Fault damage zones

Kim, Young‐Seog; Peacock, David; Sanderson, David J.

doi:10.1016/j.jsg.2003.08.002

Cited by 743 publications

(452 citation statements)

References 75 publications

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“…The geometry of the faults defines the failure of rocks observed e.g., along the Gnieździska-Brzeziny Fault: strong lithologies within the restraining bands resulting in broad damage zones with numerous subsidiary faults and fractures, and weaker lithologies within the releasing bends with less common fracturing (Mastella and Konon 2002;Konon 2015;Rybak-Ostrowska et al 2015, 2016. The results of failure vary along the major and subsidiary faults and depend on the location of tip-linking or wall-damage zones (e.g., Segall and Pollard 1980;Kim et al 2004). …”

Section: Shallow Damage Zones Of Strike-slip Faults In the Area Adjacmentioning

confidence: 99%

“…Other structures useful for the precise identification of strike-slip movements in vertical cross-sections and on seismic profiles, as well as on geological maps and satellite images are: flower structures (e.g., Wilcox et al 1973), folds with a helicoidal geometry of the axial surfaces in restraining stepovers (Sylvester 1988;Babaahmadi et al 2010;Nadimi and Konon 2012), especially when they form an en échelon arrangement (Moody and Hill 1956;Jamison 1991;Woodcock and Schubert 1994), and vertical-axis rotated tectonic blocks bounded by major strike-slip faults (Woodcock and Fisher 1986;Mandl 1987;Sylvester 1988;Peacock et al 1998;Woodcock and Rickards 2003;Kim et al 2004;Konon 2007;Nadimi and Konon 2012). Apart from map-scale structures, identification of minor structures associated with major faults, such as slickensides observed within the near-surface parts of fault zones, horsetail splays, wing cracks or antithetic faults at the terminations of major faults, also demonstrate the presence of strike-slip movements.…”

Section: Introductionmentioning

confidence: 99%

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Mnin restraining stepover – evidence of significant Cretaceous–Cenozoic dextral strike-slip faulting along the Teisseyre-Tornquist Zone?

Konon¹,

Ostrowski²,

Rybak-Ostrowska³

et al. 2016

Acta Geologica Polonica

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ABSTRACT:Konon, A., Ostrowski, S., Rybak-Ostrowska, B., Ludwiniak, M., Śmigielski, M., Wyglądała, M., Uroda, J., Kowalczyk, S., Mieszkowski, R. and Kłopotowska, A. 2016. Mnin restraining stepover -evidence of significant Cretaceous-Cenozoic dextral strike-slip faulting along the Teisseyre-Tornquist Zone? Acta Geologica Polonica, 66 (3), 429-449. Warszawa.A newly recognized Mnin restraining stepover is identified in the Permo-Mesozoic cover of the western part of the Late Palaeozoic Holy Cross Mountains Fold Belt (Poland), within a fault pattern consisting of dextral strikeslip faults. The formation of a large contractional structure at the Late Cretaceous -Cenozoic transition displays the significant role of strike-slip faulting along the western border of the Teisseyre-Tornquist Zone, in the foreland of the Polish part of the Carpathian Orogen. Theoretical relationships between the maximum fault offsets/mean step length, as well as between the maximum fault offsets/mean step width allowed the estimation of the values of possible offsets along the Snochowice and Mieczyn faults forming the Mnin stepover. The estimated values suggest displacements of as much as several tens of kilometres. The observed offset along the Tokarnia Fault and theoretical calculations suggest that the strike-slip faults west of the Late Palaeozoic Holy Cross Mountains Fold Belt belong to a large strike-slip fault system.We postulate that the observed significant refraction of the faults forming the anastomosing fault pattern is related also to the interaction of the NW-SE-striking faults formed along the western border of the TeisseyreTornquist Zone and the reactivated WNW-ESE-striking faults belonging to the fault systems of the northern margin of the Tethys Ocean.

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Section: Shallow Damage Zones Of Strike-slip Faults In the Area Adjacmentioning

confidence: 99%

Section: Introductionmentioning

confidence: 99%

Mnin restraining stepover – evidence of significant Cretaceous–Cenozoic dextral strike-slip faulting along the Teisseyre-Tornquist Zone?

Konon¹,

Ostrowski²,

Rybak-Ostrowska³

et al. 2016

Acta Geologica Polonica

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“…The damage zone (DZ) around the fault core typically consists of a zone of intense damage, and possibly pulverized rocks, with a width of a few hundred meters (DOR et al, 2006(DOR et al, , 2008, which is surrounded by a broader, several kilometers wide zone, of distributed damage. The latter is probably a relic structure of the progressive coalescence and localization of the active fault zone over time (AMBRASEYS, 1970;KIM et al, 2004;SIBSON, 2003).…”

