Sedimentary masses and concepts about tectonic processes at underthrust ocean margins

Scholl, David W.; Huene, Roland von; Vallier, T.L.; Howell, David G.

doi:10.1130/0091-7613(1980)8<564:smacat>2.0.co;2

Cited by 213 publications

(97 citation statements)

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“…7b). As deformation continues, motion along some thrust faults dies out, and the inactive thrusts become buried by slope sediments, thus increasing the size of slope basins (Moore and Karig, 1976;Scholl et al, 1980). Most thrust lineaments are sub-parallel to the deformation front suggesting a thrust component origin similar to the actual north-south compression regime observable in the structure of the lower slope (Fig.…”

Section: Middle Slopementioning

confidence: 99%

“…This thrusting gives rise to damage tracks throughout the deformed belt (Dominguez et al, 2000;Marques and Cobbold, 2002). The interaction of seamounts or basement highs with the thrust belt yields recesses due to two effects: lower volume of sediment being accreted and tectonic erosion (Scholl et al, 1980). Many seamounts and volcanic bodies have been observed in the central Venezuelan Basin region (Jany, 1989;Driscoll and Diebold, 1999).…”

Section: Map-view Geometry Of the Thrust Beltmentioning

confidence: 99%

“…TZ = Transfer Zone. 1976; Scholl et al, 1980;Charvet and Ogawa, 1994). Bigger slope basins show deeper sedimentary layers tilted as a result of syntectonic sedimentation, while sub-horizontal shallower reflectors have been deposited in a posterior stage of lower tectonic activity (Fig.…”

Section: Middle Slopementioning

confidence: 99%

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Morphotectonics of the central Muertos thrust belt and Muertos Trough (northeastern Caribbean)

et al. 2009

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Section: Middle Slopementioning

confidence: 99%

Section: Map-view Geometry Of the Thrust Beltmentioning

confidence: 99%

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Morphotectonics of the central Muertos thrust belt and Muertos Trough (northeastern Caribbean)

et al. 2009

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“…Basal erosion rates of 25-50 km 3 /m.y. per kilometer of trench length are estimated for northeast Japan, northern Chile and Peru, Ecuador, Costa Rica, and Alaska (Scholl et al, 1980;von Huene and Lallemand, 1990;von Huene and Scholl, 1991;Collot et al, 2004;Clift and Vannucchi, 2004). The process by which subduction erosion occurs is unclear.…”

Section: Erosive and Accretionary Convergent Marginsmentioning

confidence: 99%

Expedition 344 summary

Li¹,

Malinverno²,

Torres³

et al. 2013

Proceedings of the IODP

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Expedition 344 summaryProc. IODP | Volume 344 2 from velocity-strengthening to velocity-weakening friction, and shear becomes localized. The onset of seismogenic behavior is correlated with the intersection of the 100°-150°C isotherm and the subduction thrust (Hyndman et al., 1997;Oleskevich et al., 1999). With increasing depth down the subduction thrust, the frictional characteristics undergo a second transition either due to the juxtaposition with the forearc mantle or because the rocks are heated to 350°-450°C and can no longer store elastic stresses needed for rupture. Transitional regions between the three zones have conditional stability and can host rupture but are generally not thought to be regions where large earthquakes initiate.Although this three-zone two-dimensional view of the subduction thrust provides a reasonable framework, it is simplistic. Rupture models for large subduction earthquakes suggest significant fault plane heterogeneity in slip and moment release that in three dimensions is characterized as patchiness (Bilek and Lay, 2002). Additionally, we now know the transition zone from stable to unstable sliding is not simple but hosts a range of fault behaviors that includes creep events, strain transients, slow and silent earthquakes, and low-frequency earthquakes (Peng and Gomberg, 2010;Beroza and Ide, 2011;Ide, 2012).Fundamentally unknown are the processes that change fault behavior from stable sliding to stick-slip behavior. Understanding these processes is important for understanding earthquakes, the mechanics of slip, and rupture dynamics. For a fault to undergo unstable slip, fault rocks must have the ability to store elastic strain, be velocity weakening, and have sufficient stiffness. Hypotheses for mechanisms leading to the transition between stable and unstable slip invoke temperature, pressure, and strain-activated processes that lead to downdip changes in the mechanical properties of rocks. These transitions are also sensitive to fault zone composition, lithology, fabric, and fluid pressures.The composition of the material in the fault zone and its contrast with the surrounding wall rock play a key role in rock frictional behavior. The frictional state of the incoming sediment changes progressively with increasing temperature and pressure as it travels downdip. Important lithologic factors influencing friction are composition, fabric, texture, and cementation of rocks, as well as fluid pore pressure (Bernabé et al., 1992;Moore and Saffer, 2001;Beeler, 2007;Marone and Saffer, 2007;Collettini et al., 2009). For example, fault rocks with high phyllosilicate content are generally weaker than rocks with low phyllosilicate content (Ikari et al., 2011). Sediment properties including porosity, permeability, consolidation state, and alteration history also exert a strong influence on fault zone behavior. At erosive margins, where the plate boundary cuts into the overriding plate, the composition and strength of the upper plate is also important (McCaffrey, 1993).Field observations and la...

