Sedimentary Facies and Biota of Early Permian Deep-Water Allochthonous Limestone, Southwest Reagan County, Texas

Hobson, John P.; Caldwell, Craig D.; Toomey, Donald Francis

doi:10.2110/cor.85.06.0093

Cited by 4 publications

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“…central Turkey (Altiner, 1981); northern Spain (JRG's unpublished observations from collections of E. Villa); Dniepr-Donetz Basin (Brazhnikova et al, 1967); southeastern Urals (Malakhova, 1980); western Libya (Massa and Vachard, 1979;Vachard et al, 1993); Sverdrup Basin (Pinard and Mamet, 1998); Russian Platform (Reitlin ger, 1950) central Turkey (Altiner, 1981); Dniepr-Donetz Basin (Brazhnikova et al, 1967); northern Spain (JRG's unpub lished observations from collections of E. Villa); southwest USA (Toomey et al, 1977); midcontinent USA (Toomey, 1972(Toomey, , 1983Groves and Boardman, 1999;Groves, 2000); Carnic Alps Krainer, 2001a, 2001b); Sverdrup Basin (Pinard and Mamet, 1998); Barents Sea (Groves and Wahlman, 1997) western Urals (Baryshnikov et al, 1982); Dniepr-Donetz Basin (Kireeva, 1958;Stepanova, 1997); northeastern Siberia (Gerke and Sosipatrova, 1975); Carnic Alps (Vachard and Krainer, 2001b); midcontinent USA (Groves and Boardman, 1999;Groves, 2000); west Texas (Hobson et al, 1985); Barents Sea (Groves and Wahlman, 1997); Bolivian Altiplano Subandean Basin (Mamet, 1996); Sverdrup Basin (Pinard and Mamet, 1998) Sverdrup Basin (Pinard and Mamet, 1998) Sverdrup Basin (Pinard and Mamet, 1998); Barents Sea (Groves and Wahlman, 1997); northeastern Siberia (Gerke and Sosipatrova, 1975); midcontinent USA (Toomey, 1972(Toomey, , 1983; Carnic Alps Krainer, 2001a, 2001b) Sverdrup Basin (Pin...…”

Section: Paleobiogeographymentioning

confidence: 99%

Origin and early evolutionary radiation of the Order Lagenida (Foraminifera)

2003

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The Order Lagenida is a monophyletic group of calcareous foraminifers that originated in Middle Pennsylvanian time via acquisition of hyaline-radial wall structure and loss of microgranular wall structure, the latter being characteristic of the close sister group and likely ancestor, the Fusulinida. Early lagenides are delineated into subgroups on the basis of presence or absence of partitioning within their tests, and among partitioned forms, on continuous versus discontinuous growth styles. Partitioned, discontinuously growing forms may be further delineated on the basis of test symmetry and on modifications to chamber shape and apertural complexity. Early lagenides underwent rapid taxonomic differentiation during late Moscovian and early Kasimovian time. Taxonomic differentiation was accompanied by rapid dispersal from the presumed center of origin in the midcontinent-Andean area to tropical and subtropical shelves worldwide. By Early Permian time certain lagenides were adapted to cool water paleoenvironments, as evidenced by their occurrences in high paleolatitudes and even in glaciomarine basins. Early Permian lagenides do not exhibit marked provincialism, but there is evidence for paleolatitudinal control on assemblages. The midcontinent-Andean and present Arctic areas contain similar, diverse faunas from low- to mid paleolatitudes along the western margin of Pangaea. These faunas share many elements in common with faunas from the tropical and subtropical eastern margin of Pangaea (Paleotethys). In contrast, the Europe-Urals, Siberian and Australian areas are characterized by a slightly different faunal association from mid- to high paleolatitudes in both hemispheres. Panthalssan faunas are less well known, but seemingly contain only cosmopolitan taxa.

