Evidences of thickening and thinning
Figure 10.10a shows a schematic 1:1 geologic section with three parallel beds of equal thicknesses dipping . Assume that the sediment velocity is given by , where is the depth below the sea floor in kilometers, density changes providing the impedance contrasts. The water bottom slopes between 6 and 12 km so that the increase of velocity does not begin until the sea floor. Show how this section would appear on an unmigrated CMP seismic section. Assume coincident source and geophone.
Because source and geophone are coincident, reflection raypaths are incident on the beds at right angles; such raypaths are shown by short dashes on Figure 10.10a. We let , location, location of reflecting point, slant depth at CMP = raypath length, depth of reflecting point, depth of seafloor above reflecting point, velocity at reflecting point, is the average velocity, -way reflection time , apparent thickness in time.
In Table 10.10a we have calculated (neglecting raypath curvature) the arrival times for the four interfaces at locations 0, 6, and 10 km. Figure 10.10b shows the time section. Note that the beds, which are of equal thickness, apparently thin with depth and also downdip. Also note that an overlying water layer distorts structure and changes the apparent dips and thicknesses.
Figure 10.10c shows a geologic section with constant velocity layers. Assume constant density and no out-of-the-plane effects; draw the unmigrated zero-offset seismic section. Scale ratio is 1:1.
|**Portion of reflection travel paths in water|
|†For travel paths in sediments|
Figure 10.10d shows reflections with solid lines, diffractions with dashed lines, and multiple reflections with short-dashed lines. Note that
- reflections are tangent to the diffractions and this would make determining the ends of the reflections difficult;
- the horizontal terminations of reflections are at the same horizontal locations as the terminations of the reflectors;
- there is no unconformity reflection where there is no change in properties even though the lithology may be different;
- the angle of the high-velocity wedge is changed and features below it are distorted;
- the top of the basement layer has a kink in it at C, and there would be a small bow-tie effect [see (7) below], because of the overlying high-velocity wedge;
- there is no fault-plane reflection on this part of the display, the fault can be located by connecting the crests of the diffractions;
- the syncline reflection becomes a buried-focus bow-tie “anticline.”
Ordinary migration would not remedy the effects of velocity changes in the horizontal direction, i.e., it would continue the erroneous appearance of the high-velocity wedge, and it would not remove the kink in the basement surface. However, with the correct migration velocity, diffractions would collapse, reflections would terminate correctly, and the syncline would appear correctly. The fault could then be located by the reflection terminations.
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Also in this chapter
- Improvement due to amplitude preservation
- Deducing fault geometry from well data
- Structural style
- Mapping faults using a grid of lines
- Fault and stratigraphic interpretation
- Interpretation of salt uplift
- Determining the nature of flow structures
- Mapping irregularly spaced data
- Evidences of thickening and thinning
- Recognition of a reef
- Seismic sequence boundaries
- Effect of horizontal velocity gradient
- Stratigraphic interpretation book
- Interpretation of a depth-migrated section
- Hydrocarbon indicators
- Waveshapes as hydrocarbon accumulation thickens