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“…Additional insight into their tectonic role is needed. the wedge, considerable amounts of sediment can be subducted into the mantle along with the underlying oceanic lithosphere [Coats, 1962;Scholl et al, 1980]. Subduction erosion is defined as the process that causes a net loss of material from the hanging wall (material that may have been previously accreted sediment and/or crystalline rock).…”

mentioning

confidence: 99%

Dynamics of sediment subduction‐accretion at convergent margins: Short‐term modes, long‐term deformation, and tectonic implications

Beaumont¹,

Ellis²,

Pfiffner³

1999

J. Geophys. Res.

132

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Abstract. A conceptual model is proposed for the short-term operation of subductionaccretion systems at convergent margins. The operation is described in terms of the mass fluxes among the four system components, namely, the accretionary (or prowedge) wedge (P), an uplifted plug (U), a retrowedge (R), and the subduction zone. The latter consists of a conduit (C) of slowly moving and deforming material and an underlying subduction channel where material moves and deforms more rapidly. A broad range of convergent margin types can be accommodated within the conceptual model framework, with differing short-term modes that depend on which of the P-U-R-C components that are active. Finite element geodynamical model experiments are used to investigate whether these modes are dynamically feasible. These experiments determine excitation of modes under controls that include model entry and exit mass fluxes; flexural loading by accreted material and slab pull forces; boundary velocities corresponding to subduction and subduction zone advance/retreat; distribution, thickness, and density of accreted sediment; and internal frictional properties of the Coulomb sediments. That all modes, with the exception of P (in which only a prowedge is created), are seen in the models provides support for the concepts and allows conditions that favor particular modes to be recognized. In addition, the finite deformation predicted by the models is used to infer the long-term tectonic styles associated with both single-mode evolutions and those that exhibit mode switching. A steady state mass balance can occur for modes 0 (pure subduction), P-C (i.e., where components P and C are active), or other modes when the surface mass denudation plus the subduction flux balances accretion plus tectonic underplating. The P-C mode is favored by subduction zone retreat and/or an increasing subduction load and creates an apparent landward dipping backstop. P-U-C is predicted to be the most common mode, and it creates an apparent seaward dipping backstop. P-U-R-C is an inefficient mode but is favored by easily detached retrocrust or sediment and/or a decreasing subduction load.

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Sedimentary masses and concepts about tectonic processes at underthrust ocean margins

Cited by 213 publications

References 0 publications

Morphotectonics of the central Muertos thrust belt and Muertos Trough (northeastern Caribbean)

Morphotectonics of the central Muertos thrust belt and Muertos Trough (northeastern Caribbean)

Expedition 344 summary

Dynamics of sediment subduction‐accretion at convergent margins: Short‐term modes, long‐term deformation, and tectonic implications

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