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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

5

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

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al

Rest

rain

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bend

Ex

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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

7

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

4

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

16

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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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

18

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 ?

21

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.

21

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

e

Simplified geological map + sediment isopachs + seismic profiles & borehole locations

22

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.

27

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 !