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Charles S. Hutchison - One of the best experts on this subject based on the ideXlab platform.
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marginal Basin Evolution the southern south china sea
Marine and Petroleum Geology, 2004Co-Authors: Charles S. HutchisonAbstract:Abstract The southern South China Sea is divided into contrasting morphology by the West Baram Line. To the west is the Sundaland extinct passive margin in which rifting began in the Eocene (∼46 Ma) and ceased at 19–21 Ma (anomaly 6), where sea-floor spreading began much later than along the shelf of China. The break-up hiatus lasted ∼3–5 Ma marked by the Mid-Miocene unconformity, also preserved on land Sarawak. The post-rift strata date from ∼16 Ma and drape over the rifted topography. To the east is a convergent margin that became a collision zone in the Middle Miocene. The Sunda Shelf is of uniform ∼30 km thickness except in localised deep Basins, and extends to a water depth of ∼200 m. The continental slope is narrow. The continental rise (Dangerous Grounds), is covered by water ranging from 500 m to 3.5 km depth at the continent–ocean transition. Its width ranges from 170 to 330 km. The Rajang Delta extends over the shelf and continental slope. Its post-rift sediments drape over the rifted proximal topography of the Dangerous Grounds. To the east the drape is thinner and has not completely buried the rifted topography. The cuestas appear to have supported the carbonate build-up infrastructures of the Spratly Islands, whose slopes rise abruptly from a sea-floor of 2–3 km depth. The Sabah and Brunei margin is a collision zone that was formerly convergent. The on land geology indicates a Mesozoic ophiolitic basement. The main collision feature is the Western Cordillera, constructed mainly of sandy Eocene to Lower Miocene turbidites, predominantly Oligocene to Lower Miocene in the West Crocker (32–18 Ma), uplifted episodically throughout the Upper Miocene and Pliocene, 14–8 Ma. The 2 km deep Northwest Borneo Trough may be a relict of the convergence phase, but could also be a collisional foredeep. The oil-prolific Baram Delta, resulting from uplift and erosion of the Western Cordillera, has built out as far as the Northwest Borneo Trough. It is suggested that the passive margin continental rise (Dangerous Grounds) has been underthrust beneath Sabah to cause uplift of the Western Cordillera. The West Baram Line accordingly abruptly separates the collision zone from the western extinct passive margin; and is a now extinct major right-lateral transform fault.
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Marginal Basin Evolution: The southern South China Sea
Marine and Petroleum Geology, 2004Co-Authors: Charles S. HutchisonAbstract:The southern South China Sea is divided into contrasting morphology by the West Baram Line. To the west is the Sundaland extinct passive margin in which rifting began in the Eocene (∼46 Ma) and ceased at 19-21 Ma (anomaly 6), where sea-floor spreading began much later than along the shelf of China. The break-up hiatus lasted ∼3-5 Ma marked by the Mid-Miocene unconformity, also preserved on land Sarawak. The post-rift strata date from ∼16 Ma and drape over the rifted topography. To the east is a convergent margin that became a collision zone in the Middle Miocene. The Sunda Shelf is of uniform ∼30 km thickness except in localised deep Basins, and extends to a water depth of ∼200 m. The continental slope is narrow. The continental rise (Dangerous Grounds), is covered by water ranging from 500 m to 3.5 km depth at the continent-ocean transition. Its width ranges from 170 to 330 km. The Rajang Delta extends over the shelf and continental slope. Its post-rift sediments drape over the rifted proximal topography of the Dangerous Grounds. To the east the drape is thinner and has not completely buried the rifted topography. The cuestas appear to have supported the carbonate build-up infrastructures of the Spratly Islands, whose slopes rise abruptly from a sea-floor of 2-3 km depth. The Sabah and Brunei margin is a collision zone that was formerly convergent. The on land geology indicates a Mesozoic ophiolitic basement. The main collision feature is the Western Cordillera, constructed mainly of sandy Eocene to Lower Miocene turbidites, predominantly Oligocene to Lower Miocene in the West Crocker (32-18 Ma), uplifted episodically throughout the Upper Miocene and Pliocene, 14-8 Ma. The 2 km deep Northwest Borneo Trough may be a relict of the convergence phase, but could also be a collisional foredeep. The oil-prolific Baram Delta, resulting from uplift and erosion of the Western Cordillera, has built out as far as the Northwest Borneo Trough. It is suggested that the passive margin continental rise (Dangerous Grounds) has been underthrust beneath Sabah to cause uplift of the Western Cordillera. The West Baram Line accordingly abruptly separates the collision zone from the western extinct passive margin; and is a now extinct major right-lateral transform fault. © 2004 Elsevier Ltd. All rights reserved.
