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We present a comprehensive 3D lithospheric-scale model of the South China Sea region (SCS), which reveals the structural configuration of the area. This model delineates seven distinct geological units: (1) seawater, (2) sedimentary cover, (3) continental crystalline crust, (4) oceanic crust, (5) upper lithospheric mantle, (6) lower lithospheric mantle, and (7) sub-lithospheric mantle. The model covers an area of 960 km × 1260 km and reach down to a depth of 250 km. It is provided as uniformly spaced grids with 10 km intervals for each unit. The geometries and density distributions within the crust have been compiled and interpolated from a variety of datasets, predominantly seismic data (see section 6). To eliminate boundary effects, the model boundaries have been extended by more than 500 km in all horizontal directions, incorporating additional constraining data from the extended region. Additionally, we provide gridded gravity field data, a density voxel cube for the sub-lithospheric mantle, and relevant tomography data. Notably, the density of the lower lithospheric mantle was derived from 3D gravity inversion modeling.
This dataset contains a series of analog models for comparing and testing positive tectonic inversion mechanisms and wedge structure formation. Furthermore, it includes a 2-D seismic reflection profile that can be compared with the models presented here. Finally, several photos of some structural features that cab be associated with wedge structure are shown. Both seismic lines and photos are located on a segment of Andean forearc, specifically, in the eastern Domeyko Cordillera and the Salar de Atacama Basin in northern Chile. Specifically, the models were deformed under extensional and compressional conditions, inducing a positive tectonic inversion, using a pure/simple-shear deformational apparatus. Our models intended to simulate the tectonic conditions presented in López et al. (2022), which illustrated the structural setting of the Domeyko Cordillera as resulting from the interplay between positive inversion tectonics and pure shortening faulting. Moreover, our models simulated three geological environments that developed sequentially through time: (a) syn-rift sedimentation, (b) post-rift and pre-shortening sedimentation, and (c) syn-shortening sedimentation. Post-rift and syn-shortening sedimentation incorporated a ductile layer (PDMS) during the shortening phase, simulating the presence of evaporitic deposits (i.e., gypsum) to test the conditions that could have controlled the formation of pure-shortening-related structures in the case study under consideration.
The profile DEKORP 3B/MVE, consisting of the two segments West and East, was recorded in 1990 as part of the DEKORP project, the German deep seismic reflection program. The focus of the DEKORP project was on deep crustal and lithospheric structures and therefore originally not on structures at shallower depths. From today's perspective, however, this depth range is of great interest for a wide range of possible technical applications (including medium-depth and deep geothermal projects). The original data is published by Stiller et al. (2021). The westernmost 91 km of the 208 km long profile 3B (West) were reprocessed on behalf of the Hessian Agency of Nature Conservation, Environment and Geology (HLNUG). As a particularity, also a set of 18 cross-lines, each ca. 12 km in length and perpendicular to the main lines, were surveyed along DEKORP 3B/MVE to get information about possible cross-dips. Four of those short cross-lines were reprocessed in 2D as well. The focus of the reprocessing of the old data was on improving the resolution / mapping of geological structures down to a depth of 6 km (approx. 3 s TWT) to describe the prolongation of faults and geological structures in more detail than in previous studies. In order to achieve these goals and in view of the fact that today's processing and evaluation methods have been improved considerably compared to the 1990‘s, a state-of-the-art reprocessing was implemented. In comparison with the original processing (Stiller et al. (2021)), more sophisticated processing steps like CRS (Common Reflection Surface) instead of CDP (Common Depth Point) stacking, turning-ray tomography and prestack time and depth migration were carried out. The reprocessing results of the DEKORP 3B (West) survey comprise all datasets newly achieved in addition to the datasets from the original processing (Stiller et al. (2021)), i.e. (1) the migrated CRS image gathers as unstacked data, and (2) the pure CRS stack, the poststack-time as well as prestack-time and prestack-depth migrated sections as stacked data. Moreover, (3) all velocity models used for the different versions including (4) the