Fault propagation and segmentation: insight from the microstructural examination of a small fault

Vermilye, Jan; Scholz, Christopher H.

doi:10.1016/s0191-8141(99)00093-0

Cited by 76 publications

(28 citation statements)

References 38 publications

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“…The fracture process zone (FPZ) in rocks is defined as the region affected by microcracking and frictional slip surrounding the visible crack tip propagating under stress, (LABUZ et al, 1987;VERMILYE and SCHOLZ, 1999). The width of the FPZ is defined as the longest distance between visible cracks on either side of the main fracture and/or fault and its length is defined as the length between the fault tip and the crack with the greatest distance in front of the fault tip.…”

Section: Fracture Process Zonementioning

confidence: 99%

Fracture Toughness Measurements and Acoustic Emission Activity in Brittle Rocks

Nasseri

Mohanty

Young

2006

Pure appl. geophys.

104

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Fracture toughness measurements under static loading conditions have been carried out in Barre and Lac du Bonnet granites. An advanced AE technique has been adopted to monitor real-time crack initiation and propagation around the principal crack in these tests to understand the processes of brittle failure under tension and related characteristics of the resulting fracture process zone. The anisotropy of Mode I fracture toughness has been investigated along specific directions. Microcrack density and orientation analysis from thin section studies have shown these characteristics to be the primary cause of the observed variation in fracture toughness, which is seen to vary between 1.14 MPa.(m) 1/2 and 1.89 MPa.(m) 1/2 in Barre granite. The latter value represents the case in which the crack is propagated at right angles to the main set of microcracks. The creation of a significant fracture process zone surrounding the propagating main crack has been confirmed. Real-time imaging of the fracture process and formation of fracture process zone by AE techniques yielded results in very good agreement with those obtained by direct optical analysis.

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Section: Fracture Process Zonementioning

confidence: 99%

Fracture Toughness Measurements and Acoustic Emission Activity in Brittle Rocks

Nasseri

Mohanty

Young

2006

Pure appl. geophys.

104

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“…As pointed out by Kim and Sanderson (2006), distinction between these two tip-damage zones is not always clear. Commonly, fractures of a horsetail termination are sub-parallel to regional r 1 and form relatively low angles to the master strike-slip fault at its tips (usually \30°) (Segall and Pollard 1980;Granier 1985;Vermilye and Scholz 1999), whereas normal faults strike at a higher angle to the master fault (Kim and Sanderson 2006). Considering the fault system pattern previously described, we favor the interpretation of a horsetail termination structure (Fig.…”

Section: Regional Inversion Of Seismic Wavesmentioning

confidence: 50%

The M = 5.1 1980 Arudy earthquake sequence (western Pyrenees, France): a revisited multi-scale integrated seismologic, geomorphologic and tectonic investigation

Courjault‐Radé

Darrozes

Gaillot

2008

Int J Earth Sci (Geol Rundsch)

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This paper presents a combination of seismic imaging, geomorphologic, and tectonic data and an interpretation of the M = 5.1 1980 Arudy earthquake sequence putting in relation the seismicity, the inherited faults, and the geomorphologic (Würm and postwürm) markers in this region of the Pyrenees. Since the anticlockwise rotation of the regional compression axis in Oligocene time, western Pyrenees are under a dextral regime and the resulting motion is accommodated along major inherited E-W dextral strike-slip faults. The Arudy aftershocks sequence is controlled by antecedent horsetail splay faults built at the boundary between two shallow Mesozoic crustal blocks most probably due to their differing rheology. This boundary has played the role of a seismic barrier stopping the E-W slip motion. The Arudy earthquake has reactivated the eastern segment of the main E-W strike-slip fault, while the post-seismic aftershocks correspond to local relaxation processes in normal tectonic behavior.

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“…The local distribution of the NNE-SSW, the ENE-WSW and the N-S fractures is, in part, due to the spatial limitation of the studied exposure, but also reflects the role of earlier fractures in controlling the location of later events. The fractures are interpreted to have formed as extension (mode I) fractures, but some of them show evidence for later slip and/or oblique loading, mainly in the form of secondary fractures developed as en echelon arrays at the terminations of fractures (McGrath and Davision, 1995;Vermilye and Scholz, 1999;Kim et al, 2000Kim et al, , 2003Kim et al, , 2004 (Fig. 3).…”

Section: Description Of the Fracture Networkmentioning

confidence: 99%

Fractal analysis of the evolution of a fracture network in a granite outcrop, SE Korea

et al. 2010

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Kinematical and fractal analyses were conducted on a fracture network in a well-exposed granite outcrop in SE Korea. The objective of this study is to examine the temporal and spatial evolution of the fracture network. From the orientation and abutting relationships of fracture sets, six fracturing events and their relative ages were established, several of which included strike-slip reactivations of earlier formed fractures. These events may be correlated with the Cenozoic to Recent evolution of the Yangsan Fault and surrounding areas. 2-D box counting analyses were performed on maps of the fracture network at the six stages of its evolution. For the earliest event D = 1.11, and represents a clustered development of fractures. Event 2 leads to a large increase of D = 1.51, with subsequent events producing a gradual increase up to 1.55 after the final event. This stabilization of the fractal dimension involved a change from the widespread development of new fractures (event 2) to the greater importance of reactivation of existing fractures, with only localized development of new fractures, usually as tip and linkage damage around pre-existing fractures. Fracture density was greatest for the event 2 fractures and increased only gradually after that. This pattern is similar to that of the fractal dimension and a good linear correlation was found between these two parameters. Although fractal dimensions and density show little change during the late stages of deformation, the fracture connectivity continued to increase due to the formation of local secondary fractures developed during reactivation of earlier formed fractures.

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Fault propagation and segmentation: insight from the microstructural examination of a small fault

Cited by 76 publications

References 38 publications

Fracture Toughness Measurements and Acoustic Emission Activity in Brittle Rocks

Fracture Toughness Measurements and Acoustic Emission Activity in Brittle Rocks

The M = 5.1 1980 Arudy earthquake sequence (western Pyrenees, France): a revisited multi-scale integrated seismologic, geomorphologic and tectonic investigation

Fractal analysis of the evolution of a fracture network in a granite outcrop, SE Korea

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