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Bevc, D., 1992, Kirchhoff wave-equation datuming with irregular acquisition topography: SEP-75, 137-156.

Black, J. L., and Brzostowski, M. A., 1993, Systematics of time-migration errors: Accepted for publication in Geophysics.

Claerbout, J. F., 1992, Anti aliasing: SEP-73, 371-390.

Hatton, L., Larner, K. L., and Gibson, B. S., 1981, Migration of seismic data from inhomogeneous media: Geophysics, 46, no. 5, 751-767.

Hubral, P., 1977, Time migration - some ray theoretical aspects: Geophys. Prosp., 25, no. 4, 738-745.

Larner, K. L., Hatton, L., Gibson, B. S., and Hsu, I. C., 1981, Depth migration of imaged time sections: Geophysics, 46, no. 5, 734-750.

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In this Appendix, we derive the analytical formulae used to obtain the ray-tracing results for the dipping layer model and the tangent construction migration.

The first step is to model the asymmetric true-diffraction curve. This is done by applying Snell's law at the point R where the normal ray crosses the interface in Figure 10. Snell's law at R is given by  
{\sin\alpha_1 \over v_1} = {\sin\beta_1 \over v_2}\end{displaymath} (9)
where $\alpha_1$ and $\beta_1 = \theta - \theta_1$ are the angles of incidence at the interface. The vertical distances (a1,a2) are expressed in terms of the vertical distances (d1,d2) at the migrated position. From the geometry of Figure 10 we get  
{d_1} = {a_1 - a_2\tan\theta\tan\theta_1}\end{displaymath} (10)
{d_2} = {a_2 + a_2\tan\theta\tan\theta_1}\end{displaymath} (11)
We now wish to derive the x-displacement along the normal ray. From Figure 10 we see that this is the sum of two terms:  
{x_0 - x_m} = {-a_1\tan(\theta_1 + \alpha_1)} -{a_2\tan\theta}\end{displaymath} (12)
the travel time along the normal ray is given by  
t_0 = {2a_1 \over v_1\cos(\theta_1 + \alpha_1)} +{2a_2 \over v_2\cos\theta}\end{displaymath} (13)
The apparent time dip D at the earth's surface is given by  
D = -{2\sin(\theta_1 + \alpha_1) \over v_1}\end{displaymath} (14)
Equations (A-4) and  (A-5) define the true-diffraction curve (Figure 2).

Common-tangent migration is performed by matching the time dip D (equation (A-6)) with the dip of the time migration curve and moving the point to the apex of the time migration curve. Carrying out this procedure as discussed in the main text results in Figure 5.

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