Lin Liangbiao - One of the best experts on this subject based on the ideXlab platform.
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Tectonic sequence framework and sedimentary Basin Evolution of upper triassic in the sichuan Basin, China
BioTechnology: An Indian Journal, 2020Co-Authors: Lin LiangbiaoAbstract:The Late Triassic is an important geologic age for the Evolution of the Sichuan Basin. Based on data from field outcrops, drilling, and seismic acquisition, a detailed study on the sequence boundaries, division, and characteristics of the Upper Triassic in the Sichuan Basin was conducted using tectonic sequence stratigraphy to establish a sequence stratigraphic framework. The research indicates that four sequence boundaries were distinguishable in the Upper Triassic: 1) regionally structural unconformity between the Upper Triassic and Middle and Lower Triassic; 2) the boundary between the second member of the Xujiahe Formation and the Xiaotangzi Formation; 3) the secondary structural unconformity between the third and fourth members of the Xujiahe Formation; and 4) regionally structural unconformity between the Triassic and Jurassic. Based on the occurrence of sequence boundaries, three tectonic sequences could be divided in the study area, each of which was bound by the maximum flooding surface and subdivided into Basin extension (BE) and Basin wither (BW) system tracts. The Evolution of the Western Sichuan Foreland Basin was the main Evolution in the Late Triassic, in which TS1 represents the Evolution stage of the marginal foreland Basin, TS2 represents the formation of the Western Sichuan Foreland Basin with the advent of the Longmen Mountain thrusting and napping body, and TS3 represents the development of the Western Sichuan Foreland Basin. In TS3, the Longmen Mountain was thrust and folded to form the mountain, which was affected by the An County Movement, such that the entire Sichuan Basin transferred into a continental depositional environment. This provided a large amount of carbonate fragments for western Sichuan Basin and became the principal provenance in this area. Tectonic movement is a major controlling factor of the Sichuan Basin Evolution in the Late Triassic.
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Tectonic sequence framework and sedimentary Basin Evolution of upper triassic in the sichuan Basin, China
BioTechnology: An Indian Journal, 2014Co-Authors: Lin LiangbiaoAbstract:The Late Triassic is an important geologic age for the Evolution of the Sichuan Basin. Based on data from field outcrops, drilling, and seismic acquisition, a detailed study on the sequence boundaries, division, and characteristics of the Upper Triassic in the Sichuan Basin was conducted using tectonic sequence stratigraphy to establish a sequence stratigraphic framework. The research indicates that four sequence boundaries were distinguishable in the Upper Triassic: 1) regionally structural unconformity between the Upper Triassic and Middle and Lower Triassic; 2) the boundary between the second member of the Xujiahe Formation and the Xiaotangzi Formation; 3) the secondary structural unconformity between the third and fourth members of the Xujiahe Formation; and 4) regionally structural unconformity between the Triassic and Jurassic. Based on the occurrence of sequence boundaries, three tectonic sequences could be divided in the study area, each of which was bound by the maximum flooding surface and subdivided into Basin extension (BE) and Basin wither (BW) system tracts. The Evolution of the Western Sichuan Foreland Basin was the main Evolution in the Late Triassic, in which TS1 represents the Evolution stage of the marginal foreland Basin, TS2 represents the formation of the Western Sichuan Foreland Basin with the advent of the Longmen Mountain thrusting and napping body, and TS3 represents the development of the Western Sichuan Foreland Basin. In TS3, the Longmen Mountain was thrust and folded to form the mountain, which was affected by the An County Movement, such that the entire Sichuan Basin transferred into a continental depositional environment. This provided a large amount of carbonate fragments for western Sichuan Basin and became the principal provenance in this area. Tectonic movement is a major controlling factor of the Sichuan Basin Evolution in the Late Triassic. © Trade Science Inc.
