ABSTRACT Zone-diagnostic Middle to Upper Devonian ammonoids and conodonts occur in a sequence of thin carbonate beds in siliciclastic sections along the Allegheny front and northern fold belt of central Pennsylvania. The lowest, in the upper Tully Formation, and the succeeding four in the Harrell Shale, are southward continuations of marker beds long known in the Tully Limestone and overlying basin, slope, and shelf facies of the Genesee Group of New York State. These pelagic beds are Appalachian Basin signals of transgressive condensed intervals within global high-sea-level episodes and are associated with a worldwide biotic overturn in the tropical marine realm. The Upper Givetian Tully Pharciceras amplexum bed has close lithic and faunal equivalents in the Taghanic biocrisis interval in Morocco and southern Europe. The Lower Frasnian styliolinid upper Genundewa Limestone, with the entry of Manticoceras , and, in the succeeding dark West River Shale, the Bluff Point Bed, with the entry of late Koenenites and early palmatolepid conodonts, are Appalachian highstand signals of the worldwide Timan bioevent transgression recognized in Western Australia, the Russian Platform, southern Europe, Morocco, western Canada, and now Pennsylvania. The widespread occurrences of discrete ammonoid beds, even in the more proximal or shoreward sedimentary settings of the Catskill Delta, reinforce the view that they accumulated under conditions of sequestered sediment supply when transgressions flooded the newly vegetated and deep-root-forested delta flats. As such, they overprinted or interrupted the westward progradation of siliciclastic sediments generated by mountain-building tectophases of the Acadian orogeny. The Lower Frasnian ammonoid Epitornoceras dennisoni n. sp., described herein, from the Crosby Beds in the Harrell Shale at Milesburg, Pennsylvania, is named in honor of John Dennison.

ABSTRACT This study examines the usefulness of accommodation plots (Fischer plots) as a means of correlating mixed carbonate-siliciclastic strata in the subsurface. Fischer plots have been widely used to extract accommodation changes from carbonate platforms, but there are few published studies of siliciclastic or mixed carbonate-siliciclastic environments. The Middle Devonian of the Appalachian Basin is penetrated by thousands of wells, is exposed in numerous exceptional outcrops, and is an excellent place to test the usefulness of accommodation history plots as correlation tools. In the past, researchers have used cores, well cuttings, well logs, and outcrop gamma-ray profiles to correlate between outcrop and subsurface data, but all these methods have their limitations. Gamma-ray logs for wells penetrating the Middle Devonian from eight locations, from Preston County in the east to Wetzel County, West Virginia, in the west, were used in this study. Accommodation cycle thicknesses were measured from gamma-ray logs, printed at a vertical scale of one inch per ten feet (2.5 cm/3 m). The accommodation cycle thickness data were entered into Antun Husinec’s FISCHERPLOTS program to produce accommodation plots. Next, well-documented, outcrop-based sequence stratigraphy was used to help interpret the results of the accommodation plots. This study demonstrates that using accommodation plots is a novel way of overcoming the uncertainties and biases of other methods. The use of this approach in other mixed carbonate-siliciclastic successions with abundant subsurface data would help to demonstrate that Fischer plots are a novel and useful approach that can help remove many of the uncertainties and biases encountered in stratigraphic correlation.

The Catskill Delta complex is interpreted to be the aggregate of delta-alluvial wedges and associated facies that developed in the central Appalachians and on adjacent parts of the stable craton from the Early-Middle Devonian transition to the Middle Mississippian during the Acadian orogeny. Recent interpretations of the Acadian orogeny suggest that it probably was related to oblique convergence and transcurrent movement along a major strike-slip fault zone separating the eastern margin of the North American landmass from a linear continental fragment called the Avalon terrane. Distribution of clastic wedges and basinal deposits resulting from this orogeny support a general southwestward progression of orogeny and indicate that the major clastic wedges emanated from areas near promontories on the continental margin during successive phases of Acadian deformation. Three and possibly four such tectophases have been noted. Each tectophase appears to represent increased convergence or possible collision between a specific continental promontory and the Avalon terrane, but some delta development occurred continually along many parts of the orogen in response to each tectophase. The four tectophases are: (1) Collision near the St. Lawrence promontory during the Early-Middle Devonian transition with initiation of the Catskill Delta complex represented by the Needmore and Esopus shales and associated clastics near promontories. (2) Southward migration of deformation and collision near the New York promontory during the Middle Devonian with the development of a large peripheral basin having an east-dipping, western paleoslope. This basin was filled with cyclic delta clastics and carbonates of the Hamilton Group and Tully Limestone. (3) Southward migration of deformation and collision near the Virginia promontory during the Late Devonian to earliest Mississippian accompanied by intense clastic influx of the Genesee-through-Canadaway groups. As a result, the basin was progressively filled from the east so that basinal environments migrated westward out of the peripheral basin and onto adjacent parts of the stable craton. Eventually the basin was filled and a regional west-dipping paleoslope was established. (4) Migration of deformation southward from the Virginia promontory during the Early to Middle Mississippian as basinal environments in cratonic seas were destroyed and Pocono and equivalent clastic wedges essentially filled the epicontinental sea. Middle Mississippian carbonates mark the end of the Acadian orogeny and Catskill Delta complex.

