Abstract

In the eastern Gulf of Mexico, the pattern of early stage salt flow is complicated by basement topography consisting of a series of plunging arches that trend obliquely to the early flow direction. Seismic lines downdip of the Florida Middle Ground Arch reveal a puzzling array of structures. Sections trending roughly north–south (parallel to the regional dip) document predominantly extensional structures; however, east–west sections reveal shortening structures. Both sets of structures occur well updip of the downdip salt pinchout. We designed a physical-modeling study to investigate these puzzling relationships. Models presented in Part 1 of this paper indicate that localized shortening and extension can occur as salt passes over simple base-salt steps. Physical models were run with complex salt isopachs featuring plunging arches oblique to dip and salt flow. Models reveal the formation of shortening belts as the salt and its thin prekinematic overburden are translated across the arches. The complex salt isopachs deflect salt flow to produce convergent and divergent flow, which, along with flow-velocity gradients, results in the rotation of early formed thrust belts. Rotations of up to 70° were recorded in the most complex model, resulting in transported fold belts with trends that were close to dip parallel, similar to those observed on seismic data from the eastern Gulf of Mexico. Additional zones of shortening are found in and around complex salt pinchouts in the updip zones of the gravity-gliding system. The dynamic nature of these salt-related tectonic systems can result in the downdip translation of fold belts far from the basement topography over which they were created.

Introduction

As documented by the companion paper, Dooley et al. (2017), salt-flow patterns can be perturbed by base-salt relief. Examples of this type of topography include fault steps that localize deposition of thick salt or basement arches that produce complex salt isopachs. Subsalt topography can impart a degree of radial gliding during early stage salt tectonics, such as that in the Campos Basin (Cobbold and Szatzmari, 1991). Suprasalt deformation patterns can be influenced by a residual topography imparted by extensional faulting during rifting (e.g., Gaullier et al., 1993).

More recently, Pilcher et al. (2014) document radial gliding from a portion of the eastern Gulf of Mexico (Figure 1). In this region of the gulf, a series of basement arches and associated base-salt relief has had a strong influence on the early stage (Upper Jurassic to Early Cretaceous) rafting and associated deformation patterns (Figure 2). The Jurassic Louann Salt is continuous from the Apalachicola Embayment over the Florida Middle Ground Arch system and then into the main salt basin (Figure 3). In parts of this region, seismic data often paint a confusing pattern: Extensional structures dominate in the north–south dip direction as expected (Figures 3 and 4a); however, in strike sections (east–west lines), deep shortening structures involving the Upper Jurassic Norphlet and Smackover Formations are observed overlain and surrounded by extensional features (Figure 4b). The geometry and evolution of these rafts are very relevant to the petroleum system in the northeastern Gulf of Mexico because the eolian sandstones of the Norphlet Formation and the lime mudstones of the Smackover Formation are an important reservoir and source rock, respectively (Pilcher et al., 2014).

In this paper, we address three pertinent questions about these shortening structures: (1) How did they form, and why are they surrounded, overlain, and dissected by extensional structures? (2) Why are the shortening structures located so far updip from the typical compressional toe regime, in which shortening in gravity-driven systems is typically observed? (3) Why are the structures best seen in east–west-trending sections, thus oriented subparallel to the dominant salt-flow direction?

To address these questions, physical models are used to explore the role that base-salt relief plays in deformation patterns in strata overlying the salt layer in time and space. In our companion paper (Dooley et al., 2017), we explored the role of simple base-salt steps on the localization of extensional and contractional structures in strata overlying salt. When salt carrying a thin overburden passes over a high block, shortening structures form parallel to the boundaries of the block near its updip edge and adjacent to its downdip edge (Figures 5 and 6). In this paper, we expand on the work presented by Dooley et al. (2017) to include models with more complex salt isopachs that thin onto plunging basement highs, similar to the base-salt relief in the eastern Gulf of Mexico.

Methodology

As in our companion paper, we simulated rock salt using ductile silicone and simulated its siliciclastic overburden using brittle, dry, granular materials. The silicone is a near-Newtonian viscous polydimethylsiloxane, a long-chain polymer with a density of 950980  kgm3 and a dynamic shear viscosity of 2.5×104  Pas at a strain rate of 3×101  s1 (Weijermars, 1986; Weijermars et al., 1993). Prekinematic and synkinematic strata were composed of a mixture of silica sand (bulk density of 1700  kgm3; grain size of 300  μm; internal coefficient of friction, μ=0.550.65; see material properties studies in, e.g., McClay, 1990; Krantz, 1991; Schellart, 2000) and hollow ceramic microspheres to achieve a density equal to that of our model salt (bulk density of 600  kgm3, grain size of 90  μm, and typical μ=0.45; Rossi and Storti, 2003). This was done to avoid complexities introduced by the foundering of the brittle overburden.

