Evidence for Eustasy at the Kinderhookian-Osagean (Mississippian) Boundary in the United States: Response to Late Tournaisian Glaciation?

The Geological Society of America Special Paper 441 2008

Evidence for eustasy at the Kinderhookian-Osagean (Mississippian) boundary in the United States: Response to late Tournaisian glaciation?

Thomas W. Kammer† Department of Geology and Geography, West Virginia University, Morgantown, West Virginia 26506-6300, USA

David L. Matchen Division of Natural Sciences, Concord University, Athens, West Virginia 24712, USA

ABSTRACT

Evidence for eustasy at the Kinderhookian-Osagean boundary is presented here in a new synthesis based on detailed analysis of the boundary in the central Appala- chian Basin and regional mapping of the Kinderhookian-Osagean boundary unconformity in the conterminous United States. Detailed stratigraphic analysis within the central Appalachian Basin shows that coarse-grained, ﬂ uvial sandstones (Black Hand, Burgoon, Big Injun, Purslane) are associated with valley incision up to 60 m and a widespread sequence boundary (SB2) that is inferred to have resulted from a forced regression during the Kinderhookian-Osagean boundary interval. The extent of unconformity at the boundary was evaluated by mapping the inferred positions of shorelines during the Kinderhookian, Kinderhookian-Osagean boundary interval, and early Osagean based on stratigraphic data from Correlation of Stratigraphic Units of North America (COSUNA) charts. This analysis shows areas of extensive unconformity at the Kinderhookian-Osagean boundary across the United States inferred to be the result of sea-level fall and recovery during a period of ~2 m.y. or less, based on missing conodont zones. The Kinderhookian-Osagean boundary is equivalent in age to the global Tn2-Tn3 boundary, and supporting evidence for global regression and eustasy at this boundary is also reviewed. The combination of this evidence for eustasy with recently reported middle to early late Tournaisian (Tn2a-Tn3b) diamictites in South America permits the inference of continental glaciation at this time. Previous studies of oxygen and carbon isotope data from marine carbonates and fossils have shown strong positive anomalies suggestive of global cooling at the Kinderhookian-Osagean and Tn2-Tn3 boundary, providing further support for the hypothesis of continental glaciation in the late Tournaisian.

Keywords: eustasy, Kinderhookian, Osagean, Tournaisian, glaciation, Black Hand Sandstone, Burgoon Sandstone, incised valley, Appalachian Basin, sea-level maps.

†E-mail: [email protected].

Kammer, T.W., and Matchen, D.L., 2008, Evidence for eustasy at the Kinderhookian-Osagean (Mississippian) boundary in the United States: Response to late Tournaisian glaciation?, in Fielding, C.R., Frank, T.D., and Isbell, J.L., eds., Resolving the Late Paleozoic Ice Age in Time and Space: Geological Society of America Special Paper 441, p. 261–274, doi: 10.1130/2008.2441(18). For permission to copy, contact [email protected]. ©2008 The Geological Society of America. All rights reserved.

