Ausich et al.—Fort Payne Formation Batocrinidae


683


Figure 2. North-South cross section of early and middle Viséan strata from southern Indiana to north-central Kentucky. Tournaisian conodonts that were recovered from the basal meter of the Fort Payne Formation indicate a highly condensed interval (Leslie et al., 1996). Tournaisian strata are designated (although not to scale) with a T.


between autochthonous and allochthonous facies is based on a combination of sedimentologic, stratigraphic, and taphonomic criteria. These interpretations were strengthened by the demonstration that each of the autochthonous facies supported statistically different crinoid and blastoid faunas (Krivicich et al., 2014). Further, partially complete echinoids are only present in facies interpreted to have been autochthonous (Thompson and Ausich, 2016). The siltstone and sheet packstone facies comprise the vast


majority of the volume of the Fort Payne sediments. The auto- chthonous facies are a small fraction of the total volume of the Fort Payne Formation and tend to co-occur in restricted geographic clusters, presumably along the toe-of-slope near the mouths of submarine canyons (Ausich and Meyer, 1990; Greb et al., 2008).


Regional distribution of crinoids


As noted above, early Viséan facies vary from carbonate ramps in Iowa, Illinois, and Missouri, to deltaic settings in Indiana, to mixed carbonate-siliciclastic settings of Kentucky, Tennessee, and Alabama. Because early Viséan crinoids have been well documented across this entire region (Hall, 1858, 1859a, b, 1860; Lane, 1973; Ausich and Lane, 1982; Kammer, 1984; Ausich and Kammer, 1990, 1991a, b, 1992; Ausich and Meyer, 1992; Kammer and Ausich, 1992, 1993, 1994, 1996; Ausich et al., 1997, 2000; Meyer and Ausich, 1997; Krivicich et al., 2013, 2014; Rhenberg et al., 2016), the paleogeographic dis- tribution of batocrinds can be evaluated with a considerable degree of confidence. During the early Viséan (late Osagean), the distribution of individual genera and species through this region was variable.


Abatocrinus, Alloprosallocrinus, Eretmocrinus, Macrocrinus, and Uperocrinus occurred through the region in both silici- clastic and carbonate facies and in both shallow- and deep-water settings. As noted by Krivicich et al. (2014), one of the most striking aspects of crinoid distributions is that all species of the genus Dizygocrinus were confined to shallower water facies in the Eastern Interior Basin. Dizygocrinus was present in the carbonate ramp setting of the Keokuk Limestone as well as the same basic setting when siliciclastics overtopped the Keokuk ramp (lower part of the Warsaw Formation). Dizygocrinus also occurred in various delta platform facies of the Borden Delta (Edwardsville Formation; Van Sant, 1964; Ausich, 1983), as well as in the Muldraugh Member of the Borden Formation, which was the platform facies equivalent of the Fort Payne Formation (Ausich et al., 2000). However, Dizygocrinus was absent from toe-of-slope facies of the New Providence Shale (Kammer, 1984) and the Fort Payne Formation. Other genera also had more restricted distributions.


Eutrochocrinus is only known from the shallow-water carbo- nates of the Keokuk Limestone on the western portion of the basin. Magnuscrinus only occurred in deeper water settings in the eastern portion of the Eastern Interior Seaway, where it was present in carbonate and siliciclastic settings. Gongylocrinus is only known from three specimens, so any statements about its environmental preferences are tentative. However, the only early Viséan species of this genus occurred in a channel sand- stone facies in the shallow-water delta platform facies of the Edwardsville Formation in Indiana. At the species level, only Abatocrinus steropes (Hall,


1859a), Alloprosallocrinus conicus Casseday and Lyon, 1862, Macrocrinus mundulus (Hall, 1859a), and Uperocrinus


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