The setup for the three models — models 10, 11, and 12 — presented in this study is illustrated in Figure 7a7c, respectively. These models differ from those of our companion paper (Dooley et al., 2017) by their more complex salt. Model 10 consisted of a simple plunging high block oriented 60° oblique to the dip direction. The salt thickness increased from 3 mm in the south to 20 mm in the north (Figure 7a). Model 11 consisted of two plunging arches oriented approximately 50° oblique to the dip direction (Figure 7b). Our model salt (silicone) thins from 12 mm thick off the arches to zero directly over the updip part of the arch to form a complex salt pinchout geometry. Model 12 consisted of a single plunging arch oriented 40° oblique to the dip direction (Figure 7c). In this case, the model salt thinned from a maximum of 15 mm to zero in a complex pinchout along the arch. In models 11 and 12, thick polymer/salt in an embayment was partly surrounded in the dip direction by thinner polymer/salt across the plunging arch system. In all models, the subsalt topography was built by sculpting wet sand. Once the topography was built, the salt analog (silicone) was emplaced and allowed to settle. A thin (5 mm thick) prekinematic layer with a unique color was placed on top of the salt analog, and the model was tilted to 3° to initiate deformation. As in part 1 of this paper, we chose to minimize the effects of gravity spreading and focus on gliding, mixing the silica sand and ceramic beads such that their density was equal to that of our model salt.

Computer-controlled digital cameras recorded the evolution of the obliquely lit upper surface of the models at set time intervals. A 3D digital image correlation (DIC) system, consisting of a pair of high-resolution charge-coupled devices and associated software, tracked the surface-strain history, subsidence, and uplift values, as well as displacement vectors for the prekinematic layer and for each subsequent synkinematic layer added to the model. For more details on DIC monitoring techniques, see Adam et al. (2005).

The base of the deformation rig was transparent to allow us to monitor deformation of the prekinematic layer even after burial by synkinematic strata in models 12 and 13. The prekinematic layer was viewed from below through the transparent silicone of the model salt layer. Models with synkinematic sedimentation were wetted with a gelatin solution to allow sectioning. Coregistered digital photographs of the closely spaced serial sections (3.5  mm apart) yielded a 3D voxel model of orthogonal cross sections and depth slices. Inlines (parallel to the regional dip direction) are sliced and photographed cross sections, whereas crosslines and depth slices are virtual sections constructed from the voxel model; as a result, the crossline and depth-slice images are not as high resolution as those derived directly from photographed inlines.

Effects of salt thickness — Flow across a plunging high block

Model 10 investigated the effects of a simple plunging ridge on salt flow (Figure 7a). Tilting the deformation rig to 3° initiated deformation. Figure 8 illustrates the early-stage topographic evolution of model 1. After 3.5 h, a block-parallel structural high formed above the updip end of the ridge. A structural low formed just downdip of the edge of the ridge (Figure 8a). The topographic high formed because of compression and thickening as more salt was fed onto the high block than could be accommodated — a result of inhibited flow across the subsalt high block, similar to that seen in Figure 5. The low was the downdip portion of an extensional monocline similar to that seen in Figure 6. Eventually, this early high became thick enough to partly overcome the effects of basal drag and collapsed under extension as salt-flow velocity accelerated (Figure 8b). The topographic hinge continued to develop just downdip of the subsalt high block (Figure 8b). With continued deformation, extension dominated throughout the zone updip of the high block (Figures 8c and 9a). Extensional graben that passed through the downdip compressional hinge were inverted to form a fold belt that was initially subparallel to the plunging high (Figures 8c and 9a).

After 71 h, major extension was seen throughout most of the model, with significant separation of raft blocks (Figure 9b). Raft blocks also recorded significant clockwise rotation, as do the folds that originally formed in the compressional hinge. The earliest formed folds recorded clockwise rotations of up to 20° (Figure 9b). Streamlines from an earlier stage of the model illustrate a component of northward flow on the updip side of the plunging high and southward flow across the high block (Figure 9c). The flow is greatly perturbed above areas of thinner salt. The associated velocity gradient (faster above thick salt), recorded in the DIC data, drove the rotations of the fold belts and the raft blocks as these structures were translated downdip (Figure 9d). Note that the fold belts, heavily dissected by extension, were translated far downdip from where they formed, blurring the spatial link between their present location and their cause of formation (Figure 9b).

Complex salt isopachs — Flow across basement arches

Model 10 illustrates that subsalt topography can have a profound influence on salt flow and the structures formed in the suprasalt overburden. It also shows that variations in salt thickness can drive significant rotations within the overburdens because of velocity gradients. Models 11 and 12 expand on the findings of model 10 with setups that contain elements of base-salt relief, similar to those present in the eastern Gulf of Mexico, which are likely to have significantly impacted early stage salt flow (Figure 7b and 7c).

