Changes

==Example: the GOM basin==

==Example: the GOM basin==

[[file:sedimentary-basin-analysis_fig4-11.png|thumb|{{figure number|1}}Schematic diagram showing a series of cross sections representing the four phases of Late Triassic to Early Cretaceous evolution of the GOM basin. Modified. Copyright: Buffler (1991); courtesy New Orleans Geological Society.]]

[[file:sedimentary-basin-analysis_fig4-11.png|thumb|{{figure number|1}}Schematic diagram showing a series of cross sections representing the four phases of Late Triassic to Early Cretaceous evolution of the GOM basin. Modified from Buffler.<ref name=Buffler_1991>Buffler, R. T., 1991, Early evolution of the Gulf of Mexico basin, ''in'' D. Goldthwaite, ed., An introduction to Central Gulf Coast geology: New Orleans Geological Society, p. 1-16.</ref> Courtesy New Orleans Geological Society.]]

Tectonic evolution of the [[basin::Gulf of Mexico basin]] has resulted in five primary tectonostratigraphic phases (A–E), each with a different sediment accumulation and deformation history. [[:file:sedimentary-basin-analysis_fig4-11.png|Figure 1]] is a schematic diagram showing a series of cross sections representing the four phases of Late Triassic to Early Cretaceous evolution of the GOM basin (see [[:file:sedimentary-basin-analysis_fig4-6.png|Figure 2]] for the location).

Tectonic evolution of the [[basin::Gulf of Mexico basin]] has resulted in five primary tectonostratigraphic phases (A–E), each with a different sediment accumulation and deformation history. [[:file:sedimentary-basin-analysis_fig4-11.png|Figure 1]] is a schematic diagram showing a series of cross sections representing the four phases of Late Triassic to Early Cretaceous evolution of the GOM basin (see [[:file:sedimentary-basin-analysis_fig4-6.png|Figure 2]] for the location).

===Phase A===

===Phase A===

[[file:sedimentary-basin-analysis_fig4-6.png|thumb|{{figure number|2}}Location of Figure 1. Modified. Copyright: Buffler (1991); courtesy New Orleans Geological Society.]]

[[file:sedimentary-basin-analysis_fig4-6.png|thumb|{{figure number|2}}Location of Figure 1. Modified from Buffler.<ref name=Buffler_1991 /> Courtesy New Orleans Geological Society.]]

[[:file:sedimentary-basin-analysis_fig4-11.png|Figure 1A]] consists of Late Triassic to Early Jurassic rifting along linear zones within brittle crust with deposition of synrift nonmarine sediments and volcanics within half-grabens.

[[:file:sedimentary-basin-analysis_fig4-11.png|Figure 1A]] consists of Late Triassic to Early Jurassic rifting along linear zones within brittle crust with deposition of synrift nonmarine sediments and volcanics within half-grabens.

[[:file:sedimentary-basin-analysis_fig4-11.png|Figure 1D]] of Early Cretaceous age is characterized by broad carbonate platforms rimmed by reef buildups along the margins established at the boundary of differential subsidence between thin and thick crust. Fine-grained carbonates were deposited in the adjacent deep basin. Terrigenous clastics continued to be input at local points along the northern margin. Known and potential reservoirs occur within both carbonate and clastic depositional systems of these early Cretaceous rocks.

[[:file:sedimentary-basin-analysis_fig4-11.png|Figure 1D]] of Early Cretaceous age is characterized by broad carbonate platforms rimmed by reef buildups along the margins established at the boundary of differential subsidence between thin and thick crust. Fine-grained carbonates were deposited in the adjacent deep basin. Terrigenous clastics continued to be input at local points along the northern margin. Known and potential reservoirs occur within both carbonate and clastic depositional systems of these early Cretaceous rocks.

[[file:sedimentary-basin-analysis_fig4-9.png|thumb|{{figure number|3}}Phase E 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 .]]

[[file:sedimentary-basin-analysis_fig4-9.png|thumb|{{figure number|3}}Phase E 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.]]

===Phase E===

===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, [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>

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, [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, DOI: 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==