Exact seismic velocities for TI media and extended Thomsen formulas for stronger anisotropies |
Thomsen's weak anisotropy formulation (Thomsen, 1986), being a collection of approximations designed specifically for use in velocity analysis for exploration geophysics, is clearly not exact. Approximations incorporated into the formulas become most apparent for angles greater than about 15 from the vertical, especially for compressional and vertically polarized shear wave velocities and , respectively. For VTI media, angle is measured from the -vector pointing directly into the earth.
For reference purposes, I include here the exact velocity formulas for;
quasi-P, quasi-SV, and SH seismic waves at all angles in a VTI elastic medium.
These results are available in many places
(Postma, 1955; Musgrave, 1959, 2003; Rüger, 2002; Thomsen, 2002),
but were taken directly from Berryman (1979)
with only some minor changes of notation; specifically, the ,,,,, notation for stiffnesses
has been translated to the Voigt stiffness notation wherein , ,
, , , and . The results are:
For VTI symmetry, the stiffness matrix is defined for
by
Expressions for phase velocities in Thomsen's weak anisotropy
limit can be found in many places, including Thomsen (1986, 2002)
and Rüger (2002).
The pertinent expressions for phase velocities in VTI media
as a function of angle ,
measured as previously mentioned from the vertical direction, are
All three of these parameters , , can play important roles in the velocities given by equations 7-9 when the anisotropy is large, as would be the case in fractured reservoirs when the crack densities are high enough. If crack densities are very low, then the SV shear wave will actually have no dependence on angle of wave propagation. Note that the so-called anellipticity parameter (Dellinger et al., 1993; Fomel, 2004; Tsvankin, 2005, p. 253), , vanishes when -- which (as will be shown) does happen to a very good approximation for low crack densities. Then, the results are anisotropic but have the special (elliptical) shape to the wave front mentioned previously.
For each of these phase velocities, the derivation of Thomsen's approximation has included a step that removes the square on the left-hand side of equations 1, 2, and 4 -- obtained by expanding a square root of the right hand side. This step introduces a factor of multiplying the terms on the right hand side, and -- for example -- immediately explains how equation 8 is obtained from equation 4. The other two equations for and , i.e., equations 7 and 8, involve additional approximations. More of the details about the nature of these approximations are elucidated by first obtaining an alternative approximate formulation.
Exact seismic velocities for TI media and extended Thomsen formulas for stronger anisotropies |