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Famennian conodont zonation (CZ) after Spalletta et al. (2017) with spa...
Ostracodes of the Maple Mill Shale Formation (Upper Devonian) of southeastern Iowa, U.S.A.
The standard Late Devonian conodont zonation between the top of the Upper marginifera Zone and the earliest Carboniferous Siphonodella sulcata Zone is revised to replace the former velifer , styriacus , and costatus zonal groups, which were based primarily on genera other than Palmatolepis , and to eliminate a hiatus above the Upper costatus Zone. The changes were enabled by a new phylogenetic model of Palmatolepis , by range extensions that bridge former gaps between the records of some Palmatolepis taxa, and by further taxonomic revisions of some double-rowed Bispathodus taxa. Basing the standard zonation on conodonts of primarily pelagic biofacies permits construction of parallel, alternative zonations for shallower water biofacies and estimation of phylogenetically more precise zonal timespans.
North American Devonian Conodont Biostratigraphy
The Lower Devonian of Nevada provides a reference sequence of nine conodont faunas, five of which are also at Royal Creek, Yukon Territory. The first appearance of Icriodus woschmidti is comparable to that in the lower Gedinnian in Europe; the Polygnathus dehiscens-P. foveolatus lineage correlates with the Emsian. Directly associated graptolite and brachiopod zones in Nevada date the intervening conodont succession as upper Gedinnian and Siegenian. Five faunas characterize the lower Middle Devonian (Eifelian) in New York ; at least two of the lower three are present in the Illinois Basin. Illinois Basin faunas correlative to the upper two New York faunas (Seneca and Cherry Valley) have Icriodus angustus, which is absent in New York, but lack Polygnathus kockelianus, which marks the top of the New York Eifelian. Three faunas subdivide the upper Middle Devonian (Givetian) in the Illinois Basin; the lower two occur in New York and Michigan. The Middle Devonian-Upper Devonian boundary possibly falls at the base of or within beds carrying the Spathognathodus insitus fauna. Alberta and Iowa sequences from the Lower Polygnathus asymmetricus through Upper Palmatolepis gigas Zones closely correspond to the lower Upper Devonian in Germany. An Iowa section yields the standard lower Famennian zonal succession (Middle Palma-tolepis triangularis through Upper Palmatolepis quadrantinodosa Zones). Higher Devonian faunas, in the western and central United States, are assigned with difficulty to the Scaphignathus velifer, Upper Polygnathus styriacus, and Spathognathodus costatus Zones. The faunal sequence of the S. costatus Zone differs significantly from that in Germany.
Famennian biostratigraphic species. (a) Palmatolepis triangularis Sannema...
Protosalvinia Dawson and Associated Conodonts of the Upper Trachytera Zone, Famennian, Upper Devonian, in the Eastern United States
Palaeoenvironmental changes at Col des Tribes (Montagne Noire, France), a reference section for the Famennian of north Gondwana-related areas
A LATE DEVONIAN HYDROCARBON-SEEP DEPOSIT DOMINATED BY DIMERELLOID BRACHIOPODS, MOROCCO
Palmatolepis gracilis expansa Zone and Bispathodus aculeatus aculeatus Zone conodonts from the Three Lick Bed at the type locality, Ohio Shale, Upper Devonian, eastern Kentucky
The global Annulata Events: review and new data from the Rheris Basin (northern Tafilalt) of SE Morocco
Abstract A review of the literature shows that the Famennian global Annulata Event(s) can be recognized as a transgressive, often hypoxic and eutrophic, interval that interrupts an overall regressive eustatic trend in more than 40 regions of North America, Europe, North Africa, Asia and Australia. According to differences in palaeogeography, sedimentology and biota, these occurrences are assigned to 10 event settings. The first detailed data on facies, ammonoid and conodont faunas are presented for the Rheris Basin of the eastern Anti-Atlas (southern Morocco) and compared with previously studied sections of the adjacent Tafilalt Platform, Tafilalt Basin and Maider Basin. The rather argillaceous succession at El Gara resembles the Tafilalt Basin (Hassi Nebech section) in its lack of black shales/limestones and similar ammonoid and conodont assemblages. However, the Sulcoclymenia sulcata Zone (Upper Devonian III-C2) below the Annulata Events contains ammonoid taxa that are unique for all of the Anti-Atlas and North Africa: Protornoceras ornatum Dybczynski, 1913 , Genuclymenia aff. angelini ( Wedekind, 1908 ), Protactoclymenia aff. implana ( Czarnocki, 1989 ) and ? Pleuroclymenia sp. juv. The first regional record of the marker conodont Pseudopolygnathus granulosus Ziegler, 1962 also distinguishes the pre-event assemblage. As in many other regions, there is a major decline in ammonoids well before the Lower Annulata Event, which suggests an episode of extreme oligotrophy. Both Annulata Events at El Gara are whitish-weathered marly shales with only small specimens of Platyclymenia and Prionoceras ( sensu lato ), which are also typical for the annulata Zone (UD IV-A) of other Tafilalt sections, but benthonic organisms are nearly absent. This suggests local low-oxygen conditions, but only a moderate production of organic carbon, insufficient for black shale formation, unlike many German sections or in the Maider Basin (section Mrakib). The latter region represents a deeper shelf basin that had much higher productivity and a unique ‘ Gundolficeras – Erfoudites – Protactoclymenia – Stenoclymenia – Guerichia biofacies’ of the Lower Annulata Shale. The upper part of the annulata Zone at El Gara is characterized by Platyclymenia ( Platyclymenia ) levata n. sp. Other new taxa of the same zone in the Anti-Atlas are Posttornoceras ascendens n. sp. and Stenoclymenia rectangula n. sp. Whilst the ammonoid faunal overturn between UD III-C and UD IV-A was severe, the strong reduction in conodont diversity with the two Annulata Events was mostly (apart from two taxa) a palaeoecologically triggered, only episodic, feature. The comparison of the various Anti-Atlas Annulata Event beds and assemblages enables the distinction of event biofacies types, which reflect local differences of bathymetry, trophic conditions and seafloor ventilation.
