An inverse problem in microtectonics for the determination of stress tensors from fault striation analysis

Etchecopar, A.; Vasseur, G.; Daignières, M.

doi:10.1016/0191-8141(81)90056-0

Cited by 602 publications

(212 citation statements)

References 7 publications

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“…Paleostress inversion provides an analysis of fault orientation and kinematic indicators to infer principle paleostresses (Carey and Burinier 1974;Etchecopar et al 1981;Angelier 1990Angelier , 1994. The result of the analysis contains information of the stress conditions that were responsible for brittle deformation events.…”

Section: Methods and Datamentioning

confidence: 99%

A Miocene onset of the modern extensional regime in the Isparta Angle: constraints from the Yalvaç Basin (southwest Turkey)

Koç

Kaymakçı

Hinsbergen

et al. 2014

Int J Earth Sci (Geol Rundsch)

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Section: Methods and Datamentioning

confidence: 99%

A Miocene onset of the modern extensional regime in the Isparta Angle: constraints from the Yalvaç Basin (southwest Turkey)

Koç

Kaymakçı

Hinsbergen

et al. 2014

Int J Earth Sci (Geol Rundsch)

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“…Since Wallace (1951) and Bott (1959) Figure 2. Detail of a multichannel seismic section across the toe of the Nankai accretionary wedge (from Moore et al, 1990) showing Holes 808C and 808B of Leg 131 as well as age and lithofacies distribution (Taira et al, 1992). plane suffering a given stress tensor, many authors addressed the inverse problem (e.g., Carey and Brunier, 1974;Armijo and Cisternas, 1978;Angelier, 1979 and1984;Etchecopar et al, 1981;Angelier et al, 1982;Gephart and Forsyth, 1984). Basically, most of these approaches assume that the slip direction is parallel to the maximum shear stress on the fault plane.…”

Section: Stress Tensor Inversionmentioning

confidence: 99%

Stress Tensors at the Toe of the Nankai Accretionary Prism: An Application of Inverse Methods to Slickenlined Faults

Byrne¹,

Maltman²,

Karig³

et al. 1993

Proceedings of the Ocean Drilling Program

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Drilling at Site 808 (ODP Leg 131) provided an extensive record of the discrete brittle structures (small faults and shear bands) at the toe of the Nankai accretionary complex. Brittle failure is occurring throughout the hole, although most of the deformation has been observed between the frontal thrust and the décollement (from 365 to 963 mbsf). Brittle failure occurs in the turbiditic trench fill (0 to 600 mbsf) but also in the ash-bearing hemipelagites from the upper Shikoku Basin (600 to 800 mbsf) and the ash-free hemipelagites of the lower Shikoku Basin sequences, down to the décollement (963 mbsf). The geometry of the tectonic features has been recorded in a local frame related to the core liner and then corrected to an absolute frame by the use of paleomagnetic measurements. We used the resulting geometry of homogeneous populations of slickenlined faults to estimate the reduced stress tensor. The main result is to show three consistent stress patterns. Most of the fault clusters from the frontal thrust down to the décollement are in good agreement with a compressional regime with a northwest-trending σj (azimuth N305° to N315 °). The compression direction is thus roughly parallel to the local direction of the relative convergence. It is also perpendicular to the trend of the anticlinal ridges. Discrete faults, locally appearing as clusters (e.g., 30 m above the décollement) agree with a quite different compression direction (west-southwest-east-northeast) and are restricted to the hemipelagic sequences above the décollement. They could be related to the heterogeneous internal deformation of this layer. Although isolated normal faults exist, their occurrence as clusters is restricted to the Shikoku Basin hemipelagic sequences and indicate a east-west to northwest-southeast extension axis (σ 3 ). Finally, the analysis of Mohr diagrams related to the best-fitting tensors shows some similarities and differences between the fault populations of the turbidite and those of the hemipelagite sequences. The angle of friction corresponding to 95% of the data is 30° ± 5°, whereas including the remaining 5% in turbidites and hemipelagites would result in a lower friction angle (18° ± 8°). The major difference concerns the angle between conjugate sets which are about 60° in the turbidites and lower (35°-40°) in a 200 m thick zone above the décollement and can be explained by higher fluid pressure in the hemipelagites or by odd mechanical properties of this hemipelagic material.