separate first-break tomography inversion, are contained. Additionally, the results of the 2D-reprocessing of cross-lines Q21-Q24 are included. All reprocessed data come in SEGY trace format, the final sections additionally in PDF graphic format. A reprocessing report is included as well as again all meta information for each domain (source, receiver, CDP) like coordinates, elevations, locations and static corrections combined in ASCII-tables for geometry assignment purposes. The DEKORP 3 survey was a combined seismic survey investigating the Variscan structures of the Rhenohercynian and the Saxothuringian. Consisting of three seismic lines it starts in the Rhenohercynian Hessian Depression (DEKORP 3A), crosses the Saxothuringian Mid-German Crystalline High (DEKORP 3B/MVE (West)) and runs parallel to the northern margin of the Moldanubian (DEKORP 3B/MVE (East)). The 207.65 km long DEKORP 3B (West) profile trends NW-SE and intersects DEKORP 3A in the Tertiary volcanic field within the "Northern Phyllite Zone". It crosses the Hessian Depression of the Rhenohercynian, runs through the Rhön Tertiary volcanic province and the Mesozoic Franconian Basin to the Bohemian Massif. The line ends at the Franconian Line. The reprocessed datasets contain a sub-section of the entire 3B (West) profile with a total length of 90.8 km of full CDP coverage, covering the territory of the state of Hesse, i. e. from the profile’s starting point in the NW to the SE until the Rhön volcanic complex. The reprocessed part of 3B (West) is intersected by four short cross-lines along the profile at km 8.75, 32.6, 64.75, 84.35 and by DEKORP 3A at km 42.3. The DEKORP '90-3B profile is of particular interest to investigate the seismic resolution of the Hessian depression, the east-hessian Buntsandstein nappe as well as the tertiary volcanic fields of the Kellerwald and Rhön.
The 47 km long KTB Line 1 was recorded in 1985 as part of deep seismic reflection investigations for the DEKORP (German Continental Seismic Reflection Program) and KTB (German Continental Deep Drilling Program) projects. The network of lines consists of two DEKORP profiles, DEKORP 4N and its appendix 4Q, and six shorter KTB profiles, KTB 8501 – 8506, arranged in the form of a grid parallel and perpendicular to the main tectonic lineaments. high-fold near-vertical incidence vibroseis acquisition. The main focus was on the crustal structure of the central Mid-European Variscides down to the Moho and the uppermost mantle and, in particular, on the suture between the Moldanubian Zone and the northward adjacent Saxothuringian Zone as well as on the metamorphic Zone of Erbendorf-Vohenstrauss. The array of the KTB profiles represents the pre-cursor of the 3-D seismic survey ISO 1989 (Integrated Seismics Oberpfalz). Details of the experiment, first results and interpretations were published by DEKORP Research Group (1987, 1988). Results discussed together with the drilling site were presented in a number of works which can be found in Emmermann & Wohlenberg (1989). The Technical Report of KTB 8501 gives complete information about acquisition and processing parameters. The European Variscides, extending from the French Central Massif to the East European Platform, originated during the collision between Gondwana and Baltica in the Late Palaeozoic. Due to involvement of various crustal blocks in the orogenesis, the mountain belt is subdivided into distinct zones. The external fold-and-thrust belts of the Rhenohercynian and Saxothuringian as well as the predominantly crystalline body of the Moldanubian dominate the central European segment of the Variscides. Polyphase tectonic deformation, magmatism and metamorphic processes led to a complex interlinking between the units. The Saxothuringian represents the infill of a Cambro-Ordovician basin. The Moldanubian contains blocks of pre-Variscan crust and their Palaezoic cover. During the Variscan orogeny the Moldanubian crust was thrust toward the northwest over the Saxothuringian foreland. Both units were welded to one another by a low-pressure metamorphism accompanied by polyphase deformation (DEKORP Research Group, 1987, 1988). The WSW – ENE striking line KTB 8501 is located ca. 12 km north of the KTB borehole. From southwest to northeast KTB 8501 crosses KTB 8504, DEKORP 4N, KTB 8505 and KTB 8506. As well as the lines KTB 8502 and 8503 the profile 8501 was arranged parallel to strike running across the NW-SE directed system of block-faults at the southwestern margin of the Bohemian Massif (DEKORP Research Group, 1988). The most important tectonic lineament, crossed by KTB 8501, is the NW-trending Franconian Line. The fault zone separates the crystalline Bohemian Massif from the foreland, which is covered by Mesozoic and Upper Palaeozoic sedimentary rocks (DEKORP Research Group, 1987).
