[1] In the Basque-Cantabrian Basin (Spain), normal faulting and associated folding occurred during Late Jurassic to Early Cretaceous rifting. Cenozoic Pyrenean thick-skinned transpressive inversion in the western parts of the basin preserved the first-order extensional architecture. Integration of geological maps and seismic profiles has permitted to fully constrain the style of extensional deformation and subsequent inversion in the western portion of the Basque-Cantabrian Basin. Extensional faults offset the Paleozoic basement up to Lower Triassic rocks. The presence of an efficient décollement level represented by Triassic evaporites produced the decoupling between basement rocks and the Upper Triassic to Middle Jurassic prerift cover sequence. Extensional forced folding occurred in the cover, driven by basement faulting and the migration of evaporites toward the hanging wall of the extensional faults, with salt welds developing away from them. Upper Jurassic to Lower Cretaceous syn-rift sediments deposited synchronously with forced folding, which led to the development of extensional growth geometries associated with both master faults and nearly-transverse faults. Syn-rift growth sequences are characterized by downlap and onlap relationships with the underlying prerift units, interpreted as the result of along-strike variations of master fault extensional displacement rate. Cenozoic Pyrenean contraction generated the right-lateral transpressive inversion of basement master faults and the almost dip-slip reactivation of transverse extensional faults.

Bullets:-Determination of the transition from thick-skinned to thin-skinned in the Burgalesa Platform of the Basque-Pyrenees.-New interpretation model for the Burgalesa Platform with thick-skinned tectonics at the western boundary and thin-skinned tectonics at the eastern one.-Thickness distribution of the Upper Triassic salt allowed the detachment of the Mesozoic succession.

In the south-verging portion of the western Pyrenean Orogen, a Mesozoic basin and part of the adjacent continental margin were deformed during the Pyrenean collisional stage. The slight obliquity between extensional and compressional trends, and the presence of a Mesozoic Transfer Zone, implied that both extensional domains were exposed along-strike of the belt in the same structural position. These two areas are not only characterized by the widespread reactivation of inherited fault systems but also by different styles of deformation related to the presence or absence of an evaporitic detachment level. To the east, in the Mesozoic basin, a large-displacement south-directed low-dipping thrust detached above Triassic evaporites is present. To the west, in the Mesozoic continental margin, thick-skinned and deeply rooted right-lateral and reverse faults become first-order elements. The presence of a strike-slip component produced the eastwards extrusion of the eastern portion of the Mesozoic continental margin, which imposed an along-strike shortening at the edge of the extruded block. The transitional area from thin- to thick-skinned style of deformation, from a dip-slip to a transpressive framework, and the area accommodating the extrusion are located along a north–south-orientated band representing the southern extension of a Mesozoic Transfer Zone.

The relationships between deformation and fluid flow have been investigated in the Paleozoic basement of an isolated horst of the Catalan Coastal Ranges. A structural, petrological and geochemical study has been performed in a complex fracture network that resulted from a long-lived tectonic history (from Carboniferous to Miocene). Nine fracture types, developed from a ductile regime in the greenschist facies to a shallow brittle regime, have been characterized in order to establish P, T and fluid compositions during the evolution of the horst. Syn-cleavage and late-cleavage quartz veins (qtz1-chl1±mu and late qtz2-chl2-dol1) formed during the Hercynian ductile deformation. These minerals precipitated from metamorphic fluids, possibly evolved from seawater, at temperatures between 240 and 340ºC. En-echelon albite vein arrays (ab-qtz3-chl3±ti-an) and NE-SW normal faults generating breccias mark the change from ductile to brittle, from compression to extension and from a closed to an open hydrologic regime. This paragenesis precipitated from the mixing of metamorphic and magmatic fluids at temperatures 2 between 180 and 290ºC during the early Permian extension. Dolomite veins (dol2-chl4-qtz4), precipitated at 210-280ºC from the mixing of previous fluids with hypersaline oxidizing external brines, possibly during the late stage of the early Permian extension. Reverse faults and calcite veins (Cc1-ba) formed either during the Paleogene compression or during the Langhian to early Serravallian minor compression. Calcite and barite precipitated from meteoric or marine waters in an open hydrological system at temperatures below 50ºC. The Miocene extension is represented by NE-SW normal faults with fault gouges and NNW-SSE normal faults cemented by calcite 2 that precipitated at temperatures below 50ºC from meteoric fluids in an open basin-scale hydrological system. The studied horst was part of a relay zone between two segments of the NNW-SE Llobregat fault during the early Permian, explaining the high fracture density and the fast upflowing of hydrothermal fluids at that time, thus controlling the development of albite veins exclusively in this area.