Length–displacement scaling and fault growth

Guðmundsson, Ágúst; Guidi, Giorgio De; Scudero, Salvatore

doi:10.1016/j.tecto.2013.06.012

Cited by 49 publications

(29 citation statements)

References 48 publications

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“…We propose that moving the fault away from this supplying region should promote internal deformation of the footwall. While the frequency of the fractures defining the damage zone at any given time decreases with distance from the fault core (Gudmundsson et al, 2010(Gudmundsson et al, , 2013, we thus propose that fault displacement becomes partitioned over a wider finite damage region as fault displacement increases. This is schematically represented here with 1.6 km additional plate divergence (or 115 kyr) between Figures 14a and 14b.…”

Section: Detachment Faulting and Serpentinizationmentioning

confidence: 82%

“…This seismically defined domain could either be a finite damage zone, created over time due to strain localization in a succession of subparallel fault segments within the footwall, or an instantaneous damage zone due to distribution of active deformation over a thick domain of subparallel fractures, or a combination of both. The abundance of the fractures defining a fault's damage zone at any given time decreases with distance from the fault core (Gudmundsson et al, ; Gudmundsson et al, ). A broad zone of distributed instantaneous deformation could form if the rheology of the footwall rocks is such that strain localization is not efficient.…”

Section: Interpretation and Discussionmentioning

confidence: 99%

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Quasi‐3‐D Seismic Reflection Imaging and Wide‐Angle Velocity Structure of Nearly Amagmatic Oceanic Lithosphere at the Ultraslow‐Spreading Southwest Indian Ridge

et al. 2017

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We present results from 3‐D processing of 2‐D seismic data shot along 100 m spaced profiles in a 1.8 km wide by 24 km long box during the SISMOSMOOTH 2014 cruise. The study is aimed at understanding the oceanic crust formed at an end‐member mid‐ocean ridge environment of nearly zero melt supply. Three distinct packages of reflectors are imaged: (1) south facing reflectors, which we propose correspond to the damage zone induced by the active axial detachment fault: reflectors in the damage zone have dips up to 60° and are visible down to 5 km below the seafloor; (2) series of north dipping reflectors in the hanging wall of the detachment fault: these reflectors may correspond to damage zone inherited from a previous, north dipping detachment fault, or small offset recent faults, conjugate from the active detachment fault, that served as conduits for isolated magmatic dykes; and (3) discontinuous but coherent flat‐lying reflectors at shallow depths (<1.5 km below the seafloor), and at depths between 4 and 5 km below the seafloor. Comparing these deeper flat‐lying reflectors with the wide‐angle velocity model obtained from ocean‐bottom seismometers data next to the 3‐D box shows that they correspond to parts of the model with P wave velocity of 6.5–8 km/s, suggesting that they occur in the transition between lower crust and upper mantle. The 4–5 km layer with crustal P wave velocities is interpreted as primarily due to serpentinization and fracturation of the exhumed mantle‐derived peridotites in the footwall of active and past detachment faults.

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Section: Detachment Faulting and Serpentinizationmentioning

confidence: 82%

Section: Interpretation and Discussionmentioning

confidence: 99%

Quasi‐3‐D Seismic Reflection Imaging and Wide‐Angle Velocity Structure of Nearly Amagmatic Oceanic Lithosphere at the Ultraslow‐Spreading Southwest Indian Ridge

et al. 2017

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“…Topographic tilting of the floor of such basins is associated with differential subsidence, whereby there typically exists a decrease in displacement both along the length of a basin-bounding fault from its centre to the fault tips, and also away from the fault to the basin margins. Ongoing sedimentation progressively fills this accommodation in the hangingwall of the basin (Bonini et al, 2016;Gudmundsson, Guidi, & Scudero, 2013;Jackson, 1987;Marrett & Allmendinger, 1991). As a half graben develops, the pivot-like motion of the surface results from tilting by individual extensional episodes, which are associated with episodic seismic events (i.e., earthquakes) that generate accommodation.…”

Section: Introductionmentioning

confidence: 99%

“…Some studies, on the contrary, argue that the styles of fault growth essentially indicate the maturity of a fault (Walsh, Nicol, & Childs, 2002). Although active faults may propagate along their entire perimeter and grow in strike length rapidly during the early stages of fault growth (Filbrandt, Richard, & Franssen, 1994), large faults tend to be confined laterally and the fault length remains almost constant as displacement accumulates (Gross et al, 1997;Walsh et al, 2002), for example, as seen in many large Holocene normal faults in Iceland (Gudmundsson, 2005;Gudmundsson et al, 2013). Furthermore, the linkage of adjacent smaller faults into a larger fault is another important mechanism by which a fault grows (Cartwright, Trudgill, & Mansfield, 1995;Gawthorpe & Leeder, 2000;Peacock, 2002;Peacock & Sanderson, 1996;Segall & Pollard, 1980).…”