261 262 Kammer and Matchen

INTRODUCTION STRATIGRAPHY OF THE KINDERHOOKIAN-OSAGEAN BOUNDARY The purpose of this paper is to present a new synthesis of the available data on both the stratigraphic and geographic To argue the case for eustasy at the Kinderhookian-Osagean extent of the unconformity, and the correlative sequence boundary in North America, we present a review of previous boundary, at the Kinderhookian-Osagean boundary across the studies interpreted under the hypothesis of sea-level fall at the conterminous United States. The synthesis is based on our boundary. Additionally, lithostratigraphic cross sections are own detailed analysis of the Kinderhookian-Osagean bound- presented in support of regression at the Kinderhookian- ary stratigraphy; newly constructed shoreline, or sea-level, Osagean boundary. maps for the early Mississippian; and proxy data from other studies. The Kinderhookian-Osagean boundary is equivalent North American Midcontinent to the late Tournaisian Tn2-Tn3 global boundary (Ross and Ross, 1985; Jones, 1996), and we briefl y review the evidence The Kinderhookian-Osagean boundary is defi ned in the for unconformity, or the correlative sequence boundary, out- Mississippi Valley stratotype region at Kinderhook, Pike County, side of North America as well. These data are then used to Illinois, and along the Osage River, St. Clair County, Missouri support the hypothesis of an episode of eustasy at the Kinder- (Lane and Brenckle, 2005). Two conodont zones (upper part of hookian-Osagean and Tn2-Tn3 boundary during which there the upper crenulata-isosticha and punctatus biozones) are miss- was a global fall in sea level followed by a relatively rapid ing in the stratotype region where a physical unconformity is rec- recovery. The hypothesized eustasy is then related to evidence ognized (Lane and Brenckle, 2005). for early late Tournaisian glaciation, including diamictites in The unconformity at the Kinderhookian-Osagean bound- South America (Caputo et al., 2006a, 2006b, this volume), ary has long been recognized (Ham and Wilson, 1967; Craig and carbon and oxygen positive isotope anomalies in marine and Connor, 1979, pl. 9-A). In the subsurface of western Illinois, limestones and fossils from North America and Europe, which Workman and Gillette (1956) documented extensive erosion indicate apparent global cooling (Mii et al., 1999; Saltzman, of the upper Kinderhookian formations. In Missouri, the early 2002a; Buggisch and Joachimski, 2006). Together, these vari- Osagean Burlington Limestone may directly overlie the Hanni- ous lines of evidence are discussed in support of the hypoth- bal Formation (Thompson, 1986) (Fig. 1). esis for late Tournaisian glaciation. Two brief ice ages apparently occurred in the Late Appalachian Basin Devonian and early Mississippian prior to the late Mississip- pian Gondwanan ice age (Crowell, 1999; Crowley and Berner, General Stratigraphy 2001; Royer et al., 2004). The older ice age occurred in the late The Kinderhookian and Osagean stages in the central Appa- Famennian at the Devonian-Mississippian boundary, evidence lachian Basin (consisting of eastern Ohio, southwestern Pennsyl- for which includes glacial deposits and a wide range of proxy vania, western Maryland, and West Virginia) (Fig. 2) comprise a records (Crowell, 1999; Isaacson et al., 1999, 2005). Isaacson 200–300-m-thick siliciclastic succession. This siliciclastic suc- and Hladil (2003) estimated a minimum of 60 m for the sea- cession was deposited near the end of the Acadian orogeny on a level fall. The younger ice age apparently occurred in the middle foreland ramp (Castle, 2000) that extended as far west as the Illi- to late Tournaisian (Tn2-Tn3), at or near the Kinderhookian- nois Basin (Matchen and Kammer, 1994, 2006). The succession Osagean boundary; it is supported by evidence of diamictites is bounded by unconformities at the upper and lower contacts in the Solimões Basin of Brazil (Caputo et al., 2006a, 2006b, (SB1 and SB3 on Figs. 1 and 2). A third sequence boundary (SB2 this volume). on Figs. 1 and 2) occurs at the Kinderhookian-Osagean bound- Indirect, or proxy, evidence for a late Tournaisian ice age ary (Matchen and Kammer, 2006). Interpretation of SB2 includes is robust and consists of (1) a massive incised valley (60 m) evidence for incised valley fi ll at the Kinderhookian-Osagean (Matchen and Kammer, 2006), and associated sequence bound- boundary in Ohio (Matchen and Kammer, 2006) and corroborat- ary and fl uvial sandstones in the Appalachian Basin of the east- ing evidence for the sequence boundary over a wider area in at ern United States; (2) a widespread unconformity over much of least West Virginia and Pennsylvania. North America at the Kinderhookian-Osagean boundary, presented herein; (3) a global sequence boundary associated with Incised Valley Fill in Ohio widespread regression and unconformity at the Tn2-Tn3 bound- Matchen and Kammer (2006) interpreted the Black Hand ary in Saudi Arabia, Belgium, Czech Republic, Germany, west- Sandstone Member of the Cuyahoga Formation (Fig. 1) as ern Russia, Siberia, and China (Ross and Ross, 1985; Swennen incised valley fi ll. The Black Hand Sandstone extends across et al., 1986; Kalvoda, 1989, 1991, 2002; Isaacson et al., 1999; southeastern Ohio (Fig. 2), and it is a multistory, cross-bedded, Hance et al., 2002; Haq and Al-Qahtani, 2005); and (4) stable coarse-grained sandstone up to 60 m thick that is surrounded isotope anomalies (Mii et al., 1999; Saltzman, 2002a; Buggisch on all sides by fi ner-grained marine sediments of the underly- and Joachimski, 2006). ing Cuyahoga Formation and the overlying Logan Formation. section D–D the UpperMississippianGreenbrier andMaxvillelimestones.LogsforPennsylvania wereobtainedfromHarperandLaughrey (1987, SB2 isplacedatthebaseof Big InjunandBlackHandsandstones.SB3isplacedatthetopof theLower Mississippiansucce unconformity isatthebaseof SharonSandstone.Sequenceboundariesareshown inblack.SB1isplacedatthebaseofB Osagean boundary. For bothsections,datumisthebaseofSunbury Shaleoverlying theBereaSandstone. The Mississippian-Pe position andwereapparentlydeposited aspartofthesamepulsecoarse-grainedsedimentationduring regression atorneart covering northern West Virginia andsouthwesternPennsylvania. Despitethediscontinuousnature,sandbodies occupy asimil deposit surroundedonallsidesbymarinedeposits. The BigInjunsandstoneand Burgoon Sandstone aremoreextensive intheird of West Virginia arediscontinuouswiththeBlackHandSandstoneofOhiofromeasttowest. The BlackHandSandstoneis abraid correlative sandstonesfromsouthtonorth.SectionB–B Section A–A Hand SandstoneinOhioisfrom Wolfe etal.(1962).Stratigraphiccrosssectionsarebased ongamma-ray(left)anddensity(rig for eachstate: West Virginia (Cardwelletal.,1968);Ohio(Slucher2006);Pennsylvania (Berg etal.,1980).Distribut western Pennsylvania, westernMaryland, and West Virginia. The extent oftheLower Mississippianontheindex mapisfromtheg Figure 2( i—Inners etal.(2003). (1942); d—BjerstedtandKammer(1988);e—Matchen Vargo (1996);f—Vargo andMatchen(1996);g—Berg (1999);h—Brezinski(1999 boundaries, denotedbySB1,SB2,andSB3,arediscussedintext. Stratigraphyis froma—Harrelletal.(1991);b—Hyde(1953);c subdivisions (Jones,1996);(3)North American stagenames,baseduponMississippi Valley typelocalities(LaneandBrenckle,2 Figure 1.Lower MississippianchronostratigraphyintheeasternUnitedStates.(1)Europeanstagenames;Fam.—Famennian; (2) To Dev. Mississippian on followingtwopages

