Growth pattern of underlithified strata during thrust-related folding

Nigro, Fabrizio

doi:10.1016/s0191-8141(04)00068-9

Cited by 2 publications

(5 citation statements)

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“…The pre-kinematic sedimentary strata in these settings are typically well lithifi ed, and the erosional products of the folds give rise to coarse-grained clastic sediments. As discussed by Nigro and Renda (2004) and Morley (2007b) deep-water folds (Fig. 26C) are different, for three main reasons: (1) folds are protected from subaerial and wave-related erosion; hence thicker, and more widely distributed synkinematic sedimentation can occur across anticlines, as well as within synclinal piggyback basins; (2) the synkinematic sediment deposited across anticlines during growth is poorly lithifi ed, predominantly fi ne grained and weak, and hence liable to be very sensitive to the effects of gravitational force during fold growth; and (3) the main erosional processes are a variety of mass-movement and mass-wasting phenomena, including rotational slides, fast and slow creep mass movement, debris fl ows, and turbidity fl ows, and currents (e.g., McGilvery and Cook, 2003;Heinio and Davies, 2006;Gee et al, 2007).…”

Section: Discussionmentioning

confidence: 97%

“…The strong topography causes interplay between structure and gravity fl ows moving down the continental slope. The patterns of synkinematic sediment deposition, sediment removal, and sediment redistribution signifi cantly impact fold shape (e.g., McGilvery and Cook, 2003;Nigro and Renda, 2004). Using a 3D seismic data set on 23 July 2009 geosphere.gsapubs.org Downloaded from gathered across young (Pliocene-Recent) folds offshore Brunei as an example, this paper investigates the ways in which folds develop through time in a deep-water setting and interact with sediment transport down a continental slope.…”

Section: Introductionmentioning

confidence: 99%

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Growth of folds in a deep-water setting

Morley¹

2009

Geosphere

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Regional 3D seismic data of the deepwater area offshore NW Borneo provide a detailed picture of the interaction between sedimentary processes on a continental slope and the growth of major folds over a time period of ca. 3.5-5 Ma. In the deep-water area, the estimated rates of fold propagation of tens of mm/yr −1 , shortening rates of mm/yr −1 , and fold segment lengths of tens of kilometers indicate the studied folds are similar in scale and deformation rate to folds in orogenic belts such as the Zagros Mountains and Himalayas. Feedbacks between sediment dispersal patterns, anticline growth, and structural style are manifested in many ways, and are enhanced by the presence of weak, poorly lithifi ed, synkinematic sediments at fold crests that undergo mass wasting as the fold grows. As folds tighten they range in geometry through simple foldsfolds affected by crestal normal faults, folds with crestal normal faults and rotational slides, and folds with forelimb degradation complexes and pronounced erosional unconformities. The unconformity surfaces are either elongate parallel to the fold axes (related to local mass wasting) or perpendicular (related to fl ows crossing the anticlines). Mass wasting processes in the study area that are large in scale compared with folds (i.e., giant landslides) have modifi ed anticline shape by erosion, and are little affected by anticline topography. More commonly, gravity fl ows are relatively small compared with the anticlines, and transport pathways are infl uenced by anticline surface topography. The factors infl uencing sediment pathway changes during anticline growth include: proximal to distal propagation of folds, lateral propagation of folds, and changing locations of fold growth with time. Assuming an overall consistency in sediment supply, local

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Section: Discussionmentioning

confidence: 97%

Section: Introductionmentioning

confidence: 99%

Growth of folds in a deep-water setting

Morley¹

2009

Geosphere

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“…We expect some dependence of the oscillating behavior on grain size as coarse grain deposits might be more resilient against slope instabilities ( e.g., Nigro & Renda, ). In our parametrization, the Rouse number embodies this relationship through the settling velocity v s of the sedimentary particles in the suspended load layer.…”

Section: Resultsmentioning

confidence: 99%

“…Despite its limited scope, our model shows that the deepwater environment behaves differently. The large mobility of fine‐grain sediments greatly enhances the feedbacks between sediment dispersal and fold growth, deeply altering the basic patterns observed in other environments ( e.g., Morley, ; Nigro & Renda, ). Moreover, our model suggests that the sedimentary record in deepwater foldbelt environments is not necessarily complete or decipherable.…”

Section: Discussionmentioning

confidence: 99%

“…When this happens, the rate of amplification accelerates, and structures acquire an angular shape characterized by steep limbs with secondary forward and back thrusting (Figure b). Moreover, since superficial mass transport is a slope‐dependent process (e.g., Roering et al, ; Nigro & Renda, ;), the more strained detachment folds denude rapidly forming structures with crests barren of sediments flanked by minibasins of flat topography. This phenomenon resulted in the deposition of a series of sedimentary wedges on the synclines that pinch out laterally by onlap against the fold limbs (Figure b; Yarbuh & Contreras, ).…”

Section: Geologic Settingmentioning

confidence: 99%

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Autogenic Organization of Syn‐Tectonic Sedimentary Patterns in Deepwater Foldbelts: A Simple Dynamic Model

et al. 2019

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We present a dynamical model that links through multiple length and time scales the formation of detachment folds, degradation of topography, and deposition of sheet‐like sedimentary bodies in deepwater foldbelt environments based on a nonlinear reaction–diffusion equation. We represent the stratigraphic response predicted by our model in a two‐dimensional parametric space whose axes are given by the Peclet number (Pe), the ratio of the mass transported by tectonic uplift and the mass transferred by diffusive hillslope processes, and the sediment delivery number (Sd), the ratio of sediments transported by density currents to those produced by intrabasinal processes. Notably, we identify three well‐defined regions of sedimentary behavior in that parametric space: a central domain (Pe > 2,Sd > 2) of cyclic stratigraphy produced by self‐sustained oscillations in the sedimentary system and two regions near the graph axes of stable sedimentation in which a continuous stratigraphy is produced. In the central domain, all the mass fluxes are equally important. This creates the conditions for a series of complex interaction between hillslope sediment transport, fold growth, and sedimentation. The other two regions correspond to end‐members in which either the Pe or Sd is small. For small Pe values, topographic degradation and sediment dispersal by hillslope transport dominate over tectonic uplift. Thus, any tectonic perturbation appearing in the system dissipates readily. For small Sd values, sediment transport is dominated by creep, and the system rapidly evolves toward a steady state.

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Growth pattern of underlithified strata during thrust-related folding

Cited by 2 publications

References 0 publications

Growth of folds in a deep-water setting

Growth of folds in a deep-water setting

Autogenic Organization of Syn‐Tectonic Sedimentary Patterns in Deepwater Foldbelts: A Simple Dynamic Model

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