Crustal memory and basin evolution in the Central European Basin System - new insights from a 3D structural model

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 Pennian-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 Tomquist Zone, as the most prominent of these zones, limited the area affected by Permian-Cenozoic subsidence to the north. Movements along the Tomquist 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 Tomquist 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 kin thick below the Ringkobing-Fyn High and up to 45 km along the Teisseyre-Tornquist Zone. Crustal thickness gradients are present across the Tomquist 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. (c) 2004 Elsevier B.V. All rights reserved.