Fam. 1 ′ ′

). Tournaisian demonstratesthatthedrillers’ BigInjunsandstone ofthe West Virginia subsurface andthe BlackHandSandstoneofOhioare (part) Visean Tn1b Tn2 Tn3 2 a b c ab c Kinderhookian Osagean 3 Valley Section Chouteau Mississippi G Gl Limestone Form

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2 . SB Be ? ? 1 Sands rea Formation Marshall Coldwater Michigan Michigan Sunbury Shale Sandstone Basin Sha ?? tone l e ′ demonstratesthattheBurgoon SandstoneofPennsylvania andtheBigInjunsandstone a ? SB3 Berea Sandstone Berea Sunbury ShaleSunbury Logan Fm. Black Hand Black S C F andstone Rus Central o u Ohio Vint Berne Member Byer Memb Byer r y Allensville m h Member a o ville Member h n Memb a b,c o t i o g n a er er Formati Price Formation Maccr South Sunbury Shale sandstones Conglomerate “ ady B o ig Injun” West Virginia e,f n Clo yd Central sandstones “Wei No Section e,f r” Sandstone C Sand d Oswayo Riddl ussewago Shale stone Nort e sburg h e,f sandstone Rockwell Member “Big Injun”

Price Formation Pennsylvania he Kinderhookian-

ht) wirelinelogs. Rockwell Formation ion oftheBlack Ri erea Sandstone. 005). Sequence ar stratigraphic ? dd ssion beneath eologic maps Shale nnsylvanian lesbu Sand istribution, Burgoon —Holden ed-stream urnaisian stone r cross g g,h,i ? SB SB2 SB 3 ); 1

