Mechanisms of crustal subsidence  Sedimentary basins  Isostasy  Basins due to stretching  Basins due to cooling  Basins due to convergence  Basins.

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Presentation transcript:

Mechanisms of crustal subsidence  Sedimentary basins  Isostasy  Basins due to stretching  Basins due to cooling  Basins due to convergence  Basins due to tearing of crust

Principles of isostasy

Hawaiin seamount chain with flexed lithospheric lows

Basins due to stretching

Mantle plumes associated with rifting – not required, but do occur e.g. North Atlantic rifting and emplacement of Tertiary igneous province

Half-graben formation during rifting

Faults, lakes and volcanoes dominate the landscape

Lakes filling half-grabens with thinned lithosphere generating heating and volcanism

Basins due to thermal subsidence

Basins due to thermal subsidence after heating following rifting– passive margins

Typical form of a passive margin

Passive margin accumulates thick sediment that drapes the continent/ocean transition. Subsidence is slow and exponentially declines as cooling of rifted lithosphere slows.

Basins due to convergence

Crustal depressions due to loading during subduction – accretionary trench

Basins due to loading of continental lithosphere – Foreland Basins

Basins due to tearing – strike-slip basins (pull-apart)

San Andreas Fault

Basins due to tearing of crust – strike-slip basins

Summary  Sedimentary Basin form by a number of means  Lithosphere can stretch (Rift basins)  Cool and subside (Passive margins)  Be loaded and bend (accretionary trench on oceans – Foreland basin on continents)  Tear apart to form pull-apart or strike-slip basins.  Isostasy is critical