Seismic Signatures and Analysis of Reflection Data in by I. Tsvankin

By I. Tsvankin

Following the step forward within the final decade in making a choice on the most important parameters for time and intensity imaging in anisotropic media and constructing functional methodologies for estimating them from seismic info, this identify essentially makes a speciality of the a ways attaining exploration advantages of anisotropic processing.

This quantity presents the 1st entire description of mirrored image seismic signatures and processing equipment in anisotropic media. It identifies the main parameters for time and intensity imaging in transversely isotropic media and describes sensible methodologies for estimating them from seismic facts. additionally, it encompasses a thorough dialogue of the $64000 problems with distinctiveness and balance of seismic speed research within the presence of anisotropy. The booklet features a entire description of anisotropic imaging tools, from the theoretical history to algorithms to implementation matters. quite a few purposes to man made and box facts illustrate the advancements completed via the anisotropic processing and the opportunity of utilizing the anticipated anisotropic parameters in lithology discrimination.

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Extra info for Seismic Signatures and Analysis of Reflection Data in Anisotropic Media (Handbook of Geophysical Exploration: Seismic Exploration)

Example text

5- ................ 8" D e p e n d e n c e of P - w a v e p h a s e v e l o c i t y on t h e s h e a r - w a v e v e r t i c a l v e l o c i t y Vso. T h e d a s h e d c u r v e c o r r e s p o n d s t o V p o / V s o Vpo - 3 k m / s is fixed. 5; 26 C H A P T E R 1. E L E M E N T S OF BASIC T H E O R Y OF A N I S O T R O P I C WAVE P R O P A G A T I O N anisotropies e and 6, and Q denotes the quadratic and other higher-order terms in e and 5, which contain Vso. The negligibly weak dependence of the P-wave phase velocity on the S-wave vertical velocity implies that the influence of Vso should be small in all kinematic problems involving P-waves.

50) The upper bound on ~ can be found from the following constraint on the stiffness coefficients of TI media (Auld, 1973)" C123 < C33 (Cll -- C66 ) . 52) C13,max --- ~/C33 C l l . 53) put the lower and upper bounds on the value of g for a TI medium with a given Vpo/Vso ratio. 2. 5. 38. The upper limit of ~ decreases with the Vpo/Vso ratio. 67. 52) somewhat reduces c13,max and 5m~x. The dimensionless anisotropic coefficients are extremely convenient in developing the weak-anisotropy approximation ([e I << 1, I~l << 1, [7[ << 1) by expanding (most often, linearizing) seismic velocities, and group and polarization angles in e, 6, and 7.

The SH-wave polarization in VTI media is always horizontal, perpendicular to the vertical plane that contains the phase vector and the polarization vectors of P- and SV-waves. Therefore, in terms of polarization the SH-wave in TI media can be called a "pure" shear mode. In contrast to its behavior in isotropic media, however, the SH-wave polarization vector is strictly defined by the TI symmetry and cannot be arbitrarily rotated within the plane orthogonal to the propagation direction. 41)], for 0 = 0~ (symmetry axis) and 9 = 90 ~ (isotropy plane) the P-wave is polarized in the phase direction (vp = 9) and the SV-wave polarization vector is perpendicular to the phase vector.

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