Section: Introductionmentioning

confidence: 99%

Three‐dimensional forward stratigraphic modelling of the sedimentary architecture of meandering‐river successions in evolving half‐graben rift basins

2019

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The spatial organisation of meandering-river deposits varies greatly within the sedimentary fills of rift basins, depending on how differential rates of fault propagation and subsidence interplay with autogenic processes to drive changes in fluvial channel-belt position and rate of migration, avulsion frequency and mechanisms of meander-bend cut off. This set of processes fundamentally influences stacking patterns of the accumulated successions. Quantitative predictions of the spatio-temporal evolution and internal architecture of meandering fluvial deposits in such tectonically active settings remain limited. A numerical forward stratigraphic model-the Point-Bar Sedimentary Architecture Numerical Deduction (PB-SAND)-is applied to examine relationships between differential rates of subsidence and resultant fluvial channel-belt migration, reach avulsion and channel-deposit stacking in active, faultbounded half-grabens. The model is used to reconstruct and predict the complex morphodynamics of fluvial meanders, their generated channel belts, and the associated lithofacies distributions that accumulate as heterogeneous fluvial successions in rift settings, constrained by data from seismic images and outcrop successions.The 3D modelling outputs are used to explore sedimentary heterogeneity at various spatio-temporal scales. Results show how the connectivity of sand-prone geobodies can be quantified as a function of subsidence rate, which itself decreases both along and away from the basin-bounding fault. In particular, results highlight the spatial variability in the size and connectedness of sand-prone geobodies that is seen in directions perpendicular and parallel to the basin axis, and that arises as a function of the interaction between spatial and temporal variations in rates of accommodation generation and fault-influenced changes in river morphodynamics. The results have applied significance, for example, to both hydrocarbon exploration and assessment of groundwater aquifers. The expected greatest connectivity of fluvial sandbody in a half-graben is primarily determined by the complex interplay between the frequency and rate of subsidence, the style of basin propagation, the rates of migration of channel belts, the frequency of avulsion and the proportion and spatial distribution of variably sand-prone channel and bar deposits.How to cite this article: Yan N, Colombera L, Mountney NP. Three-dimensional forward stratigraphic modelling of the sedimentary architecture of meandering-river successions in evolving half-graben rift basins. Basin Res.

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“…Periodically distributed fractures in layered rock sequences are a common phenomenon (Schultz 1995;Gudmundsson 1992Gudmundsson , 2009Gudmundsson et al 2013;Bejari and Hamidi 2013). In most cases, the fractures of a given set are parallel or subparallel to each other (Narr and Lerche 1984;Narr and Suppe 1991;Gross 1993;Gillespie et al 1999;Tindall and Davis 2003;Tang et al 2008;Li et al 2012;Hooker et al 2013).…”

Section: Introductionmentioning

confidence: 99%

Effects of Interface Behavior on Fracture Spacing in Layered Rock

et al. 2015

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To better understand the periodically distributed fractures in rock sequences, the effects of the layer interfaces on the evolution of the stress distribution in a fracture-bound block and on the fracture infilling process are discussed. A three-layer model is developed based on a cohesive zone model (CZM) for layer interfaces and a plastic-damaged model for rock layers. The results indicate that the interface shear strength can greatly influence the stress distribution in a fracture-bound block so that the ratio of the fracture spacing to the layer thickness (S/T f ) is not the dominant factor in the stress state. If interface debonding occurs, the tensile stress in a fracture-bound block can decrease to zero even for a higher S/T f ratio. If the interface shear strength is high enough, a new fracture can further infill between two adjacent preexisting fractures even if the S/T f ratio is at a low level. The fracture process implies that there is a critical value for the interfacial shear strength that controls the fracture pattern between the central layer and its neighboring layers to be either interface debonding or layer-parallel fracture. Both interfacial debonding and layer-parallel fracture can separate the central layer from its neighboring layers and thus lead to fracture saturation. Further analysis indicates that the critical shear strength increases linearly with increasing tensile strength of the central layer.

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Length–displacement scaling and fault growth

Cited by 49 publications

References 48 publications

Quasi‐3‐D Seismic Reflection Imaging and Wide‐Angle Velocity Structure of Nearly Amagmatic Oceanic Lithosphere at the Ultraslow‐Spreading Southwest Indian Ridge

Quasi‐3‐D Seismic Reflection Imaging and Wide‐Angle Velocity Structure of Nearly Amagmatic Oceanic Lithosphere at the Ultraslow‐Spreading Southwest Indian Ridge

Three‐dimensional forward stratigraphic modelling of the sedimentary architecture of meandering‐river successions in evolving half‐graben rift basins

Effects of Interface Behavior on Fracture Spacing in Layered Rock

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