uGeneral setting

uFigure captions

uDepisodes

uReferences

uGeneral setting

uFigure captions

uDepisodes

uReferences

uGeneral setting

uFigure captions

uDepisodes

uReferences

uGeneral setting

uFigure captions

uDepisodes

uReferences

Figure Captions

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Depisodes 

A total of seven depositional episodes (Depisode) has been documented after 30 m.y. in the study area (Figure 2).

1) Late Oligocene-Early Miocene (30-15.5 m.y.) 

Sedimentation rate was very low (~0.016 cm/yr), and depocenters filled in the west and southwest, the paleo-geographic low, of the study area (Figure 3). The distribution of depocenters indicates that sediments mainly came from the northwest (Mississippi River) (Figure 3). Late Oligocene-Early Miocene consists of three 2nd order sequences (Figure 4).

2) Middle Miocene Depisode (15.5-10.8 m.y.) 

The sedimentation rate increased dramatically; i.e., ~ 0.071 cm/yr. Rapid deposition of this depisode followed a long period of sea level fall and extremely low sedimentation (from15.5-11.8 m.y.). Depocenters also filled in the west and southwest (Figure 3). Middle Miocene Depisode is composed of 2^nd, 3^rd and 4^th order sequence respectively (Figure 4).

3) Late Miocene Depisode I (10.8-9.0 m.y.)  

The sedimentation rate continuously increased to ~ 0.091 cm/yr. The depocenters moved toward the central and southern portion of the study area. However, the sediment sources in the northwest remain dominant (Figure 3). Late Miocene Depisode I comprises two 4^th order and one 3^rd order sequences (Figure 4).

4) Late Miocene Depisode II (9.0-5.2 m.y.) 

A lower sedimentation rate of ~0.03 cm/yr occurred, and depocenters were displaced farther to the east and south. The northwestern source remained active, but the northern source (ancestral Mobile River) had been established (Figure 3). The early lowstand systems tract had moved from basin to slope. Seismic reflection patterns show changes from oblique to sigmoidal patterns, which probably reflect a transition from sandier to more muddy deposition (Figure 2). Late Miocene Depisode II was deposited during a period of long-term lowstand sea level, and is made up of all 3rd order sequences (Figure 4).

5) Early Pliocene Depisode (5.2-3.8 m.y.) 

The sedimentation rate greatly increased ,reaching ~0.073 cm/yr, the second highest among the Depisodes. The depocenters migrated sightly southward, and sediment was derived from northern and northwestern sources, but the northern source seems to be more dominant (Figure 3). Early Pliocene Depisode was deposited in during period of highstand sea level, and consists of one 3^rd order and two 4^th order sequences (Figure 4).

6) Late Pliocene Depisode (3.8-1.9 m.y.) 

The depisode has a relatively higher sedimentation rate of ~0.058 cm/yr. The depocenters were further displaced east and then southeast. Sediment was predominantly transported from the north, and the northwestern source became less important (Figure 3). Late Pliocene Depisode was formed during a period of sea level fluctuation that included two 3^rd orders and one 4^th order sequences (Figure 4).

7) Pleistocene Depisode (1.9 m.y.-present)  

Depocenters had shifted slightly southward. The distributions of depocenters suggest that sediment was transported both from north and northwest, and the northwestern source regained its dominance (Figure 3). Pleistocene Depisode has a moderate sedimentation rate of ~0.04 cm/yr. The Pleistocene Depisode was deposited during a period of highly sea level fluctuation comprising 3^rd and one 4^th order sequences (Figure 4).

References 

Greenlee, S.M., and C. Moore, 1988, Recognition and interpretation of depositional sequences and calculation of sea-level changes from stratigraphic data—offshore New Jersey and Alabama Tertiary, in C.K. Wilgus, B.S. Hastings, C.G.St.C. Kendall, H.W. Posamentier, C.A. Ross, and J.C. Van Wagoner, eds., Sea-level Change—An Integrated Approach: SEPM, Special Publication 42, p. 329–335.

He, L., R.T. Buffler, and C. Fulthorpe, 1995, Three-dimensional sequence stratigraphic analysis, Main Pass, Northeastern Gulf of Mexico (abstract): First SEPM Congress on Sedimentary Geology, St. Petersburg Beach, Florida, Congress Program and Abstracts, p. 67.

He, L., R.T. Buffler, and C. Fulthorpe, 1996, Neogene depositional history revealed by sequence and systems tracts mapping, Main Pass Area, Northeastern Gulf of Mexico (abstract): Abstracts with Programs, Geological Society of American Annul Meeting, p. A-63.

He, L., R.T. Buffler, and C. Fulthorpe, 2002, Late Cenozoic Sequence Stratigraphy, Main Pass Area, Northeastern Gulf of Mexico, GCAGS Transactions, v. 52, p. 385-394.

Vail, P.R., F.E. Audemard, S.A. Bowman, P.N. Eisner, and C. Perez-Cruz, 1991, The stratigraphic signatures of tectonics, eustasy and sedimentology: An overview, in G. Einsele, W. Ricken, and A. Seilacher, eds., Cycles and events in stratigraphy: Springer-Verlag, p. 617-659.

Schlumberger Geco-Prakla, 1993, Gulf of Mexico Chronostratigraphic Correlation Chart (by Paleo-Data, Inc.).

Wu, S., P.R. Vail, and C. Cramez, 1990. Allochthonous salt, structure and stratigraphy of the northeastern Gulf of Mexico: Part 1: Stratigraphy. Marine and Petroleum Geology, v. 7, p. 318-333 (5 foldouts).

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