Seismic refraction

Propagating seismic waves (bottom) and related travel time diagram (top) of the direct (blue) and the first refracted phase (green)

Seismic refraction is a geophysical principle (see refraction) governed by Snell's Law. Used in the fields of engineering geology, geotechnical engineering and exploration geophysics, seismic refraction traverses (seismic lines) are performed using a seismograph(s) and/or geophone(s), in an array and an energy source. The seismic refraction method utilizes the refraction of seismic waves on geologic layers and rock/soil units in order to characterize the subsurface geologic conditions and geologic structure.

The methods depend on the fact that seismic waves have differing velocities in different types of soil (or rock): in addition, the waves are refracted when they cross the boundary between different types (or conditions) of soil or rock. The methods enable the general soil types and the approximate depth to strata boundaries, or to bedrock, to be determined.

P-Wave Refraction (aka Compression Wave Refraction)

P-wave refraction evaluates the compression wave generated by the seismic source located at a known distance from the array. The wave is generated by vertically striking a striker plate with a sledgehammer, shooting a seismic shotgun into the ground, or detonating an explosive charge in the ground. Since the compression wave is the fastest of the seismic waves, it is sometimes referred to as the primary wave and is usually more-readily identifiable within the seismic recording as compared to the other seismic waves.

S-Wave Refraction (aka Shear Wave Refraction)

S-wave refraction evaluates the shear wave generated by the seismic source located at a known distance from the array. The wave is generated by horizontally striking an object on the ground surface to induce the shear wave. Since the shear wave is the second fastest wave, it is sometimes referred to as the secondary wave. When compared to the compression wave, the shear wave is approximately one-half (but may vary significantly from this estimate) the velocity depending on the medium.

Two Horizontal Layers.

i_c₀ - critical angle
V₀ - velocity of the first layer
V₁ - velocity of the second layer
h₀ - thickness of the first layer
T0₁ - intercept

i_{{c_{{0}}}}=asin\left({V_{{0}} \over V_{{1}}}\right)

T={2h_{{0}}cos(i_{{c_{{0}}}}) \over V_{{0}}}+{X \over V_{{1}}}=T0_{{1}}+{X \over V_{{1}}}

h_{{0}}={T0_{{1}}V_{{0}} \over 2cos(i_{{c}})}

h_{{0}}={X_{{cross_{{1}}}} \over 2}{\sqrt {{V_{{1}}-V_{{0}} \over V_{{1}}+V_{{0}}}}}

Several Horizontal Layers.

h_{{n}}={V_{{n}} \over cos(i_{{n}})}\left({T0_{{n+1}} \over 2}-\sum _{{j=0}}^{{n-1}}{h_{{j}}{\sqrt {{1 \over V_{{j}}^{2}}-{1 \over V_{{j+1}}^{2}}}}}\right)

Inversion methods

The General Reciprocal method
The Plus minus method
Refraction inversion modeling (refraction tomography)
Monte Carlo simulation
Genetic algorithms

References

This article is issued from Wikipedia - version of the 11/13/2016. The text is available under the Creative Commons Attribution/Share Alike but additional terms may apply for the media files.