Seismic Depth Interpretation in Thrustbelts

Depth Reckoning Speaks Volumes

A big challenge for modern seismic is the ability to image complicated structures. Fold and thrustbelts are characterized by rapid velocity variations due to juxtaposed rock types.

Generally, if you can see a structural image on seismic, the next step is to determine where that structure is actually located in depth. Once the interpretation is correctly depth positioned, cross-section balancing can be used to help create a geologically viable three-dimensional model.

The correct depth model results in better volumetric estimates of reserves.

Time vs. Depth Migration

One of the first lessons geophysicists learn about seismic data interpretation is that the seismic image is not located where it appears. It gets "migrated" to compensate for reflections not emanating from directly beneath the surface recording point, or zero offset trace location.

Traditional time migration methods using smoothed stacking velocities are considered good when diffractions are collapsed to a point and the image appears focused — but this may not correctly position the images in depth.

Time migration appropriately locates most events for simple cases where there is not a significant lateral velocity contrast across layers or steep dip in the overlying velocity boundaries.

Image Caption

Figure 5

Structurally balanced depth-migrated interpretation of imbricate thrusts below a geologically younger layer with its own complex internal structure. Compare to figure 3.

A big challenge for modern seismic is the ability to image complicated structures. Fold and thrustbelts are characterized by rapid velocity variations due to juxtaposed rock types.

Generally, if you can see a structural image on seismic, the next step is to determine where that structure is actually located in depth. Once the interpretation is correctly depth positioned, cross-section balancing can be used to help create a geologically viable three-dimensional model.

The correct depth model results in better volumetric estimates of reserves.

Time vs. Depth Migration

One of the first lessons geophysicists learn about seismic data interpretation is that the seismic image is not located where it appears. It gets "migrated" to compensate for reflections not emanating from directly beneath the surface recording point, or zero offset trace location.

Traditional time migration methods using smoothed stacking velocities are considered good when diffractions are collapsed to a point and the image appears focused — but this may not correctly position the images in depth.

Time migration appropriately locates most events for simple cases where there is not a significant lateral velocity contrast across layers or steep dip in the overlying velocity boundaries.

Generally an interpretation is done using time-migrated data that is converted to depth by vertically stretching the observed travel times. Known depths from well ties are used to adjust the final map to fit the structure depths.

Depth converting by vertically stretching the interpretation in Figure 1 would result in the same structural shape, with each layer scaled in depth based on the velocities used for the migration.

For cases where beds are dipping, the energy is refracted at high contrast interfaces, similar to the effect on the image of a straight pole inserted at an angle into a smooth pool of water; the pole appears bent at the air-water interface.

In severe cases there may be no seismic image below high contrast boundaries.

Both "pre" and "post" stack depth migration were developed to address ray bending in areas of high velocity contrasts and dipping interfaces. However, pre-stack depth migration is expensive, time consuming and requires a detailed prior understanding of the velocity depth model to achieve a solution.

Because time and money are always limited, where there is an adequate image to start with, a simplified depth migration technique can be used. Image rays are the theoretical ray paths taken by time-migrated seismic events. The time-migrated data can be depth-migrated by image ray migrating the interpreted interfaces.

Figure 2 illustrates a depth-migrated interpretation of the same model shown in Figure 1, accounting for the refraction and ray bending at the interfaces. The model exhibits a compaction velocity in the shallowest layer and constant, highly contrasted velocities in the two deeper layers.

The time migration (Figure 1) adequately corrects for the shallowest interface, but it incorrectly positions the deeper events. The depth-migrated model (Figure 2) correctly positions the steepened flanks of the anticline with the horizontal position also changed along the dipping flanks compared to the inaccurate time-migrated structure.

Thrustbelt Example

An example from South America (Figure 3) is used to illustrate typical thrustbelt interpretation challenges.

This seismic cross-section has a similar geometry as the models with a younger formation above the main detachment fault. It has a strong compaction gradient in the velocity field combined with steeply dipping beds.

This geometry causes the apparent location of the points below this interface to be affected by the gradual bending of the rays through the velocity gradient and refraction at the interfaces.

Image ray depth migrating the interpretation results in the image produced in Figure 4, where the depth-migrated result is based on the interpreted velocity field. Deeper events that appear chaotic in this figure indicate areas where the interpreted events are not resolved by the velocity model.

The time-migrated interpretation and velocity model can be iteratively modified until the resulting depth-migrated model is geologically reasonable.

Iterating the model interactively — so one can see the changes — allows the interpreter to gain insight into the raypaths that produced the images on the time-migrated seismic section.

Seismic for Cross-Section Balancing, Reservoir Modeling

Balancing geologic cross-sections is an important geologic tool for working in thrustbelts. By using a grid of 2-D seismic profiles in which each profile is image ray depth-migrated prior to cross-section balancing, the interpreter can produce a 3-D structurally balanced interpretation based on 2-D seismic.

This in turn produces less error in drilling prognosis and tying wells in structurally complex areas — and it also improves the ultimate volume calculations of trapped hydrocarbons.

In the complex overthrust model example here, the output of the image ray depth-migrated interpretations were used as input to a balanced geologic cross-section. The resulting depth-migrated interpretation required little or no correction of the basic shape of the formations or the faults to produce a geologically feasible balanced cross-section (Gigure 5).

With a more accurate depth representation of the structural geometry of a reservoir, the resulting volume calculations are more accurate. This is commonly the largest variable in the reserve calculations.

Three-D visualization, attribute analysis and interpretation with accurate well ties, and reservoir model building for simulation are significantly improved by creating more accurate depth representation of surfaces and faults (Figure 6).

Conclusions

Today's seismic processing produces not only zero offset data (un-migrated) and time-migrated data sets; but with the increase in computer capabilities, depth-migrated volumes are becoming readily available to the interpreter.

In complex areas, accurate well ties are important to help define a proper velocity field for creating a depth-migrated image. In these cases, it is also important to understand the raypaths and to use the best estimate of travel time velocity fields before proceeding with well design, depth prognosis and volumetric estimates of the reserves.