Variscan facies and structure in central SW England
A new species of catfish (Claroteidae, Chrysichthys ) from an Eocene crater lake in East Africa
A NEW FOSSIL SPECIES OF ICTIOBUS (TELEOSTEI: CATOSTOMIDAE) FROM PLIOCENE LACUSTRINE SEDIMENTS NEAR TULA DE ALLENDE, HIDALGO, MEXICO
Abstract To the south of the Mississippian platform carbonate successions of South Wales (Chapter 5) and Bristol, Mendips and Somerset (Chapter 6), Carboniferous rocks predominantly occur within the strongly deformed Culm crop of SW England. The Culm Basin has a broad graben architecture, with an inner graben (Central Devon Sub-basin) fianked by half-grabens (Bideford and Launceston sub-basins) (Fig. 14; Leveridge & Hartley 2006; Waters et al. 2009). The Bideford Sub-basin is bounded to the north by the Brushford Fault, the Central Devon Sub-basin by the Greencliff Fault and the Launceston Sub-basin by the Rusey Fault. To the north of the Brush-ford Fault is the northern margin of the Culm Basin. The Tavy Basin has limited development of Famennian-Tournaisian strata. The Laneast High separating the Tavy Basin and Launceston Sub-basin includes a Tournaisian to ?Visean succession (Yeolmbridge and Laneast Quartzite formations). Remnants of Carboniferous strata also occur in the South Devon Basin. In many areas there is no clear lithological break between the Tournaisian and the underlying Upper Devonian rocks, both of which are dominated by shallow-marine and deeper-water mudstones. The succession, commonly referred to as the Transition Series or Group (Dearman & Butcher 1959; Freshney et al. 1972), are assigned to the Exmoor Group in north Devon, the Hyner Mudstone and Trusham Mudstone formations of the eastern part of the Central Devon Sub-basin and the Tamar Group in south Devon.
STRATIGRAPHY, AGE, AND INTERREGIONAL CORRELATION OF THE EXSHAW FORMATION, ALBERTA ROCKY MOUNTAINS
Upper Devonian miospore and conodont zone correlation in western Europe
Abstract The stratigraphical occurrence of 38 Upper Devonian miospore taxa is compared to some miospore and conodont zones in 28 intercalibrated levels. The accurate position of 15 miospore First Occurrence Biohorizons and one Last Occurrence Biohorizon in terms of the conodonts available in a few regions of western Europe is discussed in detail and their correlation evaluated.
Abstract Microvertebrate samples from the Upper Devonian Hojedk section, southeastern Iran, and the Napier Formation, northwestern Australia, have yielded scales of agnathan thelodonts, dated as early/mid-Famennian ( crepida–marginifera/trachytera conodont zones). These scales are referred to Arianalepis megacostata , a new genus and species, and Arianalepis sp. indet., a second indeterminate species of this new turiniid genus. Further recorded scales of Australolepis seddoni from the Napier Formation confirm the age range for this taxon as extending into the late Frasnian. The new remains post-date the previously youngest thelodonts from Iran and Western Australia and provide the first evidence of thelodonts surviving the Frasnian–Famennian extinction events.
