# Difference between revisions of "Field data examples"

Series Investigations in Geophysics Öz Yilmaz http://dx.doi.org/10.1190/1.9781560801580 ISBN 978-1-56080-094-1 SEG Online Store

## Deconvolution

The deconvolution parameters discussed in Oz Yilmaz's Seismic Data Analysis are examined using field data examples below. Application of statistical deconvolution to pre- and poststack data is discussed. Additionally, application of deterministic deconvolution to marine data to convert the recorded source signature to its minimum-phase equivalent, and to land data recorded using a vibroseis source to convert the autocorrelogram of the sweep signal to its minimum-phase equivalent are addressed in the pages below.

## Velocity analysis and statics corrections

We shall analyze field data with three different nearsurface characteristics. Specifically, near-surface models with combinations of irregular topography and refractor geometry are examined. Refraction statics solutions are based on the variable-thickness scheme based on equation (52) and residual statics solutions are based on equation (25), both solved by the generalized linear inversion schemes (Sections C.4 and C.8).

The first field data example is from an area with nearly flat topography and presumably irregular base of weathering. Shown in Figure 3.4-29a is a CMP-stacked section based on elevation statics corrections that involved a flat datum and constant weathering velocity. Note the presence of traveltime distortions along the major reflections down to 2 s caused by the unresolved long-wavelength statics anomalies. We also note very short-wavelength traveltime distortions, much less than a cable length. This latter component of the statics can be resolved by surface-consistent residual statics corrections as shown in Figure 3.4-29b. Although the CMP stacking quality has been improved after the residual statics corrections, the long-wavelength statics anomalies remain unresolved.

Figure 3.4-30 shows plots of the first-break picks from the far-offset arrivals associated with the refracted energy. While most of the first-break picks consistently follow a linear moveout from shot to shot, note that there are some local deviations that indicate a moderate degree of complexity in the near surface. Figure 3.4-31 shows the CMP-stacked section after the application of refraction statics using the generalized reciprocal method. Compare with Figure 3.4-29a and note the significant elimination of long-wavelength statics. Also plotted are the intercept time anomalies at all shot-receiver stations. Recall that equations (50a, 50b) yield multiple values of intercept time estimates at each station. These multiple values need to be reduced to unique intercept time values at each station so as to be able to estimate the thickness of the weathering layer at each station, uniquely. The statics solution at all shot and receiver stations shows that the generalized reciprocal method can correct for all wavelengths of statics caused by undulations along the base of the weathering layer. Any remaining (residual) very short-wavelength statics should be corrected for by using a reflection-based method (Residual statics corrections).

Figure 3.4-32a shows the CMP-stacked section after the application of refraction statics corrections based on the variable-thickness, least-squares scheme (equation 52a). Compare this result with Figure 3.4-29a and note that the long-wavelength statics anomalies have been removed. Also, note that both the generalized reciprocal method (Figure 3.4-31a) and the least-squares method (Figure 3.4-32a) yield comparable results. The section in Figure 3.4-32a can further be improved by applying residual statics corrections to remove the short-wavelength statics components (Figure 3.4-32b).

The results of the least-squares statics estimates are summarized in Figure 3.4-33. The weathering velocity was assumed to be 450 m/s. Frame 1 shows the estimated intercept times as a function of the shot/receiver station number. Frame 2 shows the pick fold, namely the number of picks in each shot and receiver gather. Note the tapering of the pick fold at both ends of the line.

A quantitative measure of the accuracy of the least-squares solution is the sum of the differences between the observed picks tij and the modeled traveltimes ${\displaystyle t'_{ij}}$ (equation 52a) over each shot and receiver gather. These cumulative residual time differences over each shot and receiver are plotted in frame 3 of Figure 3.4-33. Large residuals often are related to bad picks. Nevertheless, even with good picks, there may be large residuals attributable to the inappropriateness of the model assumed for the near-surface.

Figure 3.4-33 also shows the estimated thickness of the weathering layer at all shot-receiver stations (frame 4). Finally, the computed statics and the near-surface model are shown in frames 5 and 6, respectively.

