Quantifying One and Two Dimensional Lateral Heterogeneities in Fluvio- Deltaic Reservoirs Using 3-D Seismic Data: ABSTRACT

AAPG Bulletin ◽  
1996 ◽  
Vol 80 ◽  
Author(s):  
Anil Deshpande, Peter B. Flemings,
Keyword(s):  
Seismic Data ◽  
Two Dimensional ◽  
Lateral Heterogeneities

Comparison of Different Edge Detectors on General Public Images and Two-Dimensional Seismic Data

2019 ◽  
Vol 16 (5) ◽  
pp. 1794-1805
Author(s):  
Fahd A Alhaidari ◽  
Saleh A Dossary ◽  
Wadha M Al-Mattar ◽  
Mahi M Kamaleldin ◽  
Areej H Abed ◽  
...  
Keyword(s):  
Seismic Data ◽  
General Public ◽  
Two Dimensional ◽  
Edge Detectors

Approximate traveltimes in laterally inhomogeneous media

Geophysics ◽  
1988 ◽  
Vol 53 (1) ◽  
pp. 129-130
Author(s):  
F. Wenzel
Keyword(s):  
Velocity Field ◽  
Differential Equations ◽  
Ray Tracing ◽  
Convenient Method ◽  
Arbitrary Shape ◽  
Two Dimensional ◽  
Seismic Modeling ◽  
Homogeneous Part ◽  
Analytic Expression ◽  
Lateral Heterogeneities

A particularly convenient method for the calculation of approximate traveltimes in a two‐dimensional (2-D( medium has become popular in recent years. In this method, the slowness of a velocity field varying in both coordinates x and z is considered as being the sum of a slowness [Formula: see text], depending upon depth only, and a perturbation Δu of arbitrary shape but small compared with [Formula: see text]. The ray from the origin to any point can be easily traced for the laterally homogeneous part of the slowness, and the associated traveltime is quickly evaluated. The traveltime perturbation due to the lateral heterogeneities is approximated by the integral over the slowness perturbations along this raypath. The purpose of this note is to derive this approximation rigorously. Advantages of the method are the availability of an analytic expression for the time perturbation and the fact that no complicated ray tracing by solving differential equations is necessary. Consequently, the method allows several applications, e.g., in seismic modeling, migration, and tomography.

Two representations of the fan filter

Geophysics ◽  
1982 ◽  
Vol 47 (6) ◽  
pp. 957-959 ◽  
Author(s):  
Steve T. Hildebrand
Keyword(s):  
Seismic Data ◽  
Noise Suppression ◽  
Apparent Velocity ◽  
Two Dimensional ◽  
Velocity Filter ◽  
Slant Stacking

The fan filter is a two‐dimensional (2-D) velocity filter that removes low apparent velocity events from seismic data. The convolutional representation was derived by Embree et al (1963) and by Fail and Grau (1963). Treitel et al (1967) extended the representation to include a recursive realization. Its basic use includes migration dip suppression, multiple suppression, slant stacking, and noise suppression in stacking.

Separation of PP‐ and PS‐wave reflected seismic data using two‐dimensional finite offset common‐reflection‐surface traveltime approximation

2020 ◽  
Vol 68 (7) ◽  
pp. 2046-2063
Author(s):  
Raphael Di Carlo Silva dos Santos ◽  
João Carlos Ribeiro Cruz ◽  
Manuel de Jesus dos Santos Costa
Keyword(s):  
Seismic Data ◽  
Two Dimensional ◽  
Common Reflection Surface

THREE-DIMENSIONAL DATA COLLECTION AND PROCESSING

1978 ◽  
Vol 18 (1) ◽  
pp. 116
Author(s):  
E. G. Selby
Keyword(s):  
Data Collection ◽  
Seismic Data ◽  
Signal To Noise Ratio ◽  
Three Dimensional ◽  
Depth Map ◽  
Seismic Survey ◽  
Seismic Exploration ◽  
Two Dimensional ◽  
Additional Advantage ◽  
Information Giving

There are many limitations in the ultimate accuracy of a conventional two dimensional seismic survey. One of the most important of these is that, in general, a prospect is not a two dimensional model but a three dimensional one. For a complete interpretation of a prospect area the final result should be a migrated time or depth map. With limited sampling (a seismic grid typically consists of loops with dimensions at least 1 km by 1 km) it is necessary to interpolate grid points to allow map migration and this method has inherent inaccuracies.The three dimensional seismic exploration technique is designed to provide a sufficiently close sampled grid of seismic traces, typically with a line and depth point spacing as close as 50-100 m, to allow the seismic data itself to be migrated three dimensionally. This allows the interpreter to work with migrated seismic sections and to contour directly the migrated map.Several techniques exist to allow practical and economic collection of seismic data to provide this close sampling. These techniques can be adapted to various terrain and cultural conditions.The main advantages of three dimensional data collection are correct imaging of the seismic information giving true vertical reflection time sections and improved signal-to-noise ratio due to the increased fold inherent in the three dimensional migration process. The additional advantage to the interpreter is that the data has a sampling which gives a line intersection at each depth point in the prospect.

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