Changes

===Phase E===

===Phase E===

[[:file:sedimentary-basin-analysis_fig4-9.png|Figure 3]] began during the mid-Cenomanian with a rapid fall and rise of sea level superimposed on a long-term rise that terminally drowned the outer margins of the carbonate platforms, causing the margins to retreat landward. Widespread submarine erosion created a prominent mid-Cretaceous unconformity. Subsequent deposition was dominated by terrigenous sedimentation as large clastic prisms prograded first from the west and northwest in the Late Cretaceous and early Cenozoic and then from the north (Mississippi River drainage) during the late Cenozoic. Most of the offshore and many onshore reservoirs occur within these Late Cretaceous and Cenozoic siliciclastic deposits. The prograding prisms of siliciclastic sediment differentially loaded the underlying salt, resulting in deformation by both salt mobility and down-to-the-basin growth faulting along the shelf-slope break.<ref name=ch04r24>Bruce, C., H., 1973, Pressured shale and related sediment deformation: mechanism for development of regional contemporaneous faults: AAPG Bulletin, vol. 57, p. 878–886., 10., 1306/819A4352-16C5-11D7-8645000102C1865D</ref><ref name=ch04r117>Winker, C., D., Edwards, M., B., 1983, Unstable progradational clastic shelf margins: SEPM Special Publication 33, p. 139–157.</ref>

[[:file:sedimentary-basin-analysis_fig4-9.png|Figure 3]] began during the mid-Cenomanian with a rapid fall and rise of sea level superimposed on a long-term rise that terminally drowned the outer margins of the carbonate platforms, causing the margins to retreat landward. Widespread submarine erosion created a prominent mid-Cretaceous unconformity. Subsequent deposition was dominated by terrigenous sedimentation as large clastic prisms prograded first from the west and northwest in the Late Cretaceous and early Cenozoic and then from the north (Mississippi River drainage) during the late Cenozoic. Most of the offshore and many onshore reservoirs occur within these Late Cretaceous and Cenozoic siliciclastic deposits. The prograding prisms of siliciclastic sediment differentially loaded the underlying salt, resulting in deformation by both salt mobility and down-to-the-basin growth faulting along the shelf-slope break.<ref name=ch04r24>Bruce, C., H., 1973, [http://archives.datapages.com/data/bulletns/1971-73/data/pg/0057/0005/0850/0878.htm Pressured shale and related sediment deformation: mechanism for development of regional contemporaneous faults]: AAPG Bulletin, vol. 57, p. 878–886., 10., 1306/819A4352-16C5-11D7-8645000102C1865D</ref><ref name=ch04r117>Winker, C., D., Edwards, M., B., 1983, Unstable progradational clastic shelf margins: SEPM Special Publication 33, p. 139–157.</ref>

==See also==

==See also==