An analytical model of hanging-wall and footwall deformation at ramps on normal and thrust faults

Kilsdonk, Bill; Fletcher, Robert J.

doi:10.1016/0040-1951(89)90123-6

Cited by 33 publications

(17 citation statements)

References 13 publications

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“…Processes that cause damage zone growth include fault and process zone propagation and linkage [e.g., Cowie and Scholz, 1992;McGrath and Davison, 1995;Vermilye and Scholz, 1998], wear related to fault geometry [e.g., Scholz, 1987;Wilson et al, 2003], and off-fault plasticity accompanying earthquake rupture [e.g., Rice et al, 2005; J. P. Ampuero and X. Mao, Upper limit on damage zone thickness controlled by seismogenic depth, in Fault Zone Dynamic Processes: Evolution of Fault Properties During Seismic Rupture, AGU Monogr., edited by M. Y. Thomas, H. S. Bhat, and T. Mitchell, manuscripts in preparation, 2016]. Fracture modes and attitudes in the damage zone are a function of the stress field when they form, suggesting that fracture characteristics can be useful for constraining off-fault stresses [e.g., Kilsdonk and Fletcher, 1989;Saucier et al, 1992;Chester and Fletcher, 1997;Chester and Chester, 2000;Di Toro et al, 2005;Griffith et al, 2010]. Based on this relation, the types, distributions, and orientations of damage zone structures corresponding to each fault evolution process have been recognized in some cases, including mature faults that have experienced many slip events [e.g., Vermilye and Scholz, 1998;Wilson et al, 2003;Mitchell and Faulkner, 2009].…”

Section: Introductionmentioning

confidence: 99%

The damage is done: Low fault friction recorded in the damage zone of the shallow Japan Trench décollement

Keren

Kirkpatrick

2016

JGR Solid Earth

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Fault damage zones record the integrated deformation caused by repeated slip on faults and reflect the conditions that control slip behavior. To investigate the Japan Trench décollement, we characterized the damage zone close to the fault from drill core recovered during Integrated Ocean Drilling Program Expedition 343 (Japan Trench Fast Drilling Project (JFAST)). Core‐scale and microscale structures include phyllosilicate bands, shear fractures, and joints. They are most abundant near the décollement and decrease in density sharply above and below the fault. Power law fits describing the change in structure density with distance from the fault result in decay exponents (n) of 1.57 in the footwall and 0.73 in the hanging wall. Microstructure decay exponents are 1.09 in the footwall and 0.50 in the hanging wall. Observed damage zone thickness is on the order of a few tens of meters. Core‐scale structures dip between ~10° and ~70° and are mutually crosscutting. Compared to similar offset faults, the décollement has large decay exponents and a relatively narrow damage zone. Motivated by independent constraints demonstrating that the plate boundary is weak, we tested if the observed damage zone characteristics could be consistent with low‐friction fault. Quasi‐static models of off‐fault stresses and deformation due to slip on a wavy, frictional fault under conditions similar to the JFAST site predict that low‐friction fault produces narrow damage zones with no preferred orientations of structures. These results are consistent with long‐term frictional weakness on the décollement at the JFAST site.

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Section: Introductionmentioning

confidence: 99%

The damage is done: Low fault friction recorded in the damage zone of the shallow Japan Trench décollement

Keren

Kirkpatrick

2016

JGR Solid Earth

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“…Each half-space slides at a constant rate relative to an interface that is fixed in the coordinate system. The analysis follows that of Johnson [1980, 1982], Kilsdonk and Fletcher [1989], and Johnson and Fletcher [1994] and provides an approximate analytical solution accurate to first order in the slope of the interface. Tensile stress is positive, deformation is plane flow, the deforming material is incompressible, and the fault is assumed to have zero strength.…”

Section: Model Descriptionmentioning

confidence: 97%

“…The velocity vector is tangent to the streamline and its magnitude is inversely proportional to the streamline spacing for a fixed contour interval [e.g., Kilsdonk and Fletcher, 1989]. Streamlines for the basic state flow are uniformly spaced and parallel to the mean orientation of the sliding surface because particle velocity is constant in the basic state flow.…”

