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Journal of Structural Geology, 19, 29-40. - - & TEYSSmR,C. 1992. Crustal-scale, en echelon 'Pshear' tensional bridges: a possible solution to the batholithic room problem. Geology, 20, 927-930. - - - - 33 & -1994. Strain modeling of displacementfield partitioning in transpressional orogens. Journal of Structural Geology, 16, 1575-1588. TRUESDELL, C. 1953. Two measures of vorticity. - - Journal of Rational Mechanical Analysis, 2, 173-217. VAUCHZZ,A. & NICOLAS,A. 1991. Mountain building: strike-parallel displacements and mantle anisotropy.

8 o ++ ,+ . " O~ -1 = 0. / i c. " ,",; -10 )'xy=2 -7 -6 ,, . 3 + J,r ,2 ,3 4, ,s 678,, 910I A d d i t i o n a l strain c o m p o n e n t s Although, mathematically, a n u m b e r of additional strain components can be added to increase the complexity of the transpressional strain matrix, it is difficult to visualize the interplay of more than four separate strain factors using a three-dimensional object such as a tetrahedron (higher-order phase-space is needed to analyse more than four independent factors).

The example shown models heterogeneous, steady-state type B transpression with maximum strain in the central part of the zone. strain zone. In the first case, the kinematic vorticity number and boundary conditions may be constant. The deformation zone can be modelled by using multiple deforming elements instead of just one (Fig. 9), and Table 1 is still applicable. However, the shape and the orientation of the finite strain ellipsoid generally change during deformation, even if W k and the angle of convergence do not.

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A H Grebe 61-R Receiver


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