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

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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 uncon- formity 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 fur- ther 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, pre- sented 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. Mississippi Michigan Central West Virginiad Pennsylvaniag,h,i 1 2 3 Valley Section Basina Ohiob,c Southe,f Centrale,f Northe,f Keokuk Limestone No Section Michigan Visean Osagean Formation ? ?? c Burlington SB3 Limestone Rushville Member Tn3 Vinton Member s. Allensville en L Maccrady n Gl Member Fer Formation Meppen Byer Member SB3 Logan Fm. ab Berne Member Marshall Burgoon c Black Hand “Big Injun” “Big Injun” Sandstone Sandstone SB2 Sandstone sandstones sandstone SB2 ? ? Tn2 Tournaisian b Cuyahoga Chouteau Coldwater “Weir” Mississippian Shale Formation sandstones a Group Hannibal Rockwell Member Kinderhookian Formation Price Formation Sunbury Price Formation Riddlesburg Riddlesburg Rockwell Formation Tn1b Shale Sunbury Shale Glen Park Ls. Sunbury Shale Shale Shale Cloyd Cussewago Berea Sandstone Berea Sandstone Conglomerate Sandstone ? SB1 ?SB1 Oswayo Fam. Louisiana (part) Dev. Limestone Sandstone Figure 1. Lower Mississippian
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