatic level changes parasequences The sequences produced by moderate amplitude 100 y glacio transition from the conditions of the 100 k eustatic sea level atime of greenhouse were likely produced by fifth order 10 y glacio changes during conditions of the late Paleozoic This transition is reflected in from carbonate dominated dis Early Mississippian to the icehouse upward change lowstand erosion at the lowstand erosion at thebase to mixed carbonate clastic sequences with significant conformity bounded sequences with little cou These were caused an increase in the magnitude of sea level fluctuations top of the study interval and in overlying sequences changes likely by climate The be stacked into one or two third order 0 5 5 m y composite sequences pled with increasingly humid wet dry seasonal sequences may of lhe fourth order makes third order less that are bounded by relatively well developed unconformities However the magnitude signal bundling fourth and fifth order sea level fluctuations The dominance of fourth clear than in strata deposited during greenhouse times of lower amplitude flat facies reflect moderate associated with the transition order disconformity bounded sequences and the lack of regional tidal amplitude eustasy ice in thelate Paleozoic from global greenhouse climates of the Early Mississippian to times of abundant global

INTRODUCTION km of the eastern southern and western outcrop belts of the Illinois basin The cross sections show that despite the lateral work on the lower Chesterian Ste Genevieve to Previous heterogeneity of much of the stratigraphy several sequence in the Paoli Formations Illinois basin includes regional surface over much of the bounding paleosol horizons can be correlated and subsurface of limestone sandstone and shale for mapping basin within a framework of biostratigraphic and lithologic Butts Weller and Sutton 1940 Swann and a mations by 1917 markers Smith and Read 1995 Smith et 1995 The pale Atherton McFarlan et al 1955 Swann 1963 1964 that make it 1948 osols provide additional lithologic markers possible Potter 1962 Sable and Dever 1990 and Droste and to correlate parasequences within the sequences The cross sec local 1990 and detailed sedimentologic studies by to the Carpenter tions provide an opportunity better understand relative and Choquette and Steinen 1980 Cluff and to test Kissling 1967 effects of eustasy tectonics and tides sequence Lineback Liebold 1982 1991 and Dodd et 1981 Merkley stratigraphic concepts on carbonate and mixed carbonate a others of the ooid among The lateral heterogeneity on a 1996 siliciclastic sequences deposited updip geritly dipping reservoirs has made the Ste Genevieve a correlation into the grainstone ramp This study also provides insight stratigraphic sig in the subsurface 1993 Most the nightmare Zuppann paleosols nature of the transition from global greenhouse conditions of and have as a were considered to be local in extent to formed in the Early Mississippian to times of abundant global ice of local island Droste and 1990 result shoaling Carpenter Pennsylvanian and Early Permian Recent work has shown that some sequences and parasequences bounded by paleosols and eolianite horizons can be correlated a GEOLOGIC SETTING both locally and regionally Smith et 1995 Smith and Read 1995 Smith 1996 Dodd et aI 1996 Tectonic and Paleogeographic Setting of This paper demonstrates the value combining detailed of sedimentology with a basin wide stratigraphic approach Only The Illinois basin was located between 50 and 150 south all and through sedimentologic study of rock types exposure the equator during the Late Mississippian Craig and Connor be surfaces can the sequence stratigraphy accurately interpreted 1979 Scotese and McKerrow 1990 Fig lA Throughout and only through basin wide stratigraphic study can local fea much of the Paleozoic the basin was an embayment open to the extensive marker horizons tures be distinguished from laterally present day south which covered southern Illinois southwest surfaces Detailed of The was of and genetically significant lithologic logs ernIndiana and western Kentucky embayment part used to construct that was continuous from 57 outcrops and cores were regional lithologic an extensive carbonate ramp and the Paoli cross sections of the Ste Genevieve Formation Pennsylvania to western Canada Craig and Connor 1979 and its time units more than 600 of Formation equivalent along Fig 1 A The ramp was separated from the Antler foredeep

Publication No 63 Advances in Carbonate Sequence Stratigraphy Application to Reservoirs Outcrops and Models SEPM Special ror ISBN 1 565760603 p 107 126 Copyright il1999 SEPM Society Sedimentary Geolngy 108 LANGHORNE B SMITH JR AND 1 FRED READ

A B

ILLINOIS INDIANA

v f v f

O v

11 I MISSOURI

r I I Jf 100 MILES TENNESSEE

SHALLOW MARINE DEEP MARINE

FIG l A map of the Illinois basin modified from and Connor 1979 Paleogeographic showing regional setting Craig B Tectonic map of Illinois basin Isopachs in feet forthe interval from the Bethel to the MississippianPennsylvanian boundary from Swann 1963 800 ft isopach is approximate boundary of basin interior Faults Wabash fault WV Creek Valley system Rough Shawneetown fault system RCS Fluorspar District fault complex FD

the western United States by the Transcontinental arch which was emergent throughout the Chesterian Craig and Connor z TAR SPRINGS 1979 The Illinois basin lay at least 300 km updip from the z Z GLEN DEAN ramp that may have started to 0 zen margin develop along the Z II 0 Ouachita to the south W II i foredeep en c 0 HARDINSBURG The Illinois basin can be subdivided into en5 three main o the belt eastern W provinces along outcrop the shelf basin lL HANEY interior and the western shelf Fig IB The term shelf is used by local geologists to distinguish areas of lower subsidence Z 1 BIG CLlFTY rates from the more rapidly subsiding basin interior The eastern a shelf the western flank of W BEECH CREEK formed along the Cincinnati arch and l the western shelf formed over t CYPRESS the DuQuoin monocline The W J I basin interior appears to be centered on the Wabash Valley and 0 REELSVILLE Z lwOcr district fault systems that trend northeast and 1 Fluorspar may 1 SAMPLE ii en have been active during the Late the BEND Mississippian Despite c BEAVER subsidence rates facies BETHEL varying that en interpretations suggest to U PAOLV shallow marine nonmarine conditions prevailed throughout en RENAULT the Illinois basin the and U SALEM during early middle Chesterian i l w a w w D Stratigraphic Setting w FT PAYNE z w CJ The Ste Genevieve and Paoli lie at the Cl Formations top of a ui l thick Middle succession that I Mississippian carbonate includes en the Osagean to Meramecian Muldraugh Warsaw Salem and St Louis Formations Cluff and Lineback 1981 Fig 2 The St KIN BLACK J SHALES ST LOUIS Louis Formation directly underlies the study interval Figs 2 3 and is primarily composed of shallow water muddy carbonates and skeletal limestone Cluff and Lineback 1981 The base of the Ste Genevieve is picked at a biostratigraphic zone boundary FIG 2 Left column is a generalized stratigraphic column for the that coincides a in the Illinois basin with regional disconformity that Mississippian Right column shows more detailed stratigra commonly of lower to middle Chesterian units occurs within a carbonate unit the Lost phy This paper concentrates on the Ste muddy overlying River Genevieve to Paoli interval For Chert of Elrod In explanation of patterns of units see Figure 4 1899 outcrops and cores the Lost River HIGH RESOLUTION SEQUENCE STRATIGRAPHY OF UPPER MISSISSIPPIAN CARBONATES 109

zone the base of the Tafarocrinus zone C KENTUCKY and Strata above the Pfatycrinites penicillus zone and below the Bethel Sandstone Renault Shetlerville Yankeetown Downeys i HARDINSBURG SST j Bluff and Paoli Formations will be referred to as the Paoli HANEY LST interval in this the eastern belt the Paoli I t BIG CLlFTY SST paper Along outcrop 3 is shallow water carbonates sim 16s interval primarily composed of ilar to those in the Ste Genevieve In the basin interior the Paoli Z interval is ofskeletal limestone and fossiliferous dark Il composed FM shallow water 3 GIAK1N gray shales and on the western shelf of lime f3 sandstone which en J stones fossiliferous shale and quartz suggests en i PAOLI that the clastic source remained to the northwest Potter 1962 LST I The Paoli is capped by a regional disconformity and is generally 16i t 3 overlain the Bethel Sandstone In the southeastern part of the 3 by basin the Bethel Sandstone pinches out and the Paoli is 330 H included in the Girkin Limestone The Girkin Limestone includes the Paoli Beaver Bend Reelsville and Beech Creek ST LOUIS LST ffi 15 Limestones each separated by well developed carbonate pale osol horizons The Paoli interval is overlain by middle and FIG 3 Biostratigraphy and correlation chart for Ste Genevieve to Glen upper Chesterian mixed carbonate clastic sequences Swann Dean interval modified from Sable and Dever 1990 and Maples and Waters 1987 MER Meramecian SST sandstone LST limestone Fm formation 1963 1964 Smith 1996