The next field data example is from an area with irregular topography associated with a sand dune and presumably a near-flat base of weathering. Figure 3.4-34a shows the CMP-stacked section with elevation statics corrections. Note the severe distortions of the geometry of shallow reflections and a very poor signal-to-noise ratio in the central part of the section. Residual statics corrections (Figure 3.4-34b) cannot improve the interpretation, especially in the center of the line where the first breaks show significant departures from a consistent linear moveout (Figure 3.4-35).

Figure 3.4-36 shows the CMP-stacked section with the application of refraction statics corrections using the generalized reciprocal method. Again, note the multiple-valued intercept time values at shot/receiver stations. The statics solution based on the reduced intercept times shows a significant medium- to long-wavelength variations. After the application of these statics corrections, the near-surface effects on the reflector geometries have been largely removed (compare with Figure 3.4-34a).

Figure 3.4-37a shows the CMP-stacked section after the application of refraction statics corrections based on the least-squares method. Compare with Figure 3.4-34a and note the significant improvement in the center of the line. This section can be improved further by applying residual statics corrections and thus removing the short-wavelength statics components (Figure 3.4-37b).

The results of the least-squares statics estimates are summarized in Figure 3.4-38. The weathering velocity was assumed to be 800 m/s. (The description of the frames in Figure 3.4-38 is the same as that of Figure 3.4-33.)

The third field data example is from an area with an abrupt change in topography and presumably surface-following the base of weathering. The CMP-stacked section with elevation statics corrections is shown in Figure 3.4-39a. Residual statics corrections significantly improve the stacking quality (Figure 3.4-39b); but the long-wavelength statics anomalies remain on the section and appear as spurious structural anomalies.

Figure 3.4-40 shows the first-break picks from the far-offset arrivals associated with the refracted energy. Figure 3.4-41 shows the CMP-stacked section with the refraction statics applied using the generalized reciprocal method and the first-break picks in Figure 3.4-40. Compare with Figure 3.4-39b and note the removal of the spurious structural discontinuity along the strong reflection just above 2 s on the left half of the section.

By using the first-break picks shown in Figure 3.4-40, the variable-thickness least-squares parameters for the near-surface were computed (equation 52a). The corresponding CMP-stacked section is shown in Figure 3.4-27a. Note the elimination of the spurious structural discontinuities seen in Figure 3.4-39b between 1 and 2 s. The CMP stacked section can be improved further by applying residual statics corrections (Figure 3.4-42b).

The results of the least-squares statics estimates are summarized in Figure 3.4-43. For the variablethickness estimate, the weathering velocity was assumed to be 900 m/s. (The description of the frames in Figure 3.4-43 is the same as that of Figure 3.4-33.)

Figure 3.4-44 is a stacked section with only the field statics applied. The pull-up at midpoint location A probably is caused by a long-wavelength statics anomaly. Start with CMP gathers (Figure 3.4-45a) and apply linear-moveout (LMO) correction (Figure 3.4-45b). Assuming that the first breaks correspond to a near-surface refractor, we use the estimated velocity from the first breaks (usually from a portion of the cable) to apply the LMO correction. The CMP-refraction stack of the shallow part of the data after the LMO correction is shown in Figure 3.4-45c. This section is the equivalent of the pilot trace section that is associated with the reflection-based statics corrections. (An example of this is shown in Figure 3.3-37.)

Traveltime deviations are estimated from the LMO-corrected gathers (Figure 3.4-45b) and are decomposed into shot and receiver intercept time components based on equation (52a). These intercept times are used to compute shot and receiver static shifts, which are then applied to the CMP gathers shown in Figure 3.4-45a. A comparison of the CMP-refraction stack section with (Figure 3.4-45d) and without (Figure 3.4-45c) refraction statics corrections clearly indicates removal of the significant long-wavelength statics anomaly centered at midpoint location A (Figure 3.4-44). The CMP-stacked section after the refraction statics corrections shown in Figure 3.4-46 no longer contains the false structure (compare with Figure 3.4-44). This long-wavelength anomaly cannot be removed by reflection statics corrections alone (Figure 3.4-47). Nevertheless, the residual statics corrections resolved the short-wavelength statics components that were present in the data. By cascading the two corrections — refraction and residual statics, we get the improved section in Figure 3.4-48.

