Physical modelling of overburden deformation around salt diapirs

Davison, Ian; Insley, Martin; Harper, Max; Weston, Peter; Blundell, D. J.; McClay, Ken; Quallington, Andrew

doi:10.1016/0040-1951(93)90344-j

Cited by 50 publications

(23 citation statements)

References 9 publications

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“…Though the pressure source is not located at the surface, this undeformed wedge shares strong similarities with the well‐known Prandtl's wedge for shallow strip footings in geomechanics (see, e.g., Davis & Selvadurai, ). These results show that the final damage spatial distribution reproduces quite accurately the results of published geological field observations (see, e.g., Merle et al, ) and analog modeling (Acocella et al, ; Brothelande & Merle, ; Davison et al, ; Marti et al, ; Merle et al, ; Merle & Vendeville, ; Sanford, ): Resurgent domes are structures with reverse faulting on their external boundaries and internal normal faulting (see, e.g., Acocella et al, ; and, for a typical example, the Yenkahe complex; Brothelande, Peltier, et al, ; Merle et al, ). Field geological observations show that magmatic intrusions associated with resurgence are bordered by reverse faults (Fridrich et al, ), which can explain the abrupt transition between the flat caldera moat and the dipping layers of the dome flanks.…”

Section: Resultssupporting

confidence: 82%

Damage and Strain Localization Around a Pressurized Shallow‐Level Magma Reservoir

et al. 2019

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Structures developing above long‐term growing shallow‐level magma reservoirs, such as resurgent domes, may contain information on the reservoir itself. To understand the formation of such tectonic features, we have investigated the deformation process around a shallow pressurized magma reservoir embedded in a damaging elastic volcanic edifice. Our model allows evidencing the effect of the progressive damage in producing the fault pattern associated to tectonic surface deformation. Damage is first isotropic around the cavity and constitutes a damaged zone. Then the free‐surface effect appears, and an anisotropic shear strain develops from the boundary of the damaged zone; it localizes on reverse faults that propagate upward to the surface. When the surface deformation is sufficient, normal faulting appears. Finally, the complete structure shows an undeformed wedge above the damaged zone. This structure is similar to those found by analog modeling and from field geologic observations. From this model, we found a relation to estimate the reservoir radius and depth from the graben and dome widths. From limit analysis, we deduced an analytical expression of the magma reservoir pressure which provides a better understanding of the magma pressure buildup during doming. The dip of reverse faults limiting the dome can be inferred from the minimal pressure required to rupture the crust around the reservoir. Finally, the magma reservoir overpressure, the dip of the faults, the reservoir depth, and the damaged zone radius are inferred from three parameters: the ratio ρR computed from the dome and graben widths, the cohesion, and the friction angle.

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Section: Resultssupporting

confidence: 82%

Damage and Strain Localization Around a Pressurized Shallow‐Level Magma Reservoir

et al. 2019

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“…4C, 5C & E), suggesting that the mounds were emplaced on the seabed (Riis et al, 2005). Had these mounds been emplaced in the subsurface, substantial deformation of stratigraphy above the mounds would be expected similar to that predicted around diapirs (Davison et al, 1993). This is not observed.…”

Section: Moundmentioning

confidence: 73%

The stratigraphic and geographic distribution of giant craters and remobilised sediment mounds on the mid Norway margin, and their relation to long term fluid flow

Lawrence

Cartwright

2010

Marine and Petroleum Geology

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“…and abundance of the ductile material, on the physical‐geological characteristics of the overburden (e.g., density, strength, thickness, etc. ), on the timing relationships between diapirism and tectonics, and on the effect of deformation on both the overburden and the underlying source horizon [e.g., Koyi , 1988; Schultz‐Ela et al , 1993; Davison et al , 1993; Daudré and Cloething , 1994; Letouzey et al , 1995; Waltham , 1997; Cotton and Koyi , 2000; Sans , 2003].…”

Section: Mechanism Of Emplacement: Discussionmentioning

confidence: 99%

“…Because salt intrudes along a fracture, the lower levels of the diapiric structure are likely to be elliptical rather than circular in plan. Along with flexuring and compaction of the cover rocks, the creation of space will also be accomplished by the displacement of the roof of the diapir upward either by faulting, folding, or by the conjunction of both mechanisms [e.g., Schultz‐Ela et al , 1993; Davison et al , 1993; Tikoff et al , 1999].…”

Section: Mechanism Of Emplacement: Discussionmentioning

confidence: 99%

Geometry and kinematics of compressional growth structures and diapirs in the La Popa basin of northeast Mexico: Insights from sequential restoration of a regional cross section and three‐dimensional analysis

Millán-Garrido

2004

Tectonics

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[1] Diapirism in the La Popa basin NE Mexico was triggered and sustained by compressional décollement tectonics. Coeval development of contractional structures and diapirs was recorded by growth strata of Late Cretaceous-Tertiary age. A palinspastic reconstruction of a regional cross section, based on the restoration of growth strata related to both diapirs and detachment folds, was carried out. On the basis of this reconstruction and field data, a three-dimensional geometrical study was done to quantify the movement of evaporites within the detachment horizon and two diapirs. The latter allowed determining the tectonodiapiric potential of a structure or set of structures (i.e., the amount of ductile rocks forced to flow in association with the growth of a tectonic structure, which is not accommodated by thickening of the ductile horizon nor by the tectonic structure itself, and is capable of producing diapiric phenomena). This study demonstrates that there is a direct coupling between tectonodiapiric potential and diapiric activity. Geometrical results show that the main factors that controlled the amount of ductile material moved as a consequence of compressional tectonics were shortening, the depth to detachment, the folding style, and the style of deformation process (i.e., pure shear/simple shear). In response to folding, the overburden experienced a downward movement that was the major cause of diapiric phenomena. In addition to field and geometrical data, mechanical data indicate that forceful intrusion was the prevailing emplacement mechanism. Temperatures (>150°-197°C) and strain rates (in the order of 10 À16 -10 À17 s À1 ) calculated for top of the evaporite layer were adequate for the flow of these rocks from the initiation of compression onward. However, an inferred overpressure in the ductile layer should be considered the key factor for the emplacement mechanism.

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Physical modelling of overburden deformation around salt diapirs

Cited by 50 publications

References 9 publications

Damage and Strain Localization Around a Pressurized Shallow‐Level Magma Reservoir

Damage and Strain Localization Around a Pressurized Shallow‐Level Magma Reservoir

The stratigraphic and geographic distribution of giant craters and remobilised sediment mounds on the mid Norway margin, and their relation to long term fluid flow

Geometry and kinematics of compressional growth structures and diapirs in the La Popa basin of northeast Mexico: Insights from sequential restoration of a regional cross section and three‐dimensional analysis

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