Deep-water, salt-cored foldbelts: Lessons from the Mississippi Fan and Perdido foldbelts, northern Gulf of Mexico

Rowan, Mark G.; Trudgill, Bruce D.; Fiduk, J. Carl

doi:10.1029/gm115p0173

Cited by 62 publications

(61 citation statements)

References 21 publications

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“…It should be noted that the seismic cross section shown in Figure 3b does not run perpendicular to the fold axis in the distal part and therefore displays larger apparent wavelengths. Furthermore, eight individual folds have been identified in the recent work of Camerlo and Benson [2006] (Figure 3a), whereas previous studies identified less folds [Trudgill et al, 1999;Fiduk et al, 1999;Rowan et al, 2000] (inset of Figure 1 and Figure 3b).…”

Section: Description Of the Perdido Fold Beltmentioning

confidence: 79%

“…Other estimates of the total thickness of the prekinematic layer can be obtained from prestack depth migrated seismic sections [Meyer et al, 2005;Camerlo and Benson, 2006;Waller, 2007;Radovich et al, 2007a] and give values ranging between 4.3 km and 5.4 km. Indicators for salt acting as a very weak detachment are the high symmetry of folds as well as their magnitude, indicating flow of the substrate from beneath synclines into anticlines [Rowan et al, 2000]. Out-of-plane salt flow has probably not played a significant role since the fold structures, including the salt thickness, are to first order similar along strike.…”

Section: Description Of the Perdido Fold Beltmentioning

confidence: 99%

“…The prekinematic section remains at $4.5 km thickness throughout the fold belt. It consists of shallow and deep marine carbonates and marls ($2.1 km), chalks and marls ($0.5 km), and deep marine muds and turbidites ($2.0 km) [Rowan et al, 2000]. Deep marine sediments also form the thin, synkinematic layer present in the synclinal regions (<0.4 km) as well as the postkinematic, Neogene sequence ($2.0 km).…”

Section: Description Of the Perdido Fold Beltmentioning

confidence: 99%

“…Only one major phase of shortening and folding of less than 10 Ma duration occurred during late Oligocene -early Miocene in the PFB region, which resulted in relatively simple structures with very little syndeformational sedimentation. Several unique features distinguish it from many other deep water fold belts including the large thickness (4.5 km) of the prekinematic Late Jurassic to Miocene section together with the absence of earlier folding, the highly symmetric kink-banded folds, the seaward tilt of the entire fold belt, the almost synchronous evolution of its folds, and its vicinity to the large allochthonous salt structure of the Sigsbee Canopy [Trudgill et al, 1999;Rowan et al, 2000] (Figures 2 and 3). Despite the relative simplicity of the PFB, its relationship to the older, more landward depositional regimes and the evolution of allochthonous salt is complex and remains subject of discussion.…”

Section: Introductionmentioning

confidence: 99%

“…It is one of several deep water fold-and/or-thrust belts that are known from several continental margins worldwide including the Gulf of Mexico (Atwater or Mississippi Fan Fold Belt, Perdido Fold Belt, Mexican Ridges, Port Isabel Fold Belt) [Weimer and Buffler, 1992;Peel et al, 1995;Fiduk et al, 1999;Trudgill et al, 1999;Rowan et al, 2000;Wu and Bally, 2000;Marton et al, 2000;Hall, 2002;Rowan et al, 2004], offshore Brazil [Demercian et al, 1993;Cobbold et al, 1995;Mohriak et al, 1995;Davison, 2007], offshore Africa [Morley and Guerin, 1996;Spathopoulos, 1996;Cramez and Jackson, 2000;Marton et al, 2000;Rowan et al, 2004;Fort et al, 2004;Hudec and Jackson, 2004] and several others [Rowan et al, 2004, and references therein]. These fold-and-thrust belts are generally interpreted to be the result of gravity spreading and/or gliding of sedimentary overburden above a weak substratum of salt (strictly evaporites) or overpressured shale, which produces linked proximal extensional and distal contractional domains.…”

Section: Introductionmentioning

confidence: 99%

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Factors controlling the evolution of the Perdido Fold Belt, northwestern Gulf of Mexico, determined from numerical models

2009

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[1] The Perdido Fold Belt (PFB) is a prominent saltcored deep water structure in the northwestern Gulf of Mexico. It is characterized by symmetric, kink-banded folds of a $4.5 km thick prekinematic layer and its vicinity to the extensive Sigsbee Salt Canopy. We use 2-D finite element numerical models to study the evolution of the PFB as a gravity-driven fold belt both in a local context and in the context of the larger-scale passive margin, influenced by adjacent allochthonous salt structures. We show that parameters such as overburden strength, salt geometry, or salt viscosity determine timing, extent, and location of the modeled fold belt. Simplified models of the Gulf of Mexico show that toe-of-slope folding is a viable mechanism to develop diapirs in the deep salt basin and to delay folding of the distal overburden. In this scenario, the PFB likely represents the terminal folding of a much larger, diachronously formed fold belt system.