Figure 10a shows an overhead view of model 11 39 h into the experiment. The white model surface is the first synkinematic layer deposited above the prekinematic overburden. Deformation is dominated by extension, with associated reactive diapirs in the embayment, adjacent to the salt pinchout and downdip of the basement arches. However, minor shortening structures are seen in which the prekinematic layer pokes through the synkinematic layer in the form of anticlines, along the arch and at the downdip edges of the arches. Shortening strains from just before the addition of this first synkinematic layer are illustrated in Figure 11a. Shortening is concentrated against the complex updip pinchout that flanks the embayment, along the arch, and near the toe of the arch (Figure 11a). The minor folds seen in the earlier stage of the model were significantly amplified and rotated counterclockwise in the north and clockwise in the south. Shortening strains are recorded along the plunging arches and out into thicker salt as these structures were translated and rotated (Figure 11b). Views of the underside of the model illustrate the folds forming at the toe of the plunging arches and their gradual rotation as they are translated downdip (Figure 12). A total of 56° counterclockwise rotation was recorded for the northern folds (Figure 12c).

DIC data from model 11 (Figure 13) reveal similar but more complex patterns of topography, flow direction, and velocity gradients than those seen in model 10. Tracking northward and southward flow reveals that convergent flow dominates updip of the arches, thickening salt in the embayment, whereas divergent flow dominates downdip of the arches, resulting in rotational strains (Figure 13b). Figure 13c illustrates that dip-parallel displacements were at their maximum in the center of the model, where there was a narrow gap in the arch system and where the salt was thickened by the convergent flow shown in Figure 13b. The shear couples associated with this velocity gradient drove significant rotation of the fold belts (Figures 1012).

Model 12 tested whether shortening structures would form in the suprasalt section moving over a single plunging arch (Figure 7c). An overhead view and DIC map indicating shortening strains is shown in Figure 14. As shown in model 11, a proximal fold belt formed adjacent to the complex salt pinchout, and a zone of arch-parallel folds formed above the plunging arch before being translated further downdip (Figure 14a and 14b). An underside view of model 12 reveals a series of fold belts downdip of the nose of the subsalt arch (Figure 14c).

Complex salt isopachs — Cross-section description

Dip sections through model 11 reveal a deformation style dominated by extension (Figure 15). However, shortening structures are seen in various locations. A section that cuts through the updip breakaway and lateral salt pinchout reveals extension dominating updip and downdip of this pinchout, whereas the crest of the arch and pinchout reveals significant shortening structures (Figure 15b). Moving further south in the model, the structures appear to be predominantly extensional (Figure 15d; similar to the style seen in Figure 3), but detailed views reveal oblique sections through the translated fold belts downdip of the arch, as well as a squeezed diapir and partially inverted graben above the arch system (Figure 15f and 15g). This diapir originally formed in the extensional zone updip of the arch system, but it is not clear whether it was shortened because it climbed up on the arch or because it approached the downdip side of the arch. However, a partial section through an updip part of the southern arch reveals a shortened diapir (Figure 15h). In this case, shortening was clearly related to basal drag or buttressing by the arch (Figure 15h). In the center of the model, major raft development occurred in this region of continuous thick salt through the gap between the subsalt arches (Figure 15e). Closely spaced faults characterize deformation above the pinchout ramp where the salt thins, forming a series of prerafts until thicker salt is reached where major rafting occurred (Figure 15e).

Figure 16a illustrates stacked virtual depth slabs through the reconstructed 3D volume of model 11. In the shallower depth slab, structures appear to be entirely extensional; however, dip lines reveal squeezed diapirs in the proximal domain and low-amplitude folds further downslope. The lower slab illustrates the final orientation of the deep, translated, and rotated fold belts (Figure 16a), which are flanked by major reactive diapirs in the central part of the model. A detailed view of a dip section illustrates that late-stage shortening above the oblique arch was accommodated by squeezing of reactive diapirs, resulting in partial inversion of an extensional graben (Figure 16b). Because of the significant rotations of the early-formed fold belts, shortening structures are best seen in virtual strike lines from the model 3D volume (Figure 16c). In this example, deep thrusting of a fold places our prekinematic strata (Norphlet equivalent) above the first synkinematic layer (Figure 16c), similar to structures seen in the east–west seismic data from the eastern Gulf of Mexico (Figure 4b).