This data publication contains (i) a slab model of the Cascadia subduction zone, derived from receiver functions, parameterized as depth to the three interfaces: t (top), c (central) and m (Moho), in NetCDF format; (ii) the station measurements of all parameters in the model in tabular and Raysum model file format; (iii) the raw receiver functions in SAC format; and (iv) auxiliary scripts for loading and plotting the data. A total of 45,601 individual receiver functions recorded at 298 seismic stations distributed across the Cascadia forearc contributed to the slab model. For each station, 100 s recordings symmetric about the P -wave arrival (i.e. 50 s noise and 50 s signal) of earthquakes with magnitudes between 5.5 and 8, in the distance range between 30 and 100 degree, were downloaded from the Incorporated Research Institutions for Seismology (IRIS) data center, the Northern California Earthquake Data Center (NCEDC), and the Natural Resources Canada Data Center (NRCAN). After quality control, radial and transverse receiver functions were computed through frequency-domain simultaneous deconvolution, with an optimal damping factor found through generalized cross validation. The continental forearc and subducting slab were parameterized as three layers over a mantle half-space, with the subduction stratigraphy bounding interfaces labeled as t (top), c (central) and m (Moho). Synthetic receiver functions were calculated through ray-theoretical modeling of plane-wave scattering at the model interfaces. The thickness, S -wave velocity (VS) and P - to S -wave velocity ratio (VP/VS) of each layer, as well as the common strike and dip of the bottom two layers and the top of the half space (in total 11 parameters) were optimized simultaneously through a simulated annealing global parameter search scheme. The misfit was defined as the anti-correlation (1 minus the cross-correlation coefficient) between the observed and predicted receiver functions, bandpass filtered between 2 and 20 s period duration. In total, 171, 143 and 137 quality A nodes were determined to constrain the t, c and m interfaces, respectively. At the trench, 105 nodes at 3 km below the local bathymetry were inserted to constrain the t and c interfaces, and at 6.5 km deeper to constrain the m interface, representing typical sediment and igneous crustal thicknesses. A spline surface was fitted to these nodes to yield margin-wide depth models. The spline coefficients were found using singular value decomposition, with the nominal depth uncertainties supplied as weights. The solution was damped by retaining the 116, 117, and 116 largest singular values for the t, c and m interfaces, respectively, based on analysis of L-curves and the Akaike information criterion. The data set is the supplemental material to Bloch, W., Bostock, M. G., Audet, P. (2023) A Cascadia Slab Model from Receiver Functions. Geochemistry, Geophysics, Geosystems.
The present dataset is a comprehensive earthquake catalogue for the Northern Chile subduction zone forearc covering the period 2007-2021, determined from IPOC seismic station data (GFZ and CNRS-INSU 2006; https://doi.org/10.14470/pk615318) plus some auxiliary stations (IPOC = Integrated Plate Boundary Observatory Chile; http://www.ipoc-network.org). The method of automatized earthquake catalogue retrieval, the different relocation steps as well as the different earthquake class labels, and the structures outlined by the seismicity are described in detail in Sippl et al. (2023). The catalogue builds on the one from Sippl et al. (2018; https://doi.org/10.5880/GFZ.4.1.2018.001), but uses a slightly deviating parameter set and a new event category. The columns of the data files are: year, month, day, hour, minute, second, latitude [dec. degrees], longitude [dec. degrees], depth [km], magnitude [ML], identifier The identifier term provides a first-order spatial classification of the seismicity, an explanation is given in Sippl et al. (2023).
This dataset presents the raw data of an experimental series of analogue models performed to investigate the influence of inherited brittle fabrics on narrow continental rifting. This model series was performed to test the influence of brittle pre-existing fabrics on the rifting deformation by cutting the brittle layer at different orientations with respect to the extension direction. An overview of the experimental series is shown in Table 1. In this dataset we provide four different types of data, that can serve as supporting material and for further analysis: 1) The top-view photos, taken at different steps and showing the deformation process of each model; they can be used to interpret the geometrical characteristics of rift-related faults; 2) Digital Elevation Models (DEMs) used to reconstruct the 3D deformation of the performed analogue models, allowing for quantitative analysis of the fault pattern. 3) Short movies built from top-view photos which help to visualize the evolution of model deformation; 4) line-drawing of fault and fracture patters to be used for fault statistical quantification. Further details on the modelling strategy and setup can be found in Corti (2012), Maestrelli et al. (2020), Molnar et al. (2020), Philippon et al. (2015), Zwaan et al. (2021) and in the publication associated with this dataset. Materials used for these analogue models were described in Montanari et al. (2017) Del Ventisette et al. (2019) and Zwaan et al. (2020).