Rohitash Chandra - One of the best experts on this subject based on the ideXlab platform.
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Surrogate-assisted Bayesian inversion for landscape and Basin Evolution models
2019Co-Authors: Rohitash Chandra, Danial Azam, Arpit Kapoor, R. Dietmar MulllerAbstract:Abstract. The complex and computationally expensive features of the forward landscape and sedimentary Basin Evolution models pose a major challenge in the development of efficient inference and optimization methods. Bayesian inference provides a methodology for estimation and uncertainty quantification of free model parameters. In our previous work, parallel tempering Bayeslands was developed as a framework for parameter estimation and uncertainty quantification for the landscape and Basin Evolution modelling software Badlands. Parallel tempering Bayeslands features high-performance computing with dozens of processing cores running in parallel to enhance computational efficiency. Although parallel computing is used, the procedure remains computationally challenging since thousands of samples need to be drawn and evaluated. In large-scale landscape and Basin Evolution problems, a single model evaluation can take from several minutes to hours, and in certain cases, even days. Surrogate-assisted optimization has been with successfully applied to a number of engineering problems This motivates its use in optimisation and inference methods suited for complex models in geology and geophysics. Surrogates can speed up parallel tempering Bayeslands by developing computationally inexpensive surrogates to mimic expensive models. In this paper, we present an application of surrogate-assisted parallel tempering where that surrogate mimics a landscape Evolution model including erosion, sediment transport and deposition, by estimating the likelihood function that is given by the model. We employ a machine learning model as a surrogate that learns from the samples generated by the parallel tempering algorithm and the likelihood from the model. The entire framework is developed in a parallel computing infrastructure to take advantage of parallelization. The results show that the proposed methodology is effective in lowering the overall computational cost significantly while retaining the quality of solutions.
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Surrogate-assisted Bayesian inversion for landscape and Basin Evolution models
arXiv: Machine Learning, 2018Co-Authors: Rohitash Chandra, Danial Azam, Arpit Kapoor, R. Dietmar MüllerAbstract:The complex and computationally expensive nature of landscape Evolution models pose significant challenges in the inference and optimisation of unknown parameters. Bayesian inference provides a methodology for estimation and uncertainty quantification of unknown model parameters. In our previous work, we developed parallel tempering Bayeslands as a framework for parameter estimation and uncertainty quantification for the Badlands landscape Evolution model. Parallel tempering Bayeslands features high-performance computing with dozens of processing cores running in parallel to enhance computational efficiency. Although we use parallel computing, the procedure remains computationally challenging since thousands of samples need to be drawn and evaluated. \textcolor{black}{In large-scale landscape and Basin Evolution problems, a single model evaluation can take from several minutes to hours, and in some instances, even days. Surrogate-assisted optimisation has been used for several computationally expensive engineering problems which motivate its use in optimisation and inference of complex geoscientific models.} The use of surrogate models can speed up parallel tempering Bayeslands by developing computationally inexpensive models to mimic expensive ones. In this paper, we apply surrogate-assisted parallel tempering where that surrogate mimics a landscape Evolution model by estimating the likelihood function from the model. \textcolor{black}{We employ a neural network-based surrogate model that learns from the history of samples generated. } The entire framework is developed in a parallel computing infrastructure to take advantage of parallelism. The results show that the proposed methodology is effective in lowering the overall computational cost significantly while retaining the quality of solutions.
Ji Xiang-tian - One of the best experts on this subject based on the ideXlab platform.