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“…Las primeras estructuras se han representado en estereogramas (falsilla de Schmidt, hemisferio inferior), realizando en algunos casos diagramas de densidad. En el análisis poblacional de fallas se han utilizado los métodos de Diedros Rectos (Arthaud y Choukroune, 1972), Etchecopar (Etchecopar et al, 1981) Y Diagrama y-R (Simón, 1986). El empleo combinado de estos tres métodos ha sido descrito y discutido por Casas et al (1990).…”

Section: Objetivos Y Metodologíaunclassified

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Carrera¹,

Gómez²

1994

Estud. geol.

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RESUMENEl análisis de la deformación tectónica frágil a distintas escalas en un sector de la Cordillera Ibérica oriental ha permitido definir el patrón de fracturación, caracterizado por tres familias principales de fracturas (NNE a NE, ENE YE a ESE). Las estructuras frágiles (estilolitos, juntas de extensión, zonas de cizalla semifrágil y, fundamentalmente, fallas) registran una tectónica alpina polifásica. Del análisis poblacional de las microfal1as se infieren dos campos de esfuerzos compresivos, principalmente en régimen de desgarre, de los cuales sólo el primero tiene reflejo a nivel macroestructural, y un estado distensivo en ré-gimen de extensión radial o multidireccional. Las relaciones de corte observadas entre las ditintas estructuras ha mostrado la evolución temporal siguiente: 1) compresión ENE; 2) compresión ESE y 3) distensión NNE tendente a radial.El estudio de la fracturación mediante distintas metodologías adaptadas a la escala macro, meso y microestructural ha permitido establecer nexos de relación entre los resultados de todas ellas y poner de relieve la influencia que las estructuras mayores tienen en aquellas de menor rango. Así, la cartografía detallada de fracturas (fundamentalmente a escala mesoestructural) ha permitido observar variaciones en la distribución y orientación de las mismas. Tales variaciones han sido interpretadas como fenómenos de perturbación de esfuerzos por estructuras mayores que, en la mayoría de los casos, han podido ser identificadas. Se han estudiado ejemplos de estas perturbaciones en relación con familias de fallas tanto de desgarre como de componente normal.Palabras clave: falla, campo de esfuerzos, tectónica alpina, Cordillera Ibérica. ABSTRACTThe analysis of the brittle tectonic deformation on all scales in one area of the eastern Iberian Chain (Mosqueruela, Teruel) allows us to define a fracture pattern characterized by three main sets: NNE to NE, ENE and E to ESE. Brittle structures (stylolites, tension gashes, brittle-ductile shear zones and faults) show a poliphase Alpine tectonics. From the analysis of fault populations two compressive (wrench regime) phases and a multidirectional extension regime have been inferred. Their chronological evolution is the fol1owing: 1) ENE compression; 2) ESE compression; 3) nearly multidirectional NNE extension.The study of fractures using a number of methodologies at macro-, meso-and microstructural scales allows us to suggest a model of stress distribution and relationships between different structures in sorne areas. The detailed fracture mapping on a hectometric scale shows the distribution and strike variations of fractures. These changes have been interpreted as stress deflection phenomena due to major structures which, in many cases, were identified. Examples of stress deflections have been analyzed both for strike-slip and normal fault sets.

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An inverse problem in microtectonics for the determination of stress tensors from fault striation analysis

Cited by 602 publications

References 7 publications

A Miocene onset of the modern extensional regime in the Isparta Angle: constraints from the Yalvaç Basin (southwest Turkey)

A Miocene onset of the modern extensional regime in the Isparta Angle: constraints from the Yalvaç Basin (southwest Turkey)

Stress Tensors at the Toe of the Nankai Accretionary Prism: An Application of Inverse Methods to Slickenlined Faults

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