Changes

==Biofacies distribution during lowstand==

==Biofacies distribution during lowstand==

[[file:sedimentary-basin-analysis_fig4-30.png|300px|thumb|{{figure number|1}}Traditional biofacies model is based on the modern distribution of organisms. After Armentrout.<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><ref name=ch04r9>Armentrout, J., M., 1996, High-resolution sequence biostratigraphy: examples from the Gulf of Mexico Plio–Pleistocene, in Howell, J., Aiken, J., eds., High Resolution sequence stratigraphy: Innovations and Applications: The Geological Society of London Special Publication 104, p. 65–86.</ref> Copyright: Springer-Verlag, Geological Society of London.]]

[[file:sedimentary-basin-analysis_fig4-30.png|300px|thumb|{{figure number|1}}Traditional biofacies model is based on the modern distribution of organisms. After Armentrout.<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><ref name=ch04r9>Armentrout, J., M., 1996, High-resolution sequence biostratigraphy: examples from the Gulf of Mexico Plio–Pleistocene, in J. Howell, and J. Aiken, eds., High Resolution sequence stratigraphy: Innovations and Applications: The Geological Society of London Special Publication 104, p. 65–86.</ref> Copyright: Springer-Verlag, Geological Society of London.]]

The lowering of sea level moves the water mass- and substrate-linked [[Fossil assemblage|biofacies assemblages]] seaward—possibly far enough to place the inner neritic biofacies at the physiographic shelf/slope break. This movement causes the middle to outer neritic biofacies to shift basinward onto the upper slope of the clinoform ([[:file:sedimentary-basin-analysis_fig4-30.png|Figure 1B]]). The magnitude of relative sea level fluctuation, as well as the angle of the basin slope, controls how far the biofacies move across the physiographic profile. This pattern of low sea level biofacies distribution is confusing because the commonly used biofacies nomenclature is based on high sea level patterns where, by convention, the neritic biofacies are on the shelf ([[:file:sedimentary-basin-analysis_fig4-30.png|Figure 1A]]). During a lowstand, neritic biofacies may occur in situ on the physiographic slope.

The lowering of sea level moves the water mass- and substrate-linked [[Fossil assemblage|biofacies assemblages]] seaward—possibly far enough to place the inner neritic biofacies at the physiographic shelf/slope break. This movement causes the middle to outer neritic biofacies to shift basinward onto the upper slope of the clinoform ([[:file:sedimentary-basin-analysis_fig4-30.png|Figure 1B]]). The magnitude of relative sea level fluctuation, as well as the angle of the basin slope, controls how far the biofacies move across the physiographic profile. This pattern of low sea level biofacies distribution is confusing because the commonly used biofacies nomenclature is based on high sea level patterns where, by convention, the neritic biofacies are on the shelf ([[:file:sedimentary-basin-analysis_fig4-30.png|Figure 1A]]). During a lowstand, neritic biofacies may occur in situ on the physiographic slope.