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NARROW
GeoRef Subject
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all geography including DSDP/ODP Sites and Legs
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Europe
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Central Europe
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Bohemian Massif (1)
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Germany
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Rhineland-Palatinate Germany (1)
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Rhenish Schiefergebirge (1)
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Western Europe
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France (1)
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geologic age
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Mesozoic
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Triassic
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Lower Triassic
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Bunter
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Voltzia Sandstone (1)
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Middle Triassic
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Anisian (1)
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Rhenohercynian (1)
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Saxothuringian (1)
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Primary terms
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Europe
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Central Europe
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Bohemian Massif (1)
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Germany
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Rhineland-Palatinate Germany (1)
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Rhenish Schiefergebirge (1)
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Western Europe
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France (1)
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faults (1)
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geophysical methods (1)
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Mesozoic
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Triassic
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Lower Triassic
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Bunter
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Voltzia Sandstone (1)
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Middle Triassic
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Anisian (1)
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Mohorovicic discontinuity (1)
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plate tectonics (1)
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Pirmasens Germany
Figure 2. Stratigraphic profile of the Triassic strata at the locality ( Fi...
EVIDENCE OF PALEOWILDFIRE IN THE EARLY MIDDLE TRIASSIC (EARLY ANISIAN) VOLTZIA SANDSTONE: THE OLDEST POST-PERMIAN MACROSCOPIC EVIDENCE OF WILDFIRE DISCOVERED SO FAR
Figure 1. Geological map showing the geographic position of the locality at...
Figure 1. Geological map showing the geographic position of the locality at...
Geophysical constraints and model of the “Saxothuringian and Rhenohercynian subductions – magmatic arc system” in NE France and SW Germany
Seismological notes
Post-Variscan evolution of the lithosphere in the Rhine Graben area: Constraints from subsidence modelling
Abstract In the area of the Cenozoic Rhine rift system, crustal and lithospheric thicknesses range between 24 and 35 km, and 60 and 120 km, respectively. This rift system transects the deeply truncated Variscan Orogen and superimposed Permo-Carboniferous wrench-induced troughs, and Late Permian and Mesozoic thermal sag basins. At the time of its Westphalian consolidation, the Variscan Orogen was probably characterized by 45–60 km deep-crustal roots that were associated with its Rheno-Hercynian-Saxo-Thuringian, Saxo-Thuringian Bohemian and Bohemian-Moldanubian sutures, all of which are transected by the Cenozoic Rhine rift system. During the Stephanian-Early Permian wrench-induced disruption of the Variscan Orogen, subducted lithospheric slabs were detached causing upwelling of hot mantle material. During the resulting thermal surge, partial delamination and/or thermal thinning of the continental mantle-lithosphere induced regional uplift. At the same time the Variscan orogenic roots were destroyed and crustal thicknesses reduced to 28–35 km in response to the combined effects of mantle-derived melts interacting with the lower crust, regional erosional unroofing of the crust and, on a more local scale, by its mechanical stretching. Towards the end of the Early Permian, the potential temperature of the asthenosphere returned to ambient levels. With this, regional, long-term thermal subsidence of the lithosphere commenced, controlling the development of a new system of Late Permian and Mesozoic thermal sag basins. However, the evolution of these basins was repeatedly overprinted by minor short-term subsidence accelerations that reflect the build-up of far-field stresses related to rifting in the Tethyan and Atlantic domains. Comparison of observed and modelled subsidence curves suggests that in the area of the Rhine rift system the lithosphere had equilibrated with the asthenosphere at the end of the Cretaceous at depths of 100–120 km, before it became thermally destabilized again by Cenozoic rifting and plume-related magmatism. Modelled subsidence curves indicate that by the end of Early Permian times the thermal thickness of the remnant mantle-lithosphere ranged between 10 and 50 km in areas that were later incorporated into Mesozoic thermal sag basins; this corresponds to mid-Permian thermal lithosphere thicknesses of 40–80 km.
Post-Variscan evolution of the lithosphere in the area of the European Cenozoic Rift System
Abstract The European Cenozoic Rift System (ECRIS) transects Variscan basement, Permo-Carboniferous troughs and Late Permian to Mesozoic series, deposited in thermal sag basins, which are exposed on rift-related arches. We have analysed processes governing the transformation of the orogenically destabilized Variscan lithosphere into end-Cretaceous stabilized cratonic lithosphere, prior to its renewed Cenozoic rift-related destabilization. In the ECRIS area, crustal and lithospheric thicknesses at present are in the range of 24–35 km and 60–120 km, respectively. The Variscan orogen was characterized at the time of its end-Westphalian consolidation by 45–60 km deep crustal roots, marking major sutures. During the Stephanian-Early Permian wrench-induced collapse of the Variscan orogen, subducted lithospheric slabs were detached, causing upwelling of the asthenosphere, thermal thinning and/or partial delamination of the lithospheric mantle, and regional uplift. By mid-Permian times, the crust was thinned to 28–35 km owing to its regional erosional unroofing, localized mechanical stretching and the interaction of mantle-derived melts with its basal parts. By mid-Permian times, when the temperature of the asthenosphere returned to ambient levels, thermal subsidence of the lithosphere commenced, controlling development of a system of Late Permian and Mesozoic intracratonic basins. These experienced repeated minor subsidence accelerations, related to the build-up of far-field stresses, which did not involve renewed lithospheric destabilization. Modelling of observed subsidence curves indicates that during the mid-Permian lithospheric thicknesses ranged in the ECRIS area between 40 and 80 km, but had increased by the end of the Cretaceous to 100–120 km. Cenozoic rifting and mantle-plume activity caused renewed lithospheric thinning.