iv – other types of basins - géosciences montpellier · sedimentary sources & depocentres...
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IV – OTHER TYPES OF BASINS
1- Strike-slip basins 2- Aulacogens 3- Cratonic basins 4– Late orogenic basins and more…
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Tectonic setting of strike-slip faulting
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Woodcock 1986
1- Strike-slip Basins
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Seismic examples of strike-slip faults
« Flower structure »
Normal fault component
of mvt.
Reverse fault component
of mvt.
- 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)
1- Strike-slip Basins
Sub-vertical fault
Growth structures +unconformities
Offshore California
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Seismic examples of strike-slip basins
1- Strike-slip Basins
NW SE
Ghab Basin (Syria)
Brew & al, 2001, J.GeolSoc. London
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Altyn-Tagh strike-slip fault and associated basins
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1- Strike-slip Basins
10 km
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Strike-slip structures in maps
Christie-Blick et al, 1985 Allen & Allen, 2005
Right-lateral Left-lateral
Com
pres
sion
al
Rest
rain
ing
bend
Ex
tens
iona
l Re
slea
sing
ben
d
Opposite block moves towards the left
Opposite block moves towards the right
Guiraud & Séguret 1986
Stress distribution in a releasing overstep (pull-
apart basin). Note extensional structures
in the overstep and compression outside, at
the fault tip.
1- Strike-slip Basins
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Structure of strike-slip basin: Northern Gulf of California
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Low-angle and oblique to bounding faults = extensional
High-angle and // to major bounding faults = Strike-slip
Unconformities : jumps of faults activity Aragon & Martin 2007
1- Strike-slip Basins
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Strike-slip basins : Lithosphere structure
Sedimentary basins in extensional relay zone, between strike-slip faults - extensional faults => rift features - stretching parallel to strike-slip faults
Relay zone Transverse section Longitunidal section
Pull apart Basin
Rm: Transpression = strike-slip + compression Transtention = strike-slip + extension
1- Strike-slip Basins
extension in relay
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Strike-slip basins : Lithosphere deformation
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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
Petrunin & Sobolev, Geology 2006
1- Strike-slip Basins
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Thin-skinned vs lithosphere structure
Deformation above a decollement (thrust nappe) ⇒ no thermal effect ⇒ average heat flow (+/- 60mW/m2) ⇒ Vienna Basin
Deformation affecting the entire lithosphere ⇒ important, localised thermal effect ⇒ High heat flow (80-120 mW/m2) ⇒ Salton Trough
Allen & Allen, 2005
1- Strike-slip Basins
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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)
Wu & al , 2009
1- Strike-slip Basins
Basin subsidence
Geological Society of America Bulletin, January/February 2009 59
300 200 100Ma
00
2
4
kilometers
INTRACONTINENTAL BASINS
1 23
4 5
6
7 8
500 400
Seafloor subsidence
Figure 4. Tectonic subsidence of intracontinental basins. Locations shown in Figure 1. See thermal decay curve (dashed) for subsidence of cooling seafl oor (Stein and Stein, 1992), minus 1500 m, is shown for comparison. 1—Illi-nois Basin, Farley well (Bond and Kominz, 1984); 2—Michigan Basin (Bond and Kominz, 1984); 3—Williston Basin, North Dakota (Bond and Kominz, 1984); 4—Williston Basin, Saskatchewan (Fowler and Nisbet, 1985); 5—Northeast German Basin (Scheck and Bayer, 1999); 6—Southwest Ordos Basin (Xie, 2007); 7—Paris Basin (Prijac et al., 2000); 8—Parana Basin (Zalan et al., 1990).
STRIKE-SLIP BASINS100 Ma 0
0
2
4
kilometers
Seafloor subsidence
Seafloor subsidence
4 5a
5b
6
Ma100 00
2
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kilometers
Seafloor subsidence
1 2 3
Ma100 00
2
4
kilometers
7 89
Figure 3. Tectonic subsidence curves for strike-slip basins. Locations shown in Figure 1. Thermal decay curve (dashed) for subsidence of cooling seafl oor (Stein and Stein, 1992), minus 500 m, is shown for comparison. 1—Chuck-anut Basin (Johnson, 1984, 1985); 2—Ridge Basin (Crowell and Link, 1982; Karner and Dewey, 1986); 3—Death Valley (Hunt and Mabey, 1966); 4—Salinian block (Graham, 1976); 5—Los Angeles Basin (Rumelhart and Ingersoll, 1997); 6—Gulf of California (Curray and Moore, 1984); 7—Cuyama Basin (Dickinson et al., 1987); 8—Bozhang Depression (Hu et al., 2001); 9—Salton Trough (Kerr et al., 1979).