Chert is a bed that occurs in the of distinctive marker upper part CONSTRUCTION OF LITHOFACIES CROSS SECTIONS fen a laterally extensive grainstone unit in which the outlines of estrate bryozoans are commonly preserved within chert nodules Cross sections through the study interval have been con Conodont foraminifer and coral biostratigraphic zone bound structed on the basis of closely spaced measured sections ofcore Each core and bed aries occur at this unconformity Rexroad and Fraunfelter and outcrop Fig 4 outcrop was logged by 1977 Maples and Waters 1987 moved the bed and the thickness color grain size type and shape deposi Meramecian Chesterian provincial series boundary to this tional texture biota sedimentary structures and evidence for unconformity because the fauna above the boundary more subaerial exposure were noted for each unit In outcrop units where closely resembles the fauna in the middle and upper Chesterian were traced laterally to determine facies relationships than the fauna in the underlying St Louis Formation Thus age possible The Ste Genevieve cross sections AA and of the Ste Genevieve to Paoli interval is early Chesterian or late BB Fig 4 are hung on the disconformity that coincides with the Visean middle V3b to early V3c the top of the Pfatycrinites penicillus zone and Bryantsville The Ste Genevieve Formation Fig 3 is primarily com Breccia Bed in Indiana and western Kentucky The overlying 4 have been on posed of ooid grainstone a common reservoir facies skeletal Paoli cross sections C C and DD Fig hung grainstone commonly dolomitized muddy carbonates and the disconformity at the top of the interval except where pre the section numerous disconformities that can be recognized by the pres Bethel erosion occurred In these locations cross the ence of caliche breccia and eolianites The boundary between was hung on a regional disconformity I within Paoli and Aux Vases made marker beds such the middle and upper Ste Genevieve the Correlations were by using distinctive and Sandstone in the western part of the basin was thought to be gra as the Lost River Chert Bed numerous paleosol horizons dational Cluff and Lineback 1981 but has recently been inter laterally extensive muddy carbonate and shale units preted to be primarily erosional Leetaru 1997 The source of Parasequences have been numbered to help describe the the Aux Vases Sandstone lay to the northwest the formation is cross sections We are not suggesting that this numbering sys it on composed of quartz sandstone flaser wavy and lenticular tem be adopted by others because is based interpretive bedded sandstone and shale and slickensided mudrock and cross sections and subject to change with the addition of new caliche paleosols beneath disconformities The Rosiclare data For clarity measured sections have been equally spaced on Tongue of the Aux Vases extends east into western Kentucky the cross sections except in areas of major changes in thickness where are and separates the lower Ste Genevieve from the overlying or larger than usual gaps between sections they Levias Member of the Renault Formation The Levias Member spaced farther apart Actual distances between sections can be contains the crinoid Pfatycrinites penicillus and is time determined from the location maps Fig 4 equivalent to the uppermost Ste Genevieve Formation in and Indiana Swann 1963 The Ste Genevieve Kentucky LITHOFACIES AND DEPOSITIONAL ENVIRONMENTS Formation and the Levias Member of the Renault Formation are the capped by a regional disconformity called Bryantsville Characteristics ofmajor rock types are summarized in Table 1 This Breccia Bed in Indiana and Kentucky Mallot 1952 The relative abundance of facies at each location Fig 5 field boundary coincides with the top of the Platycrinites penicillus observations and subsurface data from the literature Choquette 110 LANGHORNE B SMITH JR AND J FRED READ

WEST

WESTERN SHELF BASIN INTERIOR

C ILLINOIS I KENTUCKY 2 130 km 4 65 km 8 10 12 13 14 15 18 21 23 24 25 26

l X

I Jt STE GENEV EVE

A ILLINOIS KENTUCKY 1 2 4 5 6 7 8 10 12 13 14 16 17 18 21 22 23 25 26

FIG 4 cross sections of I 5 in the Ste Genevieve Interpretive sequences through to Paoli interval Measured sections are equally spaced except where there are between sections see location for actual horizontal Disconformities major gaps maps spacing are lettered from A to J and parasequences are numbered from I to 25 The Bethel channel is not drawn to scale its actual is 75 et al 1969 depth m Friberg Cross sectionAA includes the Ste Genevieve and trends west to east from location I to location 35 and south to north from location 35 to location 75 Cross section BB shares location 35 and tr nds south to north parallel and downdip of cross sectionAA Cross section C C trends west to east from location I to location 33 and south to north from location 33 to location 74 Cross section DD shares location 33 and trends south to north and down of cross section CoC o parallel dip MFS maximum flooding surface GRST grainstone PKST packstone MDST mudstone WKST wackestone LST limestone III HIGH RESOLUTION SEQUENCE STRATIGRAPHYOF UPPER MISSISSIPPIAN CARBONATES

EAST SOUTH NORTH

SOUTHEASTERN SHELF NORTHEASTERN SHELF C INDIANA

56 57 62 64 65 68 70 71 74 29 33 37 38 41 43 47 49 50 51 52

0 KENTUCKY INDIANA 0

3 42 44 45 46 48 57 63 67 69 73 BETHELl13 x x tx 17 9 5 1 v I i r w 0 45 w STE GENEVIEVE 1Il

INDIANA A KENTUCKY

62 64 65 68 70 71 74 75 30 34 35 36 38 41 43 47 49 50 51 52 56 57

1Il w CJ 2z W l di 1Il

MUDROCK CALICHE BRECCIA 1T PALEOSOL

EROSION SURFACE w

PARASEQUENCE BOUNDARY w 100 ft m z w QUARTZ PELOID GRST PKST EOLIANITE REGOLITH ui I 1Il COAL SWAMP

SHALE NONFOSSILIFEROUS o 0 SUPRATIDAL SALT MARSH

130 HETEROLITHIC SST SHALE TIDAL FLAT

QUARTZ SANDSTONE W TIDAL RIDGE CHANNEL FILL

FOSSILIFEROUS SHALE D BACK BANK

LIME MOST WKST PELLETAL D LST DOLOMITE LAGOON

0010 GRAINSTONE SHOAL

SKELETAL GRAINSTONE SHOAL BANK

CHERT

INTRACLAST

@ SEISMITE Il2 LANGHORNE B SMITH JR AND J FRED READ

BRECCIA CALICHE QUARTZ PELOID GRST MUDDY CARBONATES

FIG 6Schematic depositional environment for carbonate dominated ramp in theSte Genevieve Formation not to scale SeeFigure 4 forlegend and rock types

Ettensohn et aI 1988 Ambers and Petzold 1992 The overall upward increase in siliciclastic sedimentation up through the study interval is related to the source area s becoming more humid with time Increased influx of shale into the basin in sequences 3 and 4 coincides with a decrease in ooid production in the basin possibly related to increased fresh water influx from rivers to the northwest The trend of increasingly humid wet dry the seasonality continued into overlying sequences which have more siliciclastics as well as thin coal beds Smith 1996

FIG 5 Facies distribution on the ramp based on percentage of rock type at each location Curves Carbonate Dominated smoothed by using three point average A Ste Ramp Genevieve facies distribution sequences 1 and 2 B Paoli interval facies dis The Ste Genevieve Formation and most of the interval tribution sequences 3 and 4 Paoli of central Kentucky and southeastern Indiana were deposited on a carbonate dominated part of the ramp Fig 6 facies summa and Steinen 1980 Cluff and Lineback 1981 and Zuppann rized in Table 1 Keith 1988 were used to determine relative facies distribution and depositional environments for carbonate dominated and Skeletal grainstone and packstone mixed carbonate siliciclastic parts of the ramp Fig 6 The Skeletal and 7A formed in ramp slope was very gentle average 15 cmkm 0 0010 for the grainstone packstone Fig moderate to energy conditions on the basis of the lack of basin and no more than 5 cmkm 0 0030 along the margins of high mud the medium to coarse size and the abundance the shelves Smith 1996which accounts for the similarity of very grain of echinoderms In this skeletal formed land facies deposited in the central and eastern parts of the basin in setting grainstone ward in between and seaward of ooid shoals in water the Ste Genevieve Formation Smith 1996 Although the depths that exceeded 10 m Smith 1996 facies on the eastern shelf and the basin interior are different in rarely sequences 4 and 5 this variation is primarily due to the north Ooid western location of the clastic source rather than a change in grainstone ramp slope This reservoir facies Fig 7B formed in a high energy Increasingly humid wet dry seasonality prevailed throughout shallow marine setting where strong tidal currents shaped tidal the Ste to interval oriented to the and Genevieve Paoli as indicated by the presence ridges subparallel paleoslope Choquette of caliche breccia and red slickensided mudrock paleosols Steinen 1980 and locally cut tidal channels into underlying strata Evaporites which are common in the underlying St Louis Ooid grainstone is widespread in the Ste Genevieve with the Formation are absent in the Ste Genevieve to Paoli interval thickest accumulations in the basin interior but largely confined to the eastern shelf in the Paoli which suggests that the climate became more humid in the early interval Chesterian The duration of the wet season must have been rela short Ste tively during Genevieve time on the basis of the abun Tidal influence on grainstone units dance of ooids dolomite and eolianites all of which are most tidal Strong influence on the gently sloping ramp caused common in areas with arid and semiarid climates Witzke 1990 much lateral heterogeneity of facies Ooid grainstone reservoir TABLE1.--CARBONATE AND MIXED CARBONATE-CLASTIC RAMP FACIES

Lithology Blocky mudrock Quartz-peloid Muddy carbonates Ooid grainstone Skeletal grain- Quartz sandstone Fossiliferous Shale (Depositional and calichelbrec- grainstone (lagoon and (tidal bar and stone and pack- (tidal sand ridge, (carbonate-clastic Environment) cia (paleosol) (eolianite) intershoal) shoal) stone (hank, shoal) channel fill) transition)

Occurrence Common throughout Dune-forms; units Commonly occur as Dip-parallel oolitic Common throughout Commonly fills Common throughout basin, better commonly thicken regional, traceable bar-forms (Zuppann, basin in all limestone incised valleys and basin. Transition developed on shelves. and thin over short sheets capping 1993); commonly units. Forms sheet- forms in linear sand between siliciclastic Commonly underlies distances; underlie parsequences. Also occur at base of like units at base of ridges. and carbonate rock and overlies marginal and overlie discon- lagoons and local inter- parasequences in Ste. most regressive types. marine shale with formities at tops and shoal swale-fills. Genevieve and Paoli parasequences. plant fragments. bases of sequences, of eastern shelf. respectively.

Color Caliche is light Dark gray. Dolomitized units are Wlute to light gray. Light to medium to White to light Olive green and dark brown; Breccia zones tan; limestone units dark gray. graylgreen. Day are dark gray; light gray brown to Mudrock is red and dark gray. maroon.

