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File:Refracted wave.png

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.

Two layers model.

Two layers model.

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

$i_{c_0}=asin\left(\frac{V_0}{V_1}\right)$

$T=\frac{2h_{0}cos(i_{c_0})}{V_0}+\frac{X}{V_1}=T{0}_1+\frac{X}{V_1}$

$h_0=\frac{T{0}_1{V}_0}{2cos(i_c)}$

$h_0=\frac{X_{cros{s}_1}}{2}\sqrt{\frac{V_1-V_0}{V_1+V_0}}$

Several Horizontal Layers.

$h_n=\frac{V_n}{cos(i_n)}(\frac{T{0}_{n+1}}{2}-\sum _{j=0}^{n-1}{h}_j\sqrt{\frac{1}{V_j^2}-\frac{1}{V_{j+1}^2}})$

Inversion Methods

• The General Reciprocal Method
• The Plus/Minus Method
• Refraction Inversion Modeling (Refraction Tomography)
• Monte Carlo simulation
• Genetic Algorithms

See also

• Reflection seismology

References

• US Army Corp of Engineers EM 1110-1-1802
• Central Federal Lands Highway Division