Reverse drag revisited: Why footwall deformation may be the key to inferring listric fault geometry

Resor, Phillip G; Pollard, David D.

doi:10.1016/j.jsg.2011.10.012

Cited by 39 publications

(12 citation statements)

References 72 publications

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“…Linear elasticity theory has enjoyed success over a range of problems, including fault-related folding (Gupta and Scholz, 1998;Resor, 2008), and, more recently, it has been useful in examining fault propagation (Martel and Langley, 2006). Our code has been translated into MATLAB (Martel and Langley, 2006) and modifi ed to accommodate displacement discontinuity (relative displacements across the fault) boundary conditions (Resor and Pollard, 2012). We drive the models by applying constant slip across the dipping portions of the fault.…”

Section: Methodsmentioning

confidence: 99%

“…In this section, we use numerical models to explore how changes in a few basic fault parameters (lower tip depth, upper tip depth, and slip magnitude) might lead to the observed differences in structure between these two faults. Footwall stratigraphy is not exposed over most of the map area, ruling out a formal inversion for fault geometry (Resor and Pollard, 2012). Instead, we take an illustrative approach.…”

Section: Modeling the Deformationmentioning

confidence: 99%

“…Reverse-and normal-drag fold geometry is a function of fault geometrical properties (Resor and Pollard, 2012;Resor, 2008;Willsey et al, 2002;Withjack et al, 1990), mechanical properties of the deforming strata (Wilson et al, 2009), mechanical effects due to fault linkage (Crider and Pollard, 1998;Willemse, 1997), and/or slip distribution along the fault (White and Crider, 2006;Grasemann et al, 2005). Furthermore, modeling efforts using a wide range of techniques have found a positive correlation between fault upper tip depth and width of the hangingwall syncline created by blind faulting (e.g., Withjack et al, 1990;Erslev, 1991;Johnson and Johnson, 2002;Willsey et al, 2002).…”

Section: Variation In Fault and Fold Geometry Along Strikementioning

confidence: 99%

“…For example, a concave-upward (listric) fault geometry has long been assumed to be a necessary and suffi cient condition to form reverse-drag folds in the hanging wall of normal faults (Hamblin, 1965). However, there is a growing body of evidence that suggests reverse drag may be caused by slip on planar or antilistric faults as well (Reches and Eidelman, 1995;Grasemann et al, 2005;Resor, 2008), and footwall fold structure may be more diagnostic of specifi c fault geometries (Resor and Pollard, 2012); similarly, normal-drag folds are now thought to result from fault propagation below and past the deforming strata (Willsey et al, 2002;White and Crider, 2006). However, the full range of possible fold geometries associated with normal faulting is not clear, nor is the specifi c way in which fault geometry may be responsible for folds visible in outcrop.…”

Section: Introductionmentioning

confidence: 99%

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Constraints on the evolution of vertical deformation and Colorado River incision near eastern Lake Mead, Arizona, provided by quantitative structural mapping of the Hualapai Limestone

et al. 2015

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The 12-6 Ma Hualapai Limestone was deposited in a series of basins that lie in the path of the Colorado River directly west of the Colorado Plateau and has been deformed by an en-echelon normal fault pair (Wheeler and Lost Basin Range faults). Therefore, this rock unit represents an opportunity to study the sedimentological and structural setting over which the Colorado River fi rst fl owed after integration through western Grand Canyon and Lake Mead. In this study, we quantify the structural geometry of the Hualapai Limestone and separate the deformation into syn-and postdepositional episodes. Both the Wheeler and Lost Basin Range faults were active during Hualapai Limestone deposition, as shown by thickening of strata and fanning of time lines toward half-graben faults that bound the Hualapai subbasins. The structure is characterized by a prominent reverse-drag fold and broad, shallow syncline adjacent to the Lost Basin Range fault, and a small-magnitude reverse-drag fold and short-wavelength normal-drag fold adjacent to the Wheeler fault. We fi nd ~450 m of throw between the footwall and hangingwall Hualapai Limestone sections, suggesting faulting was ongoing after Hualapai Limestone deposition ceased and during Colorado River incision. To investigate a range of possible fault geometries that may have been responsible for Hualapai Limestone deformation, we compared our structural results against surface defl ections calculated by a two-dimensional (2-D) geomechanical model. While nonunique, our results are consistent with a scenario in which the Wheeler fault was surface rupturing, or nearly surface rupturing throughout deposition of the Hualapai Limestone, but was inundated at ca. 6 Ma by coalescing paleolakes in Gregg and Grand Wash Basins as sedimentation kept pace with deformation. In contrast, we fi nd evidence suggesting the Lost Basin Range fault was deeply buried by the Hualapai Limestone and likely propagated upward and laterally to break the surface sometime after 6 Ma. Therefore, we interpret the landscape over which the Colorado River fi rst fl owed to be of low relief within the terrain bounded by the Grand Wash Cliffs, the Hiller Mountains, and subtle topographic highs to the north and south of our fi eld area. This original low-relief depositional surface was defl ected into the structure exposed today by continuing deformation by the Wheeler and Lost Basin Range faults, allowing for calculation of apparent incision rates of the modern Colorado River drainage system that spatially vary between 33 and 42 m/m.y. in the hanging wall and between 108 and 115 m/m.y. in the footwall. Hanging-wall incision rate values are similar to, but faster than, a previously published point measurement, and footwall values are similar to measured incision rates in the western Grand Canyon, suggesting the Wheeler fault system may resolve as much as ~410 m of Colorado Plateau uplift in the last 6 m.y.

