Structural evolution of extensional basin margins

Gibbs, A. D.

doi:10.1144/gsjgs.141.4.0609

Cited by 881 publications

(386 citation statements)

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“…5), so they must be listric, becoming horizontal in depth. As Gibbs (1984) has demonstrated, listric faulting cre ates highly asymmetric half-grabens because folding (roll-over) on the hanging wall is a consequence of this type of fa ults. The need to thin the roll-over leads to the fonnation of antithetic or counter faults in a fan migrating towards the hanging wall and, with further extension, to a crustal collapse le ading to the fonnation of secondary grabens and central highs bounded by antithetic and synthetic faults.…”

Section: The Geometry Of the Iberian Basin Boundary Faultsmentioning

confidence: 99%

Origin of the Permian-Triassic Iberian Basin, central-eastern Spain

Arché¹,

López-Gómez²

1996

Tectonophysics

131

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The Iberian Basin was an intracratonic rift basin in central-eastern Spain developed since Early Permian times. The basin boundary faults were normal, listric faults controlling an asymmetric extension propagating northeast with time.Hercynian or older lineaments controlled the orientation of the Iberian Basin and extension was accommodated basically in the hanging wall block by the formation of secondary grabens and a central high. The basin was related with the coeval Ebro, Catalan and Cuenca-Mancha Basins and their connections are discussed.Subsidence curves show that the Early Permian-Early Jurassic period of extension can be subdivided into three rifting episodes and a flexural one. Extension factor increases from 1.17 in the northwest to 1.29 near the Mediterranean coast.The increasing extension rate was accommodated by transfer faults trending NNE-SSW, more important in the Levante area. The rift evolution is intermittent and seems to reflect distinct stress fields.The collapse of the late Hercynian orogen and related increased heat flux, extension and rifting is the most probable origin of the Iberian Basin and related basins. The origin of the Catalan and the Valencia-Prebetic Basins is related to the southwards migration of the Hesse-Burgundy Rift along the eastern margin of the Iberian Microplate.

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Section: The Geometry Of the Iberian Basin Boundary Faultsmentioning

confidence: 99%

Origin of the Permian-Triassic Iberian Basin, central-eastern Spain

Arché¹,

López-Gómez²

1996

Tectonophysics

131

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“…For internal consistency of the extensional models the structural style and geometric evolution of extensional faults must follow a kinematically feasible scheme [Proffett, 1977;Gibbs, 1984 The south-southeast directed low-angle extension is roughly orthogonal to the axis of greatest regional shortening.…”

Section: Timingmentioning

confidence: 99%

“…Minor reverse faulting is created locally and is needed to accommodate relative block displacement (section CC', blocks 3-4 and 14-15) in a way similar to that described by Brumbaugh [1984]. Toward the border of the extended domain, hanging wall rollover [Gibbs, 1984] and BB', down-to-the-Tyrrhenian high-angle normal faults are associated with rifting and may have given rise to regional uplift of the coastal region similar to that observed in the Quaternary [Westaway, 1993]. Convergence between the thrust belt and foreland still attached to the subducting slab results in frontal accretion similar to that proposed by Royden et al [1987].…”

Section: Timingmentioning

confidence: 99%

History and tectonic implications of low‐angle detachment faults and orogen parallel extension, Picentini Mountains, Southern Apennines fold and thrust belt, Italy

Ferranti¹,

Oldow

1999

Tectonics

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Abstract. Late Miocene to Pliocene movement on low-angle extensional faults within the internal Southern Apennines orogenic belt was superposed on an earlier, Miocene imbricate thrust stack. The low-angle faults formed within the interior of the belt during orogen parallel extension as thrust imbrication continued in the foreland. Extreme tectonic thinning defines discrete structural domains of hyperextension which are linked by a complex system of extensional and transcurrent faults. Some of the best examples of hyperextension structures in the Southern Apennines are exposed in the Picentini Mountains. In this area, detailed mapping, fault-kinematic analysis, and excellent stratigraphic control contributed to the construction of restorable cross sections and forward models of deformation.With these constraints, it is possible to document extensional displacement on shallowly dipping supercrustal faults whose orientation is a primary feature and is not due to later tilting. During movement, upper plate rocks were disarticulated by listric and planar normal faults that soled into a ramp-flat detachment system. The depth of the basal detachment increased in the direction of upper-plate motion and ranged from 5 to 10 km. Displacement on the low-angle detachment was accompanied by block tilting in the upper plate assemblage, incisement and excisement of the upper and lower plate rocks as fault trajectories changed through time, and the progressive cataclasis of hanging wall and footwall assemblages. Preexisting thrusts were only locally reactivated during extension, and faults emanating from the underlying decollement systems cross the imbricated thrust sheets at moderate to high angles. Longitudinal extension resulted in thinning of the thrust stack to less than half the original thickness and had a cumulative magnitude of between 200 and 250 % (beta > 2).

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“…Transfer faults usually transfer displacement between two normal fault systems, having a significant strike-slip component in the map view (Peacock et al, 2000). They trend at a high angle to the major extensional faults (Gibbs, 1984;Peacock et al, 2000), approximately synonymous with cross-strike fault features (Morley, 1995). It is worth noting that transfer faults are part of accommodation zones, simply linking normal faults rather than fault systems (Gibbs, 1984;Bosworth, 1985).…”

mentioning

confidence: 99%

“…They trend at a high angle to the major extensional faults (Gibbs, 1984;Peacock et al, 2000), approximately synonymous with cross-strike fault features (Morley, 1995). It is worth noting that transfer faults are part of accommodation zones, simply linking normal faults rather than fault systems (Gibbs, 1984;Bosworth, 1985). Thus, such faults are not confused with accommodation zones because they have smaller scale.…”

mentioning

confidence: 99%