Intraplate mountain building in response to continent–continent collision—the Ancestral Rocky Mountains (North America) and inferences drawn from the Tien Shan (Central Asia)
“…By later Mississippian time, shallow marine carbonates and sandstone were deposited across much of the region (Sandberg et al, 1982). During Pennsylvanian time, the Oquirrh basin subsided in NW Utah with deposition of up to 6 km of marine strata, simultaneous with uplift of the Ancestral Rockies during collision of Laurentia with Gondwana (Dickerson, 2003). Permian deep marine sedimentary and volcanic rocks accumulated in another western basin, and were thrust eastward in the Golconda allochthon during the Triassic Sonoma orogeny (Speed and Sleep, 1982;Oldow et al, 1989).…”
Section: North American Sedimentary Covermentioning
The thin-skin Sevier and thick-skin Laramide belts of the North American Cordillera provide a long-term record of the interrelations between evolving styles of mountain building and plate dynamics over a complete tectonic cycle, from onset of rapid subduction, to protracted growth of a composite orogenic system, to final collapse. Primary architecture of basement and sedimentary cover rocks, which included a thick passive margin section deposited along the western continental margin, influenced patterns of subsequent deformation. The Cordilleran orogenic system, comprised of an interrelated forearc accretionary complex, magmatic arc, retroarc hinterland, Sevier fold-thrust belt, and foreland basin locally deformed by Laramide arches, developed during Jurassic to Paleogene Andean-style subduction and terrane accretion. The Sevier belt formed as a foreland-propagating (west to east) wedge mostly during Cretaceous to Paleogene time, and included a western thrust system with aerially extensive thrust sheets that carried thick passive margin strata, and an eastern thrust system that carried thinner strata. Within the Wyoming salient of the Sevier belt, major thrust and fold traces display systematic map-view curvature about an average N-S structural trend, reflecting a component of primary curvature related to sedimentary prism architecture, followed by 60-80% vertical-axis rotation of thrust sheets related to curved fault slip and interaction with Laramide arches at the salient ends. Internal deformation in the western thrust sheets was limited within strong shallower levels, whereas deeper levels underwent shear and vertical flattening near a weak basal fault zone. Internal deformation in the eastern thrust sheets included widespread early layer-parallel shortening (LPS), followed by concentration of slip onto weak fault zones. Approximately 200 km of thin-skin shortening in the Sevier belt was transferred into lower crustal thickening and uplift of an orogenic plateau in the hinterland to the west. Synorogenic strata were deposited in an evolving foreland basin to the east that formed 11 Jurassic with deposition of marine carbonates and evaporites in the Twin Creek Formation and correlative strata (Imlay, 1967), synchronous with early terrane accretion along the western plate margin (Dickinson, 2008). These evaporites subsequently formed detachments during Sevier thrusting (Coogan and Yonkee, 1985). Late Jurassic and Cretaceous to Paleogene strata deposited in the foreland are described in section 4.5. 2.3. Accreted terranes The western part of the Cordilleran orogenic system was constructed on accreted terranes that included: (1) peri-cratonic rocks with fossil and detrital zircon (DZ) signatures typical of North America (Roberts Mountain and Golconda allochthons, Kootenay terrane); (2) Paleozoic to Mesozoic arc and ophiolite rocks of the Intermontane terrane group in Canada, and the Sierra Foothills, Klamath Mountains, and Blue Mountains provinces; and (3) Paleozoic to Mesozoic distal arc and ophiolite rocks of t...
“…By later Mississippian time, shallow marine carbonates and sandstone were deposited across much of the region (Sandberg et al, 1982). During Pennsylvanian time, the Oquirrh basin subsided in NW Utah with deposition of up to 6 km of marine strata, simultaneous with uplift of the Ancestral Rockies during collision of Laurentia with Gondwana (Dickerson, 2003). Permian deep marine sedimentary and volcanic rocks accumulated in another western basin, and were thrust eastward in the Golconda allochthon during the Triassic Sonoma orogeny (Speed and Sleep, 1982;Oldow et al, 1989).…”
Section: North American Sedimentary Covermentioning
The thin-skin Sevier and thick-skin Laramide belts of the North American Cordillera provide a long-term record of the interrelations between evolving styles of mountain building and plate dynamics over a complete tectonic cycle, from onset of rapid subduction, to protracted growth of a composite orogenic system, to final collapse. Primary architecture of basement and sedimentary cover rocks, which included a thick passive margin section deposited along the western continental margin, influenced patterns of subsequent deformation. The Cordilleran orogenic system, comprised of an interrelated forearc accretionary complex, magmatic arc, retroarc hinterland, Sevier fold-thrust belt, and foreland basin locally deformed by Laramide arches, developed during Jurassic to Paleogene Andean-style subduction and terrane accretion. The Sevier belt formed as a foreland-propagating (west to east) wedge mostly during Cretaceous to Paleogene time, and included a western thrust system with aerially extensive thrust sheets that carried thick passive margin strata, and an eastern thrust system that carried thinner strata. Within the Wyoming salient of the Sevier belt, major thrust and fold traces display systematic map-view curvature about an average N-S structural trend, reflecting a component of primary curvature related to sedimentary prism architecture, followed by 60-80% vertical-axis rotation of thrust sheets related to curved fault slip and interaction with Laramide arches at the salient ends. Internal deformation in the western thrust sheets was limited within strong shallower levels, whereas deeper levels underwent shear and vertical flattening near a weak basal fault zone. Internal deformation in the eastern thrust sheets included widespread early layer-parallel shortening (LPS), followed by concentration of slip onto weak fault zones. Approximately 200 km of thin-skin shortening in the Sevier belt was transferred into lower crustal thickening and uplift of an orogenic plateau in the hinterland to the west. Synorogenic strata were deposited in an evolving foreland basin to the east that formed 11 Jurassic with deposition of marine carbonates and evaporites in the Twin Creek Formation and correlative strata (Imlay, 1967), synchronous with early terrane accretion along the western plate margin (Dickinson, 2008). These evaporites subsequently formed detachments during Sevier thrusting (Coogan and Yonkee, 1985). Late Jurassic and Cretaceous to Paleogene strata deposited in the foreland are described in section 4.5. 2.3. Accreted terranes The western part of the Cordilleran orogenic system was constructed on accreted terranes that included: (1) peri-cratonic rocks with fossil and detrital zircon (DZ) signatures typical of North America (Roberts Mountain and Golconda allochthons, Kootenay terrane); (2) Paleozoic to Mesozoic arc and ophiolite rocks of the Intermontane terrane group in Canada, and the Sierra Foothills, Klamath Mountains, and Blue Mountains provinces; and (3) Paleozoic to Mesozoic distal arc and ophiolite rocks of t...
