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Different scales of salt–sediment interaction during passive diapirism
Interpreting the nature of the Aulet and Adons diapirs from sedimentologic and stratigraphic analysis of flanking minibasin strata, Spanish Pyrenees, Catalunya, Spain
Passive versus active salt diapirism
Sedimentologic, stratigraphic, and structural evolution of minibasins and a megaflap formed during passive salt diapirism: The Neoproterozoic Witchelina diapir, Willouran Ranges, South Australia
Controls on the structural and stratigraphic evolution of the megaflap-bearing Sinbad Valley salt wall, NE Paradox Basin, SW Colorado
Halokinetic sequences and diapiric structural kinematics in the field: Two-day excursion to La Popa Basin, northeastern Mexico
Megaflaps adjacent to salt diapirs
Allochthonous salt initiation and advance in the northern Flinders and eastern Willouran ranges, South Australia: Using outcrops to test subsurface-based models from the northern Gulf of Mexico
Halokinetic deformation adjacent to the deepwater Auger diapir, Garden Banks 470, northern Gulf of Mexico: Testing the applicability of an outcrop-based model using subsurface data
Abstract Halokinetic sequences are unconformity-bound packages of thinned and folded strata adjacent to passive diapirs. Hook halokinetic sequences have narrow zones of deformation (50–200 m), >70° angular discordance, common mass-wasting deposits and abrupt facies changes. Wedge halokinetic sequences have broad zones of folding (300–1000 m), low-angle truncation and gradual facies changes. Halokinetic sequences have thicknesses and timescales equivalent to parasequence sets and stack into composite halokinetic sequences (CHS) scale-equivalent to third-order depositional cycles. Hook sequences stack into tabular CHS with sub-parallel boundaries, thin roofs and local deformation. Wedge sequences stack into tapered CHS with folded, convergent boundaries, thicker roofs and broad zones of deformation. The style is determined by the ratio of sediment-accumulation rate to diapir-rise rate: low ratios lead to tabular CHS and high ratios result in tapered CHS. Diapir-rise rate is controlled by the net differential load on deep salt and by shortening or extension. Similar styles of CHS are found in different depositional environments but the depositional response varies. CHS boundaries (unconformities) develop after prolonged periods of slow sediment accumulation and so typically fall within transgressive systems tracts in shelf settings and within highstand systems tracts in deepwater settings. Sub-aerial settings may lead to erosional unroofing of diapirs and consequent upward narrowing of halokinetic deformation zones.
Abstract La Popa Weld in La Popa Basin, Mexico, is a 24 km long near-vertical structure with a prominent bend approximately halfway along its length. Halokinetic folding, local unconformities and diapir-derived detritus in flanking strata document a precursor salt wall. Shortening during the latest Cretaceous to Eocene Hidalgoan Orogeny squeezed the salt wall to form the weld. Deformation varies significantly along the weld. The northwestern third has remnant gypsum (including a diapir at the northwestern end), little large-scale folding of flanking strata and only background fracture intensity. Directly NW of the bend are pods of gypsum linked by complete welds, a large-scale cuspate anticlinal geometry and significant fracturing within 5–10 m of the weld. The southeastern half is completely welded with no remnant gypsum, a prominent cuspate anticlinal geometry and a 50 m wide damage zone. The variable deformation was controlled by the original width of the salt wall and the amount and direction of shortening. Where orthogonal to the wall, shortening locally closed the diapir but little further deformation took place. Where oblique, shortening caused post-weld dextral strike-slip movement and significant fracturing and shearing of the wall rock. The resulting deformation variability likely impacted the sealing capability of the weld.
Abstract The Eocene Carroza Formation in La Popa Basin, Mexico, represents fluvial sedimentation in a shortening-influenced salt-withdrawal minibasin, termed the Carroza Syncline. The Carroza Syncline lies adjacent to the La Popa salt weld, which was formerly a passively-rising salt wall that was shortened during the Hidalgoan Orogeny in Late Cretaceous and Palaeogene time. The Carroza Formation displays distinct upsection changes in fluvial facies distribution and geometry of halokinetic drape folding. Fluvial channel distribution changes upwards from widespread thin, broad channels with variable palaeocurrents in the lower part of the formation to thick, stacked channels concentrated in the hinge of the Carroza Syncline with weld-parallel palaeocurrent directions in the upper part. The upper and middle members of the Carroza contain debris-flow facies derived from diapir roof strata and the diapir itself. The style of halokinetic drape fold upturn and thinning towards the weld changes upsection from a broad (800–1500 m) to a narrow (50–200 m) zone, where upper Carroza strata are overturned and in direct contact with remnant gypsum along the weld. The upsection changes in fluvial facies distribution and geometry reflect an overall decrease in local sediment-accumulation rates relative to salt-rise rates controlled by both Hidalgoan shortening and passive diapirism.