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Section: Paleobiogeographymentioning

confidence: 99%

Origin and early evolutionary radiation of the Order Lagenida (Foraminifera)

2003

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“…Directly precipitated calcite cements also are present in upper slope strata where fresh-water input has occurred (Given and Lohmann, 1986;Mruk, 1985Mruk, , 1989Scholle et al, 1992;Wiggins et al, 1993). Slope strata, either despite or because of these varied diagenetic events, form hydrocarbon reservoirs in some of the older (mainly Wolfcampian and Leonardian) sections along the edges of the Delaware and Midland basins (Wiggins and Harris, 1985;Hobson et al, 1985;Mazzullo and Reid, 1987).…”

Section: Introductionmentioning

confidence: 99%

Classic Upper Paleozoic reefs and bioherms of West Texas and New Mexico

Scholle¹,

Goldstein²,

Ulmer-Scholle³

2007

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All rights reserved. This work may not be translated or copied in whole of in part without the written permission of the authors except for brief excerpts in connection with scholarly analysis or review. Use in connection with any form of information storage or retrieval, electronic adaptation, computer software, or by similar or dissimilar methodologies now known or hereafter developed is specifi cally forbidden.

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Biostratigraphy and evolution of Late Carboniferous and Early Permian smaller foraminifers from the Barents Sea (offshore Arctic Norway)

Groves¹,

Wahlman²

1997

J. Paleontol.

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Nearly continuous cores from a 500-meter interval of upper Moscovian through post-Artinskian carbonate strata on the Finnmark Platform have yielded rich assemblages of fusulinaceans and smaller foraminifers. The fusulinaceans provide an independent time framework for evaluating stratigraphic occurrences of associated smaller foraminifers. Information derived from this study has been integrated with that from previous investigations to produce a smaller foraminiferal biostratigraphic model for the High Arctic. Kasimovian strata are characterized by occurrences of Nodosinelloides spp., Protonodosaria spp. and Hemigordius schlumbergeri. Overlying lower Gzhelian beds are identified by the appearances of Raphconilia modificata and Amphoratheca iniqua. Tezaquina clivuli and Cribrogenerina gigas first occur in upper Gzhelian strata, and Asselian rocks contain appearances of Geinitzina postcarbonica and Pachyphloia spp. Phylogenetic reconstructions suggest that the Late Carboniferous-Early Permian pseudovidalinids (Archaediscacea) derived from the Pseudoammidiscidae, as did the older group of predominantly Early Carboniferous archaediscaceans. The repeated development of similar morphologies within the two groups of archaediscaceans includes examples of both convergence and iterative evolution. The Protonodosariidae and Syzraniidae most likely evolved from an earlandiid ancestor. The syzraniids gave rise to the Geinitzinidae, which in turn gave rise to the Pachyphloiidae. As in the archaediscaceans, evolution within and among the Earlandiidae, Protonodosariidae, Syzraniidae, Geinitzinidae and Pachyphloiidae includes multiple examples of repeated patterns. Two key phenotypic developments seemingly led to bursts of diversification in different groups throughout late Paleozoic foraminiferal evolution. The acquisition of an outer hyaline or pseudofibrous wall layer was a morphologic breakthrough followed by taxonomic radiation in both groups of archaediscaceans and in the Earlandia-Syzrania lineage. The second major event was the shift from an undivided tubular morphology to uniserial morphology in both the Earlandiidae-Protonodosariidae and Syzraniidae-Geinitzinidae lines. Nodosinelloides pinardae is proposed as a new name for Nodosaria grandis Lipina, 1949 (preoccupied).

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Sedimentary Facies and Biota of Early Permian Deep-Water Allochthonous Limestone, Southwest Reagan County, Texas

Cited by 4 publications

References 0 publications

Origin and early evolutionary radiation of the Order Lagenida (Foraminifera)

Origin and early evolutionary radiation of the Order Lagenida (Foraminifera)

Classic Upper Paleozoic reefs and bioherms of West Texas and New Mexico

Biostratigraphy and evolution of Late Carboniferous and Early Permian smaller foraminifers from the Barents Sea (offshore Arctic Norway)

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