Depositional Caliche is sb-ingy to Grainstone; fine to Mudstone and Grainstone. rare pack- Grainstone and Very-fine to medium- Wackestone/fissile texture and grain laminated micrite. medium, tightly wackestone; stone; radial and con- packstone with up to grained, subangular, shale; whole type Breccia has fined fab- packed and well predominantly centric, fme- to medi- 15% shale. Medium to well-sorted; may have brachiopods and ric. Mudrock is sorted within composed dolomitic um-grained ooids with very coarse grained. up to 15% shale. bryozoans. blocky, brecciated, laminae; dominated or lime mud and variable amounts of slickensided clay by peloids, rounded 20-100 Lm pellets; skeletal grains; ooid w/dolomitic nodules, lithoclasts, subangular common whole thin- nuclei include skeletal quartz; lesser ooids shelled fossils. grains, lithoclasts, (whole and broken), quartz and peloids. echinoderm grains.

Bedding and Mudrock occurs in Millimeter-scale Massive to burrowed, Cross-bedded, less Thick-bedded, Cross-bedded, flat- Fissile, flat-bedded. sedimentary breccia and calichified inverse-graded rare fenestrae, commonly thick massive and cross- bedded and massive structures zones up to three laminations form laminations, and mud- bedded and massive; bedded. bedded, flaser- meters thick. Massive cross-beds that dip cracks. foresets dip as much bedding common. beds up to one meter 40%; cross-beds dip as 25%. hick; rooting and multidirectionally but reduction halos com- dominantly to the mon. north (Hunter, 1993). Terrigenous Average 15% very Green shale, quartz Quartz grains form Quartz sand and silt clastics admixed fine quartz sand on silt and quartz sand nuclei of ooids above are rare; thin green or interbedded eastern shelf; up to common. some quartz sandstone and gray shale beds 75% quartz sand in units. and stringers are basin interior and common. western shelf. ------Biota Abraded, rounded Lagoonal facies: Echinoderm and Abundant Rare echinoderm frag- Bryozoans, skeletal grains ostracodes and brachiopod fragments echinoderms, menls, could be trans- brachiopods and common. gastropods; Intershod common. brachiopods, ported or eroded from echinoderms. swales: bryozoans, bryozoans, common underlying limestone. brachiopods and mollusks and echinoderms. foraminifera. 114 LANGHORNE B SMITH JR AND J FRED READ

FIG 7 Photomicrographs of important rock types A skeletal grainstone B ooid grainstone C microcrystalline dolomite D quartz peloid grainstone eolianite E caliche F breccia Scale on A represents 0 25 mm and is same for all photographs facies thicken thin and pinch out into skeletal grainstone and basin were a mosaic ofooid ridges and skeletal grainstone sheets muddy carbonates and reappear along the same horizon Facies differentiation was due to local tidal rather than water energy Muddy carbonates or on the If the had depth regional position ramp ramp slopes These have been interpreted as low energy subtidal lagoon been steeper or if the ramp had been wave dominated then facies Choquette and Steinen 1980 as open shelf facies strike facies belts would have formed The parallel dip parallel formed seaward of ooid and skeletal grainstone Dodd et a orientation of the tidal sand focused and increased the ridges 1996 and as facies formed both landward and seaward of the of the tidal currents which have allowed velocity may synchro ooid shoals Cluff and Lineback 1981 On the basis of the nous ooid formation over a area The lack of a continuous large fauna grain size regional distribution and stratigraphic rela barrier allowed open marine such as echinoderms to organisms tionships it is likely that most muddy carbonates formed in 10w live landward of and between ooid shoals times of During energy environments updip of the ooid shoals but also filled maximum tidal influence the central and eastern of the parts topography in swales and channels between and in front of CARBONATES 115 HIGH RESOLUTION SEQUENCE STRATIGRAPHY OF UPPER MISSISSIPPIAN

shoals Open marine biota especially echinoderms in some Skeletal grainstone andpackstone Where with siliciclastics skeletal and units indicate that some muddy carbonates formed in waters associated grainstone in a more distal environment with normal salinity whereas dolomitized ostracode bearing packstone likely formed deeper in the Ste on the basis of the lack of cross mudstone and wackestone Fig 7C likely formed in more than Genevieve lack ooids of beds saline restricted settings Close association of these facies sug bedding of and common presence graded that storm influence Skeletal and gests that waters in lagoons and intershoal swales fluctuated suggest grainstone packstone of into fossiliferous shale that a from open marine to restricted The lack laminites suggests grade laterally represents gradation carbonate and siliciclastic environments that microbial matcovered carbonate tidal flats were rare between despite the arid Late Mississippian climate Fossiliferous shale This with muddy carbon Quartz peloid grainstone rock type commonly interfingers east ates to the east and into influenced het This rock type Fig 7D is most common on the central grades laterally tidally of the east interlaminated sandstone and shale toward the ernshelf in the Ste Genevieve and on the south part erolithic source The heterolithic facies formed ern shelf in the Paoli interval but also occurs beneath northwestern siliciclastic tidal flats and in the zone seaward of disconformities in the basin interior The cross bedded quartz both on transition quartz peloid grainstone units are eolianites on the basis of their sandstone inverse grading sorting rhizoliths rounded broken ooids lack with of fossils or coarse grains and close association carbonate Quartz sandstone paleosols Merkley 1991 Hunter 1993 Dodd et aI 1993 Quartz sandstone was deposited in a tide dominated shal Some subhorizontally laminated quartz peloid grainstone with low marine environment on the basis of abundant channel form be and coarse grained fossiliferous laminae may beach facies structures with tidal fills bidirectional cross bedding sand Quartz peloid grainstone eolianites have also been reported in ridges oriented parallel to the paleoslope Seyler 1986 Cole time equivalent strata in Kansas Abegg 1994 eastern 1990 Huff 1993 Although they are somewhat smaller the Kentucky and West Virginia AI Tawil and Read 1996 sand ridges resemble those found in tide dominated environ or is Quartz peloid grainstone commonly overlies capped by ments such as the North Sea Off 1963 Huff 1993 Quartz caliche and breccia and occurs in beds that are as much as 6 m sandstone with conglomerate beds also commonly fills channels distances thick and that thicken and thin over short scoured by strong tidal currents

Carbonate paleosols Paleosols Quartz peloid packstone caliche and breccia are paleosols On the mixed carbonate siliciclastic ramp paleosols are that formed during subaerial exposure of carbonate rocks in a most commonly blocky slickensided mudrock that formed from Late also seasonally wet dry climate In the early stages of clay on exposed shale beds but caliche and breccia are red Mississippian carbonate paleosol development quartz peloid common exposure features on quartz sandstone The green when sand and ooids are root packstone formed eolian peloids quartz or dark gray mudrock paleosols brecciated disrupted accumulated along with clay carried by wind or sheetwash and commonly have brecciated carbonate nodules and tepee Some lithoclasts eroded from underlying carbonates were trans structures Smith 1996 ported and deposited in swales between eolian dunes and on Hunter lithoclasts be in situ exposure surfaces 1993 other may calcrete ooids or Relative Ranking ofDisconformities pedogenic concretions of caliche analogous to Read 1974 With continued exposure caliche coated pisolites Disconformities lettered from A to J oldest to youngest on and fine carbonate were to interstitial grained precipitated terms grains cross sections can be crudely ranked in of the relative With time form gray brown quartz peloid packstone paleosols duration of exposure estimated from the relative abundance of 7E lined the sediments were cemented and laminar caliche Fig the exposure features Fig 8 From immature to most mature vertical fractures and In the most mature joints bedding planes are and exposure features I eolianite 2 dirty packstone carbonates were brecciated Fig 7F and lam profiles exposed minor caliche 3 thick laminar caliche extending deep beneath inar caliche crusts and of caliche formed as subhorizontallayers the surface and 4 brecciated or karst weathered limestone 4 the surface and much as m below along joints bedding are exposed Blocky slickensided mudrock paleosols and incised valleys Walls et aI 1975 Ettensohn 1975 Harrison and planes treated separately because they are difficult to rank relative to Steinen 1978 Ettensohn et aI 1988 other features that indicate carbonate exposure Disconformities Hand J on which the cross sections are

are the best and the longest Mixed Carbonate Siliciclastic Ramp hung developed likely represent H period of emergence major disconformities Disconformity The Aux Vases Formation and the Paoli interval of Illinois has the highest occurrence of caliche and breccia and there is western Kentucky and western and central Indiana were major incision associated with Disconformity J Although depth deposited on a mixed carbonate siliciclastic part of the ramp of incision is a better measure of sea level fall than of duration have taken a oftime Smith 1996 of exposure it would relatively long period 116 LANGHORNE B SMITH JR AND J FRED READ