266 Kammer and Matchen

Lithofacies of the Black Hand Sandstone include massive gravel, Regressive Sandstones in the Central Appalachian Basin gravel with intraclasts, and medium- to coarse-grained sand- A thick, coarse-grained sandstone occurs near the top of stone. Interpreted architectural elements (Miall, 1985) for these the Lower Mississippian succession in the central Appalachian lithofacies include channel lags, gravel bars, dunes, and trans- Basin. This sandstone is known by several names, including verse bars that formed in a braided-stream setting (Matchen and the Burgoon Sandstone in Pennsylvania (and the correlative Kammer, 2006, their Tables 1 and 2). The contact between the Purslane Sandstone of Maryland) (Brezinski, 1999), and the Black Hand Sandstone and the underlying Cuyahoga Forma- drillers’ informal “Big Injun” sandstone (Vargo and Matchen, tion is sharp and scoured, and large (up to 1 m) intraclasts of the 1996) of the subsurface in West Virginia (Fig. 1). Regional Cuya hoga Formation are incorporated into overlying conglom- stratigraphic cross sections produced for this study show that eratic sandstone. Limited paleocurrent data and the geographic the Black Hand Sandstone occupies the same lithostratigraphic distribution of the Black Hand Sandstone suggest that the paleo- position as the Big Injun and Burgoon sandstones (Fig. 2). The river fl owed from the southeast to the northwest (Holden, 1942; base of the Burgoon/Big Injun sandstone in northern West Vir- Ver Steeg, 1947; Hyde, 1953; Kittredge and Malcuit, 1985). ginia is at approximately the same elevation above the top of the Matchen and Kammer (2006) hypothesized that the paleoriver Berea Sandstone as is the base of the Black Hand Sandstone in fl owed to the Michigan Basin, where it deposited the early Ohio. In southwestern Pennsylvania, the Burgoon Sandstone is Osagean Marshall Sandstone (Richardson, 2006a, 2006b) (Fig. 1). 25–90 m thick and “exhibits abundant cross-bedding, basal lag The age of the Black Hand Sandstone is constrained deposits, clay galls, plant fossil debris, scour and fi ll sequences, between latest Kinderhookian and earliest Osagean based on sole markings, and other features typical of fl uvial sandstones” the age of marine invertebrates and miospores in the surround- (Harper and Laughrey, 1987, p. 16). ing rocks. The underlying Cuyahoga Formation is mostly, if not Although the Big Injun sandstone does not crop out, litho- entirely, Kinderhookian. The overlying Logan Formation is early stratigraphic correlation to the Burgoon Sandstone (Harper and Osagean in age based on biostratigraphic data from ammonoids, Laughrey, 1987) and the Black Hand Sandstone (Fig. 2) suggests brachio pods, conodonts, and miospores reviewed in Matchen and that it is fl uvial in origin as well. Reports from the subsurface of Kammer (2006). Ammonoids from the Logan Formation have West Virginia indicate coarse-grained fl uvial facies within the Big previously been assigned a Kinderhookian age (Manger, 1971; Injun sandstone (Hohn et al., 1993; Vargo and Matchen, 1996). Manger et al., 1999), but more recent work indicates that these Based on the lithostratigraphic correlations, we hypothesize that taxa are Osagean in age (Sandberg et al., 2002; Work and Manger, all these sandstones were deposited during the Kinderhookian- 2002; Work and Mason, 2003). Miospores from the Logan For- Osagean and Tn2-Tn3 boundary interval, and their bases are mation are from the PC (Spelaeotriletes pretiosus-Raistrickia likely time correlative with SB2 beneath the Black Hand Sand- clavata) Biozone, which ranges from the late Tn2 to early Tn3 stone (Fig. 1). in Europe (Higgs et al., 1988; Clayton et al., 1998). Manger et al. Biostratigraphically, how well constrained is the time of (1999) interpreted the Logan Formation as late Kinderhookian deposition for these sandstones? The Marshall Sandstone of the in age (Tn2) on this basis, but the miospore zonation also sup- Michigan Basin, which is the inferred marine lowstand wedge ports an early Osagean age (Tn3), which agrees with the recent for the Black Hand Sandstone (Matchen and Kammer, 2006), ammonoid studies. The Black Hand Sandstone is inferred to have contains miospores interpreted as early Osagean (Richard- been deposited during the interval represented by the two missing son, 2006b). The Black Hand Sandstone apparently can be conodont biozones in the Mississippi Valley. dated to the Kinderhookian-Osagean boundary, as sum- To better understand the mechanisms that produced the marized already. The Burgoon Sandstone has been dated as Kinderhookian-Osagean unconformity and the incised-valley-fi ll Osagean-Meramecian in age on the basis of the plant fossil Black Hand Sandstone, the time available to produce these fea- Triphyllopteris (Read, 1955; Scheckler, 1986; Brezinski, tures must be estimated. The duration of the Tournaisian has been 1999), which in Europe ranges from the late Tournaisian estimated at either 11 m.y. (Jones, 1996) or 14 m.y. (Gradstein through Visean (Read and Mamay, 1964; Wagner, 1984). How- et al., 2004). There are 12 conodont biozones (Lane and Brenckle, ever, recent work (Knaus, 1994, 1995) has determined that the 2005) spanning the Tournaisian; thus, each conodont biozone is Appalachian specimens are not Triphyllopteris, rendering the ~1 m.y. in duration. Therefore, the two missing conodont biozones previous correlation invalid. Until independent palynological at the Kinderhookian-Osagean boundary unconformity in the evidence is available for the age of the Burgoon Sandstone, the Mississippi Valley may represent as much as 2 m.y., or possibly previous age determination of Osagean-Meramecian based on less, of missing time during which the Kinderhookian-Osagean the Triphyllopteris zone is unreliable (Knaus, 1994, p. 112). In unconformity was formed and the Black Hand Sandstone was central Pennsylvania, Streel and Traverse (1978) reported that deposited. This is similar to the 2 m.y. duration estimate made the strata beneath the Burgoon Sandstone contained earliest by Saltzman (2001) for the δ13C event at the Kinderhookian- Kinderhookian miospores. Thus, the Burgoon Sandstone may Osagean boundary. This is the best estimate because there are be as old as late Kinderhookian, but it sits unconformably on no reported radiometric dates specifi cally at the Kinderhookian- the underlying sediments (Harper and Laughrey, 1987), mak- Osagean boundary (Gradstein et al., 2004). ing a younger Tn2-Tn3 age possible. Evidence for eustasy: Response to late Tournaisian glaciation? 267

