Titlebook: Seismic Reflection Processing; With Special Referen S. K. Upadhyay Textbook 2004 Springer-Verlag Berlin Heidelberg 2004 Anisotropy.Earth Re

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Concepts and Methods in Seismic Migration,g. 14.1 b) whereas the geological inhomogeneity (a diffractor) is a single point. It is evident that the reflection or diffraction events distributed on a hyperbola shown in Fig. 14.1 b are to be brought to their actual (point) position. This step is taken care of in the process of ‘.’.

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Exploration Value of Fracture-Induced Anisotropy,c is smaller than the seismic wavelengths that measure it (refer to Subsection 5.3.1 for details). The fabric may originate from thin layering or from oriented micro-cracks or fractures. Further, in some situations, anisotropy may be quite complex resulting from fractures in a previously anisotropic

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,Analysis of t2?x2 Relations,l velocities are calculated. This type of analysis holds in general for an isotropic medium but is not valid when one of the layers is anisotropic. It is pertinent to analyze the relationship between the true velocities and the velocities calculated from the t.?x. curves for anisotropic models.

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Estimation of Anisotropy and Layer Parameters,et Vertical Seismic Profiles and Surface Seismic Surveys may be utilized to determine the stiffness constants for azimuthally isotropic media (Section 10.1); and the elastic stiffness constants and axis of symmetry for azimuthally anisotropic (Section 10.2) media. Section 10.3 deals with . for determining anisotropy and model parameters.

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Introduction,al (P) and shear (S) wave velocities and densities on two sides of the reflector. It is the acoustic impedance contrast (i.e. (.... ? ....) for a P-wave and .... ? .... for the S-wave), which controls the absolute value of the normal incidence reflection coefficient.

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