682


Journal of Paleontology 92(4):681–712


Delta prograded from present-day east and northeast, and the Fort Payne Formation prograded from present-day east and southeast. Both advanced as clinoforms with recognizable platform, slope, toe-of-slope, and basinal facies. (Swann et al., 1965; Lewis and Potter, 1978; Ausich and Meyer, 1990; Greb et al., 2008). The time-transgressive nature of the prograding Borden and Fort Payne formations has been documented in several studies (e.g., Ausich et al., 1979; Ausich and Meyer, 1990; Leslie et al., 1996; Richardson and Ausich, 2004), as has the sequence stratigraphy and facies architecture (Lewis and Potter, 1978; Ausich and Meyer, 1990; Khetani and Read, 2002; Krause et al., 2002; Krause and Meyer, 2004; Greb et al., 2008). The time of interest for the present study is the early Viséan


Figure 1. County occurrences of crinoids from the Fort Payne Formation and coeval strata from north-central Kentucky to northern Alabama (Cumb.=Cumberland; Lawr.=Lawrence; Pick.=Pickett).


outcrop belt from north-central Kentucky to northeastern Alabama (Fig. 1). Revisions resulting from this study include description of one new species, one species is reassigned to a different genus, and thirteen species are designated as junior synonyms.


Geologic setting


For being part of the ‘stable’ craton, the Eastern Interior Seaway of Laurentia was a dynamic setting during the early and middle Mississippian. The Tournaisian was punctuated by a glacial epoch that resulted in the draining of epicontinental seas from much of middle and eastern Laurentia (Kammer and Matchen, 2008). Following the glacial epoch (by at least the late Tournaisian) epicontinental seas were re-established from the continental arch to the emerging Appalachian highlands (Matchen and Kammer, 2006). The Eastern Interior Seaway, an epicontinental basin, ran north-south encompassing much of present-day Tennessee, Kentucky, Illinois, and Indiana. Maxi- mum water depths in this epicontinental basin are estimated to have exceeded 90m(Sedimentation Seminar, 1972; Ausich and Meyer, 1990). The western margin of this basin was flanked by the Burlington Limestone-Keokuk Limestone carbonate ramp (H.R. Lane, 1978), and the eastern margin was dominated by two separate and sometimes overlapping, prograding sediment wedges: the mixed carbonate-siliciclastic Fort Payne Formation and the siliciclastic Borden Group (or Formation). The Borden


(late Osagean) (Ausich and Meyer, 1990; Leslie et al., 1996; Krivicich et al., 2013) and is represented by a variety of epi- continental basinal and toe-of-slope facies (Lewis and Potter, 1978). During this time, recognized in present-day outcrops and subsurface stratigraphy, the toe-of-slope and basinal facies of the Fort Payne Formation extended along a line from north- central Alabama to south-central Kentucky (with the most sig- nificant exposures in south-central Kentucky and north-central Tennessee) (Krivicich et al., 2013) (Fig. 1). The Muldraugh Member of the Borden Formation in central and north-central Kentucky represents the platform facies that is time-equivalent of the toe-of-slope Fort Payne facies in south-central Kentucky (Lewis and Potter, 1978; Greb et al., 2008) (Fig. 2). Farther north, the early Viséan Borden delta is represented by prodeltaic sediments of the New Providence Shale in north-central Kentucky and southern Indiana (Kammer, 1984, 1985), delta slope facies of the Spickert Knob Formation in southern Indiana (Ausich et al., 1979; Rexroad and Lane, 1984) and the delta platform facies (Edwardsville Formation) in southern (Monroe County) and central (Montgomery County) Indiana (Lane, 1973; Ausich and Lane, 1980; Ausich, 1983) (Fig. 2). On the western margin of the basin, the early portion of the early Viséan is represented by the Keokuk Limestone, whereas siliciclastic sediments overrode the northern reaches of the western basin margin by later early Viséan time, yielding the lower part of the Warsaw Formation (Kammer et al., 1990). New collections reported here are largely from south-


central Kentucky and north-central Tennessee, which are particularly instructive because in most cases the depositional settings of fossiliferous localities are well constrained (Ausich and Meyer, 1990; Meyer et al., 1995; Greb et al., 2008). Batocrinids and other faunal elements occur in both auto- chthonous and allochthonous Fort Payne Formation facies (Ausich and Meyer, 1988, 1990, 1992; Meyer et al., 1989; Ausich et al., 1997; Meyer and Ausich, 1997; Rhenberg et al., 2016; Thompson and Ausich, 2016). The Fort Payne Formation is a mixed carbonate-siliciclastic depositional system with contemporaneous, laterally contiguous facies. The most promi- nent autochthonous facies are carbonate buildups, crinoidal packstone buildups, and wackestone buildups (Ausich and Meyer, 1990) (Fig. 3). An autochthonous green shale facies and the fauna that lived in incised channels (the sediment fill of the channels was allochthonous) were autochthonous. Allochthonous facies were the background siltstone facies,


sheetlike packstones, deposition that filled in the channel-form packstones, and the Jabez Sandstone Member. The distinction


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