MAPPING EARLY MISSISSIPPIAN orogeny (Craig and Connor, 1979). We consulted previous paleo- SEA-LEVEL CHANGES geographic reconstructions, including those of Craig and Varnes (1979, pl. 12) and Gutschick and Sandberg (1983), but these were We constructed new maps to show the changing positions of generalized and did not resolve changes in paleogeography for the shorelines, a proxy for sea-level change, during the early Missis- three time slices shown here (Fig. 3). They were also produced sippian in the conterminous United States. Three intervals were prior to the COSUNA charts used in this study (1983–1987). mapped: (1) the Kinderhookian (Tn1b-Tn2 interval) maximum Many areas of the U.S. interior lack Mississippian rocks marine transgression (Fig. 3A); (2) the Kinderhookian-Osagean because of post–early Mississippian uplift and erosion, which and Tn2-Tn3 boundary (Fig. 3B); and (3) the early Osagean (Tn3) must be considered when reconstructing early Mississippian maximum marine transgression (Fig. 3C). paleogeography. Based on timing of uplifts, many of these areas These maps were constructed using COSUNA (Correla- can be assumed to have been covered by early Mississippian seas tion of Stratigraphic Units of North America) charts (Ballard (Fig. 3). Late Mississippian to Permian uplift associated with the et al., 1983; Hills and Kottlowski, 1983; Bergstrom and Morey, Appalachian-Ouachita orogeny produced or reactivated the Ozark 1984; Hintze, 1985; Patchen et al., 1985a, 1985b; Shaver, 1985; Dome (McBride and Nelson, 2000; Hudson, 2002), the Nemaha Mankin, 1986; Adler, 1987; Kent et al., 1988). Each chart lists anticline (Kansas-Nebraska) (Merriam, 2005), central Kansas stratigraphic data distributed across several columns, and each uplift (Rascoe and Adler, 1983), the Cincinnati and Kankakee column represents a geographic area within a single U.S. state. arches (Root and Onasch, 1999), and the Nashville Dome (Kolata Each data point plotted on the maps is centered in the area for its and Nelson, 1990). The Transcontinental arch (extending through column on the chart (see Fig. 3 caption for explanation of sym- New Mexico, Colorado, Nebraska, South Dakota, and Minnesota) bols). Thus, the data points are generalized in their locations, but is a series of highs and lows (or sags) (Gutschick and Sandberg, they are sufﬁ cient to show major patterns on a continental scale. 1983, their Figs. 5 and 6) associated with Phanerozoic reactiva- The designation of marine versus nonmarine rocks was tion of basement zones of weakness (Carlson, 1999, 2004). Craig based on the paleontologic and stratigraphic literature for the and Varnes (1979, pl. 12) showed an extensive marine connec- Kinderhookian and Osagean formations listed on the COSUNA tion across the Transcontinental arch in their paleogeographies for charts. Data points on the maps (Fig. 3) are designated as marine both the Kinderhookian and Osagean. if fossils include typical marine organisms such as crinoids, corals, brachiopods, bryozoans, cephalopods, trilobites, cono- DISCUSSION donts, etc. Nonmarine rocks lacked such fossils and included typical terrestrial features such as plant fossils, coals, or red Interpretation of Sea-Level Maps beds. Primary sources for information on the depositional environments of individual formations are the chapters on each state The Kinderhookian map (Fig. 3A) shows the maximum in U.S. Geological Survey Professional Paper 1110 (1979), The extent of marine rocks during either the early (Tn1b) or the late Mississippian and Pennsylvanian (Carboniferous) Systems in Kinderhookian (Tn2). The epicontinental sea was widespread the United States; the regional chapters in Craig and Connor throughout the eastern and western United States. A large emer- (1979); and Dutro et al. (1979). Depositional environments gent area was situated over parts of Colorado, New Mexico, and of Lower Mississippian formations in the Appalachian Basin Texas. The central Kansas uplift appears to have been emergent, are summarized in Bjerstedt and Kammer (1988), Carter and as well as a forebulge of the Antler orogeny in Utah. Kammer (1990), Matchen and Kammer (2006). Marine rocks are less extensive on the Kinderhookian- Shorelines were drawn on each map with a hachured bound- Osagean boundary map (Fig. 3B), which we interpret as resulting ary line between areas of marine deposition and nondeposition from the widespread unconformity associated with a sea-level in the central and western United States, or between marine fall. In the northeastern United States, the shoreline receded west- and nonmarine rocks in the eastern United States. Positions of ward from a combination of siliciclastic progradation (Bjerstedt the interpreted shorelines are approximate and are dependent and Kammer, 1988; Matchen and Kammer, 1994) and forced on the density of data points; they are more precise where data regression (Matchen and Kammer, 2006). In the southeastern points were denser. Eastern and western shorelines of the Mis- United States, the Kinderhookian emergent area in Alabama and sissippian epicontinental sea were constrained on all three maps Mississippi expanded into Georgia and Tennessee. In the central by the Appalachian orogen in the east and the Antler orogen in United States, a large peninsula formed over parts of Iowa, Illi- the west (Craig and Varnes, 1979). From Maine to Minnesota, nois, Missouri, and Kansas, presumably from a fall in sea level. the northern shoreline was constrained by the northern limit of The Kinderhookian emergent area in Colorado, New Mexico, Mississippian rocks. The Mississippian sea extended north into and Texas expanded further into Colorado and Texas. The west- Canada from North Dakota and Montana and south into Mexico ern seaway was less affected by the fall in sea level where most from Texas and New Mexico (Craig and Connor, 1979). There is sections are conformable (Chen et al., 1994; Saltzman, 2002a). little data control along the Gulf of Mexico coastal plain because Foreland basin development associated with the Antler orogeny of destruction of any original Mississippian rocks by the Ouachita on the western edge of the craton may have kept the western sea

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Figure 3 (on this and following page). Sea-level, or shoreline, maps during early Mississippian (Miss.) time in the conterminous United States, based on COSUNA (Correlation of Stratigraphic Units of North America) charts (Ballard et al., 1983; Hills and Kottlowski, 1983; Bergstrom and Morey, 1984; Hintze, 1985; Patchen et al., 1985a, 1985b; Shaver, 1985; Mankin, 1986; Adler, 1987; Kent et al., 1988). (A) Maximum extent of marine rocks at any time during the Kinderhookian (Tn1b-Tn2). (B) Extent of marine rocks at the Kinderhookian-Osagean (K-O) (Tn2-Tn3) boundary. Areas on the maps where Mississippian sedimentary (sed.) rocks are absent are denoted by a cross (+). These data points indicate Mississippian rocks were either never present or were subsequently eroded. A ﬁ lled circle (•) indicates that rocks are missing for the mapped interval, but younger Mississippian sedimentary rocks are present, thus indicating that the missing rocks were either never deposited or were eroded during the Mississippian, rather than later. An open square ( ) indicates that marine rocks are present for the mapped interval. Two other data types include an asterisk (Ã) for the latest Kinderhookian marine Gilmore City Limestone on the Kinderhookian-Osagean boundary map, and a solid triangle (S) for Osagean nonmarine rocks. Evidence for eustasy: Response to late Tournaisian glaciation? 269

