Changes

Each clinoform package defines a locally thick progradational unit interpreted as a relative sea level lowstand delta.<ref name=ch04r92>Sutter, J., S., Berryhill, H., L. Jr., 1985, [http://archives.datapages.com/data/bulletns/1984-85/data/pg/0069/0001/0050/0077.htm Late Quaternary shelf-margin deltas, northwest Gulf of Mexico]: AAPG Bulletin, vol. 69, p. 77–91.</ref> They are lateral to other clinoform packages and are bounded above and below by regionally extensive, parallel, often uniformly high-amplitude seismic reflections. The regionally extensive parallel reflections correlate across faults and have the same relative thickness on both sides of most outershelf and upper-slope faults.

Each clinoform package defines a locally thick progradational unit interpreted as a relative sea level lowstand delta.<ref name=ch04r92>Sutter, J., S., Berryhill, H., L. Jr., 1985, [http://archives.datapages.com/data/bulletns/1984-85/data/pg/0069/0001/0050/0077.htm Late Quaternary shelf-margin deltas, northwest Gulf of Mexico]: AAPG Bulletin, vol. 69, p. 77–91.</ref> They are lateral to other clinoform packages and are bounded above and below by regionally extensive, parallel, often uniformly high-amplitude seismic reflections. The regionally extensive parallel reflections correlate across faults and have the same relative thickness on both sides of most outershelf and upper-slope faults.

The seismic reflection profile of [[:file:sedimentary-basin-analysis_fig4-19.png|Figure 1]], from the East Breaks field area, illustrates both clinoform and parallel reflection patterns in late Pleistocene sediments immediately below the sea floor (between two sets of bold arrows). Three listric growth faults (down arrows) cut through the clinoforms. These growth faults are part of the regional fault system bounding the shelf edge and upper slope salt-withdrawal basins in the High Island and East Breaks areas.

The seismic reflection profile of [[:file:sedimentary-basin-analysis_fig4-19.png|Figure 1]], from the East Breaks field area, illustrates both clinoform and parallel reflection patterns in late Pleistocene sediments immediately below the sea floor (between two sets of bold arrows). Three listric [[growth fault]]s (down arrows) cut through the clinoforms. These growth faults are part of the regional fault system bounding the shelf edge and upper slope salt-withdrawal basins in the High Island and East Breaks areas.

The arrow at the far left edge of [[:file:sedimentary-basin-analysis_fig4-19.png|Figure 1]] marks the trough (white) between parallel, high-amplitude, continuous reflections (black) that underlie the clinoforms (best expressed toward the left side of the figure). Two up arrows show the correlation of this trough across the faults. The clinoforms toplap to the right (north) against the sea floor reflection, defining the overlying transgressive surface above the clinoform tops and below the regionally extensive sea floor reflection. Additionally, the clinoform downlaps basinward, defining a downlap surface. In this case, the downlap surface coincides with the underlying sequence boundary.<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 Weimer, P., Link, M., H., eds., Seismic Facies and Sedimentary Processes of Submarine Fans and Turbidite Systems: New York, Springer-Verlag, p. 137–170.</ref>

The arrow at the far left edge of [[:file:sedimentary-basin-analysis_fig4-19.png|Figure 1]] marks the trough (white) between parallel, high-amplitude, continuous reflections (black) that underlie the clinoforms (best expressed toward the left side of the figure). Two up arrows show the correlation of this trough across the faults. The clinoforms toplap to the right (north) against the sea floor reflection, defining the overlying transgressive surface above the clinoform tops and below the regionally extensive sea floor reflection. Additionally, the clinoform downlaps basinward, defining a downlap surface. In this case, the downlap surface coincides with the underlying sequence boundary.<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 Weimer, P., Link, M., H., eds., Seismic Facies and Sedimentary Processes of Submarine Fans and Turbidite Systems: New York, Springer-Verlag, p. 137–170.</ref>