OF SECTIONS WITH OF SECTIONS they were deposited hundreds of kilometers updip from the shelf FEATURE PRESENT WI EXPOSURE BIOSTRAT In this in which lowstand tracts are 0 20 40 60 80 EVIDENCE BOUNDARY RANK edge updip setting systems II I absent and are represented only by unconformities it is difficult I 100 to sets and and J I NO MAJOR recognize parasequence transgressive highstand I systems tracts or entire sequences may be composed of as few I as one are called in MAJOR parasequence Stratigraphic units sequences I 100 NO INTERMEDIATE this if have maximum and are I study they flooding surfaces I bounded by regionally extensive disconformities On the basis H 100 YES MAJOR of this definition there are five disconformity bounded sequences in the Ste Genevieve to Paoli interval that are each

composed of as many as nine parasequences G 93 NO INTERMEDIATE A parasequence is defined as a relatively conformable suc cession of genetically related beds and bedsets bounded by F 96 NO INTERMEDIATE marine flooding surfaces and their correlative surfaces Mitchum and Van Wagoner 1991 Most parasequences in the study interval can be traced across the eastern shelf and into the E 66 NO MINOR basin interior within a framework of disconformities and later

ally extensive marker beds Some parasequences are confined to D 74 NO MINOR local topographic lows and form multilateral discontinuous units especially beneath sequence boundaries Parasequences are 1 to 8 m on the eastern shelf C 70 NO MINOR thick where some parase quences are capped by disconformities and 4 to 12 m thick in the basin where are 16 NO interior conformable B MINOR they generally Typical parasequences consist of from base to top I a dis MAJOR and or 2 devel 41 conformity marine flooding surface YES INTERMEDIATE locally oped muddy carbonates and or quartz peloid grainstone eolianite 3 laterally discontinuous ooid grainstone ridges FIG 8 Relative of disconformities based on ranking percentage of loca and channel fills that overlie underlie and tions measured with breccia pass laterally into B caliche C dirty packstone P eolianites E skeletal and 4 and slickensided mudrock M Incision grainstone sheets banks extensive section I only occurs on the upper laterally carbonate most and is a better of or fossiliferous units 5 devel boundary measure how far sea level fell rather than the muddy shale locally duration of Disconformities exposure that coincide with biostratigraphic oped quartz peloid grainstone eolianite units and 6 a dis boundaries term may represent relatively long exposure conformity and or marine flooding surface The facies within sequences 1 through 5 vary from the western shelf to the basin to incise a more than 75 m valley through underlying carbonate interior to the eastern shelf and are discussed individually to strata Disconformity A may also represent a major hiatus illustrate their differences and similarities because it shows evidence for a major biostratigraphic break but paleosols are poorly developed or absent at this horizon I Exposure surfaces F G I and J can be traced into sections in the Sequence more rapidly subsiding basin interior and therefore represent Sequence 1 is bounded at the base by disconformity A and at periods of widespread emergence but the lesser development of the top by disconformity F It includes the Fredonia Member and caliche and breccia the suggests that duration may not have been the lowerMcCloskey oolite reservoirs of the Ste Genevieve and as long intermediate disconformities Disconformities B C D the lower half of the Aux Vases Formation on the western shelf and E can only be traced along the eastern and western shelves and it is capped by the Spar Mountain Member of the Aux Vases and are marked predominantly by eolianites and dirty packstone in the basin interior Sequence 1 is 27 m thick on the western and therefore are minor disconformities that paleosols represent to shelf thickens 63 m in the basin interior thins to 20 m near relatively short periods of exposure the Cincinnati arch and 9 m on the northern part ofeastern shelf On the updip parts of the eastern shelf A A the lower SEQUENCE STRATIGRAPHY boundary is picked at an undulose surface in a dolomite unit overlying the Lost River Chert Bed that coincides with a major A is defined as a related succession sequence genetically of biostratigraphic zone boundary at the St Louis Ste Genevieve strata lacking apparent internal unconformities and of contact composed Rexroad and Fraunfelter 1977 Maples and Waters parasequences and sets in tracts parasequence arranged systems 1987 Merkley 1991 Dodd et aI 1996 Caliche and eolianites and bounded by unconformities or their correlative conformities mark the boundary in the basin interior and the downdip sec Mitchum and Van 1991 It is notpossible to meet all Wagoner tions of the eastern shelf cross section BB Well developed ofthese criteria with the bounded units disconformity preserved breccia and conglomerate have been reported at the basal in the Upper strata of the Illinois basin Mississippian because boundary in Missouri and in the Appalachian basin Weller and HIGH RESOLUTION SEQUENCE STRATIGRAPHY OF UPPER MISSISSIPPIAN CARBONATES II

Sutton 1940 AI Tawil and Read 1996 Although it appears Sequence 2 that there was topography on the Lost River Chert on cross sec 2 is bounded at the base by disconformity F and at tion AA on the northern part of the eastern shelf the cross sec Sequence the top disconformity H It is composed of the Karnak and tion is composed of locations that are on either side of the hinge by Joppa Members of the Ste Genevieve and the Rosiclare of a northwest trending structural high that caused thinning of Member of the Aux Vases Sequence 2 is 16 m thick on the west as much as 16 mover 35 km in the basal part of sequence I see ern shelf thickens to 30 m in the basin interior and thins to 13 location map Fig 4 Locations 29 35 36 and 4046 were on to 15 m on the eastern shelf Sequence 2 is composed of tidally the structural high and sections 26 32 33 37 38 and probably influenced siliciclastics on the western shelfthat cannot be sub 39 were on the more rapidly subsiding basinward side of the divided without a more extensive data set hinge This structure parallels the northwest trending part ofthe Disconformity F is an intermediate rank paleosol that com Cincinnati arch and the Lasalle anticlinal belt Fig IB monly overlies eolian facies in the basin interior and underlies The transgressive systems tract TST of sequence 1 is com eolianites on the eastern shelf Fig 8 The TST of sequence 2 posed offouronlapping parasequences 14 Fig 4 Parasequences consists of parasequence 10 that is composed of patchy eolian 1 and 2 are thin regional skeletal grainstone muddy carbonate ites and grainstone capped by a l lO m thick muddy carbonate parasequences that onlap the margin of the eastern shelf and are unit that can be correlated over most of the basin interior and present only in the basin interior Parasequences 3 and 4 are well eastern shelf The MFS is picked at the base of parasequence 11 defined ooid grainstone muddy carbonate units in the downdip because it was the first laterally extensive grainstone unit to be sections of the eastern shelf cross section BB that onlap the deposited on the eastern shelf The HST is composed of five structural high in the northeastern part of the basin In the basin parasequences 11 15 Parasequences II and 12 are generally interior it is difficult to correlate these parasequences because conformable grainstone muddy carbonate units that can be cor they are commonly amalgamated in thick ooid grainstone and related across most of the basin interior and eastern shelf In muddy carbonate deposits locations 17 22 and 26 The maxi many sections on the eastern shelf the absence of the muddy mum flooding surface MFS is picked at the base of the grain cap to parasequence 11 suggests either nondeposition or erosion stone unit in parasequence 5 because it is the first laterally at the base of parasequence 12 Parasequence 13 which under extensive grainstone to be deposited on the structural high in the lies disconformity GG consists of multilateral grainstone units northeastern part of the basin and is laterally discontinuous across the basin The HST is The highstand systems tract HST is composed of five 14 a bounded can capped by parasequence disconformity parase throughgoing parasequences 5 9 Parasequence 5 be corre quence of influenced siliciclastics and multi lated across the eastern shelf but is difficult to correlate in parts composed tidally ple local disconformities the HST is only present in the basin of the basin interior because it is amalgamated with parase interior and is capped by a well developed unconformity dis quences 3 and 4 in sections 17 22 and 26 and correlates later The contact between the Aux Vases and Ste at conformity G ally with two parasequences locations 5 12 and 14 Genevieve is commonly erosional near the top of this sequence Parasequences 5 6 7 and 9 are capped by offlapping disconfor and has also been picked as a sequence boundary Leetaru mities on the eastern shelf and are primarily composed of muddy 1997 However the fact that the regional disconformity can carbonates and eolianites These HST parasequences are con be traced the siliciclastic unit suggests that any formable in much of the basin interior and are locally amalga again through erosion occurred tidal scour in the late of the highstand mated into thick ooid grainstone units locations 5 and 12 by part rather than during sea level lowstand Parasequence 9 which underlies the sequence boundary consists ofthin multilateral grainstone units confined to local lows on the eastern shelf and is by an eolianite in the basin interior capped Sequence 3 The eolianite which is the Spar Mountain Member of the Ste Genevieve passes westward into marine siliciclastics that pro Sequence 3 is bounded at the base by disconformity G and graded east at the top of the sequence Swann 1964 On the at the top by disconformity H This sequence is composed of a western shelf the HST is composed of siliciclastic parase single disconformity bounded parasequence at the top of the quences bounded by four paleosols that may correlate with the Ste Genevieve Formation in Kentucky and Indiana and the four regional disconformities on the eastern shelf disconformi Levias Member of the Renault Formation in Illinois The lower ties C to F The sequence is bounded at the top by disconformity boundary disconformity G is a well developed basin wide F Leetaru 1997 mapped an erosional contact with as much as paleosol that caps siliciclastics of the Rosiclare Tongue of the 24 m of relief at the contact between the siliciclastics of the Aux Aux Vases Sequence 3 is predominantly composed of grain Vases and the carbonates of the Ste Genevieve However this stone and minor siliciclastics in the basin interior eolianites on erosion is notrelated to the sequence bounding disconformity F the southern part of the eastern shelf and muddy carbonates and that can betraced through the middle of the siliciclastic unit The grainstone on the northern part of the eastern shelf The MFS is erosion may be the result of scour caused by a prograding tidal interpreted to be coincident with the lower sequence boundary delta in the late HST of the sequence If this erosion were related The upper sequence boundary disconformity H is the best to a sea level lowstand the sequence bounding paleosol would developed paleosol in the study interval which is called the be absent in locations where erosion occurred Bryantsville Breccia Bed in Indiana and central Kentucky In earlier work Smith 1996 this unit was called a disconformity 118 LANGHORNE B SMITH JR AND J FRED READ