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Early Osagean marine rocks ? Early Osagean nonmarine rocks ? C Osagean rocks absent, but younger ? Miss. rocks present Miss. sed. rocks absent 250 0 km ? Stratigraphy or age of rocks poorly resolved 125 500 120° W 110° 100° 90° 80° W

Figure 3 (continued). (C) Maximum extent of marine rocks during the early Osagean (Tn3).

deep enough to avoid emergence during the fall in sea level at sea level on a continental scale is too rapid for any known tec- the Kinderhookian-Osagean boundary, although a large foreland tonic processes and strongly implies large-scale changes in ice bulge emerged in Utah (Giles, 1996) (Fig. 3B). volume on the planet (Abreu and Anderson, 1998; Coe, 2003). In the early Osagean (Fig. 3C), marine rocks were more Regional changes in sea level may have involved tectonic or extensive than in the Kinderhookian (Fig. 3A), and much progradational factors, but such large-scale areal changes docu- more extensive than at the Kinderhookian-Osagean boundary mented by the maps of this study are interpreted as too rapid to (Fig. 3B). The position of the eastern shoreline in Pennsyl- have had a signiﬁ cant tectonic cause. vania and West Virginia is based on previous studies (Harper and Laughrey, 1987; Bjerstedt and Kammer, 1988) combined Regression at the Kinderhookian-Osagean Boundary with the COSUNA chart (Patchen et al., 1985a). The shoreline later prograded westward, reaching the Illinois Basin in the late North American Midcontinent Osagean (Kepferle, 1977; Matchen and Kammer, 1994). In the Witzke and Bunker (1996, their Fig. 8) placed a sequence southeastern United States, the Kinderhookian-Osagean emer- boundary at the Kinderhookian-Osagean boundary in southeast gent area in Alabama, Mississippi, Georgia, and Tennessee was Iowa. They recognized sub-Burlington erosional beveling of the submerged. The large Kinderhookian-Osagean peninsula in the Wassonville Formation (Chouteau Group equivalent). Witzke central United States was submerged as the early Osagean Bur- and Bunker (2002, 2005) further commented that this seemed lington shelf formed over Iowa, Illinois, Missouri, and Kansas anomalous because the beveling is in an offshore direction, and (Lane, 1978). The emergent area centered over New Mexico strata are thicker and more complete toward the Transconti- was smaller than during the Kinderhookian, and much smaller nental arch in northwest Iowa, where the latest Kinder hookian than at the Kinderhookian-Osagean boundary. Gilmore City Limestone occurs. They suggested the cause was Viewed in combination, the three maps (Fig. 3) clearly either structural upwarping of the southeast Iowa area before show a large-scale regression at the Kinderhookian-Osagean deposition of the Burlington Limestone, or submarine erosion. boundary that was bracketed by higher sea levels in both They did not suggest a eustatic drop in sea level. Brenckle the Kinderhookian and Osagean. As argued previously, the and Groves (1986) reported that foraminifera from the earli- Kinderhookian-Osagean boundary interval may have spanned est Osagean Humboldt oolite, which immediately overlies the as much as 2 m.y., a relatively short period of time difﬁ cult to Gilmore City Limestone in north-central Iowa, were previ- resolve more precisely. Such a rapid fall and subsequent rise in ously unknown east of the Transcontinental arch, indicating 270 Kammer and Matchen