IDAHO LOST RIVER SHELF TO MONTANA CRATON: NORTH AMERICAN LATE DEVONIAN STRATIGRAPHY, SURFACES, AND INTRASHELF BASIN
ABSTRACT: Understanding of very thick Late Devonian shelf strata in Idaho is hindered by formation terminologies. Interpreted genetically, and in combination with lower accommodation settings in Montana, strata reveal craton-to-basin geometries and analogues similar to other western Laurentian basins. The Jefferson Formation Birdbear Member and Three Forks Formation in Montana are correlated to the Jefferson Grandview Dolomite in Idaho using regional sequence stratigraphic surfaces. A new stratigraphic framework defines three widely deposited latest Frasnian sequences and Early Famennian intrashelf basin paleogeography. Peritidal to marine mixed siliciclastic and carbonate rocks of the Middle Devonian lower Jefferson Formation in Idaho are overlain by the Frasnian Dark Dolomite. These rocks are overlain by similar lithologies, including thick evaporite solution breccias of the latest Frasnian and Early Famennian upper Jefferson Formation. Latest Frasnian sequences are similar to Nisku–Winterburn sequences in western Canada. Overlying Famennian successions are correlatives to the Three Forks Formation Logan Gulch Member in Montana and the Palliser–Wabamun units of Alberta. Biohermal Dark Dolomite in the central Lemhi Range and Borah Peak area of the Lost River Range was deposited west of the Lemhi Arch, with buildups also established on ramps near the shelf break in the Grandview Canyon area (Grandview Reef). During onset of the Antler Orogeny, prior to deposition of the Middle Famennian Three Forks Trident Member and widespread disconformities, a latest Frasnian outer shelf barrier formed above the Grandview Reef. Cyclic, heterolithic, peloidal western Grandview Dolomite facies were deposited and are ~330 m thick, although correlative facies of the Jefferson D4 through D6 members are twice as thick behind the shelf edge in the central Lemhi and Borah Peak area. Lower Grandview Dolomite black subtidal carbonate and Nisku buildups (Gooseberry Reef) formed in three late Frasnian sequences and under a basal Famennian sequence boundary. At this time, the Lemhi Arch foundered, but remained unstable—it was termed the “Beaverhead Mountains uplift.” An intrashelf basin dominated midshelf paleogeography during the Early Famennian, accommodating thick shallow water barrier sandstone, solution-collapse breccia, and restricted marine dolostone and limestone of the upper Grandview Dolomite. Crinoid packstone beds near the top of the Jefferson Formation occur below the Three Forks Trident Member in the Lost River Range. Similar nodular, crinoidal limestone with cephalopods occurs under an unconformity with the Sappington Formation in the Beaverhead Mountains. These rocks were previously called the False Birdbear and were grouped with the Jefferson Formation; however, they comprise their own ~15-m-thick sequence and are unrelated to the rarely fossiliferous and dolomitized upper Grandview Dolomite. Open marine shale–limestone sequences of the 80-m-thick Trident Member were deposited on the Idaho shelf above and below regional surfaces and hiatuses. These rocks were variably accommodated on reactivated paleohighs and in local seaways on the craton margin. An unconformity developed on the outer Idaho shelf in the latest Devonian during deposition of the Sappington Formation on the Lemhi Arch and in the Central Montana Trough. Sappington strata were either not deposited on the western shelf or accumulated under deep water conditions and were eroded during regional Mississippian basin inversion and turbidite deposition.
ABSTRACT The purpose of this trip is to visit an internationally famous Quaternary vertebrate paleontology site, Friesenhahn Cave, on the eastern margin of the Edwards Plateau in the heart of the central Texas Hill Country. This site has a very long history of scientific investigations beginning in the early twentieth century and continuing today. The cave has produced the fossil remains of more than 50 vertebrate taxa, including amphibians, reptiles and mammals. However, the abundant remains of an extinct scimitar cat, Homotherium serum, including juvenile individuals along with hundreds of teeth, cranial, and postcranial elements of juvenile mammoths, Mammuthus cf. M. columbi, make it an especially unique site. Our visit to Friesenhahn Cave will focus on its physical setting, cave sediment stratigraphy, potential age and taphonomy as they relate to the adaptations of Homotherium in the late Pleistocene of central Texas and its relationship to its potential prey, juvenile mammoths. We will also discuss recent studies of the cave itself, and its protection for future investigations by Concordia College.
The Variscan Orogeny: the development and deformation of Devonian/Carboniferous basins in SW England and South Wales
Abstract The upper Palaeozoic Orogenic Province of SW England is a part of a belt of Devonian and Carboniferous basins that extended from Devon and Cornwall through to Germany, some 800 km to the east. Their complex sequence of basin development and phases of deformation, described in this chapter cumulatively comprise the Variscan Orogeny in this region. Synchronously with the Devonian events within the Variscan Orogen, the mainly fluvial facies of the Old Red Sandstone filled basins in the Avalonian continent north of the Variscan front (Chapter 6). During the succeeding Carboniferous, basins within the continent were mainly extensional in origin, until a period in the late Carboniferous when many basement faults were inverted (Chapter 7) resulting in uplift of the basin fill, that initiated a new palaeogeography at the start of the Permian. The South Wales Basin represents a transitional zone between the mobile Variscan belt and the continent to the north. This transitional position is reflected in the Devonian by the interdigitationof the Old Red Sandstone facies and marine sediments at the northern margins of the Variscan basins (Chapter 6). Throughout the Dinantian and Namurian the succession within the South Wales basin had much in common with successions in basins within the continent to the north (Chapter 7). It was not until the Silesian that Variscan deformation affected basin development and caused its deformation (see this chapter).