The Tully Limestone is an anomalous unit which interrupts the thick sequence of detrital rocks constituting the Catskill Delta. The Tully disconformably overlies gray shale, grades upward into black shale, pinches out to the west, and grades eastward into a thicker sequence of sandstone and siltstone. Intensive stratigraphic work has delineated several key beds which afford detailed correlation within the formation. Several facies are recognized. Detrital facies include (1) laminated muddy quartz siltstone , with restricted fauna, which records salinity variation and rapid deposition from an active clastic source, and (2) burrowed quartz sandstone , with more diverse fauna, which records slower deposition under more marine conditions with a stabilized clastic source. Carbonate facies indicate protection from clastic influx: (3) abraded calcarenite, containing various abraded and residual grain types, records slow deposition with long-term winnowing and grain battering; (4) chamosite oölite, with evenly coated grains and phosphorite pebbles, records long-term agitation and slow deposition; (5) bedded skeletal calcilutite, forming the greatest part of the Tully, records a quiet marine environment under long-term protection from clastic influx; (6) dark, barren shaly calcilutite records fouling of substrate and increase in fine clastic influx. Three facies are associated with calcilutite mounds: (7a) pure massive mound calcilutite , with smooth-bottomed sparry “stromatactis” and a distinct slender-tabulate-coral assemblage, records rapid local accumulation of carbonate mud; (7b) sparsely fossiliferous, bedded backmound calcilutite , partly surrounded and overridden by the mound, records a quiet, perhaps lagoonal environment on one side of the elongate mound; (7c) encrinite records proliferation of pelmatozoans along the opposite side of the mound. Deposition of the Tully Limestone was controlled by contemporaneous structures at its east end where an anticline, followed by a down-to-the-east fault (or monocline), formed a clastic trap to the east and acted as barriers to the major westward spread of Catskill Delta clastics. After an initial period of submarine nondeposition, the western protected area became a site of lime-mud accumulation. The pure calcilutite mounds (7) at one of the northernmost New York exposures indicate a northern source of lime mud, probably in a shoal abounding with carbonate-secreting organisms along the west side of the nonorogenic Adirondack Dome, also protected by the clastic trap. Supporting this source direction is the southward trend of decreasing purity of the limestone through Pennsylvania, where the Tully eventually becomes calcareous shale. An erosional unconformity divides the Tully in New York into two distinct members (Lower and Upper) which underwent slightly different histories. The Lower Member developed west of a rising anticline, which blocked major eastern clastic influx but shed limited sediments west, resulting in alternate deposition of laminated muddy siltstone (1) when active, and burrowed sandstone (2) when stabilized, in the east end of the member. The sandstones grade westward into skeletal calcilutite (5). With continued rise, the anticline was breached, and erosion truncated the east end of the Lower Member. A down-to-the-east fault in the east flank of the anticline maintained the clastic trap but caused the anticline and western platform to act subsequently as a unit. Calcarenites (3) mark the unconformity on the Lower Tully and form the basal bed of the Upper Member where it transgressed in the core of the breached anticline. Upper Tully calcilutite (5) spread evenly over the eroded Lower Tully, thickening over older rocks in the breached anticline core and thinning eastward onto the Chenango Valley shoal, the upthrown side of the fault where chamosite oölite (4) formed. Later deepening and bottom fouling caused Tully Limestone deposition along outcrop to end with barren shaly calcilutite (6), marking the upward transition into black shale. The protecting structures lost effect at greater depths, and clastics ultimately spread westward again, overwhelming any remaining carbonate deposition in this region and resuming normal development of the Catskill Delta.