Stress relaxation in a semi-infinite viscoelastic earth model

1973 ◽  
Vol 63 (6-1) ◽  
pp. 2145-2154
Author(s):  
Martin Rosenman ◽  
Sarva Jit Singh
Keyword(s):  
Free Surface ◽  
Stress Relaxation ◽  
Half Space ◽  
Epicentral Distance ◽  
Strike Slip ◽  
Strike Slip Fault ◽  
Earth Model ◽  
Contour Maps ◽  
Surface Stresses ◽  
Stress Components

Abstract Expressions for quasi-static surface stresses resulting from a finite, rectangular, vertical, strike-slip fault in a Maxwellian viscoelastic half-space are derived. Variation of the stresses with time and epicentral distance is studied. Contour maps are obtained in some representative cases. It is found that all nonvanishing stress components at the free surface die exponentially with time. This is in contrast to the behavior of the displacements and strains which, in general, do not vanish for large times.

Crustal deformation by earthquakes and explosions

1970 ◽  
Vol 60 (1) ◽  
pp. 193-215 ◽  
Author(s):  
Ari Ben-Menahem ◽  
Allon Gillon
Keyword(s):  
Half Space ◽  
Crustal Deformation ◽  
Surface Deformation ◽  
Epicentral Distance ◽  
Single Layer ◽  
Strike Slip ◽  
Earth Model ◽  
Homogeneous Half Space ◽  
Layer 2 ◽  
A New Technique

abstract Static displacements were calculated for an earth model which consists of a single layer of thickness H overlying a homogeneous half space. Localized sources simulating earthquake and explosion foci are placed at depths h=H2andh=32H. The ensuing surface deformation is evaluated as a function of the epicentral distance for a typical continental crust model. A new technique is used for the quadrature of the displacement integrals. By this method one is able to calculate 1000 layer-integrals of the type F m n ( x , t ) = ∫ 0 ∞ y n e − x y J m ( t y ) d y 1 + ( A + B y 2 ) e − 2 y + D e − 4 y , with an accuracy of 0.1 per cent, in less than 2 minutes. It is found that for epicentral distances r > 20H the displacements decay like (r/H)−α where 2 < α < 5. For compressional and strike-slip displacements at all depths and for dip-slip source above the layer, 2 < α < 3. For a dip-slip source located below the layer, 3 < α < 5. Maximal displacements for wr, ur, ux, uy and uz occur at approximately r ≃ 0.8h and decay with source's-depth like h−3/2.

The stress changes that accompany strike-slip faulting

1963 ◽  
Vol 53 (5) ◽  
pp. 921-932
Author(s):  
M. A. Chinnery
Keyword(s):  
Stress Distribution ◽  
Fault Plane ◽  
Strike Slip ◽  
Strike Slip Fault ◽  
Stress Change ◽  
Contour Maps ◽  
Stress Changes ◽  
Limiting Case

Abstract In a previous paper (Chinnery, 1961) an investigation of the deformation of the ground around a strike-slip fault was described. This work is now extended to a calculation of the change in stress distribution that is brought about by such a fault. Contour maps of the components of the stress change are included, both for the general rectangular fault, and for the limiting case of a long shallow fault. These maps have a number of interesting features, and show clearly the complexity of the stress change in the neighborhood of the edges of the fault plane. The assumptions involved in the calculation are discussed at some length.

Effect of earth layering on earthquake displacement fields

1972 ◽  
Vol 62 (6) ◽  
pp. 1629-1639 ◽  
Author(s):  
Michael A. Chinnery ◽  
Dushan B. Jovanovich
Keyword(s):  
Half Space ◽  
Displacement Field ◽  
Upper Mantle ◽  
Strike Slip ◽  
Strike Slip Fault ◽  
Displacement Fields ◽  
Earth Models

abstract The displacement fields due to a very long vertical strike-slip fault are calculated for earth models consisting of two layers over a half-space. It is shown that if zones of low rigidity are present beneath the Earth's surface, they will result in an amplification of the displacement field observed at the Earth's surface. The amount of amplification depends both on the structure and the distance from the fault. If thin soft layers exist in the upper mantle, it is shown that they will have a very strong effect on the observed displacements. It may eventually be possible to use static observations at the surface to detect such layers.

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