Conclusion

Part 1 of this paper demonstrates that extensional diapirs and compressional fold belts can be initiated anywhere on a slope as salt accelerates and decelerates when flowing across base-salt relief; thus, structural evolution is likely to be more complex than a simple extension-translation-shortening model commonly invoked for gravity-driven deformation above mobile substrates. The three physical models presented in this paper possessed more complex, plunging, base-salt relief and complex salt isopachs, resulting in far-more-variable salt flow, similar to what we suspect occurred during early stage rafting of the Norphlet and Smackover Formations in the northeastern Gulf of Mexico.

Despite the additional complexities, the basic principles outlined in the simple models of our companion study (Figures 5 and 6) also remain valid in these more complicated geologic scenarios. Fold belts formed as the salt and its thin overburden flowed across the plunging base-salt arches. Early-formed fold belts were enhanced, and later-formed extensional grabens were inverted because they flowed off the highs through contractional hinges into regions of thicker salt downdip. The models may explain how and why similar structures seen in 3D seismic data from the northeastern Gulf of Mexico formed above autochthonous salt so far from the toe-of-salt zone typically associated with shortening in gravity-driven systems. Additional zones of shortening in our models formed in and around complex updip salt pinchouts associated with base-salt relief, generating unexpected updip-pinchout-proximal fold and thrust belts.

The fold belts are surrounded, overlain, and dissected by extensional structures because their formation is spatially limited to the base-salt relief that produces shortening strains; once transported away from this localized shortening zone, the overburden is free to extend as the salt flows downslope at variable rates. In addition, fold-thrust structures only form when the overburden is thin enough to fail under the typically low shortening strains produced by base-salt relief (Figures 10 and 12). As the system evolves and the overburden thickens and strengthens, local shortening is cryptic, typically accommodated by layer-parallel shortening or by squeezing of preexisting diapirs, as observed in our model 11 (Figures 15 and 16).

The more-complex salt isopachs in the physical models presented in this study have a fundamental impact on salt flow, producing flow directions that deviate from dip-parallel and velocity gradients across the model. These velocity gradients are the driving force behind the extreme rotations of early-formed shortening structures so that their trend is almost dip parallel (Figure 16), similar to the situation seen in seismic data from the northeastern Gulf of Mexico (Figure 4b). Continued downdip translation obscures the relationship between such structures and the base-salt relief that caused their formation. In addition, weak zones such as diapirs are likely to be rejuvenated under extension and contraction if they encounter additional base-salt relief downslope.

Acknowledgments

T. P. Dooley thanks J. Donnelly, N. Ivicic, J. Lambert, and B. Williamson for logistical support in the modeling laboratories. We are extremely grateful to V. Mount, C. Schneider, K. McClay, T. Hearon, and O. Ferrer for their thorough and constructive reviews of an earlier version of this manuscript. S. Jones is thanked for editing the manuscript. A special thank you goes to L. Moscardelli for reviewing the initial submission. The project was funded by the Applied Geodynamics Laboratory Industrial Associates program, comprising the following companies: Anadarko, Apache, Aramco Services, BHP Billiton, BP, CGG, Chevron, Cobalt, Condor, ConocoPhillips, EcoPetrol, ENI, ExxonMobil, Freeport-McMoRan, Fugro, Hess, Ion-GXT, LUKOIL Overseas Services, Maersk, Marathon, Murphy, Nexen USA, Noble, Pemex, Petrobras, PGS, Repsol, Rockfield, Samson, Shell, Spectrum, Statoil, Stone Energy, TGS, Total, Venari Resources, and Woodside. The authors received additional support from the Jackson School of Geosciences, the University of Texas at Austin. Publication authorized by the irector, Bureau of Economic Geology, the University of Texas at Austin.

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Tim P. Dooley received a B.Sc. (1988) from Trinity College Dublin and a Ph.D. (1994) from the University of London. He spent the next nine years with the Fault Dynamics Research Group at Royal Holloway University of London. He has conducted experiments studying structural processes since 1988. He joined the Applied Geodynamics Laboratory (AGL), a research group focused on salt tectonics, at the University of Texas at Austin in 2003, where he managed the physical modeling laboratories. His current research interests include the growth, advance, and coalescence of salt sheets; salt-stock canopy systems; strike-slip deformation above salt; the effects of shortening on salt diapirs and minibasins; and the effects of base-salt relief on salt flow and suprasalt deformation patterns. He is a corecipient of AAPG’s Braunstein award.

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Michael R. Hudec a Ph.D. (1990) from the University of Wyoming. He joined the Bureau of Economic Geology in 2000, where he directed the Applied Geodynamics Laboratory consortium. His current research interests include the evolution of salt basins and seismic interpretation of salt structures. He is a recipient or corecipient of AAPG’s  Matson, Braunstein, and Levorsen awards.

Freely available online through the SEG open-access option.