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Section: Methodsmentioning

confidence: 99%

Section: Modeling the Deformationmentioning

confidence: 99%

Section: Variation In Fault and Fold Geometry Along Strikementioning

confidence: 99%

Section: Introductionmentioning

confidence: 99%

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Constraints on the evolution of vertical deformation and Colorado River incision near eastern Lake Mead, Arizona, provided by quantitative structural mapping of the Hualapai Limestone

et al. 2015

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“…In nature, extensional faults may have a listric geometry that induces hanging wall deformation driven by the sliding of rocks on a curved fault surface (e.g. rollover and drag folds), potentially broadening the newly-generated accommodation space (Resor and Pollard, 2012). Friction on the master fault plane and secondary normal-and reverse-drag folds or a combination thereof may also control hanging wall deformation (e.g., Schlische, 1995).…”

Section: Modeling Limitationsmentioning

confidence: 99%

The role of pre-existing discontinuities in the development of extensional faults: An analog modeling perspective

Bonini

Basili

Toscani

et al. 2015

Journal of Structural Geology

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Elucidating the geometry of the active Shanchiao Fault in the Taipei metropolis, northern Taiwan, and the reactivation relationship with preexisting orogen structures

et al. 2014

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The Shanchiao Fault is an active normal fault with documented paleoearthquakes in the Taipei metropolis, Taiwan. While posing direct seismic threat on the multimillion population, its crustal-scale fault plane configuration has not been constrained. This study presents the first attempt to resolve the fault plane dip changes of the Shanchiao Fault within the upper crust by forward modeling late Quaternary deformation. Tectonic subsidence over the last~23 ka is estimated from vertical displacements of a rapidly formed alluvial fan horizon deformed into a dramatic rollover monocline. A 2-D profile across the Shanchiao Fault is chosen for elastic half-space dislocation modeling, and the results suggest that the fault is listric in the shallow crust with an abrupt change from subvertical ramp (85°-75°) to near-horizontal flat (10°-15°) at 3-4 km depth, consistent with an origin from the inversion of an orogen-related thrust detachment. Given the presence of rift-related fabrics in the underthrust Chinese Continental Margin basement beneath the Taiwanese orogenic wedge, listric ramp-flat-ramp models with a second deeper bend to 60°dip are also tested. Reasonable fits with the geological observations are produced when the lower ramp is located at greater than 8 km depth, which correlates with the hypocentral location of a moderate earthquake in 2004. Joint reactivation of preexisting thrust and rift faults by the Shanchiao Fault is therefore plausible with implications for seismic hazard in the Taipei area.

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Reverse drag revisited: Why footwall deformation may be the key to inferring listric fault geometry

Cited by 39 publications

References 72 publications

Constraints on the evolution of vertical deformation and Colorado River incision near eastern Lake Mead, Arizona, provided by quantitative structural mapping of the Hualapai Limestone

Constraints on the evolution of vertical deformation and Colorado River incision near eastern Lake Mead, Arizona, provided by quantitative structural mapping of the Hualapai Limestone

The role of pre-existing discontinuities in the development of extensional faults: An analog modeling perspective

Elucidating the geometry of the active Shanchiao Fault in the Taipei metropolis, northern Taiwan, and the reactivation relationship with preexisting orogen structures

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