Xie & Heller, 2009
1: Chuckanut Basin (NW Washington) 2: Ridge Basin , 3: Death Valley, 4: Salinian Block, 5 : Los Angeles, 6: Gulf of California
Geodynamic subsidence curve of typical strike-slip basins
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Sedimentation model Death Valley, Ca.
Wide alluvial fans on inactive border
Narrow & steep alluvial fans along active faulted border
Sabkha
Axial drainage
1- Strike-slip Basins
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Strike-slip movement => lateral migration of
sedimentary sources & depocentres
• 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 1982
Steel, 1988
Sedimentation pattern in strike-slip basins
1- Strike-slip Basins
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Aulacogen basins 2- Aulacogen Basins
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Examples of Aulacogen basins
15 Stampfli & Borel, 2002
Ziegler, 1990
2- Aulacogen Basins
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Examples of Aulacogen basins
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2- Aulacogen Basins
Iapetus Ocean (Cambrian-Early Mississipian)
Appalachian orogen front (late Palaeozoic)
William Thomas, 2011, Geosphere,7, 97-120
S. Oklahoma « aulacogen » (Proterozoic-
Cambrian)
1: Rifting + thermal subsidence
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Soreghan & al 2012, Geosphere,8,654-668
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Mic
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éran
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foreland basin
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Cratonic Basins: Michigan Basin -> old rift ???
100km
Geological map
stratigraphy Ordovician
Cretaceous
Precambrian Keweenawan rift
outcrops
Precambrian Keweenawan rift (positive gravity
anomaly)
Iospachs (1000ft)
Carboniferous
3- Intra-cratonic Basins
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Taoudenni Basin : the largest sedimentary basin in the World
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From Moussine & al. From Moussine & al.
3- Intra-cratonic Basins
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Hypotheses for subsidence of intra-cratonic basins
3- Intra-cratonic Basins
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Flow in the mantle responsible for subsidence & uplift ? 3- Intra-cratonic Basins
Dynamic topography : vertical displacement of the Earth surface generated in response to flow in the mantle (differs from topography = near surface density contrasts) • Long wavelength (>1000km) • Heterogeneities within mantle imaged by seismic tomography Ex: Congo Basin ???
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Buiter & al, 2011
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A new model for subsidence of cratonic basins ?
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Armitage & Allen, 2010
3- Intra-cratonic Basins
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.
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Extensional strain rate
Stre
tchi
ng f
acto
r β
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.
Armitage & Allen, 2010
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3- Intra-cratonic Basins
The Congo intra-cratonic basin
Kadima & al, 2012
Age (Ma)
Geod
ynam
ic s
ubsi
denc
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Simplified geological map + sediment isopachs + seismic profiles & borehole locations
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Age (Ma) Age (Ma) Geodynamic subsidence from the wells + McKenzie type subsidence for normal and thick lithosphere (100 & 250 km)
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3- Intra-cratonic Basins
The Congo intra-cratonic basin Kadima & al, 2012
Age (Ma)
Residual gravity anomaly obtained by removing the basin effect to the surface free air anomaly Evidence of an ancient rift ?
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Late orogenic extensional basins East Shetland platform: Devonian extension following Caledonian orogeny
4- Late-orogenic Basins
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Model of late-orogenic extensional basin
Seguret & al. 1989
Séranne 1988
4- Late-orogenic Basins
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Driving forces for late orogenic basins
Séranne 1993
e.g. : Variscan Europe e.g. : Scandinavian Caledonides e.g. : W. Mediterranean; Aegean
4- Late-orogenic Basins
Extensional collapse Lateral extrusion Roll-back
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Subsidence of all type of basins.
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Compare and discuss !
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Heat flow of all type of basins. flow of all type of basins.
Allen & Allen 2006
Compare and discuss !