The core of the Punchbowl Fault is surrounded by anĪpproximately 15 m thick damage zone ( Chester and Logan, 1986 Chester et al., 2005). Single, continuous gouge layer with 30 cm thickness on average hosts the Single PSZ embedded in a fault core and the surrounding damage zone. System, typifies this conceptual model of fault zone architecture. The Punchbowl Fault, an inactive, exhumed part of the San Andreas Fault ( 2003) are more complexĪnd consist of a damage zone hosting multiple, anastomosing principal slip (b)įaults described by the model of Faulkner et al. Single, quite narrow fault core hosting a principal slip zone. Relatively simple structure, where most of the strain is accommodated at a (a) According to the model of Caine et al. (e.g., Antonellini and Aydin, 1994) to a few hundred metersįigure 1Conceptual end-member models of fault zone architecture. Increasing displacement ( Evans, 1990 Faulkner et al., 2010 Ben-Zion and Sammis, 2003, and references therein). Up to 1 m thick ( Sibson, 2003) and thicknesses tend to increase with Although most commonly less than 10 cm thick, PSZs may be Ultracataclasites or fault gouges ( Sibson, 2003 Janssen et al., 2014 Toy et al., 2015). May be localized along one or more principal slip zones (PSZs) defined by Lithologically heterogeneous, and most of the displacement it accommodates Leads to granulation of rocks, distinct from a damage zone within whichįracture density is high but fracturing has “not sufficient to That a fault core should be defined as the zone within a fault where strain ThisĬonceptual framework has been found to be applicable to faults across theįull range of natural and experimental spatial scales Most of the displacement has been accommodated ( Caine et al., 1996). The damage zone contains the fault core (III) where Host rock ( Chester et al., 1993 Biegel and Sammis, 2004 Faulkner et al., 2010). Protolith (I) hosts a damage zone (II) that is characterized by a fractureĭensity significantly higher than the background values of the surrounding ( 1996) presented a conceptual model of the structure ofįault zones that has three primary components (Fig. Thus, from a georesource, seismic hazard and risk perspective, it is important toĬharacterize the seismo-mechanical properties of faults Many of these faults are located in densely populatedĪreas so they pose a significant geohazard ( Eguchi et al., 1998 Sahin and Tari, 2000 Martínez-Garzón et al., 2015). (Turkey) and the San Andreas Fault (USA) rupture in large ( M w>7) earthquakes ( Toppozada et al., 2002 Sutherland et al., 2007 Bohnhoff et al., 2016). Such as the Alpine Fault (New Zealand), the North Anatolian Fault Zone

Furthermore, large, plate-bounding strike-slip faults How important it is to understand fault zone properties and their spatial and Repositories ( Laurich et al., 2018) are practical examples demonstrating ( Cox et al., 1986) and long-term integrity of potential nuclear waste ( Van Eijs et al., 2006), exploitation of fault-hosted mineral deposits Hydrocarbon production from fault-compartmentalized reservoirs Substantially fluid flow ( Caine et al., 1996 Wibberley et al., 2008).

( Townend and Zoback, 2000 Bürgman and Dresen, 2008) and govern Stress field and stress magnitudes ( Sibson, 1985 Faulkner et al., 2006 Lindsey et al., 2014).įaults control the strength of the Earth's lithosphere Such as lithology ( Faulkner et al., 2003 Schleicher et al., 2010 Holdsworth et al., 2011 Rybacki et al., 2011), fluid pressure Interactions also govern strain distribution and depend on various factors, Seismo-mechanical behavior of faults are typically intimately related. The structure, composition, hydrological properties and Self-similar geometry ( Ben-Zion and Sammis, 2003 Twiss and Moores, 2007 Peacock et al., 2016). Networks of smaller, individual, but related and interacting, faults of Large fault zones are typically composed of ( Twiss and Moores, 2007 Ben-Zion, 2008 Fossen, 2016 Fossen and Cavalcante, 2017).

Mechanical manifestation of localized deformation The other parallel to the discontinuity plane, constitutes a rheological and A fault, a planar discontinuity in rock where one side has moved relative to

A strike slip fault