Strike‐slip basins, Part 2

Nilsen, Tor H.; Sylvester, Arthur G.

doi:10.1190/1.1438194

Cited by 34 publications

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“…If large-scale lateral extrusion of the Alxa Block had occurred, then there should be coeval deformation and sediments distributed in the Alxa Block and regions to the east; however there have been no reports yet of such deformation and Oligocene-Miocene depressions in the Alxa Block. Generally, basins develop along large strike-slip faults in relation to their mode of displacement (Nilsen and Sylvester 1995). Therefore, if 185-250 km (Darby et al 2005;Webb and Johnson 2006;Lamb et al 1999) or 400 km (Yue and Liou 1999) left-lateral strike-slip displacement had occurred in the Alxa Block before the Miocene, it would be hard to imagine that no related deformation and basins had developed.…”

Section: Discussionmentioning

confidence: 99%

How did the Alxa Block respond to the Indo-Eurasian collision?

Zhang

et al. 2009

Int J Earth Sci (Geol Rundsch)

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Section: Discussionmentioning

confidence: 99%

How did the Alxa Block respond to the Indo-Eurasian collision?

Zhang

et al. 2009

Int J Earth Sci (Geol Rundsch)

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“…7d, 8 and 9a). These faults show reverse and normal components of slip that develop simultaneously with grabens and arches, in positions that vary rapidly through time (Crowell 1982;Christie-Blick and Biddle 1985;Wood et al 1994;Nilsen and Sylvester 1995;Barnes and Audru 1999;Barnes et al 2001). The dip on the master strike-slip fault controls the width of the releasing-bend basin.…”

Section: Volcanic Facies Model For the Santa Rita Glance Intraarc Strmentioning

confidence: 97%

“…These are interpreted as phreatoplinian ash fall deposits, which record explosive eruptions through water Fig. 7 Three major types of strike-slip basins (after Nilsen and Sylvester 1995), including a pull-apart basin, b releasing bend basin, and c transrotational basins. Also shown is d releasing-and restraining-bend couplet along an overall trantensional strike-slip fault, where the restraining bend is smaller than the releasing bend (after Cowan et al 1989;Cowan and Pettinga 1992); bends are exaggerated to display geometries clearly, whereas in nature, very subtle bends produce similar structures The basin also contains numerous intrabasinal syndepositional high-angle faults (Figs.…”

Section: Syndepositional Faultsmentioning

confidence: 99%

“…Strike-slip basins largely occur as three major types (Nilsen and Sylvester 1995): (1) classical pull-apart basins, which form at a releasing stepover between en echelon segments of a strike-slip fault (Fig. 7a), (2) releasing bend basins, which form along a gently curved strike-slip fault (Fig.…”

Section: Volcanic Facies Model For the Santa Rita Glance Intraarc Strmentioning

confidence: 99%

“…Strike-slip faults, transtensional faults, and block rotations play an important role in modern volcanic arcs; examples include the Central American arc (Burkhart and Self 1985;Jarrard 1986b;Weinberg 1992); the Trans-Mexican Volcanic belt (IsradeAlcantara and Garduno-Monroy 1999); the Andean arc of southern Chile and Patagonia (Cembrano et al 1996;Thomson 2002); the Sumatra arc (Bellier and Sebrier 1994); the Aeolian arc (Gioncada et al 2003); the Calabrian arc (Van Dijk 1994); the Aleutian arc (Geist et al 1988); the Taupo Volcanic Zone (Cole and Lewis 1981); the central Philippine arc (Sarewitz and Lewis 1991); and others. Strike-slip basins are the most tectonically active type of basin (Nilsen and Sylvester 1995), so the effects of strike-slip faulting on the development of volcanic successions within arcs must be profound.…”

Section: Introductionmentioning

confidence: 99%

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Volcanic facies architecture of an intra-arc strike-slip basin, Santa Rita Mountains, Southern Arizona

Busby

Bassett

2007

Bull Volcanol

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The three-dimensional arrangement of volcanic deposits in strike-slip basins is not only the product of volcanic processes, but also of tectonic processes. We use a strike-slip basin within the Jurassic arc of southern Arizona (Santa Rita Glance Conglomerate) to construct a facies model for a strike-slip basin dominated by volcanism. This model is applicable to releasing-bend strike-slip basins, bounded on one side by a curved and dipping strike-slip fault, and on the other by curved normal faults. Numerous, very deep unconformities are formed during localized uplift in the basin as it passes through smaller restraining bends along the strike-slip fault. In our facies model, the basin fill thins and volcanism decreases markedly away from the master strike-slip fault ("deep" end), where subsidence is greatest, toward the basin-bounding normal faults ("shallow" end). Talus cone-alluvial fan deposits are largely restricted to the master fault-proximal (deep) end of the basin. Volcanic centers are sited along the master fault and along splays of it within the master fault-proximal (deep) end of the basin. To a lesser degree, volcanic centers also form along the curved faults that form structural highs between sub-basins and those that bound the distal ends of the basin. Abundant volcanism along the master fault and its splays kept the deep (master fault-proximal) end of the basin overfilled, so that it could not provide accommodation for reworked tuffs and extrabasinally-sourced ignimbrites that dominate the shallow (underfilled) end of the basin. This pattern of basin fill contrasts markedly with that of nonvolcanic strike-slip basins on transform margins, where clastic sedimentation commonly cannot keep pace with subsidence in the master fault-proximal end. Volcanic and subvolcanic rocks in the strike-slip basin largely record polygenetic (explosive and effusive) small-volume eruptions from many vents in the complexly faulted basin, referred to here as multi-vent complexes. Multi-vent complexes like these reflect proximity to a continuously active fault zone, where numerous strands of the fault frequently plumb small batches of magma to the surface. Releasing-bend extension promotes small, multivent styles of volcanism in preference to caldera collapse, which is more likely to form at releasing step-overs along a strikeslip fault.

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Initiation and development of pull-apart basins with Riedel shear mechanism: insights from scaled clay experiments

Atmaoui

Kukowski

Stöckhert

et al. 2005

Int J Earth Sci (Geol Rundsch)

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Typical pull-apart structures were created in scaled clay experiments with a pure strike-slip geometry (Riedel type experiments). A clay slab represents the sedimentary cover above a strike-slip fault in the rigid basement. At an early stage of the development of the deformation zone, synthetic shear fractures (Riedel shears) within the clay slab display dilatational behaviour. With increasing basal displacement the Riedel shears rotate and open further, developing into long, narrow and deep troughs. The shear displacement and the low angle with the prescribed principal basal fault set them apart from tension gashes. At a more evolved stage, synthetic segments (Y-shears) parallel to the basal principal fault develop and accommodate progressive strike-slip deformation. The Y-shears connect the tips of adjacent troughs developed from the earlier Riedel shears, resulting in the typical rhomb-shaped structures characteristic for pull-apart basins. The Strait of Sicily rift zone, with major strike-slip systems being active from the Miocene to the Present, comprises pull-apart basins at different length scales, for which the structural record suggests development by a mechanism similar to that observed in our experiments.

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Strike‐slip basins, Part 2

Cited by 34 publications

References 0 publications

How did the Alxa Block respond to the Indo-Eurasian collision?

How did the Alxa Block respond to the Indo-Eurasian collision?

Volcanic facies architecture of an intra-arc strike-slip basin, Santa Rita Mountains, Southern Arizona

Initiation and development of pull-apart basins with Riedel shear mechanism: insights from scaled clay experiments

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