The last field data example for refraction and residual statics corrections is from an overthurst belt with irregular topography and large elevation differences along the line traverse. Figures 3.4-49 and 3.4-50 show selected shot records. Note that the first breaks are very distinct, and the first arrivals do not manifest significant departures from linear moveout. Nevertheless, there are significant distortions along the reflection traveltime trajectories; these are largely attributed to the subsurface complexity associated with the overthrust tectonism in the area.

Figure 3.4-51 shows selected CMP gathers with elevation corrections applied and the data referenced to a flat datum of 1800 m above the topographic profile of the line. Following the normal-moveout correction (Figure 3.4-52), note that the CMP gathers exhibit short-wavelength deviations less than a cable length along the reflection traveltime trajectories. Velocity analysis and moveout correction were performed from a floating datum — a smoothed version of the topographic profile. The CMP stack with elevation corrections is shown in Figure 3.4-53.

The same CMP gathers as in Figures 3.4-51 and 3.4-52 with refraction statics applied are shown in Figures 3.4-54 and 3.4-55. A comparison of these sets of gathers indicates that the statics problem is primarily of residual nature — differences between refraction and elevation statics are not significant. In other words, long-wavelength statics, in this case, are associated for the most part with irregular topography. Differences between the CMP stack with refraction statics (Figure 3.4-56) and the CMP stack with elevation statics (Figure 3.4-53) are marginal.

Short-wavelength traveltime deviations observed on the CMP gathers in Figures 3.4-54 and 3.4-55 have been resolved by residual statics corrections as shown in Figures 3.4-57 and 3.4-58. Reflection traveltimes in Figure 3.4-57 are much like hyperbolic and those in Figure 3.4-58 are reasonably flat after moveout correction. The corresponding CMP stack shown in Figure 3.4-59, when compared with Figure 3.4-56, clearly demonstrates the improvement attained by residual statics corrections.

Figure 3.4-47  The CMP stack associated with the data in Figure 3.4-45 after field statics and residual statics corrections. Compare with Figure 3.4-44 and 3.4-46.

In areas with severely irregular topography and large elevation changes along line traverses, one may consider extrapolating the recorded data from the topographic surface to a flat datum above the topography by using the wave-equation datuming technique (further aspects of migration in practice). [1] applied this technique to the data as in Figures 3.4-49 and 3.4-50. You still will need to apply residual statics corrections to account for short-wavelength statics not associated with topography, but related to the near-surface layer geometry.

Finally, in the presence of a permafrost layer or a series of lava flows at the near-surface, the problem inherently is dynamic in nature. Specifically, under such circumstances, rays through the near-surface do not follow near-vertical paths, and thus the near-surface problem cannot be posed as a statics problem. Instead, one needs to estimate accurately a velocity-depth model that accounts for the near-surface complexity so as to honor ray bending through the near-surface layer.

Figure 3.4-48  The CMP stack associated with the data in Figure 3.4-45 after refraction and residual statics corrections. Compare with Figure 3.4-44 and 3.4-46.

Figure 3.4-60 shows a CMP-stacked section from an area with a permafrost layer at the near-surface. Note that refraction statics followed by residual statics corrections (Figure 3.4-61) yield a section with improved event continuity. Nevertheless, there still exist a number of spurious structural features that have to be accounted for. Figure 3.4-62 shows a CMP-stacked section from an area with lava flows at the near-surface. Although residual statics corrections have improved event continuity, spurious faults are troublesome (Figure 3.4-63). The traveltime distortions on the stacked sections in Figures 3.4-61 and 3.4-63 strongly suggest that they cannot be resolved by statics corrections alone. Additional work, such as velocity-depth modeling (earth modeling in depth) and imaging in depth (earth imaging in depth), is required to account for lateral velocity variations associated with near-surface complexities that result from lava flows and a permafrost layer.