# Reflection coefficient

The concept of a reflection coefficient is fundamental to reflection seismology. The result (derived below) for the p-wave reflection coefficient (RC) at normal incidence is:

**(**)

where and are the density and compressional wave velocity of the medium below a reflecting interface and and are the density and compressional wave velocity of the medium above a reflecting interface.

## Contents

## Definition of reflection coefficient

**1.**The ratio of the amplitude of the displacement of a reflected wave to that of the incident wave; reflectivity. The relationship is obtained by solving boundary condition equations which express the continuity of displacement and stress at the boundary. The normal-incidence reflection coefficient at an interface that separates media of densities and and velocities and for a plane wave incident from medium 1 is

(*NI* is the symbolism often used in AVA-AVO analysis). A negative reflection coefficient implies phase inversion, that a compression is reflected as a rarefaction. Where displacement is measured with respect to a space-fixed coordinate system (e.g., if positive means downward displacement), the signs differ from this. In the more general case of a plane-wave incident at an angle, both reflected P- and S-waves and transmitted P- and S-waves may be generated. The amplitude of each of these waves may be found from Zoeppritz's equations (q.v.) (or Knott’s equations).

**2.**The ratio of the reflected energy density to the incident energy density is the energy reflectivity; this value is the square of the value given by the above definition.

**3.**Reflectivity function (q.v.).

**4.**Albedo (q.v.).

**5.**A ratio of resistivities ; as derived from the method of images.

Used in describing type curves. Also called resistivity-contrast factor or reflection factor.

## Derivation of reflection coefficient

Equation **1a** is well known to all practicing geophysicists, but its derivation from first principles may not be so well known. The following treatment is an expanded version of the derivation given by Dix (p.344-7), in which the direction of wave propagation is shown as horizontal (in the x direction - see the diagram below).^{[1]} This description is simply for convenience, since the actual direction of propagation is vertical (in the z direction) with normal incidence at a horizontal reflecting boundary.

Notation according to Dix^{[1]}

Critical conditions are that both normal stresses and normal displacements are continuous across the reflecting interface (at x = 0) for all time, that is,

**(**)

**(**)

The key to this derivation is recognizing that these conditions mean the particle displacement above (with reference to Dix’s figure, to the left of) the reflecting interface, which is the sum of the particle motions of the incident and reflected pulses, must be equal to the particle displacement below (with reference to Dix’s figure, to the right of) the reflecting interface, which is the particle motion of the transmitted pulse.

**(**)

**(**)

From the general form of Hooke’s Law for small strains (Dix, p.304)^{[1]},

**(**)

where and are Lame’s first and second elastic parameters ( is also known as the shear or rigidity modulus). From equations (**5**) and (**4**), strain (dilatation) in the x-direction only is

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### Incident, transmitted and reflected pulses

Assume the incident, transmitted and reflected pulses have the following forms, and note with reference to Dix’s original figure that the incident and transmitted pulses travel to the right and the reflected pulse travels to the left:

- where
*a*and*b*are scalars for partitioning of energy at the reflecting interface.

- At x=0,

**(**)

**(**)

**(**)

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### Velocity of displacement

Equation (**2**) implies that , which means that both displacement and velocity of displacement are continuous across the reflecting interface for all time. The velocity of displacement is related to dilatation by:

By equation (**2**),

**(**)

Substituting into equation (**11**) from equations (**7**) through (**9**),

**(**)

Divide equations (**10**) and (**12**) by ,

**(**)

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By definition of elastic parameters , so equation (**13**) is

**(**)

### Solving for the reflection coefficient for normal incidence

Equations (**14**) and (**15**) are simultaneous in *a* and *b* and so can be solved for *b*, which is the reflection coefficient for normal incidence. Solving equation (**14**) for *a*,

**(**)

Solving equation (**15**) for *b*,

**(**)

Substituting for *a* from equation (**16**) into equation (**17**),

**(**)

Solving equation (**18**) for *b*,

**(**)

Equation (**19**) is the definition of a reflection coefficient for normal incidence as originally stated in Equation (**1a**).

## See also

## References

^{[2]}

^{[3]}

^{[4]}

## External links

- ↑
^{1.0}^{1.1}^{1.2}Dix, C. H. (1952), Seismic prospecting for oil: Harper & Brothers. - ↑ Whaley, J., 2017, Oil in the Heart of South America, https://www.geoexpro.com/articles/2017/10/oil-in-the-heart-of-south-america], accessed November 15, 2021.
- ↑ Wiens, F., 1995, Phanerozoic Tectonics and Sedimentation of The Chaco Basin, Paraguay. Its Hydrocarbon Potential: Geoconsultores, 2-27, accessed November 15, 2021; https://www.researchgate.net/publication/281348744_Phanerozoic_tectonics_and_sedimentation_in_the_Chaco_Basin_of_Paraguay_with_comments_on_hydrocarbon_potential
- ↑ Alfredo, Carlos, and Clebsch Kuhn. “The Geological Evolution of the Paraguayan Chaco.” TTU DSpace Home. Texas Tech University, August 1, 1991. https://ttu-ir.tdl.org/handle/2346/9214?show=full.