bounded parasequence at the top of sequence 2 but is here rein are only present in the basin interior Sequence 4 is capped by terpreted as a separate sequence The progradation of siliciclas disconformity 1 tics at the top of the underlying unit and the intensity of the brecciation at the top of the sequence suggest that it is a thin 5 extension of a that Sequence updip sequence is better developed downdip Sequence 5 is bounded at the base by disconformity I and at the J In the basin interior and Sequence 4 top by disconformity western shelf sequence 5 includes the upper part of the Paoli interval a Sequence 4 is bounded at the base by disconformity Hand second disconformity bounded unit in the Girkin Limestone at the top by disconformity 1 Sequence 4 includes the lower part and the Downeys Bluff Formation Sequence 5 is 6 m thick on of the Paoli interval the basal disconformity bounded unit in the the western shelf thickens to 20 m in the eastern part of the Girkin Limestone on the eastern shelf and the Shetlerville basin interior and thins to 7 m near the Cincinnati arch and to Member of the Renault Formation and the Yankeetown less than 3 m on the northern part of the eastern shelf The Formation in the central and western parts of the basin The sequence may have been thicker in the basin interior but was sequence is 6 m thick on the western shelf thickens to 20 m in eroded during pre Bethel incision the basin interior and thins to 4 m near the Cincinnati Arch and Disconformity I is an intermediate unconformity that over 2 m in the northeastern sections lies a thin eolianite in the basin interior Fig 8 The TST is Disconformity H is a major disconformity characterized by composed of parasequence 22 that consists of a thin basal shale accumulations of breccia and caliche as much as 4 m thick and in the eastern part of the basin interior overlain by a grainstone called the Bryantsville Breccia Bed in Indiana and Kentucky unit that is very patchy on the eastern shelfand a laterally exten Mallot 1952 Liebold 1982 Disconformity H coincides with sive fossiliferous shale or muddy carbonate cap The MFS is the top of the Platycrinites penicillus zone and the base of the picked at the base of the grainstone unit in parasequence 23 Talarocrinus zone Swann 1963 The TST of sequence 4 is because it is the first laterally extensive grainstone unit to cover composed of parasequences 16 and 17 Parasequence 16 is a the shelves The HST is composed of parasequences 23 to 25 in thin parasequence confined to the most rapidly subsiding parts the basin interior but only parasequence 23 was deposited on of the basin interior which onlaps the shelves and a local tec the shelves Parasequence 23 is composed of a thick skeletal tonic high in the basin interior Parasequence 17 has a patchy oolitic grainstone unit overlain by a patchy muddy carbonate grainstone unit at the base that pinches out onto tectonic highs unit on the eastern shelf ooid skeletal grainstone capped by fos and is capped by a laterally extensive muddy carbonate siliferous shale and tidally influenced siliciclastics on the west fossiliferous shale unit that can be correlated across most of the ernshelf and skeletal limestone capped by fossiliferous shale in basin interior and eastern shelf On the western shelf the TST is the basin interior Parasequences 24 and 25 are only preserved absent except at section 3 where parasequence 16 is composed basinward of the shelves suggesting that progradational offlap of quartz sandstone and parasequence 17 is composed of a fos occurred at the top of sequence 5 These parasequences are com siliferous shale capped by quartz sandstone The Yankeetown posed of thick accumulations of ooid grainstone along the mar Shale that occurs near the top of the sequence grades updip into gin of the eastern shelf and skeletal limestone and shale in most quartz sandstone to the northwest Swann 1963 of the basin interior A widespread eolianite overlies the The MFS is picked at the base of parasequence 18 because sequence on much of the southern part of the eastern shelf The it is the first laterally extensive grainstone unit to be deposited sequence is capped by an unconformity disconformity J that on the eastern and western shelves The HST consists ofparase consists of a well developed paleosol on the eastern and western quences 18 to 21 in the basin interior but only parasequences 18 shelves that can be traced into an incised valley that trends and 19 were deposited on the shelves On the eastern shelf southwest from south central Indiana to western Kentucky and parasequence 18 is a grainstone muddy carbonate parasequence is as deep as 75 m Friberg et aI 1969 with the exception of a few downdip sections where it is com posed of muddy carbonates and green fossiliferous shale Parasequence 19 is composed of multilateral grainstone deposits Composite Sequences that underlie the sequence boundary on the eastern shelf In the A composite sequence is a succession of genetically related basin interior parasequences 18 and 19 have skeletal grainstone sequences in which the individual sequences stack into low or packstone bases with fossiliferous shale caps that grade later stand transgressive and highstand sequence sets Mitchum and ally to muddy carbonates in the eastern basin interior Ooid Van Wagoner 1991 The updip location of the Illinois basin on grainstone is rare in the basin interior but does occur at the base the ramp makes it difficult to trace sequence boundaries to of the HST near tectonic Parasequence 19 is capped by a highs determine which extends the farthest downdip In this setting local disconformity at sections 10 11 and 12 On the western composite sequence boundaries can only be distinguished from shelf para sequence 18 is composed of skeletal grainstone over higher frequency sequence boundaries by the degree ofpaleosol lain by tidally influenced siliciclastics and capped by a paleosol development depth of incision and or coincidence with bios and parasequence 19 is of quartz siltstone Late composed tratigraphic zone boundaries Smith 1996 On the basis of highstand parasequences 20 and 21 progradation ally offlap and these criteria the major disconformities at the base of sequence HIGH RESOLUTION SEQUENCE STRATIGRAPHY OF UPPER MISSISSIPPIAN CARBONATES 119

level Smith et aI Smith The 1 disconformity A at the top of sequence 3 disconformity H eustatic sea change 1995 1996 conclusion that the caused and at the top of sequence 5 disconformity J may be compos sequence boundaries likely were by ite sequence boundaries Smith 1996 In Smith 1996 fourth order 0 10 5 m y eustatic sea level changes is based four facts distinct marker beds and sequences 1 through 5 were picked as a composite sequence on on 1 by using biostratigra the basis of the development ofthe bounding unconformities A phy the sequence bounding unconformities in both siliciclastics and carbonates can be across Illinois basin and in and J and apparent backstepping of ooid grainstone upward correlated the 2 through the interval Disconformity H was picked as a higher some cases into the Appalachian basin Smith et aI 1995 frequency composite sequence boundary Disconformities A and the unconformities coincide with biostratigraphic zone bound H have been interpreted to be composite sequence boundaries in aries 3 disconformity bounded sequences with similar char the Appalachian basin AI Tawil 1998 but J is not any better acteristics occur in time equivalent strata in Kansas Abegg developed than the other sequence boundaries Thus the 1994 Great Britain Walkden 1987 and Kazakhstan sequences are likely bundled into composites sequences but the Lehmann et aI 1996 and 4 the duration of the sequences updip location of the Illinois basin and the intensity of the roughly coincides with the Milankovitch long term 400 k y and the for the sequence development make it difficult to confidently pick eccentricity signal calculated period overlying 1986 If the composite sequence boundaries Pennsylvanian cyclothems Heckel sequences boundaries were made by local tectonic uplift the sequence would be confined to the area of uplift but instead they are DISCUSSION basin wide If the unconformities were caused by a migrating would be diachronous but the fact that Duration ofSequences and Parasequences peripheral bulge they the unconformities coincide with biostratigraphic zone bound of the The most recent ages for the duration Mississippian aries suggests that they are relatively synchronous across the Period come from SHRIMP dating of volcanic rocks interbed basin Sequence bounding disconformities formed during peri ded with marine sedimentary rocks in Australia Roberts et aI ods of high moderate and low differential subsidence in the 1995 Brachiopod biostratigraphy was used to correlate with Illinois basin Smith 1996 Regional uplift of the Illinois and European and North American conodont and foraminiferal Appalachian basins could have caused the unconformities but dates from zones that tied the SHRIMP ages to radiometric there is no known mechanism that would cause rhythmic uplift basis and Europe Roberts et aI 1995 On the of foraminiferal and subsidence of the craton with a period on the order of 400 the Ste Genevieve to Glen Dean interval is variations in siliciclastic sed conodont zones k y If the sequences were made by uppermost Visean middle ofV3b to V3c Baxter and Brenckle iment supply caused by climate change Swann 1963 the duration of 3 m 1982 This interval has a approximately y unconformities would be present only in areas of mixed carbon but is constrained because the Roberts et aI 1995 poorly of ates and clastics but they can be traced from mixed carbonate difficulties inherent in correlating between brachiopod con clastic intervals into carbonate dominated strata odont and foraminiferal zones on different continents and the

error bars on the radiometric dates Sequence development There are five bounded sequences in the Ste disconformity The magnitude of sea level fluctuations that produced the Genevieve to Paoli interval and four in the overlying Bethel to in the fol boundaries of sequences 1 through 4 can be estimated Glen Dean interval Smith 1996 for a total of nine sequences lowing manner After deposition of the Lost River Chert Bed ten into 3 m an average of 333 Dividing sequences y gives period which can be traced from the basin interior to the northern part k which is of the term y per sequence suggestive long of the eastern shelf the sea level fall was sufficient to expose Milankovitch signal 414 k y Berger 1988 and eccentricity the basin interior as subsidence continued The exposed profile to the calculated duration for some of the comparable can be roughly reconstructed by using the thickness of the TST Heckel 1986 Such fourth order 0 1 Pennsylvanian cyclothems of sequence 1 which is 27 m thick in the basin interior thinning to 0 5 m are with times of abundant y sequences compatible to less than I m on the northern part of the eastern shelf These ice Weber et aI 1995 Calculated average duration of the global data suggest that a sea level change of about 30 m formed the would about k 1 55 preserved parasequences be 37 y in sequence at that the sequence boundary the base of sequence 1 given k in 2 and 4 and 83 k in 5 These results y sequences y sequence effects of compaction which would increase the estimate and that the are fifth order 10 to suggest parasequences dominantly differential subsidence during deposition of the TST which 100 k cf Weberet aI 1995 would y Any composite sequences would decrease the estimate would tend to cancel each other be third order 0 5 5 m y cf Weber et aI 1995 out The lack of incision on the boundaries of sequences 1 through 4 suggests that sea level may not have fallen far below the The incision within the Aux Vases Formation may Origin and Development ofSequences and Parasequences platform have been caused by prograding tidal deltas or local tectonics Leetaru but these surfaces are not Origin of sequences 1997 erosion sequence with in areas The sequences and sequence boundaries in the Chesterian boundaries because they do not correlate paleosols interval have been interpreted to have formed by local tectonics of no incision Thus sequences 1 through 4 likely were made by Leetaru 1997 cyclic climate change Swann 1963 and moderate amplitude sea level fluctuations of 30 m or less In 120 LANGHORNE B SMITH JR AND J FRED READ