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CLASSIFICATION OF TECTONIC SEQUENCE AND Basin Evolution OF THE UPPER TRIASSIC IN THE SICHUAN Basin
Journal of stratigraphy, 2020Co-Authors: Ji Xiang-tianAbstract:The Upper Triassic in the Sichuan Basin is a key to understand the Evolutionary history of this Basin. Using bore hole, outcrop, and seismostratigraphic data, the authors studied the tectonic sequence of the Upper Triassic in the Sichuan Basin. Four sequence boundaries were recognized, including 1) the tectonic unconformity between the Upper Triassic and Middle or Lower Triassic, 2) the lithostratigraphic boundary between the second member of the Xujiahe Formation and the Xiaotangzi Formation, 3) the tectonic unconformity between the third and fourth members of the Xujiahe Formation, 4) the Jurassic-Triassic tectonic unconformity.Therefore, the Upper Triassic is divided into three tectonic sequences, which can be correlated across the entire Basin. Each sequence is divided into two system tracts using the largest lake flooding surface, and these represent the Basin-expansion system tract and Basin-reduction system tract. On the basis of tectonic sequence data,the Evolution history of the Sichuan Basin is discussed. The Late Triassic in the Sichuan Basin are divided into three stages, which are the marginal foreland Basin Evolution stage (TS1), the western Sichuan Foreland Basin formation stage (TS2), and the western Sichuan Foreland Basin development stage (TS3). Because of influence by the An’xian Movement in TS2, the Longmenshan Thrust Belt was uplifted and became a mountain, which changed the Sichuan Basin into a terrestrial sedimentary environment. The most important factor controlling the Basin Evolution of the Late Triassic in the Sichuan Basin is tectonic activity.
Juliette Lamarche - One of the best experts on this subject based on the ideXlab platform.
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crustal memory and Basin Evolution in the central european Basin system new insights from a 3d structural model
Tectonophysics, 2005Co-Authors: Magdalena Scheckwenderoth, Juliette LamarcheAbstract:Abstract The Central European Basin System (CEBS) is composed of a series of subBasins, the largest of which are (1) the Norwegian–Danish Basin (2), the North German Basin extending westward into the southern North Sea and (3) the Polish Basin. A 3D structural model of the CEBS is presented, which integrates the thickness of the crust below the Permian and five layers representing the Permian–Cenozoic sediments. Structural interpretations derived from the 3D model and from backstripping are discussed with respect to published seismic data. The analysis of structural relationships across the CEBS suggests that Basin Evolution was controlled to a large degree by the presence of major zones of crustal weakness. The NW–SE-striking Tornquist Zone, the Ringkobing-Fyn High (RFH) and the Elbe Fault System (EFS) provided the borders for the large Permo–Mesozoic Basins, which developed along axes parallel to these fault systems. The Tornquist Zone, as the most prominent of these zones, limited the area affected by Permian–Cenozoic subsidence to the north. Movements along the Tornquist Zone, the margins of the Ringkobing-Fyn High and the Elbe Fault System could have influenced Basin initiation. Thermal destabilization of the crust between the major NW–SE-striking fault systems, however, was a second factor controlling the initiation and subsidence in the Permo–Mesozoic Basins. In the Triassic, a change of the regional stress field caused the formation of large grabens (Central Graben, Horn Graben, Gluckstadt Graben) perpendicular to the Tornquist Zone, the Ringkobing-Fyn High and the Elbe Fault System. The resulting subsidence pattern can be explained by a superposition of declining thermal subsidence and regional extension. This led to a dissection of the Ringkobing-Fyn High, resulting in offsets of the older NW–SE elements by the younger N–S elements. In the Late Cretaceous, the NW–SE elements were reactivated during compression, the direction of which was such that it did not favour inversion of N–S elements. A distinct change in subsidence controlling factors led to a shift of the main depocentre to the central North Sea in the Cenozoic. In this last phase, N–S-striking structures in the North Sea and NW–SE-striking structures in The Netherlands are reactivated as subsidence areas which are in line with the direction of present maximum compression. The Moho topography below the CEBS varies over a wide range. Below the N–S-trending Cenozoic depocentre in the North Sea, the crust is only 20 km thick compared to about 30 km below the largest part of the CEBS. The crust is up to 40 km thick below the Ringkobing-Fyn High and up to 45 km along the Teisseyre–Tornquist Zone. Crustal thickness gradients are present across the Tornquist Zone and across the borders of the Ringkobing-Fyn High but not across the Elbe Fault System. The N–S-striking structural elements are generally underlain by a thinner crust than the other parts of the CEBS. The main fault systems in the Permian to Cenozoic sediment fill of the CEBS are located above zones in the deeper crust across which a change in geophysical properties as P-wave velocities or gravimetric response is observed. This indicates that these structures served as templates in the crustal memory and that the prerift configuration of the continental crust is a major controlling factor for the subsequent Basin Evolution.