This dataset shows the original data of a series of enhanced-gravity (centrifuge) analogue models, which were performed to test the influence of the pre-existing fabrics in the brittle upper crust on the evolution of structures resulting from oblique rifting. The obliquity of the rift (i.e., the angle between the rift axis and the direction of extension) was kept constant at 30° in all the models. The main variable of this experimental series was the orientation of the pre-existing fabrics (indicated as the angle between the trend of the fabric and the orthogonal to extension), which varied from 0° to 90° (i.e., from orthogonal to parallel to the extension direction). The inherited discontinuities were reproduced by cutting with a knife through the top brittle layer of models. An overview of the experimental series is shown in Table 1. In this dataset, four different data types are provided for further analysis: 1) Top-view photos of model deformation, taken at different time intervals and showing the deformation process of each model; they can be used to interpret the geometrical characteristics of rift-related faults; 2) Digital Elevation Models (DEMs) used to reconstruct the 3D deformation of the analogue models, allowing for quantitative analysis of the fault pattern. 3) Movies of model deformation, built from top-view photos, which help to visualize the evolution of model deformation; 4) Faults line-drawings to be used for statistical quantification of rift-related structures. Further information on the modelling strategy and setup can be found in the publication associated to this dataset and in Corti (2012), Philippon et al. (2015), Maestrelli et al. (2020), Molnar et al. (2020), Zwaan et al. (2021), Zou et al. (2023). Materials used to perform these enhanced-gravity analogue models were described in Montanari et al. (2017), Del Ventisette et al. (2019) and Zwaan et al. (2020).
The 128 km long profile 3A was recorded in 1990 as part of the joint seismic reflection venture DEKORP 1990-3/MVE (Muenchberg-Vogtland-Erzgebirge) between the two former German Republics shortly before their unification. The aim of DEKORP 1990-3/MVE was to explore the structure of the crust from the Rhenish Shield through the Bohemian Massif to the Ore Mountains. The entire profile consists of DEKORP 3A, DEKORP 3B/MVE (West) and its prolongation to the east DEKORP 3B/MVE (East). Its total length amounts to about 600 km. 24 short cross lines and associated 3D blocks with single fold coverage were also recorded. The seismic survey of 3A was conducted to investigate the deep crustal structure of the Hessian Depression with high-fold near-vertical incidence vibroseis acquisition, and thus to connect DEKORP 3B/MVE (West) to oil industry seismic profiles in the Leinegraben area. Details of the experiment, preliminary results and interpretations may be obtained from DEKORP Research Group (A) et al. (1994) and DEKORP Research Group (C) et al. (1994). The Technical Report of line 3A gives complete information about acquisition and processing parameters. The European Variscides, extending from the French Central Massif to the East European Platform, originated during the collision between Gondwana and Baltica in the Late Palaeozoic. Due to involvement of various crustal blocks in the orogenesis, the mountain belt is subdivided into distinct zones. The external fold-and-thrust belts of the Rhenohercynian and Saxothuringian as well as the predominantly crystalline body of the Moldanubian dominate the central European segment of the Variscides. Polyphase tectonic deformation, magmatism and metamorphic processes led to a complex interlinking between the units. The N-S trending DEKORP 3A line aimed at a seismic characterisation of the crust beneath the Permo-Mesozoic to Tertiary Hessian Depression. Running from the Solling Dome in the Rhenohercynian through the Kassel Graben and the late Tertiary volcanic fields of the Reinhardswald and Soehrewald, the 3A line ends in the Northern Phyllite Zone north of the Vogelsberg Volcano, the largest of the Cenozoic volcanoes in Europe (DEKORP Research Group (C) et al., 1994). DEKORP 3A is intersected by six short cross lines along the profile and by DEKORP 3B/MVE (West) at its southern end.
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