DIFFERENTIA PARASEQUENCE OCCURRENCE DISTRIBUTION OF PARASEQUENCES and the restriction of SUBSIDENCE DEVELOPMENT some parasequence bounding disconfor mities to updip areas suggests that the of QNLAP OF TST magnitude high 1ST OF SeQUENCE 1 PARASEQUENCES sea level fluctuations probably was not much more HIGH frequency ALL OF SEQUENCE 3 PROGRADATIONAL than 10 m QFFLAP OF HST HST OF SeQUENCE 4 PARASEQUENCES Assuming that the sequences are 400 k y in average dura tion and from 2 to 63 m thick ignoring the effects of com MINORQNLAP OF rates have been TST paction subsidence would between 0 5 and 15 PARASEQUENCES HST OF SEQUENCE 1 These rates would not drowned MODERATE cmk y have healthy shallow TST OF SeQUENCE 4 PARAS ENCES warm water carbonate many of which are of DISCONFORMITY platforms capable BOUNDED UPDIP carbonate sediment at 20 or more ONLY generating cmk y Schlager 1981 Thus parasequence NEGLIGIBLE 1ST flooding likely required rapid glacio ONLAP eustatic sea level rises of as much as 10 m to generate water LATE HST lOW PARASEQUENCES for of thick If ALLOF SeQUENCE 2 depths necessary deposition grainstone deposits DISCONFORMITY BOUNDED sea level rises occurred the first 15 of the parasequence BASIN WIDE during duration similar to Pleistocene sea level rises then rise rates would FIG 9 Effects of variations in differential subsidence of the eastern shelf have been between 60 and 300 cmk y for parasequences

on and the basin interior parasequence distribution within the sequences TST with durations of 20 to 100 k y These rise rates would have transgressive systems tract HST highstand system tract been able to incipiently drown the ramp Sea level rises much less than 10 m would have tended to generate meter scale tidal contrast sequences in the middle Chesterian mixed overlying flat cycles on the inner ramp similar to those described from carbonate clastic also have incised sequences valleys indicating greenhouse platforms Goodwin and Anderson 1985 as much as 75 m of erosion as well as water carbonate deeper Koerschner and Read 1989 Goldhammer et aI 1990 which that facies together that the of sea level are suggest magnitude notably absent on the Mississippian platform changes increased to as much as 3095 m Smith 1996 Lowstand systems tracts were not preserved in the study Parasequence development area because the Illinois basin was more than 300 km updip Parasequence deposition was initiated by high frequency from the regional ramp margin As sea level rose transgressive sea level rises that flooded both disconformable and con systems tracts composed of one to four parasequences onlapped formable surfaces on shallow water mudstone that had shoaled the shelves Onlap was greatest in the transgressive systems to or near to sea level Fig 10 High frequency 20 to 100 tracts during periods of high differential subsidence between the ky rapid eustatic sea level rise coupled with background sub shelves and the basin interior Fig 9 Smith 1996 Initial sidence generated water depths that were sufficient for the tidal widespread flooding caused the uppermost of these parase wedge to develop and generate widespread high energy tidal quences to extend onto the eastern shelf where they typically currents and wave reworking These high energy conditions consist of laterally extensive muddy carbonate units Maximum allowed deposition of skeletal and ooid grainstone in discontin flooding generated extensive grainstone units over the eastern uous sheets and tidal ridges Ooid and skeletal grainstone and shelf when water depths increased enough to accommodate the packstone accumulated to form a broadly undulating submarine tidal wedge and generate strong tidal currents The lack of topography of ridges and passes Tidal energy appears to have deeper water facies indicates that water depths never exceeded diminished in updip parts of the ramp where muddy carbonates those of ooid and skeletal grainstone lithotopes In the HST were deposited in widespread As ooid and skeletal three to five to lagoons aggradational progradational parasequences grainstone filled much of the accommodation space on the were deposited as relative sea level peaked and began to fall ramp tidal energy diminished and muddy lagoonal facies and Progradational offlap of parasequences occurred in the HST fossiliferous shale prograded to form widespread sheets that during periods of high differential subsidence in the basin and capped and filled swales between carbonate sand ridges Tidal aggradation occurred during periods of relatively low differen flat laminites were not deposited at the tops of most parase tial subsidence Fig 9 Smith 1996 quences because sea level fall caused rapid movement of the shoreline seaward across the shelf stranding any tidal flats eustatic Glacio origin parasequences areas of updip In with low accommodation rates parasequences The lateral extent and ofthe frequency regionally developed were capped by patchy eolianites and disconformities These parasequences indicate that these strata were fifth produced by disconformities pinched outinto areas ofhigher accommodation order 100 k eustatic sea level 10 y glacio Neither sea changes where relative level fall did not expose sediments for a local tectonics nor autocyclic processes could have produced period of time sufficient to develop disconformities In these that have basin wide parasequences appear to formed in tens of areas renewed conformable flooding generated parasequences thousands of The of tidal sand 8 10 m years presence ridges Shallowing upward trends within the individual carbonate 1973 Cluff and Lineback Carr 1981 suggest that are the of the high rapid parasequences complicated by gentle dip ramp and sea level rises of as much as 10m would have been to required the strong tidal currents which generated the dip parallel orien provide the necessary accommodation for typical parase tation of the ooid shoals Thus facies were as much dependent quences The lack of deep water facies extending onto the ramp HIGH RESOLUTION SEQUENCE STRATIGRAPHY OF UPPER MISSISSIPPIAN CARBONATES 121

A carbonate deposition persisted through time even though sea level was changing Other apparently amalgamated parase quences could be due to erosion of muddy carbonate caps dur o ing subsequent transgressions leaving stacked grainstone units Autocyclic shallowing associated with local island develop ment formed local parasequences within thicker regionally 3 AS SEA LEVEL FALLS MUDDY CARBONATES PROGRADE traceable parasequences Such autocycles are clearly evident with the detailed closely spaced cross sections but could not have been distinguished from regional parasequences on the basis of a single stratigraphic section 2 GRAINSTONE FILLS ACCOMMODATION TIDALCURRENTS DECREASE

Late Mississippian Sea Level Curve

Basin wide and in the 1 DURING RAPID SEA LEVEL RISE GRAINSTONE DEPOSITED AS TIDAL paleosols facies stacking patterns CURRENTS INCREASE Mississippian succession can be used to construct a detailed relative sea level curve Fig 11 Ross and Ross 1988 con B structed an onlap curve for the late Paleozoic but only correlated large scale sequences Fig 11 They picked a larger scale sequence boundary at the St Louis Ste Genevieve contact and the Ste Genevieve Paoli interval only makes up part of one of their sequences Swann 1963 constructed a transgression regression or relative sea level curve on the basis of the seaward extent of siliciclastics within the Illinois basin Fig 11 Swann s curve roughly parallels this paper s fourth order sequence curve because the siliciclastic units commonly prograded toward the tops of the sequences However the Swann 1963 curvedoes not show a regression at the St Louis Ste Genevieve boundary 1 DURING RAPID SEA LEVEL RISE SKELETAL LIMESTONE DEPOSITEDsp because there was no siliciclastic influx associated with it

FIG 1O A Development of carbonate parasequences I Rapid glacio eustatic sea level rise promotes increase in tidal energy and deposition of ooid ROSS AND ROSS 1988 ridges and skeletal banks 2 Ooid and skeletal grainstone fills much of the SEAWARD LANDWARD accommodation space and tidal energy diminishes 3 Muddy carbonates pro grade filling topography and forming laterally extensive sheets B Skeletal succes limestone shale parasequence development I During sea level rise sive siliciclastic layers are deposited farther updip toward the source and car o bonate producing organisms thrive and make skeletal limestone 2 As sea level falls shaleprogrades from the west northwest and caps parasequences In areas close to the siliciclastic source sandstone progrades over shale on local tidal energy as water depth If ooid shoals had formed wave dominated strike parallel barriers rather than dip parallel tidal ridges a more predictable succession of skeletal grain w stone to ooid to carbonate and shale to eolian grainstone muddy w ite would have been within generated by upward shallowing w z prograding parasequences Instead skeletal grainstone occurs w Cl above and below and into ooid as a E passes laterally grainstone 4 ui D I of 6 1Il product dip parallel grainstone geometries C Most apparently symmetrical parasequences with muddy rr at et can carbonates the base and top Pryor aI 1990 be traced 1 4 1 TTB where the basal units form the tops downdip muddy commonly 3 of parasequences with basal patchy high energy grainstone units Thus many updip basal mudstones are actually the updip low energy tongues of downdip parasequences At the other ST LOUIS extreme some well developed updip parasequences merge FIG ll Comparison of onlap curve from Ross and Ros 1988 trans downdip into thick ooid grainstone or mudstone units e g gression regression curve of Swann 1963 and relative sea level curve pre 4 and that 3 5 represent parase are are parasequences amalgamated pared for this paper Disconformities lettered from A to J sequences These where ooid and quences developed grainstone muddy numbered from I to 5 and parasequences are numbered from I to 25 122 LANGHORNE B SMITH JR AND J FRED READ

