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• W2027053313 abstract "Abstract An efficient means for imaging structure beneath complex water-bottom topography can be obtained using conventional time-migration algorithms and a simple modification to the migration-velocity field. The process consists of two migration steps: one with the migration velocity set to zero below the water bottom and the other with the migration velocity set to zero above the water bottom. Between the two steps the data are time-shifted to account for the so called thin-lens term used in depth-migration algorithms. Efficiency is obtained by applying the thin-lens term only once and by using existing computationally optimized time migration algorithms. Results obtained from this technique are nearly identical to more costly layer-replacement and depth-migration techniques. Introduction Structures targeted for imaging by seismic surveys are often quite simple; yet their seismic response can be significantly distorted by more complex overlying water-bottom topography. This problem is well-recognized and several solutions have been proposed, such as wave-equation layer replacement (Berryhill, 1979, 1986; Yilmaz and Lucas, 1986) and depth migration (Judson et al., 1980). Although accurate, these solutions are usually impractical to use because of their large computational requirements-especially when applied to prestack data. A more common approach is to adjust the migration-velocity field to compensate for image mispositioning caused by water-bottom topography. This rather ad-hoc approach, however, can leave considerable uncertainty as to the actual target structure. In this paper, we propose an accurate and cost-effective wave equation technique that uses conventional time-migration algorithms and a simple well-defined modification to the velocity field. Background To review the problem and lay the groundwork for our solution, consider the model in Figure 1. This model has a deep water-bottom canyon (with relief of 750 m) underlain by flat horizons. The shallowest of these horizons has a normal fault positioned under the right flank of the water bottom canyon. For simplicity, the model has only two velocities, 1500 mls in the water layer and 2200 mls below the water bottom. The zero-offset seismic response of the model recorded at the surface (Figure 2) shows a time sag in the flat horizons. This time distortion, caused by the change in water bottom depth, has made the fault in the shallow horizon less obvious; and, in fact, one might interpret both of the sub water-bottom horizons as continuous, or as faulted. Ordinary time migration, even with the exact velocity field, does not remove the uncertainty as to the true structure of these horizons. As the time-migrated section (converted to depth) in Figure 3 shows, the deep horizon has not been imaged properly and could easily be interpreted as being faulted. The reason, of course, for the improper imaging is that time migration is not appropriate when strong lateral velocity variations are present." @default.
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• W2027053313 date "1990-05-07" @default.
• W2027053313 modified "2023-09-25" @default.
• W2027053313 title "Efficient Wave-Theoretical Imaging Through Complex Water-Bottom Topography" @default.
• W2027053313 doi "https://doi.org/10.4043/6339-ms" @default.
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