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[[File:Sedimentary-basin-analysis fig4-44.png|thumb|300px|{{Figure number|1}}Schematic diagram of the seismic reflection profile along the west side of the East Breaks 160-161 field. From Armentrout and Clement;<ref name=ch04r10 /> courtesy Gulf Coast SEPM.]]

[[File:Sedimentary-basin-analysis fig4-44.png|thumb|300px|{{Figure number|1}}Schematic diagram of the seismic reflection profile along the west side of the East Breaks 160-161 field. From Armentrout and Clement;<ref name=ch04r10 /> courtesy Gulf Coast SEPM.]]

The structural/stratigraphic configuration of the East Breaks 160-161 minibasin formed well after ''Glob alt'' deposition. As discussed earlier, the High Island–East Breaks basin was a late Pliocene - early Pleistocene slope basin through which [http://cdn.intechopen.com/pdfs-wm/25729.pdf gravity flow sands] flowed southward. [[Depocenter#Sediment_supply_rate_and_facies_patterns|Progradation]] overloaded the underlying [[Halite|salt]] and minibasins formed as a succession of southward-stepping [[Growth fault|growth-fault]]/[http://www.beg.utexas.edu/indassoc/agl/pubs/Withdrawal.pdf salt-withdrawal] sediment thicks ([[:File:Sedimentary-basin-analysis fig4-44.png|Figure 1]]).

The structural/stratigraphic configuration of the East Breaks 160-161 [[minibasin]] formed well after ''Glob alt'' deposition. As discussed earlier, the High Island–East Breaks basin was a late Pliocene - early Pleistocene slope basin through which [http://cdn.intechopen.com/pdfs-wm/25729.pdf gravity flow sands] flowed southward. [[Depocenter#Sediment_supply_rate_and_facies_patterns|Progradation]] overloaded the underlying [[Halite|salt]] and minibasins formed as a succession of southward-stepping growth-fault/[http://www.beg.utexas.edu/indassoc/agl/pubs/Withdrawal.pdf salt-withdrawal] sediment thicks ([[:File:Sedimentary-basin-analysis fig4-44.png|Figure 1]]).

==Structural traps==

==Structural traps==

==Stratigraphic traps==

==Stratigraphic traps==

Pure [[stratigraphic trap]]s occur where basinal sandstones completely bypassed [[Dip|updip]] areas subsequently filled by mud, providing both top seal and updip lateral seal.<ref name=ch04r22 /><ref name=ch04r36>Galloway, W. E., and T. A. McGilvery, 1995, Facies of a submarine canyon fill reservoir complex, lower Wilcox Group (Paleocene), central Texas coastal plain, in R. D. Winn, Jr., and J. M. Armentrout, eds., Turbidites and Associated Deep-Water Facies: WEPM Core Workshop 20, p. 1–23.</ref>

Pure [[stratigraphic trap]]s occur where basinal sandstones completely bypassed [[Dip|updip]] areas subsequently filled by mud, providing both top seal and up dip [[lateral]] seal.<ref name=ch04r22 /><ref name=ch04r36>Galloway, W. E., and T. A. McGilvery, 1995, Facies of a submarine canyon fill reservoir complex, lower Wilcox Group (Paleocene), central Texas coastal plain, in R. D. Winn, Jr., and J. M. Armentrout, eds., Turbidites and Associated Deep-Water Facies: WEPM Core Workshop 20, p. 1–23.</ref>

==Timing of fault movement==

==Timing of fault movement==

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In the East Breaks 160-161 minibasin, the [[Growth fault|fault]] splay fault A′ forms the northern boundary to the field ([[:file:Sedimentary-basin-analysis fig4-43.png|Figures 2]] and [[:file:Sedimentary-basin-analysis fig4-42.png|3]]). The dynamic phase of this fault is recorded by the wedge-shaped sediment thickening into the fault, deposited between pre-''Hyal B'' (ca. 1.00 Ma) time of deposition and late ''Trim A'' (ca. 0.56 Ma) time of deposition ([[:file:Sedimentary-basin-analysis fig4-31.png|Figure 4]]). Its growth phase began about 1.20 Ma.<ref name=ch04r10>Armentrout, J. M., and J. F. Clement, 1990, Biostratigraphic calibration of depositional cycles: a case study in High Island–Galveston–East Breaks areas, offshore Texas: Proceedings, Gulf Coast Section SEPM 11th Annual Research Conference, p. 21–51.</ref><ref name=ch04r7>Armentrout, J. M., 1991, Paleontological constraints on depositional [[modeling]]: examples of integration of biostratigraphy and seismic stratigraphy, Pliocene–Pleistocene, Gulf of Mexico, in P. Weimer, and M. H. Link, eds., Seismic Facies and Sedimentary Processes of Submarine Fans and Turbidite Systems: New York, Springer-Verlag, p. 137–170.</ref> Sea-floor expression of this fault clearly indicates offset of Holocene sediments, showing that the fault is currently active ([[:file:Sedimentary-basin-analysis fig4-43.png|Figure 2]]).

In the East Breaks 160-161 minibasin, the [[Growth fault|fault]] splay fault A′ forms the northern boundary to the field ([[:file:Sedimentary-basin-analysis fig4-43.png|Figures 2]] and [[:file:Sedimentary-basin-analysis fig4-42.png|3]]). The dynamic phase of this fault is recorded by the wedge-shaped sediment thickening into the fault, deposited between pre-''Hyal B'' (ca. 1.00 Ma) time of deposition and late ''Trim A'' (ca. 0.56 Ma) time of deposition ([[:file:Sedimentary-basin-analysis fig4-31.png|Figure 4]]). Its growth phase began about 1.20 Ma.<ref name=ch04r10>Armentrout, J. M., and J. F. Clement, 1990, Biostratigraphic calibration of depositional cycles: a case study in High Island–Galveston–East Breaks areas, offshore Texas: Proceedings, Gulf Coast Section SEPM 11th Annual Research Conference, p. 21–51.</ref><ref name=ch04r7>Armentrout, J. M., 1991, Paleontological constraints on depositional [[modeling]]: examples of integration of biostratigraphy and seismic stratigraphy, Pliocene–Pleistocene, Gulf of Mexico, in P. Weimer, and M. H. Link, eds., Seismic Facies and Sedimentary Processes of Submarine Fans and Turbidite Systems: New York, Springer-Verlag, p. 137–170.</ref> Sea-floor expression of this fault clearly indicates [[offset]] of [[Holocene]] sediments, showing that the fault is currently active ([[:file:Sedimentary-basin-analysis fig4-43.png|Figure 2]]).

==See also==

==See also==

[[Category:Sedimentary basin analysis]]

[[Category:Sedimentary basin analysis]]

[[Category:East Breaks]]

[[Category:East Breaks]]