Abstract Parts of two third-order Neoproterozoic (Marinoan) depositional sequences are documented in the Wilpena Group (Wonoka Formation and Bonney Sandstone) at Patawarta diapir, located in the central Flinders Ranges, South Australia. These sequences represent an overall regressive succession transitioning upwards from outer to middle wave-dominated shelf deposits to a tidally dominated barrier bar to coastal plain. The lower, middle, upper limestone and green mudstone informal members of the Wonoka Formation comprise the Highstand Systems Tract of the lower sequence. The Sequence Boundary is at the top of the Wonoka green mudstone member and is overlain by the Lowstand Systems Tract of the upper sequence, which includes the lower dolomite, sandstone and upper dolomite beds of the Patsy Hill Member of the Bonney Sandstone. The upper sequence Transgressive Systems Tract comprises the Bonney Sandstone. These units comprise one complete tapered composite halokinetic sequence (CHS). The lower halokinetic-sequence boundary is associated with the Maximum Flooding Surface of the lower depositional sequence and the upper halokinetic-sequence boundary is interpreted as the Transgressive Surface of the overlying depositional sequence where an angular truncation of up to 90° is documented.
Abstract In the distal part of the Late Cretaceous Hidalgoan foreland basin in NE Mexico three isolated carbonate platforms nucleated on seafloor topography created by rising passive diapirs. Carbonate facies type and architecture of each platform was distinctly influenced by a combination of both short-term local conditions surrounding individual diapirs and by long-term regional conditions that affected the entire shelf. Local conditions included windward-leeward platform paleogeography, possible elevated nutrient levels at the salt- sediment interface, and halokinesis. Regional conditions included eustatic sea-level changes, foreland-basin tectonism, and siliciclastic sediment supply to the shelf. Maastrichtian carbonate-platform facies are distributed asymmetrically across individual diapirs, reflecting windward-margin versus leeward-margin paleogeographic setting and differential minibasin subsidence related to salt withdrawal. Southern (windward) margins are dominated by steep-sided sponge, coral, and red algal reefs displaying minor fore-reef progradation (< 1.5 km) into the adjacent minibasin, thick carbonate debris-flow beds containing diapir-derived detritus, and pervasive near-diapir halokinetic fracturing. In contrast, northern (leeward) margins are dominated by foraminifera, red algal grainstone banks displaying major progradation (3-4 km) into the adjacent minibasin and lack debris-flow beds or halokinetic fracturing. Carbonate facies at all the diapirs are primarily sand-prone, heterozoan faunal assemblages that are unusual for this period of time and paleogeographic location. The presence of heterozoan faunal assemblages may be in response to high nutrient levels from local methane seeps forming at the salt- sediment interface. Carbonate facies form the bases of angular-unconformity-bounded carbonate-siliciclastic cycles called halokinetic sequences. The cycles reflect local variations in net diapiric-rise rates versus local sediment accumulation rates. Halokinetic sequences vary in number and character between the different diapirs and between the windward and leeward margins of each diapir. On leeward margins, halokinetic sequences are more numerous and carbonate facies are dominated by grainstone banks, whereas on windward margins halokinetic sequences are amalgamated and carbonate facies are dominated by fore-reef debris and debris-flow facies. The isolated carbonate platforms are best developed within the transgressive systems tracts (TST) of third-order deltaic siliciclastic depositional sequences within the regionally marine foreland-basin depositional system. Late Cretaceous to Paleogene Hidalgoan shortening of La Popa foreland basin formed large-wavelength (> 10 km) NW-SE trending salt-cored detachment folds. Diapirs that lie in the hinges of folds were shortened or “squeezed” significantly more than diapirs that lie on the limbs of folds. Squeezed diapirs generated much higher and broader topographic relief in response to higher diapiric rise rates and are correspondingly dominated by extensive, thick, shallow-water (< 15 m deep) sponge, red algal reef and grainstone-bank facies with carbonate strata extending more than 4 km away from the diapir. Age-equivalent carbonate strata on limb diapirs contain thin, deeper-water (> 30 m deep) silty, red algal packstone facies that extend < 2 km from the diapir, reflecting lower carbonate production rates in a deeper-water setting.
NEW PALEOCENE RHYNCHONELLIDE BRACHIOPODS FROM THE POTRERILLOS FORMATION, NORTHEAST MEXICO
Salt diapir-influenced, shallow-marine sediment dispersal patterns: Insights from outcrop analogs
Basinward transport of Chicxulub ejecta by tsunami-induced backflow, La Popa basin, northeastern Mexico, and its implications for distribution of impact-related deposits flanking the Gulf of Mexico
Basinward transport of Chicxulub ejecta by tsunami-induced backflow, La Popa basin, NE Mexico: Comment and Reply: REPLY
Basinward transport of Chicxulub ejecta by tsunami-induced backflow, La Popa basin, NE Mexico: Comment and Reply: REPLY
Summary of Halokinetic Sequence Characteristics from Outcrop Studies of La Popa Salt Basin, Northeastern Mexico
Abstract La Popa salt basin of northeastern Mexico contains exceptional exposures of salt stocks, salt withdrawal basins, and secondary salt welds, so that the scale and geometry of structural and stratigraphic features created by salt movement can be examined in both plan view and cross section. Cretaceous through Paleogene strata exposed adjacent to diapiric structures in La Popa Basin are arranged into halokinetic sequences, which display onlap and thinning toward the diapirs and stratal geometries indicative of syn-depositional diapiric growth. Within the shelf depositional environment in La Popa basin, halokinetic sequences can be split into two end-member types (Type A and Type B ) that differ in depositional facies, maximum degree of internal folding, amount of fault reactivation on unconformities, overall sedimentation rate, and distance of halokinetic sequence termination from the salt/sediment interface. The differences in attributes of these two end-member types of halokinetic sequences have important implications for reservoir quality, geometry, and continuity.