The relationship between the magnetic and strain fabrics of some haematite-bearing Welsh slates
Reference (5)
Current views on the development of slaty cleavage
Anisotropy of susceptibility and the natural remanent magnetization of some Welsh slates
Nature (London)
(1960)
Cited by (46)
Deformation of the colliding Luzon volcanic arc: Strain analysis using magnetic fabrics of syn-orogenic mudstones in the Coastal Range, eastern Taiwan
2022, TectonophysicsCitation Excerpt :As a result, the magnetic fabric in the deformed state is composite, as a function of the magnetic fabric in the undeformed state and the tectonic deformation. This function is approximated by existing emprical correlations between magnetic fabric and finite strain (e.g., Kneen, 1976; Wood et al., 1976; Hrouda, 1979; Rathore, 1979; Kligfield et al., 1983; Cogné and Perroud, 1988; Nakamura and Borradaile, 2001; Weil and Yonkee, 2009). Use can be made of the correlations to estimate tectonic strain from the deformed magnetic fabric with the knowledge about the fabric in the undeformed state.
Inversion tectonics and magnetic fabrics in Mesozoic basins of the Western Tethys: A review
2018, TectonophysicsCitation Excerpt :AMS has targeted, with different degree of success, the characterization of multiple geological problems: emplacement of igneous bodies (e.g. Gleizes et al., 1993; Román-Berdiel et al., 1995; Bouchez, 1997, 2000; Aranguren, 1997; Auréjac et al., 2004; Antolín-Tomás et al., 2009; Kratinová et al., 2010; Izquierdo-Llavall et al., 2012; Cañón-Tapia and Mendoza-Borunda, 2014), deformation of rocks under different P-T conditions (e.g. Parés et al., 1999; Gil-Imaz et al., 2000; Hirt et al., 2000; Robion et al., 2007; Oliva-Urcia et al., 2009; Pueyo Anchuela et al., 2012), basin evolution (Mattei et al., 1997, 1999; Cifelli et al., 2005), fold geometry and internal deformation (e.g. Aubourg et al., 1999), estimation of shallowing effect in sedimentary rocks sampled for paleomagnetic purposes (see Li and Kodama, 2016), fault rocks at shallow crustal levels (Solum and van der Pluijm, 2009; Casas-Sainz et al., 2017, 2018), paleocurrents orientation in sedimentary contexts (e.g. Rees, 1965; Hamilton and Rees, 1970; Tarling and Hrouda, 1993; Piper et al., 1996; Pueyo Anchuela et al., 2013 and references therein), etc. Multiple studies have found empirical relationships between the orientations of the magnetic and strain ellipsoids (e.g. Kneen, 1976; Wood and Gibson, 1976; Kligfield et al., 1977; Rathore, 1979; Kligfield et al., 1982; Rathore and Henry, 1982; Lüneburg et al., 1999) although their magnitudes are more complexly related and empirical relationships for different lithologies has yet to be established (Kligfield, 1981; Borradaile, 1987, 1988; Hirt et al., 1988; Borradaile, 1991; Lüneburg et al., 1999; Oliva-Urcia et al., 2010b). In this sense, a number of studies about the interpretation of magnetic fabrics include correlations with magnetic and non-magnetic analyses that provide information about the minerals and their orientation distribution.
Interpreting magnetic fabrics in amphibole-bearing rocks
2018, TectonophysicsHanging wall deformation of a seismogenic megasplay fault in an accretionary prism: The nobeoka thrust in southwestern japan
2013, Journal of Structural GeologyCitation Excerpt :The occurrence of composite fabrics, characterized by the development of fabrics in two different orientations, might represent a lithological control on deformation, which differs between the thin sandstone and shale layers with a minor shear component, as suggested by Raimbourg et al. (2009). Anisotropy of magnetic susceptibility (AMS) enables the identification of the spatial arrangement of minute magnetic particles in rocks, and is used to quantify the strain that a deformed rock underwent during deformation (Kneen, 1976; Borradaile and Alford, 1988). AMS analysis was carried out to estimate the cumulative strain in phyllites within the hanging wall close to the Nobeoka Thrust plane.
Relationships between pore space anisotropy and anisotropy of physical properties of silicoclastic rocks from the Corbières-Minervois fold-and-thrust-belt (north-east Pyrenees, France)
2012, TectonophysicsCitation Excerpt :The characterization of the distribution of deformation in folds and thrust belts is frequently done through the study of magnetic fabric in general and anisotropy of magnetic susceptibility (AMS) in particular (Amrouch et al., 2010; Anchuela et al., 2010; Burmeister et al., 2009; Callot et al., 2010; Evans et al., 2003; Hirt et al., 2004; Larrasoana et al., 2011; Lee and Angelier, 2000; Luo et al., 2009; Pares et al., 1999; Pueyo-Morer et al., 1997; Robion et al., 2007; Sans et al., 2003; Tavani and Cifelli, 2010; Weil and Yonkee, 2009). This method can quickly measure the petrofabric of rocks by producing a magnetic susceptibility tensor coaxial to the strain tensor (Kliegfield et al., 1981; Kneen, 1976). It is useful in fold and thrust belts or, more generally, in structural domains poor in strain markers because it provides information about subtle fabrics unreachable through the observation of meso-structures alone (Bakhtari et al., 1998; Saint-Bezar et al., 2002).
Dynamic role of tectonic mélange during interseismic process of plate boundary mega earthquakes
2012, TectonophysicsCitation Excerpt :Except for the rarely found deformed radiolarian fossils (Kimura and Mukai, 1991), a quantitative strain analysis of shale-dominant mélange is generally difficult to perform due to the lack of appropriate strain markers. Anisotropy of Magnetic Susceptibility (AMS) provides the spatial arrangement of minute magnetic particles in the rock and is used to quantify the strain of deformed rocks (Kneen, 1976). This method is expedient and non-destructive for both consolidated and unconsolidated samples.