Stratigraphic Signature of the Greenhouse to sea level changes of as much as 95 m Smith 1996 Time Icehouse Transition equivalent strata in Great Britain show a similar upward change from nonerosional to erosional boundaries that has been attrib The first ice rafted of the late Paleozoic deposits glaciation uted to increasing amplitude of relative sea level fluctuations of Gondwana suggest that major continental ice sheets to began coupled with tectonics Walkden 1987 This increasing ampli grow the earliest Namurian or middle Chesterian during tude is likely related to the onset of continental glaciation on 12 and Harland Frakes Fig Garrasino 1981 Hambrey 1981 Gondwana et aI 1992 and Crowell 1985 Roberts et aI 1995 Caputo The Early Mississippian was dominated by precessionally The base of the overlying Glen Dean Formation is to equivalent driven low amplitude high frequency sea level fluctuations the base of the Namurian therefore the age of the Ste which suggests that it was relatively ice free Vaughn and Genevieve to Paoli interval is late Visean Baxter and Brenckle Adams 1984 Adams et aI 1990 Read and Horbury 1993 1982 Thus the interval spans the later part of the transi study The stratigraphy of the updip parts of large carbonate platforms tion from a relatively ice free in the to middle globe Early that developed during greenhouse times of little global ice is to the Permian 1ce Mississippian Pennsylvanian glaciation dominated by meter scale peritidal cycles capped by regional rafted time to the interval have not deposits equivalent study tidal flat facies especially in highstand systems tracts of third been but such would have been reported deposits likely order sequences Goodwin and Anderson 1985 Koerschner of ice sheets destroyed during buildup progressively larger and Read 1989 Goldhammer et aI 1990 Elrick 1991 The waxing and waning of progressively larger ice sheets Read 1995 These peritidal cycles may be bundled into may have caused an increase in the of sea level fluc amplitude obliquity or eccentricity cycle sets Goldhammer et aI 1990 tuations these sequences and those in the forming overlying Disconformities are poorly developed on these greenhouse plat middle Chesterian interval Fig 13 Smith 1996 I Sequences forms except at third order sequence boundaries 4 are bounded by surfaces with minimal erosion and through The parasequences formed during the transition period of were formed sea level fluctuations of 30 m or less In likely by the Late Mississippian covered by this study generally lack contrast sequences 5through 10 have bounding surfaces with as much as 75 m of incision which may have been produced by SEQUENCES SEA LEVEL HIGH LOW FREQUENCY OF 2 AGE GLEN a Robert ICE RAFTED DEPOSITS DEAN 11 J eta UJ 2 14 Z 1995 6 10 HARDINS BURG C 10 UJ HANEY z 0 Z i Z FRAILEYS Z BIG CLIFTY I 9 a BEECH CREEK f a CYPRESS l C f S UJ REELSVILLE 00 7 z z SAMPLE z BEAVER w BEND 6 0 a BETHEL a a z 5 a i o a 2 J 4 z 2 Z r

0 Z ROSICLARE 0 a UJ W 2 f 00 w 00 C Z UJ ffi SPAR MTN 00 I STUDY INTERVAL Cl 00 UJ C ui l ll 1 MER J

FIG l2 Global climate setting during Late Mississippian and Pennsylvanian Graph shows the number of occurrences of ice rafted deposits worldwide leading up to late Paleozoic glaciation of Gondwana modified from FIG 13 Composite sea level curve for the Ste Genevieve to Paoli inter Frakes et aI 1992 age from Roberts et aI 1995 The study interval occursjust val and the Bethel through Glen Dean interval sequences 6 to 10 Smith below the first glacial deposits and during thetransition from littleglobal ice to 1996 The amplitude of sea level changes increased through the Chesterian in major continental glaciation MER Meramecian DES Desmoinesian response to onset of major continental glaciation on Gondwana CARBONATES 123 HIGH RESOLUTION SEQUENCE STRATIGRAPHY OF UPPER MISSISSIPPIAN

on at the base of that extend over the intertidal supratidal caps and disconformities are developed picked regional grainstones subtidal lagoonal and shoal facies of fourth order and some eastern shelf Sequences are mainly composed of highstand sys The updip fifth order units Third order composite sequences are tems tract aggradational to progradational parasequences with those in the basin indi difficult to recognize because of the frequency of the disconfor sequences correlate Appalachian mities and the magnitude of the moderate amplitude fourth cating a eustatic origin The magnitude of sea level changes was less for the boundaries order sea level changes probably 30 m or nonerosional sequence much as m to create the erosional uncon Global icehouse times such as the Pennsylvanian and but increased to as 95 the The of Pleistocene were characterized by high frequency fourth order formity at the top of interval increasing magnitude aI Weber et aI sea level fluctuations was driven and wan sequences Heckel 1986 Goldhammer et 1991 probably by waxing the of 1995 Mitchum and Van Wagoner 1991 Read 1995 This paper ing of progressively larger ice sheets during onset shows that this type of sequence development is evident as early Gondwana glaciation record contain the individual reservoirs and consist as the Late Mississippian The oxygen isotope suggests Parasequences from base 1 a basal or conformable that the dominant episodes of waxing and waning of Pleistocene of to top disconformity 2 ooid reservoir and skeletal 3 ice sheets correlate with the 41 k y obliquity and the 100 k y boundary grainstone muddy carbonate and or and 4 a dis eccentricity periods Ruddiman et aI 1986 Given that there are fossiliferous shale caps capping dif missing beats associated with the disconformities the average conformity or conformable boundary These parasequences 40 100 k that the fer from carbonate developed during durations of the parasequences to y suggest typical cycles global sea level conditions in their lack of tidal flat and com parasequences may have been produced by changes greenhouse caps k in combina mon disconformities tidal currents formed dis associated with the 41 y obliquity signal possible Strong laterally dur continuous ooid and channel fills tion with the 100 k y short term eccentricity signal Unlike dip parallel grainstone ridges that into skeletal sheets and ing greenhouse times there is no bundling of parasequences e g reservoirs pass laterally grainstone carbonates that were precessional cycles bundled into obliquity eccentricity cycles banks Grainstones were capped by muddy in extensive sheets and swale fills This Goldhammer et aI 1990at a scale below that of the sequences deposited laterally Without The increase in siliciclastic content from sequences 1 to 4 process generated highly compartmentalized reservoirs in framework defined of discon continues into the overlying sequences and may be related the sequence by regional tracing due to be distributed The part to the increasing amplitude of sea level fluctuations to formities reservoirs appear randomly framework more shows how the onset of glaciation A similar increase in siliciclastic sedi sequence and parasequence clearly related The be cor mentation occurred in time equivalent strata in Great Britain individual reservoirs are parasequences can and local between areas with different subsidence rates thus that was attributed to increasing amplitude eustasy related vastly order level fluctuations tectonics Walkden 1987 Increasing amplitude eustasy caused they were likely formed by fifth sea erosion in the on the fourth order eustatic greater base level falls that in turn caused greater superimposed signal facies of worldwide headlands and increased siliciclastic sediment supply At the Carbonate reservoir Mississippian age and humid are to show similar same time synchronous climate change increasingly likely high frequency sequence stratigraphy the time of transi wet dry seasonality would have increased clastic influx during because of the global eustatic control during tion into the late Paleozoic lowered sea level glaciation

CONCLUSIONS ACKNOWLEDGMENTS

Steve Bachtel Brian Keith Art Saller and Zak Regional disconformities were previously thought to be of We thank also thank relatively local extent in the Ste Genevieve to Paoli interval in Lasemi for their help in revising this manuscript We the and State the Upper Mississippian Chesterian of the Illinois basin the members of Indiana Illinois Kentucky for cores and discussion However these disconformities which probably are the result of Geological Surveys providing valuable Mike Dever and John Nelson moderate amplitude fourth order eustasy can be mapped region Aus AI Tawil Pope Garland pro vided and the course of this research ally to define a high resolution sequence stratigraphic framework help guidance throughout was the Petroleum Research of fourth order sequences and component parasequences Financial assistance provided by of Five disconformity bounded fourth order sequences 2 to 63 Fund ACS PRF 30516 AC8 the Geological Society Illinois in the Ste America Xi and Tech m thick can be traced across the basin Sigma Virginia Genevieve to Paoli interval The boundaries of the lower four

