IV OTHER TYPES OF BASINS
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1 IV OTHER TYPES OF BASINS 1-Strike-slip basins 2-Cratonic basins 3 Late orogenic basins and more 1 Tectonic setting of strike-slip faulting Woodcock
2 Seismic examples of stike-slip faults «!Flower structure!» Normal fault component of mvt. Reverse fault component of mvt. Growth structures +unconformiies Sub-vertical fault Offshore California -! difficult to image in seismic (sub-vertical feature) -! evidence of deformation of surrounding sediments -! evidence of vertical components of movement (unconsistent normal or reverse fault) 3 Altyn-Tagh strike-slip fault and associated basins 4
3 Strike-slip structures in maps Right-lateral Left-lateral Christie-Blick et al, 1985 Allen & Allen, 2005 Compressional Restraining bend Extensional Resleasing bend Opposite block moves towards the right Stress distribution in a releasing overstep (pullapart basin). Note extensional structures in the overstep and compression outside, at the fault tip. Opposite block moves towards the left Guiraud & Séguret Structure of strike-slip basin: Northern Gulf of California Low-angle and oblique to bounding faults = extensional Unconformities : jumps of faults activity High-angle and // to major bounding faults = Strike-slip Aragon & Martin
4 Strike-slip basins : Lithosphere structure Transverse section Longitunidal section Relay zone extension in relay Pull apart Basin Sedimentary basins in extensional relay zone, between strike-slip faults -! extensional faults => rift features -! stretching parallel to strike-slip faults Rm: Transpression = strike-slip + compression Transtention = strike-slip + extension 7 Strike-slip basins : Lithosphere deformation Petrunin & Sobolev, Geology 2006 Deformation patterns in model m2.2.1 after 100 km of strike-slip displacement in the sections crossing the central part of a pull-apart basin parallel to the faults (A), perpendicular to the faults (B), and in horizontal cross sections in the upper crust (C), in the lower crust (D), and in the upper mantle (E). The deformation pattern is changing from "classical" pull-apart type of structure (as shown in Fig. 1A) in the upper crust to the diffuse shear zone in the mantle, with the transition pattern in the lower crustal detachment zone 8
5 Thin-skinned vs lithosphere structure Deformation above a decollement (thrust nappe)!! no thermal effect!! average heat flow (+/- 60mW/m 2 )!! Vienna Basin Deformation affecting the entire lithosphere!! important, localised thermal effect!! High heat flow ( mw/m 2 )!!Salton Trough Allen & Allen, Subsidence of strike-slip basins Subsidence origin : vertical component on SS & normal faults reduced thermally-driven subsidence =>Thin-skinned SSB: No lithospheric thinning => Thick-skinned SSB : Fast cooling (by lateral heat loss) Rm: frequent inversion (switch of active segments within a broad wrenching zone) Subsidence curve of typical strike-slip basins (compared to other types of basins) 10 Wu & al, 2009
6 Sedimentation model Death Valley, Ca. Axial drainage Sabkha Wide alluvial fans on inactive border Narrow & steep alluvial fans along active faulted border 11 Sedimentation pattern in strike-slip basins Strike-slip movement => lateral migration of sedimentary sources & depocentres Steel, 1988 Wrenching zone => several juxtaposed SSB separated by uplifted areas => Individual basins difficult to correlate Syntectonic sediments (all. fans, progr. unconf., rapid facies change) Link &Osborne, 1978, Crowell & Link
7 2- Intra-cratonic Basins Cratonic Basins: Michigan Basin -> old rift??? Cretaceous Carboniferous Geological map 100km stratigraphy Precambrian Keweenawan rift outcrops Precambrian Keweenawan rift (positive gravity anomaly) Ordovician Iospachs (1000ft) Intra-cratonic Basins 3 different hypotheses for subsidence origin 14
8 2- Intra-cratonic Basins A new model for subsidence of cratonic basins? Armitage & Allen, 2010 Cratonic basins are part of the rift drift suite, occupying a portion of the existence field at low stretch factors and low extensional strain rate. Stretching factor "# water-loaded subsidence (no sediment=> no effect of sediment load => =geodynamic subsidence) for high strain rate (left) and low strain rate (right) Thermal diffusion cools the upwelled asthenospheric mantle at a rate equal to the upward advection of the asthenosphere. Therefore when the extension is very slow, the upwelled asthenospheric mantle cools as it rises, and the thermal lithosphere thins less than by instantaneous or fast extension. This counters the buoyancy of the otherwise warmer upwelled mantle, giving prolonged thermal subsidence. Extensional strain rate Armitage & Allen, Intra-cratonic Basins Taoudenni Basin : the largest sedimentary basin in the World From Moussine & al. 16
9 3- Late-orogenic Basins Late orogenic extensional basins East Shetland platform: Devonian extension following Caledonian orogeny 3- Late-orogenic Basins Model of late-orogenic extensional basin Séranne 1988 Seguret & al. 1989
10 3- Late-orogenic Basins Driving forces for late orogenic basins Extensional collapse Lateral extrusion Roll-back Séranne 1993 e.g. : Variscan Europe e.g. : Scandinavian Caledonides e.g. : W. Mediterranean; Aegean Subsidence of all type of basins. Compare and discuss! 20
11 Heat flow of all type of basins. Compare and discuss! Allen & Allen
IV OTHER TYPES OF BASINS
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