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Lost Branch Formation

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Conclusions

  1. The long-standing miscorrelations within the Seminole Formation and Lenapah Limestone and the misapplication of the name Holdenville Shale that have recently been discovered in the upper Desmoinesian and lower Missourian shale-dominated sequence along the midcontinent outcrop belt are most reasonably resolved by recognizing and tracing the newly proposed Lost Branch Formation (figs. 3 and 4). Its stratotype is in a nearly completely exposed sequence that extends from the top of the Lenapah Limestone to the top of the South Mound shale (fig. 6). The Lost Branch Formation is distinctive enough both lithostratigraphically and biostratigraphically that it can be traced along the entire midcontinent outcrop belt (fig. 7). It extends from Iowa, where it includes the Cooper Creek Limestone Member, through Missouri, where it includes the Sni Mills Limestone Member, through Kansas into Oklahoma, where it lies above the type Lenapah Limestone and correlates with the upper part of the type Holdenville Shale, and includes the more recently named Homer School limestone, Nuyaka Creek black shale, and Glenpool limestone beds (fig. 8). It also correlates with the Lonsdale and West Franklin Limestone Members of the Illinois basin. Recognition of the Lost Branch Formation corrects previous miscorrelations of the Cooper Creek and Sni Mills limestones with the Lenapah Limestone and of the black shale above the Dawson coal in northeastern Oklahoma with the Seminole Formation. It also corrects the mistaken impression that what has been called the Holdenville Shale in Kansas and the Holdenville Formation in Missouri is equivalent to the entire type Holdenville Shale in Oklahoma.
  2. Slight revision of the type Memorial Shale in the Tulsa region, based on the addition of higher strata through the Dawson coal (which are removed from the Seminole Formation), provides an appropriate name for the underlying terrestrial formation that includes the Dawson coal and separates the marine Lost Branch Formation from the underlying marine Lenapah Limestone. The revised Memorial Shale is readily subdivided in its type area into three informal members, which can be traced northward at least to the Kansas-Missouri border. The lower two members, in ascending order, are a thick shale and a thin limestone, which are equivalent to the Perry Farm Shale Member and the Idenbro Limestone Member, respectively, of the Lenapah Limestone of northern Oklahoma and adjacent Kansas, where they are part of the type Lenapah. The upper member of the Memorial Shale includes the Dawson coal, its underclay, and the underlying Jenks sandstone around Tulsa and consists mainly of thin, blocky mudstone paleosol and terrestrial detrital strata to the north.
  3. The outcrop sequence that includes the Lost Branch stratotype also provides a good reference section for the redefined Hepler unit, which comprises the terrestrial strata overlying the Lost Branch Formation.
  4. The best placement of the Desmoinesian-Missourian (=Middle-Upper Pennsylvanian) boundary is at the top of the Lost Branch Formation (fig. 4) because (a) the Lost Branch carries the highest occurrences of several genera and species of conodonts, ammonoids, fusulinids, and brachiopods that are either common in underlying strata or confined to the Lost Branch and (b) the underlying Dawson coal carries the highest occurrence of the diverse Lycospora-dominated palynomorph flora characteristic of Desmoinesian coals, whereas the overlying "Hepler" and "Tulsa" coals carry a much less diverse flora, which is characteristic of higher Missourian coals. Because of slight diachroneity of the lithically defined upper contact of the Lost Branch Formation (e.g., the base of the lowest sandstone, whether of deltaic or fluvial channel origin), a single boundary stratotype will have to be chosen after well-exposed sequences are described paleontologically.
  5. The proposed placement of the Desmoinesian-Missourian boundary fortunately is close to its traditional placement at the supposedly unconformable base of the Hepler sandstone, because the Hepler traditionally has been considered to occupy a position just above the Lost Branch Formation. The contact, however, is often conformable upward from marine to terrestrial deposits. It is disconformable only locally, where Hepler channel sands cut through the alluvial deposits into the Lost Branch. Misidentification of sandstones at lower stratigraphic horizons (e.g., in the Lenapah Limestone) as Hepler helped to perpetuate the assumption of a major unconformity at the boundary (fig. 3). Miscorrelation of the Dawson coal and the overlying black shale with the Missourian Seminole (then called Coffeyville) Formation by Oklahoma geologists, as reported by Miller and Owen (1937), even though the shale contained an ammonoid fauna of strong Desmoinesian affinities, aggravated the problem of identifying the boundary. The apparent lack of a major unconformity on the shelf corroborates the observations of Krumme (1981, p. 26), who could find no evidence of an unconformity in the basin of central Oklahoma.
  6. The depositional history of the marine shale-dominated Lost Branch Formation is analogous to that of both older and younger limestone-dominated marine formations. The only substantive difference is the much lesser proportion and thickness of limestone units in the Lost Branch Formation. This difference may be related to a greater rate of sea-level changes and thus more rapid passage of the sea bottom through carbonate-producing depths during the Lost Branch marine inundation. Although several other limestone-rich cycles have little or no transgressive carbonates, suggesting that rapid transgression was common among Pennsylvanian marine inundations, the Lost Branch inundation is one of the few inundations that was followed by relatively rapid regression.
  7. Because the well-defined lithic and faunal nature of such a thin, widespread marine horizon extends for hundreds of miles across five states, sandwiched between two well-defined, widespread terrestrial units with coals and paleosols (figs. 4 and 8), it seems inconceivable that the controlling mechanism for this stratigraphic pattern could be anything other than relatively short-term (i.e., glacial) eustatic change. Whatever deltas are associated with the Lost Branch marine horizon are small and local, mainly regressive, and nonexistent north of Missouri. In fact, the correlation of several distinctive marine horizons across the area of the Forest City basin (fig. 9) shows the potential for determining the different extents of successive transgressions [see Heckel (1986)]. Knowledge of certain characteristics of the rock sequence, such as carbonate thickness and development and extent of soil profiles, should shed light on the speed of sea-level changes and duration of inundations and withdrawals. Thus it appears that analysis of the Pennsylvanian cyclic sequence will greatly aid in deciphering the nature and tempo of Gondwanan glaciations.

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