## Abstract

Fault analysis is required in addition to the ordinary process of structural analysis (CDP stacking) for the examination of discontinuity in the reflection horizon in question. The fault shape restoration principle is that the reflection point of a reflection wave observed at a certain receiving point is on an ellipse with the shock point and receiving point at its focal points and that the sum of the distances between the reflection point and the focal points is equal to the reflection wave propagation time. The DMO velocity is worked out by calculation using the positive travel time and inverse travel time from the common reflection surface. When the reflection surface is inclined by {theta}, the average interval velocity/cos{theta} is called the DMO velocity. When the reflection surface inclination and the average interval velocities are determined separately in this way, the position of the reflection point may be worked out, and this enables the calculation of the amount of migration (lateral movement). The reflection wave lineups carried by the original record are picked up one by one, and the average interval velocities are treated very prudently. After such a basic DMO conversion treatment, the actualities of the fault are described fairly
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## Citation Formats

Nagumo, S, Muraoka, S, and Takahashi, T.
Fault analysis in the very shallow seismic reflection method. 2; Gokusenso hanshaho ni okeru danso kaiseki. 2.
Japan: N. p.,
1997.
Web.

Nagumo, S, Muraoka, S, & Takahashi, T.
Fault analysis in the very shallow seismic reflection method. 2; Gokusenso hanshaho ni okeru danso kaiseki. 2.
Japan.

Nagumo, S, Muraoka, S, and Takahashi, T.
1997.
"Fault analysis in the very shallow seismic reflection method. 2; Gokusenso hanshaho ni okeru danso kaiseki. 2."
Japan.

@misc{etde_522628,

title = {Fault analysis in the very shallow seismic reflection method. 2; Gokusenso hanshaho ni okeru danso kaiseki. 2}

author = {Nagumo, S, Muraoka, S, and Takahashi, T}

abstractNote = {Fault analysis is required in addition to the ordinary process of structural analysis (CDP stacking) for the examination of discontinuity in the reflection horizon in question. The fault shape restoration principle is that the reflection point of a reflection wave observed at a certain receiving point is on an ellipse with the shock point and receiving point at its focal points and that the sum of the distances between the reflection point and the focal points is equal to the reflection wave propagation time. The DMO velocity is worked out by calculation using the positive travel time and inverse travel time from the common reflection surface. When the reflection surface is inclined by {theta}, the average interval velocity/cos{theta} is called the DMO velocity. When the reflection surface inclination and the average interval velocities are determined separately in this way, the position of the reflection point may be worked out, and this enables the calculation of the amount of migration (lateral movement). The reflection wave lineups carried by the original record are picked up one by one, and the average interval velocities are treated very prudently. After such a basic DMO conversion treatment, the actualities of the fault are described fairly correctly. 3 figs.}

place = {Japan}

year = {1997}

month = {May}

}

title = {Fault analysis in the very shallow seismic reflection method. 2; Gokusenso hanshaho ni okeru danso kaiseki. 2}

author = {Nagumo, S, Muraoka, S, and Takahashi, T}

abstractNote = {Fault analysis is required in addition to the ordinary process of structural analysis (CDP stacking) for the examination of discontinuity in the reflection horizon in question. The fault shape restoration principle is that the reflection point of a reflection wave observed at a certain receiving point is on an ellipse with the shock point and receiving point at its focal points and that the sum of the distances between the reflection point and the focal points is equal to the reflection wave propagation time. The DMO velocity is worked out by calculation using the positive travel time and inverse travel time from the common reflection surface. When the reflection surface is inclined by {theta}, the average interval velocity/cos{theta} is called the DMO velocity. When the reflection surface inclination and the average interval velocities are determined separately in this way, the position of the reflection point may be worked out, and this enables the calculation of the amount of migration (lateral movement). The reflection wave lineups carried by the original record are picked up one by one, and the average interval velocities are treated very prudently. After such a basic DMO conversion treatment, the actualities of the fault are described fairly correctly. 3 figs.}

place = {Japan}

year = {1997}

month = {May}

}