“…10a) is poorly documented and may result from variations in the crustal thickness of the terrane (e.g. Gilbert, Velasco & Zandt, 2007; Lowrie, 2007), possibly linked to the Ancestral Rocky Mountains orogeny or to the more recent Laramide orogeny and the building of the Rocky Mountains (Ye et al 1996; Dickerson, 2003). Figure 10.(a) Bouguer gravity anomaly map of the Sonoma Foreland Basin and its surroundings (in mGal; after Kucks, 1999).…”
Section: Resultsmentioning
confidence: 99%
“…1c) probably resulted from the complex interplay between intracratonic deformations to the east and the reactivation of Antler faults to the west (Geslin 1998: fig. 12; Trexler & Nitchman, 1990; Dickerson, 2003; Blakey, 2008). This highly subsiding basin recorded up to 6 km of marine strata (Walker, 1985; Yonkee & Weil, 2015).…”
Sediments deposited from the Permian–Triassic boundary (~252 Ma) until the end-Smithian (Early Triassic;c.250.7 Ma) in the Sonoma Foreland Basin show marked thickness variations between its southern (up toc.250 m thick) and northern (up toc.550 m thick) parts. This basin formed as a flexural response to the emplacement of the Golconda Allochthon during the Sonoma orogeny. Using a high-resolution backstripping approach, a numerical model and sediment thickness to obtain a quantitative subsidence analysis, we discuss the controlling factor(s) responsible for spatial variations in thickness. We show that sedimentary overload is not sufficient to explain the significant discrepancy observed in the sedimentary record of the basin. We argue that the inherited rheological properties of the basement terranes and spatial heterogeneity of the allochthon are of paramount importance in controlling the subsidence and thickness spatial distribution across the Sonoma Foreland Basin.
“…As no major low angle normal faults that could have produced tectonic exhumation are present in this area, we suggest that the vertical displacement leading to about 3–4 km of erosion and unroofing during the Triassic‐Early Jurassic could be related to far‐field tectonic effects related to the Cimmerian collision, in an area, where lithosphere strength contrasts occur along the Trans European Suture Zone. Spatial and temporal strength variations of the lithosphere control far field tectonic stresses that can propagate at distances of many hundreds of kilometres from the orogen (Ziegler et al ., ; Dickerson, ). Examples can be found in the deformation at the northern margin of the Tibetan Plateau, which was synchronous with the early stage of India‐Asia collision (e.g.…”
The Podolia region is located along the western border of the Eastern European Craton, which is also known as Ukrainian Shield. From the Ordovician to the Miocene, this area formed part of an epicontinental basin system. In order to investigate the effects of orogenic cycles occurring along the plate margin, a multi-disciplinary approach was used in this study. Paleotemperature analysis and lowtemperature thermochronometry were combined with stratigraphic data to obtain a burial model for the Paleozoic succession exposed in the study area. Maximum burial for Silurian and Devonian rocks occurred during the Devonian and Early Carboniferous at depths of 4-5 km, as constrained by vitrinite reflectance and illite content in mixed illite-smectite layers. Thermochronometric data indicate that exhumation through the 45-120°C temperature range took place between the Late Triassic and the Early Jurassic, and that no significant burial occurred afterwards (temperatures characterising the stratigraphically lowermost units remaining below ca. 60°C). These results point to a major exhumation event coeval with the Cimmerian orogenesis, which took place a few hundreds of kilometres away from the study area. On the other hand, no significant effect of the Alpine orogenesis was recorded, although the collisional front was located <100 km from the Podolia region. This work shows how paleothermal and thermochronometric analyses can be successfully integrated with stratigraphic data to reconstruct the burial history, and how the burial history of a basin located on a plate margin can, in some cases, be independent from the distance of the margin from the collisional fronts.
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