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GCElastic Wavefield Previous HitSeismicNext Hit Stratigraphy*

By

Bob A. Hardage1 and I.J. Aluka2

 

Search and Discovery Article #40184 (2006)

Posted January 28, 2006

 

*Adapted from the Geophysical Corner column, prepared by the authors and entitled, “Expanding an Elastic Definition,” in AAPG Explorer, January, 2006. Editor of Geophysical Corner is Bob A. Hardage. Managing Editor of AAPG Explorer is Vern Stefanic; Larry Nation is Communications Director.

 

1Senior research scientist, Bureau of Economic Geology, The University of Texas ([email protected] )

2Professor of physical science, Prairie View A&M University, Prairie View, Texas

 

General Statement 

Previous HitSeismicNext Hit stratigraphy has been an important Previous HitseismicNext Hit-interpretation science since the 1975 AAPG annual meeting, when its principles were introduced in a series of presentations--and particularly since its documentation two years later as AAPG’s Memoir 26 edited by Payton (1977). 

Emerging interest in multicomponent Previous HitseismicNext Hit technology now allows (and demands) the science of Previous HitseismicNext Hit stratigraphy be expanded to include all modes of a multicomponent Previous HitseismicNext Hit wavefield. The term “elastic wavefield Previous HitseismicNext Hit stratigraphy” is now used when the total elastic wavefield, not just the P-Previous HitwaveNext Hit component, is used in Previous HitseismicNext Hit stratigraphy applications. 

In elastic wavefield Previous HitseismicNext Hit stratigraphy, a Previous HitseismicNext Hit sequence is still defined as a succession of relatively conformable Previous HitseismicNext Hit reflections bounded by unconformities or their correlative conformities, just as Robert M. Mitchum (this year’s AAPG Sidney Powers Memorial winner), in AAPG Memoir 26, defined the term for P-Previous HitwaveNext Hit Previous HitseismicNext Hit stratigraphy decades ago--only now the definition is expanded to include interpretation and utilization of S-Previous HitwaveNext Hit Previous HitseismicNext Hit sequences in addition to P-Previous HitwaveNext Hit sequences. 

A Previous HitseismicNext Hit facies is still defined, using Mitchum’s original definition, as any Previous HitseismicNext Hit attribute that distinguishes one succession of reflection events from another. The only difference now is the term is expanded to include interpretation and use of S-Previous HitwaveNext Hit Previous HitseismicNext Hit facies as well as P-Previous HitwaveNext Hit facies.

 

uGeneral statement
uFigure captions
uSequences & facies
uExample
uReference
uAcknowledgment

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

uGeneral statement
uFigure captions
uSequences & facies
uExample
uReference
uAcknowledgment

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

uGeneral statement
uFigure captions
uSequences & facies
uExample
uReference
uAcknowledgment

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

uGeneral statement
uFigure captions
uSequences & facies
uExample
uReference
uAcknowledgment

 

 

 

 

Figure Captions

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Sequences and Facies: P-Previous HitWaveNext Hit vs. S-Previous HitWaveNext Hit 

Two arguments help explain why P-Previous HitwaveNext Hit sequences and facies often differ from S-Previous HitwaveNext Hit sequences and facies: 

1. Assume an elastic wavefield is traveling vertically through a horizontally layered medium. The P-Previous HitwaveNext Hit particle displacement vector associated with that wavefield then senses the fabric of the medium in a direction normal to the layering, and the S-Previous HitwaveNext Hit particle displacement vector senses the fabric in a direction parallel to the layering.  

The elastic constants of the medium (i.e., the fabric of the medium) differ in these two directions. For example, forces of different Previous HitmagnitudesNext Hit have to be applied to flex a deck of playing cards or the sheets of a notepad when those forces are directed normal to and parallel to layering (Figure 1). In this simple test, the medium is the same at the common point where forces are applied, but the fabric (or strength) of the material is not the same in the two force directions. 

Thus, P-Previous HitwaveNext Hit Previous HitseismicNext Hit sequences and facies sometimes differ from S-Previous HitwaveNext Hit sequences and facies simply because orthogonal P and S particle-displacement vectors sense and react to different elastic properties at the same subsurface Earth coordinates.  

2. The reflectivity of each mode of an elastic wavefield at an interface differs from the reflectivities of its companion modes.  

The principle is illustrated in Figure 2; the vertical axis Ri,S is the S-Previous HitwaveNext Hit reflectivity at an interface, the horizontal axis b is the ratio of the velocity ratio VP/VS across that interface (VP = P-Previous HitwaveNext Hit velocity and VS = S-Previous HitwaveNext Hit velocity), and the quantity Ri,P labeled on each curve is the P-Previous HitwaveNext Hit reflectivity at the interface. 

These curves show there are interfaces that:

  • Are invisible to P waves (the curve labeled Ri,P = 0) but are not invisible to S-waves unless b = 1.0.

  • Are invisible to S waves (the horizontal line Ri,S = 0) but are not invisible to P waves unless b = 1.0.

  • Cause P and S reflections to be in phase (shaded parameter region) and others that cause P and S reflections to be opposite polarity (unshaded parameter region).

  • Are robust P reflectors but weak S reflectors (elliptical domains A) and others that are robust S reflectors but weak P reflectors (elliptical domains B).

 

Thus, any combination of P and S sequences and facies can be encountered in elastic wavefield Previous HitseismicNext Hit stratigraphy, depending on how the VP/VS velocity ratio varies across interfaces illuminated by a multicomponent Previous HitseismicNext Hit wavefield.  

 

Example 

An example of elastic wavefield Previous HitseismicNext Hit stratigraphy interpretation is illustrated in Figure 3. P-P and P-SV images shown in this example come from a deep-water, 2-D, four-component ocean-bottom-cable profile. The unique geometry of depositional unit C allows that unit to be defined confidently in each image space, even though P-P and P-SV image-time coordinates are drastically different. 

There is an obvious facies change in the P-SV image that segregates the interval above unit C into two distinct Previous HitseismicNext Hit facies A and B. Sequence boundary 1 is defined at the common boundary between these two P-SV Previous HitseismicNext Hit facies. 

An equivalent facies break is not obvious in the P-P image. Boundary 1 drawn across P-P image space and the two P-P units labeled A and B are inferred from the P-SV interpretation. An interpreter would be hard pressed to justify P-P units A and B are different facies only on the basis of the P-Previous HitwaveNext Hit data. 

This is only one example whereby expanding Previous HitseismicNext Hit stratigraphy beyond the confines of P-Previous HitwaveNext Hit Previous HitseismicNext Hit data provides increased insight into depositional architecture and lithofacies distribution.

 

Reference 

Payton, C.E. (ed.), 1977, Previous HitSeismicNext Hit Stratigraphy--Applications to Hydrocarbon Exploration: AAPG Memoir 26, 502 p.

 

Acknowledgment 

The U.S. Department of Energy provided funding that allowed the Exploration Geophysics Laboratory to initiate the elastic wavefield Previous HitseismicTop stratigraphy research that is partly described here (Contract DE-FC26-03NT15396).

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