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Crustal memory and Basin Evolution in the Central European Basin System—new insights from a 3D structural model
Tectonophysics, 2005Co-Authors: Magdalena Scheck-wenderoth, Juliette LamarcheAbstract:Abstract The Central European Basin System (CEBS) is composed of a series of subBasins, the largest of which are (1) the Norwegian–Danish Basin (2), the North German Basin extending westward into the southern North Sea and (3) the Polish Basin. A 3D structural model of the CEBS is presented, which integrates the thickness of the crust below the Permian and five layers representing the Permian–Cenozoic sediments. Structural interpretations derived from the 3D model and from backstripping are discussed with respect to published seismic data. The analysis of structural relationships across the CEBS suggests that Basin Evolution was controlled to a large degree by the presence of major zones of crustal weakness. The NW–SE-striking Tornquist Zone, the Ringkobing-Fyn High (RFH) and the Elbe Fault System (EFS) provided the borders for the large Permo–Mesozoic Basins, which developed along axes parallel to these fault systems. The Tornquist Zone, as the most prominent of these zones, limited the area affected by Permian–Cenozoic subsidence to the north. Movements along the Tornquist Zone, the margins of the Ringkobing-Fyn High and the Elbe Fault System could have influenced Basin initiation. Thermal destabilization of the crust between the major NW–SE-striking fault systems, however, was a second factor controlling the initiation and subsidence in the Permo–Mesozoic Basins. In the Triassic, a change of the regional stress field caused the formation of large grabens (Central Graben, Horn Graben, Gluckstadt Graben) perpendicular to the Tornquist Zone, the Ringkobing-Fyn High and the Elbe Fault System. The resulting subsidence pattern can be explained by a superposition of declining thermal subsidence and regional extension. This led to a dissection of the Ringkobing-Fyn High, resulting in offsets of the older NW–SE elements by the younger N–S elements. In the Late Cretaceous, the NW–SE elements were reactivated during compression, the direction of which was such that it did not favour inversion of N–S elements. A distinct change in subsidence controlling factors led to a shift of the main depocentre to the central North Sea in the Cenozoic. In this last phase, N–S-striking structures in the North Sea and NW–SE-striking structures in The Netherlands are reactivated as subsidence areas which are in line with the direction of present maximum compression. The Moho topography below the CEBS varies over a wide range. Below the N–S-trending Cenozoic depocentre in the North Sea, the crust is only 20 km thick compared to about 30 km below the largest part of the CEBS. The crust is up to 40 km thick below the Ringkobing-Fyn High and up to 45 km along the Teisseyre–Tornquist Zone. Crustal thickness gradients are present across the Tornquist Zone and across the borders of the Ringkobing-Fyn High but not across the Elbe Fault System. The N–S-striking structural elements are generally underlain by a thinner crust than the other parts of the CEBS. The main fault systems in the Permian to Cenozoic sediment fill of the CEBS are located above zones in the deeper crust across which a change in geophysical properties as P-wave velocities or gravimetric response is observed. This indicates that these structures served as templates in the crustal memory and that the prerift configuration of the continental crust is a major controlling factor for the subsequent Basin Evolution.