their probable migration from the western epeiric sea across Regression at the Global Tn2-Tn3 Boundary Nebraska. This eastward extension of the western part of the epicontinental sea, expressed as the Gilmore City Limestone, The Kinderhookian-Osagean boundary is equivalent to the can be seen along the west side of the Midcontinent peninsula global Tn2-Tn3 boundary (Ross and Ross, 1985; Jones, 1996). on the Kinderhookian-Osagean boundary map (Fig. 3B), and it The fall in sea level at the Tn2-Tn3 boundary has been interpreted explains the more complete section in northwest Iowa. as a global event (Ross and Ross, 1985; Isaacson et al., 1999). A major unconformity is present in the middle to late Tournaisian Appalachian Basin of the Arabian Platform (Haq and Al-Qahtani, 2005). In Belgium, Incision of the Black Hand Sandstone paleovalley and sub- the boundary is the sequence boundary at the Hastarian-Ivorian sequent deposition of sandstone fi ll within the valley require a boundary (Hance et al. 2002). In Moravia (Czech Republic), 60 m fall in relative sea level to produce the incision and sequence the boundary is marked by regression and microfaunal changes boundary (SB2). The Black Hand Sandstone lies between two thought to be associated with global cooling (Kalvoda, 1989, 1991, marine units, the Cuyahoga and Logan Formations (Fig. 1), which 2002). In northeast Siberia, Swennen et al. (1986) recognized a together exceed 250 m in thickness in central Ohio (Fig. 2). To regional fall in sea level just below the Tn2-Tn3 boundary associ- produce this stratigraphic package, incision must have been fol- ated with anhydrite pseudomorphs indicating evaporite deposition. lowed by a rebound in sea level to fi ll the valley with terrestrial The sea-level fall at the end of Tn2 is also recognized in Germany sediment and deposit marine sediments above. Based on the bio- (the Rhenish area) and in south China (Isaacson et al., 1999). stratigraphic estimates, incision, fi ll, and transgression must have occurred within a 2 m.y. period, or less. Glacial Eustasy? If tectonic uplift was responsible for incision of the Black Hand Sandstone paleovalley, sediments should be substantially These several lines of evidence all point to a clear record thinner in Ohio, rather than representing the thickest Lower Mis- of eustasy at the Kinderhookian-Osagean and Tn2-Tn3 bound- sissippian depocenter in the central Appalachian Basin (Matchen ary on several continents, particularly North America, where the and Kammer, 2006, their Fig. 4). Structure contour maps drawn data are most abundant (Fig. 3). Although the global extent of the on the underlying Berea Sandstone show a broad ramp dipping sequence boundary at the Kinderhookian-Osagean and Tn2-Tn3 eastward into the basin (Matchen and Kammer, 2006, their Fig. 3) has long been recognized (Ross and Ross, 1985), a clear argu- and no evidence for uplift in eastern Ohio, beneath the Black ment for glacial eustasy previously has not been made, although Hand Sandstone. The combination of the predominantly marine Rygel et al. (2007) argued that the record of Tournaisian eustasy origin of Lower Mississippian rocks in Ohio with the absence of is supportive of glaciation. evidence for uplift requires an explanation other than tectonics for incision of the Black Hand Sandstone paleovalley. Diamictites If tectonic uplift as the driver for incision is excluded, we are left with the interplay of tectonics and glacio-eustasy. The Direct evidence for a middle to late Tournaisian ice age has Black Hand, Big Injun, and Burgoon sandstones represent an recently been confi rmed from miospore dating of diamictites in infl ux of coarser-grained, fl uvial sediments to the Appalachian the Solimões Basin of Brazil (Caputo et al., 2006a, 2006b, this foreland (Fig. 2). The high sediment supply was probably the volume). Diamictites in the Jaraqui Member of the Jandiatuba result of postorogenic rebound of the hinterland. In the post- Formation from wells in the Juruá subbasin contain miospores orogenic phase, subsidence had slowed considerably, produc- of the BP (Spelaeotriletes balteatus-Rugospora polyptycha) Bio- ing a foreland ramp (Castle, 2000) and allowing coarse-grained zone and PC biozones of western Europe (Caputo et al., this vol- sediment to spread across the region. Increasing sediment supply ume). The BP biozone is Tn2a-Tn2b (late Kinderhookian) in age, may produce a sequence boundary, and it is a primary control and the PC biozone is Tn2c-Tn3a,b (Kinderhookian-Osagean on the architecture of sedimentary basin fi ll because it alters the boundary) in age (Higgs et al., 1988). Caputo et al. (this volume) amount of accommodation space available for sediment deposi- report that these diamictites occur over 300 km in the subsurface tion (Posamentier and Allen, 2000, p. 19–21); however, it does and directly overlie Famennian-age diamictites. Caputo et al. not produce valley incision. (this volume) also discuss other diamictites of apparent middle to The 60 m of relief on the paleovalley requires at least early late Tournaisian age in Bolivia and Argentina. an equal magnitude of relative sea-level fall. Presumably, a Crowell (1999) reported Tournaisian-age tillites from Libya. continental-scale fall and rebound of sea level over a brief time Four episodes of Early Carboniferous glacial deposits in Tibet period (~2 m.y.) is indicative of a global eustatic event. Such an are bracketed between marine rocks of early Tournaisian and event would be linked to changing ice volumes because this is the Bashkirian ages (Garzanti and Sciunnach, 1997). These glacial only mechanism capable of producing a rapid global change in deposits are presumably Visean and Serpukhovian in age, but a sea level over a short period of time. Glacio-eustasy may be up to middle to late Tournaisian age for at least the oldest deposit can- 1000 times more rapid than tectono-eustatic mechanisms (Plint not be ruled out without a defi nitive biostratigraphic study, which et al., 1992; Coe, 2003, p. 101). is lacking (Garzanti and Sciunnach, 1997). Evidence for eustasy: Response to late Tournaisian glaciation? 271

