Numerical Models of the Formation of Extensional Sedimentary Basins:

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Presentation transcript:

Numerical Models of the Formation of Extensional Sedimentary Basins: Sensitivity to Rheology and Surface Processes Susanne Buiter, Ritske Huismans and Christopher Beaumont

Model set-up We solve the mechanical equilibrium equations using a The model is on crustal scale in order to obtain a high resolution. To achieve extension, a velocity is applied on both sides, 0.5 cm/yr each. The seed is formed by a few elements of weaker (fully strain softened) material and is used to localise extension. At the base there is a roller boundary condition, which means that the crust is completely decoupled from the mantle. Isostatic compensation of mass changes is taken into account through an elastic beam which underlies the model. Faults are not specified beforehand, but develop as shear zones in a dynamic manner as the model evolves. We solve the mechanical equilibrium equations using a 2D finite-element method (sopale, Dalhousie University)

Viscous-plastic rheology Strain softening The model is thermomechanical. Frictional-plastic strain weakening is included through a reduction in the angle of internal friction with increasing strain. Coulomb failure criterion: J2 = C cos(f) + p (1-l)sin(f) Wet quartz: Gleason and Tullis, 1995 The temperature evolution is determined by solving the heat equation

Extension of Continental Crust Full sedimentation, with strain softening 30 km The figure shows the centre 200 km out of the 400 km wide modelling domain. The grid is a tracking grid, shown is a subset of around 1/6 of the total tracking grid. The calculation (Eulerian) grid is completely regular (not shown here). This model has full sedimentation, which means that every depression that forms is immediately filled with sediments. The sediments have the same properties as the crust, only their density is lower (2400 kg/m3 instead of 2800). 50 km 70 km

Effects of softening and sedimentation No sedimentation With sedimentation no soft. soft. 80 km extension in all models

Effect of viscous strength

Effect of viscous strength - comparison All models after 70 km of extension

Susanne Buiter, Adrian Pfiffner, Ritske Huismans Numerical Models of the Formation and Inversion of Extensional Sedimentary Basins Susanne Buiter, Adrian Pfiffner, Ritske Huismans

Inversion PR e 60 km c 10 km c 30 km Shortening of the ‘reference’ extension experiment. During inversion, I applied diffusion erosion at the surface. The syn-inversion sediments can be seen in red. c 10 km c 30 km