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Section: Description Of the Perdido Fold Beltmentioning

confidence: 79%

Section: Description Of the Perdido Fold Beltmentioning

confidence: 99%

Section: Description Of the Perdido Fold Beltmentioning

confidence: 99%

Section: Introductionmentioning

confidence: 99%

Section: Introductionmentioning

confidence: 99%

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Factors controlling the evolution of the Perdido Fold Belt, northwestern Gulf of Mexico, determined from numerical models

2009

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Mechanical analysis of a natural example of onland gravity gliding: The role of river incision and deposition

2014

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Gravity gliding implies rigid translation of a body down a slope where displacements are parallel to a tilted detachment plane. Although large-scale gravity gliding is commonly observed offshore, under conditions of high fluid overpressure and abundant upslope sedimentary supply, its occurrence on land is debated. We investigate the mechanical feasibility of such a process as well as the role of fluvial incision and sedimentation down the slope in the initiation of the gliding. We use a two-dimensional (2-D) finite element model combined with a 2-D failure analysis approach. The numerical models simulate the deformation and provide quantitative estimates of the failure criteria at the head and toe of the overburden. Analytical solutions approximate the numerical results by taking into account the fluvial incision and sedimentation, the internal friction angle, and the thickness and length of the overburden. Our models are based on a field example in the Andean foothills of Argentina, where gravity gliding of a 1000 m thick section is suspected above a crustal-scale anticline. The incision and sedimentation reduce and strengthen, respectively, the downslope resistance to contractional failure. The critical slope at which the gliding is initiated is reduced by fluvial incision and increased by sedimentation. We show that tectonic uplift may lead to large-scale gravity gliding on land where the overburden thickness is less than 2000 m. Incision facilitates and localizes the frontal shortening. Incision greater than 1000 m may trigger gliding for overburden up to 4000 m thick, while sedimentation thicker than 1000 m inhibits gliding. These results show that thin-skinned onland gravity gliding could be common in tectonically active regions where incision is important.

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Factors controlling early stage salt tectonics at rifted continental margins and their thermal consequences

2013

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[1] We use 2-D thermomechanical models to investigate the early evolution of rifted margin salt tectonics in terms of the competition among margin tilt, salt flow, and sediment aggradation. Model experiments include initial geometry of the rifted margin and autochthonous salt basin, subsequent synrift and thermal subsidence, sediment and water loading, and sediment compaction. We also calculate the thermal evolution of the system to investigate the impact of the high thermal conductivity of the salt (halite). Model Set 1 demonstrates a two-phase response to salt deposition: short-term thermal equilibration between the salt and crust and longer-term relaxation in which the salt basin thermal image penetrates to a depth on the order of its width. Set 2 addresses the competition among margin tilt, salt flow, and sediment aggradation. Set 3 examines other factors, the salt basin width and depth, and the rifted margin width, which potentially affect the system evolution. Set 4 shows that sawtooth subsalt topography, representing faulted basement grabens, does not strongly impede salt flow. The model results are discussed in terms of a ternary diagram with apices representing tilt, salt flow, and sedimentation rates. Characteristic styles include the following: (1) tilt and rapid salt flow draining salt to the distal basin before the sediment aggrades, (2) an equivalent system with faster aggradation that captures draining salt as diapirs between minibasins, and (3) rapid sediment aggradation in which diapir-minibasins systems develop before the salt drains. Thermal consequences of these styles are discussed. A preliminary comparison shows that salt structures resembling these styles occur in the southwest Nova Scotian margin.

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Deep-water, salt-cored foldbelts: Lessons from the Mississippi Fan and Perdido foldbelts, northern Gulf of Mexico

Cited by 62 publications

References 21 publications

Factors controlling the evolution of the Perdido Fold Belt, northwestern Gulf of Mexico, determined from numerical models

Factors controlling the evolution of the Perdido Fold Belt, northwestern Gulf of Mexico, determined from numerical models

Mechanical analysis of a natural example of onland gravity gliding: The role of river incision and deposition

Factors controlling early stage salt tectonics at rifted continental margins and their thermal consequences

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