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in the Furness and Millom areas South Cumbria abs in M 1990 Geologic controls on porosity in Mississippian limestone reservoirs European Dinantian Environments 1st Manchester in the Illinois basin in Leighton M w Kolata D R Oltz DE and Eidel Meeting Open University JJ eds Interior Cratonic Basins Tulsa American Association of Petroleum p 120 123 WALKDEN G M 1987 and in late Dinantian car Geologists Memoir 51 p 329 359 Sedimentary diagenetic styles of Britain in Miller J Adams A E and V P eds READ J E 1974 Calcrete deposits and Quaternary sediments Edel Province bonates Wright Dinantian Environments Chichester John and Sons Shark Bay Western Australia in Logan B w Read J E Hagan G M European Wiley Hoffman P Brown R G Woods P J and Gebelein C D eds Evolution and p 131 155 WALLS R A HARRIS W B AND NUNAN W E 1975 Calcareous crust Diagenesis of Quaternary Carbonate Sequences Shark Bay Western Australia caliche and subaerial of Carboniferous carbonates Tulsa American Association of Petroleum 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carbonate platforms in Horbury AD and Robinson A WELLER J M AND SUTTON A H Mississippian Association of Interior basin American Association of Petroleum Bulletin v 24 G eds Diagenesis and Basin Development Tulsa American Geologists 765 858 Petroleum Geologists Studies in Geology No 36 p 155 197 p con WITZKE B J 1990 Paleoclimatic constraints for Paleozoic of REXROAD C B AND FRAUNFELTER GH 1977 Upper Mississippian paleolatitudes Laurentia and Euramerica in McKerrow W S and Scotese C R eds odonts and boundary relations in southern Illinois Guidebook for post meet Paleozoic and London of ing field trips IIth Annual Meeting North Central Section Geological Paleogeography Biogeography Geological Society London Memoir No 12 57 74 Society of America v 2 p 81 103 p oolite reservoirs in the Ste Genevieve ROBERTS J CLAOUE LONG J JONES P J AND FOSTER CB 1995 SHRIMP ZUPPANN C W 1993 Complex of Gondwanan in Late Carboniferous and Limestone at Folsomville field Warrick Co Indiana in zircon age control sequences Early Mississippian w eds Oolites and Modern Permian Australia in Non biostratigraphical Methods of Dating and Keith B D and Zuppann C Mississippian American Association of Petroleum Studies in Correlation London Geological Society of London Special Publication No Analogs Tulsa Geologists No 35 265 p 89 p 145 174 Geology ZUPPANN C W AND KEITH B D 1988 Geology and of Ross C A AND Ross J R P 1988 Late Paleozoic transgressive regressive petroleum production and Kendall C the Illinois basin volume 2 Indiana Survey and deposition in Wilgus C W Posamentier H W Ross C A Bloomington Geological 272 G St c eds Sea Level Changes An Integrated Approach Tulsa SEPM Lexington Kentucky Geological Survey p 227 247 Society for Sedimentary Geology Special Publication 42 p RUDDIMAN W E RAYMO M AND MACINTYRE A 1986 Matuyama 41 000 ice sheets Earth APPENDIX I OUTCROP AND CORE LOCATIONS year cycles North Atlantic Ocean and Northern Hemisphere and Planetary Science Letters v 80 p 117 129 in The are the and core locations for the data SABLE E G AND DEVER G R 1990 Mississippian Rocks Kentucky following outcrop Professional 1503 alternate Washington DC United States Geological Survey Paper in the cross sections in Figure 4 Abbreviations Alt 125 p route Co county Ill Illinois Ind Indiana Ky SCHLAGER W 1981 The of drowned reefs and carbonate platforms paradox S R state road 211 Kentucky Geological Society of America Bulletin v 92 p 197 I Core Madison Co C 141 Illinois State SCOTESE CR AND McKERROW W S 1990 Revised world maps and intro Geological Core Ill duction in McKerrow W S and Scotese CR eds Paleozoic Survey Facility Champaign Paleogeography and Biogeography London Geological Society of London 2 Core Madison Co C 140 Illinois State Geological Memoir 12 p 1 24 Survey Core Facility Champaign Ill SEYLER B 1986 Aux Vases and Ste Genevieve Formations A Core 4 Core Union Co C 13619 Illinois State Geological Workshop and Field Trip Guidebook Champaign Illinois Geological Society Survey Core Ill and Illinois State Geological Survey 34 p Facility Champaign 5 Anna East of Anna Ill northwest SMITH L B 1996 High resolution sequence stratigraphy of Late Mississippian Outcrop Quarry Side Chesterian mixed carbonates and siliciclastics Illinois basin Unpublished of junction of S R 51 and S R 146 Ph D Dissertation Virginia Tech Blacksburg 146 p 6 Outcrop I 57 milepost 274 south of Anna Ill exit evidence for SMITH L B AND READ J E 1995 increasing ampli Stratigraphic 7 Columbia Quarries Inc S R h Outcrop Cypress Quarry tude 4 order eustasy during Late Mississippian greenhouse to icehouse tran 37 3 mi about 5 km south of Ill sitions Illinois basin abs Geological Society of America Abstracts with Cypress

v no 8 Core C 46 Illinois State Programs 27 6 p A 332 Pope County Geological SMITH L B AL TAWIL AA AND READ J E 1995 Regional interbasinal Survey Core Facility Champaign Ill Illinois to fourth order sequence stratigraphy Late Mississippian 10 Core Hardin Co C I2781 Illinois State Geological Appalachian basins abs Tulsa American Association of Petroleum Survey Core Facility Champaign Ill Geologists Official Program v 4 p 90A 126 LANGHORNE B SMITH JR AND J FRED READ

12 Core Hardin Co C 12782 State Illinois Geological 43 Outcrop Stephensburg Quarry abandoned on dirt Survey Core Facility Champaign Ill road 2 mi about 3 km north of Stephensburg Ky 13 Core Hardin Co from Ozark Mahoning Fluorspar 44 Outcrop lrvington Quarry Kentucky Stone Company near Denton mine Ill S R 477 2 mi about 3 km northwest of Irvington Ky 14 Hardin Outcrop County Materials Company Pit 2 45 Outcrop Battletown Quarry Kosmos Cement Company S R 1 and S Rl46 junction of Cave in Rock Ill S R 228 0 5 mi 0 8 km northwest of Battletown Ky 15 Outcrop Cave in Rock Quarry Martin Marietta on 46 Outcrop Cape Sandy Quarry Pit I Mulzer Crushed county roads east northeast of Cave in Rock Ill Stone Inc 4 mi about 6 5 km east of Alton Ind 16 Three Rivers Outcrop Quarry Martin Marietta U S 47 Core Harrison Company C 339 Indiana Geological 60 of 6 25 mi 10 km northeast Smithland Ky Survey Core Facility Bloomington Ind 17 Outcrop Fredonia Quarry Denny and Simpson U S 48 Core Perry Company C 303 Indiana Geological 641 2 5 mi 4 km south of Fredonia Ky Survey Core Facility Bloomington Ind 18 Outcrop Princeton Quarry Kentucky Stone Company 49 Outcrop Tower Quarry Mulzer Crushed Stone S R 91 2 75 mi south of Princeton Ky Company 2 mi about 3 km north of Leavenworth Ind 21 Core Co C 220 Caldwell Kentucky Geological 50 Outcrop road cut at milepost 99 on 1 64 7 mi about II Survey Core Facility Lexington Ky km west of Corydon Ind exit 22 Outcrop S Hopkinsville Quarry Rogers Group U S 51 Outcrop Corydon Quarry Corydon Crushed Stone Inc Alt 41 4 5 mi about 7 km south of HopkinsvilIe Ky 2 5 mi 4 km northwest of Corydon Ind 23 Christian Outcrop Quarries Quarry abandoned U S 52 Outcrop Robertson Quarry Robertson Crushed Stone 68 0 5 mi 0 8 km east of Hopkinsville Ky Inc S R 64 I mi 16 km west of Depauw Ind 24 Todd Outcrop Quarry Kentucky Stone Company 56 Core Crawford Co C 626 Indiana Geological Survey Quarry U S 68 7 mi II km west of Elkton Ky Core Facility Bloomington Ind 25 Outcrop new road cut for U S 68 bypass west of 57 Core Orange Co C 338 Indiana Geological Survey RusselvilIe Ky Core Facility Bloomington Ind 26 Russelville and Outcrop Quarry Core Kentucky Stone 60 Core Orange Co C 65I Indiana Geological Survey Company S R 79 1 mi 1 6 km east of Russelville Core Facility Bloomington Ind Ky 62 Outcrop W Paoli Quarry Cave Quarries Inc U S 150 29 Outcrop road cut at milepost 9 1 on Green River 3 5 mi about 5 5 km northwest of Paoli Ind north of Parkway Bowling Green Ky 63 Core Martin Co C 214 Indiana Geological Survey 30 Outcrop Rockfield Quarry Kentucky Stone Company Core Facility Bloomington Ind U S 68 Rockfield Kentucky 64 Outcrop Mitchell Quarry Rogers Group S R 60 5 mi 33 Outcrop road cut on 1 65 N at milepost 48 north of Park 8 km west of Mitchell Ind exit City Ky 65 Core Lawrence Co C 340 Indiana Geological Survey 34 Outcrop E Park City Quarry abandoned Old Core Facility Bloomington Ind Bardstown Road 2 mi about 3 km east of Park City 67 Core Martin Co C 797 Indiana Geological Survey Ky Core Facility Bloomington Ind 35 Cave Outcrop City Quarry Scotty s Paving Company 68 Outcrop Sieboldt Quarry Rogers Group county roads Route 90 about 5 mi 8 km east of Cave City Ky 5 mi 8 km north of Oolitic Ind 36 road cut on 1 65 south Outcrop 1 mi 16 km south of 69 Core Greene Co C 487 Indiana Geological Survey MunfordvilIe Ky exit Core Facility Bloomington Ind 37 road cut on 1 65 North 0 5 mi km north 70 Outcrop 0 8 Core Monroe Co C 672 Indiana Geological Survey of MunfordvilIe Ky exit Core Facility Bloomington Ind 38 Outcrop Upton Quarry Kentucky Stone Company 71 Outcrop Bloomington Quarry Rogers Group Oard Quarry Road Upton Ky Road 4 mi about 6 5 km west of Bloomington Ind 40 Core Hardin Co C 117 Kentucky Geological Survey 73 Core Clay Co C 444 Indiana Geological Survey Core Core Facility Lexington Ky Facility Bloomington Ind 41 Cecelia Outcrop Quarry Larry Glass Paving S R 62 3 74 Outcrop PutnamvilIe Quarry Kentucky Stone Company mi about 5 km west of Cecelia Ky S R 343 I mi 1 6 km west of Cloverdale Ind 42 Core C Breckenridge Co 1l8 Kentucky Geological 75 Core Putnam Co C 105 Indiana Geological Survey Survey Core Facility Lexington Ky Core Facility Bloomington Ind