Stable Isotopes of Carbon and Oxygen 2. Valley incision in Ohio up to 60 m at the Kinderhookian- Osagean boundary followed by an early Osagean transgression Strong positive anomalies for both oxygen and carbon iso- (Matchen and Kammer, 2006). topes occur in brachiopod shells and marine carbonates from the 3. The sequence boundary, SB2, associated with valley latest Kinderhookian of North America (Mii et al., 1999; Saltz- incision in Ohio can be traced along the base of the Burgoon, man et al., 2000; Saltzman, 2002a) and at the Tn2-Tn3 bound- Big Injun, and Purslane sandstones throughout the central ary in western Europe (Bruckschen and Veizer, 1997). During Appalachian Basin, suggesting a forced regression at this time the Kinderhookian, δ18O values rose ~6‰, and δ13C values rose (Figs. 1 and 2). ~5‰. Values decreased again in the Osagean, although they did 4. Sea-level maps for the Kinderhookian, Kinderhookian- not fall to the levels of the early Kinderhookian. An increase Osagean boundary interval, and the early Osagean in the in δ18O values would be associated with some combination of conterminous United States indicate extensive regression and global cooling or sequestration of lighter oxygen in glacial ice unconformity at the Kinderhookian-Osagean and Tn2-Tn3 (Hudson, 1977; Marshall, 1992). Parallel positive anomalies of boundary (PC biozone) (Fig. 3). both oxygen and carbon isotopes in conodont apatite have been 5. Global evidence for regression in the form of an uncon- cited as evidence for global cooling in the early late Tournaisian formity, or correlative sequence boundary, at the Tn2-Tn3 bound- at the upper crenulata-isosticha conodont biozones (Buggisch ary has been reported in Saudi Arabia, Belgium, Czech Republic, and Joachimski, 2006). Germany, western Russia, Siberia, and China (Ross and Ross, Saltzman et al. (2000) and Saltzman (2002a) reported a very 1985; Swennen et al., 1986; Kalvoda, 1989, 1991, 2002; Isaac- strong δ13C anomaly of up to +7.1‰ Peedee belemnite (PDB) son et al., 1999; Hance et al., 2002; Haq and Al-Qahtani, 2005). that spans the latest Kinderhookian and earliest Osagean in lime- 6. Strong positive anomalies in both δ13C and δ18O indi- stones from Idaho and Nevada. Increased δ13C values indicate cate global cooling at or near the Kinderhookian-Osagean and a shift in the global carbon cycle that may have been related to Tn2-Tn3 boundary, which is consistent with the hypothesis of enhanced organic carbon burial associated with cooler tempera- glaciation (Bruckschen and Veizer, 1997; Mii et al., 1999; Saltzman tures during glaciation, or sequestration of light organic carbon et al., 2000; Saltzman, 2002a; Buggisch and Joachimski, 2006). in deep-ocean water (Brenchley et al., 1994, 2003; Saltzman Together these data support the hypothesis of a glaciation et al., 2000; Joachimski and Buggisch, 2002; Saltzman, 2003; event that produced a substantial, ~60 m eustatic sea-level fall and Saltzman and Young, 2005). Currently there is debate as to recovery at the Kinderhookian-Osagean and Tn2-Tn3 boundary whether or not the primary environment of organic burial at the spanning an interval of ~2 m.y., or possibly less. The global dis- Kinderhookian-Osagean boundary was marine or terrestrial (Gill tribution and relative rapidity of the event support the hypothesis et al., 2006). Burial of organic carbon would reduce atmospheric of glacial eustasy.

CO2 and contribute to global cooling (Berner, 2003, 2004; Royer et al., 2004). Alternatively, increased δ13C values may have been ACKNOWLEDGMENTS related to weathering of exposed carbonate platforms during regression (Kump et al., 1999; Saltzman, 2002b). Both the West Virginia Geological and Economic Survey Studies have clearly linked high δ13C values with global and the Ohio Geological Survey provided subsurface well data. cooling (Bruckschen et al., 1999; Brenchley et al., 2003; J. Toro, West Virginia University, provided drafting assistance. Saltzman and Young, 2005). Brenchley et al. (2003) found J. Hitzig, Concord University, digitized the well logs for Penn- carbon and oxygen isotope anomalies at the end of the Ordo- sylvania. D. Brezinski, Maryland Geological Survey, and an vician, a time of major Gondwana glaciation (Brenchley et al., anonymous reviewer provided helpful reviews that improved the 1994; Sheehan, 2001), that were similar in magnitude to those manuscript. The editorial efforts of C. Fielding and T. Frank at the end of the Kinderhookian. Saltzman (2002b) reported greatly aided the clarity and focus of the paper. that the three largest positive shifts in δ13C values occurred in the Late Ordovician, at the Silurian-Devonian transition, REFERENCES CITED and in the early Mississippian (Tournaisian), all of which were apparently associated with a eustatic fall in sea level caused Abreu, V.S., and Anderson, J.B., 1998, Glacial eustasy during the Cenozoic: by Gondwanan glaciation. Sequence stratigraphic implications: American Association of Petroleum Geologists Bulletin, v. 82, p. 1385–1400. Adler, F.J., 1987, Mid-Continent Region: Correlation of Stratigraphic Units CONCLUSIONS of North America (COSUNA) Project (folded chart): Tulsa, Oklahoma, American Association of Petroleum Geologists. Ballard, W.M., Bluemle, J.P., and Gerhard, L.C., 1983, Northern Rockies/ Both direct and indirect evidence for glacial eustasy at the Williston Basin Region: Correlation of Stratigraphic Units of North Kinderhookian-Osagean and Tn2-Tn3 boundary consists of: America (COSUNA) Project (folded chart): Tulsa, Oklahoma, American 1. Middle to early late Tournaisian (BP and PC biozones) Association of Petroleum Geologists. Berg, T.M., 1999, Chapter 8: Devonian-Mississippian transition, in Schultz, diamictites in South America (Caputo et al., 2006a, 2006b, C.H., ed., The Geology of Pennsylvania: Pennsylvania Geological Survey this volume). Special Publication 1, p. 129–137. 272 Kammer and Matchen

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