Section: Geological and Geophysical Observations Of Fault Zone Structurementioning

confidence: 99%

“…While the major fault segments reflect a positive feedback of strain weakening and strain localization along the fault cores, persisting geometrical features such as fault offsets, kinks, and bends, can produce strain hardening that leads to local complexity and secondary fractures at different scales (BEN-ZION and SAMMIS, 2003). Many studies have characterized macroscopic structural features within enlarged damage zones at geometrical irregularities (e.g., SEGALL and POLLARD, 1980;KIM et al, 2004). Our study attempts to clarify the evolution of structural properties of fault zones along relatively straight segments as well as near large persisting stepovers.…”

Section: Geological and Geophysical Observations Of Fault Zone Structurementioning

confidence: 99%

Structural Properties and Deformation Patterns of Evolving Strike-slip Faults: Numerical Simulations Incorporating Damage Rheology

Finzi

Hearn

Ben‐Zion

et al. 2009

Mechanics, Structure and Evolution of Fault Zones

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Abstract-We present results on evolving geometrical and material properties of large strike-slip fault zones and associated deformation fields, using 3-D numerical simulations in a rheologically-layered model with a seismogenic upper crust governed by a continuum brittle damage framework over a viscoelastic substrate. The damage healing parameters we employ are constrained using results of test models and geophysical observations of healing along active faults. The model simulations exhibit several results that are likely to have general applicability. The fault zones form initially as complex segmented structures and evolve overall with continuing deformation toward contiguous, simpler structures. Along relatively-straight mature segments, the models produce flower structures with depth consisting of a broad damage zone in the top few kilometers of the crust and highly localized damage at depth. The flower structures form during an early evolutionary stage of the fault system (before a total offset of about 0.05 to 0.1 km has accumulated), and persist as continued deformation localizes further along narrow slip zones. The tectonic strain at seismogenic depths is concentrated along the highly damaged cores of the main fault zones, although at shallow depths a small portion of the strain is accommodated over a broader region. This broader domain corresponds to shallow damage (or compliant) zones which have been identified in several seismic and geodetic studies of active faults. The models produce releasing stepovers between fault zone segments that are locations of ongoing interseismic deformation. Material within the fault stepovers remains damaged during the entire earthquake cycle (with significantly reduced rigidity and shearwave velocity) to depths of 10 to 15 km. These persistent damage zones should be detectable by geophysical imaging studies and could have important implications for earthquake dynamics and seismic hazard.

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“…Continuum damage rheology models (e.g., MALVERN, 1969;BUDIANSKY and O'CONNELL 1976;ALLIX and HILD, 2002) are particularly suitable for lithospheric deformation studies as they describe the brittle portion of the Earth's lithosphere as ''damaged'' in the sense that it contains an evolving distribution of weakened material (LYAKHOVSKY and MYASNIKOV, 1984;TURCOTTE and GLASSCOE, 2004). This view is supported by studies of fault-zone structures (e.g., CHESTER et al, 1993;EVANS et al, 2000;SIBSON, 2003;BEN-ZION and SAMMIS, 2003;KIM et al, 2004), and laboratory studies of brittle deformation (e.g., ALM et al, 1985;LOCKNER et al, 1992;HAMIEL et al, 2004a). In such rheology models, a damage state variable modifies the elastic properties of lithospheric materials, enabling the simulation of fault nucleation and evolution, including both damage accumulation and healing of fault-zone materials.…”

Section: Introductionmentioning

confidence: 98%

Shear Band Formation in Numerical Simulations Applying a Continuum Damage Rheology Model

Finzi

Mühlhaus

Gross

et al. 2012

Pure Appl. Geophys.

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Abstract-In seismically active regions, faults nucleate, propagate, and form networks that evolve over time. To simulate crustal faulting processes, including the evolution of fault-zone properties, a rheological model must incorporate concepts such as damage rheology that describe the various stages of the seismic cycle (strain localization, subcritical crack growth and macroscopic failure) while accounting for material degradation and healing and off-fault deformation. Here we study the fundamental patterns of strain-localisation within the framework of a continuum damage rheology by performing a shear band analysis (linear instability analysis) and comparing predictions of shear band orientations with numerical results of the nonlinear problem. We find (analytically and numerically) that the angle between the shear band and the less compressive (transverse) direction is between 47°in compression tests with a strain ratio of 0.25 (highly confined compression test), and 60°for a strain ratio higher than 1.4 (axial compression and transverse extension). In addition we find that shear bands exhibit local dilation (I 1 [ 0) in a wide range of strain ratios excluding only simulations with highly confined compression (which yield compacting shear bands or non-localized deformation). Finally, we discuss the applicability of the damage model for simulating deformation in the seismogenic, brittle crust.

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Fault damage zones

Cited by 743 publications

References 75 publications

Mnin restraining stepover – evidence of significant Cretaceous–Cenozoic dextral strike-slip faulting along the Teisseyre-Tornquist Zone?

Mnin restraining stepover – evidence of significant Cretaceous–Cenozoic dextral strike-slip faulting along the Teisseyre-Tornquist Zone?

Structural Properties and Deformation Patterns of Evolving Strike-slip Faults: Numerical Simulations Incorporating Damage Rheology

Shear Band Formation in Numerical Simulations Applying a Continuum Damage Rheology Model

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