Section: Simple Sinusoidal Sliding Surface Velocity Fieldmentioning

confidence: 99%

Stress distribution and failure in anisotropic rock near a bend on a weak fault

Chester¹,

Fletcher²

1997

J. Geophys. Res.

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Abstract. Large transform faults, thin-skinned thrust faults, and listric normal faults often contain restraining and releasing bends that can alter the state of stress in the adjacent crust during faulting episodes. Crustal rock commonly has anisotropic mechanical properties due to the presence of sedimentary layering, subsidiary fractures and faults, schistosity, or other foliation. We present an analytical solution for the stress distribution in anisotropic rock produced by sliding on a wavy, frictionless surface. The frictionless surface represents the limiting case of a weak fault. The fault shape treated is either a sinusoid, or a periodic array of isolated restraining and releasing bends. The rheological behavior of the rock is that of an incompressible linear viscous fluid with an orthotropic anisotropy characterized by a greater viscosity for shortening and extension than for shear in the principal directions of anisotropy.Our results illustrate that stress and flow associated with a bend in a fault will extend to much greater distances from the fault when the medium is anisotropic. The magnitude of the stress perturbation increases with degree of anisotropy and decreases with radius of curvature of the fault surface. Principal stress directions tend to align parallel to the principal directions of anisotropy except in the immediate region of the fault bend. Mean stress and maximum shear stress magnitudes vary along the fault in a cellular manner, with multiple maxima near a bend. Stress concentrations emanate from the bend and are elongate in directions parallel to the principal directions of anisotropy. For isotropic rock, locations and orientations of shear failure near restraining bends are distinctly different from those near releasing bends. In contrast, with application of an anisotropic failure criterion, as the magnitude of anisotropy increases, the patterns of shear failure at a restraining and a releasing bend become increasingly similar. The model may help explain field observations from dip-slip and strikeslip regimes that indicate a complex stress history and local stress reorientation adjacent to a bend in a fault.

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“…In addition, Smart et al (2009) used finite-elementbased geomechanical models of fault related folds to show the impact of interlayer slip on fracture prediction. While little attention has been afforded to the mechanics of fault-related fold buckling, the theory of folding of initial perturbations in isolated layers or multilayers without faulting is quite mature (e.g., Biot 1963Biot , 1964Chapple 1969;Fletcher 1977;Johnson 1977;Kilsdonk and Fletcher 1989;Johnson and Fletcher 1994;Mancktelow 1999). Of particular relevance to this paper are theoretical studies on the physical conditions of multilayer folding that lead to significant amplification of initially small perturbations.…”

Section: Kinematics and Mechanics Of Fault-cored Anticlinesmentioning

confidence: 99%

A Fault-Cored Anticline Boundary Element Model Incorporating the Combined Fault Slip and Buckling Mechanisms

Huang

Johnson

2016

Terr. Atmos. Ocean. Sci.

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We develop a folding boundary element model in a medium containing a fault and elastic layers to show that anticlines growing over slipping reverse faults can be significantly amplified by mechanical layering buckling under horizontal shortening. Previous studies suggested that folds over blind reverse faults grow primarily during deformation increments associated with slips on the fault during and immediately after earthquakes. Under this assumption, the potential for earthquakes on blind faults can be determined directly from fold geometry because the amount of slip on the fault can be estimated directly from the fold geometry using the solution for a dislocation in an elastic half-space. Studies that assume folds grown solely by slip on a fault may therefore significantly overestimate fault slip. Our boundary element technique demonstrates that the fold amplitude produced in a medium containing a fault and elastic layers with free slip and subjected to layer-parallel shortening can grow to more than twice the fold amplitude produced in homogeneous media without mechanical layering under the same amount of shortening. In addition, the fold wavelengths produced by the combined fault slip and buckling mechanisms may be narrower than folds produced by fault slip in an elastic half space by a factor of two. We also show that subsurface fold geometry of the Kettleman Hills Anticline in Central California inferred from seismic reflection image is consistent with a model that incorporates layer buckling over a dipping, blind reverse fault and the coseismic uplift pattern produced during a 1985 earthquake centered over the anticline forelimb is predicted by the model.

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An analytical model of hanging-wall and footwall deformation at ramps on normal and thrust faults

Cited by 33 publications

References 13 publications

The damage is done: Low fault friction recorded in the damage zone of the shallow Japan Trench décollement

The damage is done: Low fault friction recorded in the damage zone of the shallow Japan Trench décollement

Stress distribution and failure in anisotropic rock near a bend on a weak fault

A Fault-Cored Anticline Boundary Element Model Incorporating the Combined Fault Slip and Buckling Mechanisms

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