Fault-slip calculation from separations

Yamada, Eizo; Sakaguchi, Kei

doi:10.1016/0191-8141(95)00003-v

Cited by 5 publications

(5 citation statements)

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“…Unfortunately, it was not possible to reconstruct full slip vectors from this dataset, due to the lack of multiple displaced markers or striation-style transport direction indicators (c.f. Yamada & Sakaguchi, 1995, Xu et al, 2009. The observed offsets (apparent displacements) for this dataset range from 0.010 -0.410 m, consistent with a range of…”

Section: Field and Microstructural Markers Of Displacement Directionsupporting

confidence: 81%

Stress fields of ancient seismicity recorded in the dynamic geometry of pseudotachylyte in the Outer Hebrides Fault Zone, UK

Campbell

Lloyd

Phillips

et al. 2020

JGS

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Heterogeneous sequences of exhumed fault rocks preserve a record of long-term evolution of fault strength and deformation behaviour during prolonged tectonic activity. Along the Outer Hebrides Fault Zone (OHFZ), UK, numerous pseudotachylytes record palaeoseismic slip events within sequences of mylonites, cataclasites and phyllonites.To date, the kinematics and controls on seismicity within the long active history of the OHFZ have been poorly constrained. Additional uncertainties over the relative location of a meteorite impact and possible pre-OHFZ brittle faulting also complicates interpretation of the diffuse seismic record. This study presents kinematic analyses of seismicity in the OHFZ, combining observations of offset markers, en-echelon injection veins, and injection vein geometry to reconstruct slip directions and stress fields. This new dataset indicates that a range of fault orientations, slip directions and slip senses hosted seismicity in the OHFZ. Such complexity requires several stress field orientations, in contrast to NW-SE Caledonian compression traditionally attributed to frictional melting along the OHFZ, indicating that seismicity had a long-term presence across the fault zone. Persistence of strong frictional failure alongside the simultaneous development of weak fault rocks and phyllonitic shear zones in parts of the OHFZ has significant implications for understanding seismic hazard along mature continental faults.Supplementary material is available at: https://doi.org/10.6084/m9.figshare.c.5134797

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Section: Field and Microstructural Markers Of Displacement Directionsupporting

confidence: 81%

Stress fields of ancient seismicity recorded in the dynamic geometry of pseudotachylyte in the Outer Hebrides Fault Zone, UK

Campbell

Lloyd

Phillips

et al. 2020

JGS

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“…2) Most methods assume that faults are planar and have uniform slips across the portion of the fault surface analyzed. However, curved fault planes and slickenlines are commonly observed (e.g., Yamada and Sakaguchi, 1995;Xu et al, 2013). For the scissor faults, the slip is not uniform along the strike and dip in the analysis area.…”

Section: Discussionmentioning

confidence: 99%

“…In general, these conditions hold depending on the scale of analysis; competent rocks most likely fulfill the requirements of the geometric models in scales from decimeters to several hundred meters at shallow crustal levels. Diverse solutions have been proposed for calculating the net slip: graphic methods (Ragan, 2009;Babín-Vich and Gómez-Ortiz, 2010;Lisle and Walker, 2013;Waldron and Snyder, 2020), simple trigonometric equations (Xu et al, 2007;Nieto-Fuentes et al, 2014) and vector equations (Yamada and Sakaguchi, 1995;Nieto-Fuentes et al, 2022).…”

Section: Case Of Knowing Slip Direction and One Separation On A Faultmentioning

confidence: 99%

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Quantitative determination of fault slip magnitude: a review

Xu¹,

Nieto-Samaniego²,

Xu³

et al. 2023

revmexcg

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In geology, a fault is a rock fracture with perceptible relative displacement of the opposite sides of the fracture. Quantitatively obtaining the activity history of faults depends mainly on the estimation of fault slip and the study of markers, which can be used to understand and analyze the tectonic evolution of the faulted regions. Fault slip is calculated by restoring points that were originally adjacent before the deformation, those points are named piercing points. In this paper, we review some published methods to determine fault slip, using: (1) the offset of contours on structural contour maps; (2) offset on seismic reflection sections; (3) a known slip vector (fault striae) and one marker; (4) two known markers. Cases (3) and (4) are commonly applied to field work and geological maps.

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“…Similarly, the movement characteristics of geological faults relies implicitly on knowledge of the dip of the fault plane (e.g. Redmond, 1972;Yamada and Sakaguchi, 1995Xu et al, 2007Lisle and Walker, 2013); if the dip is not known, it is difficult to determine from other parameters except for specific combinations (e.g. Nieto-Fuentes et al, 2014).…”

Section: Boundary Plane Orientationmentioning

confidence: 99%