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When rainfall trapped in fluid inclusion restores the relief of an orogen: Insights from the Cenozoic Himalayas
2023, Earth and Planetary Science LettersSuperimposed structures, incremental strain and deformation path from field data to modelling: A case study from the Alpi Apuane metamorphic core complex (NW Tuscany, Italy).
2022, Journal of Structural GeologyCitation Excerpt :The deformation path recorded in our analyzed strain fringe system may be used to discuss relationships between local and regional scale structural architecture and tectonic models proposed. The geometrical relationships between Sp foliation and the internal structures and contacts within the overlying nappes and thrust sheets have been used since the end of ‘70s (Carmignani et al., 1978; Kligfield, 1979) to support an interpretation of a D1 deformation that occurred during low-angle shearing (Mattauer, 1975; Ramsay, 1980b; Mattauer et al., 1981; Coward, 1994; Williams and Jiang, 2015) in conditions of general shear (Kligfield et al., 1981; Molli and Vaselli, 2006). This frame can be also applied to our investigated area and supported by our studied FS1, which shows a rotational deformation with a local shear strain (γ) of around 4 associated with the development of the composite Sp foliation and related non-cylindric isoclinal folds.
Mountain Building: From Earthquakes to Geologic Deformation
2015, Treatise on Geophysics: Second EditionGeometry and kinematics of the late Proterozoic Angavo Shear Zone, Central Madagascar: Implications for Gondwana Assembly
2013, TectonophysicsCitation Excerpt :The D2 event is strongly preserved in this area. F2 axial planes are parallel to the foliation (Figs. 5G, 6C) and F2 fold axes are in many places parallel to the L2 stretching lineation, they are probably a-type folds (Kelly et al., 2000; Malavieille, 1987; Mattauer, 1975; Mattauer et al., 1983; Wang et al., 2005) formed during west over east dextral oblique D2 shearing. In this part of the ASZ, the D2 west over east dextral oblique shearing is prominent at the outcrop scale and the S2 foliation strikes N–S almost parallel to S1 (Fig. 3).
Structural records of the Late Cretaceous-Cenozoic extension in Eastern China and the kinematics of the Southern Tan-Lu and Qinling Fault Zone (Anhui and Shaanxi provinces, PR China)
2013, TectonophysicsCitation Excerpt :With the same geodynamic conditions, the kinematics of the faults are well explained by reactivation of pre-existing major discontinuities in a fractured body of rocks submitted to a regional NNW–SSE extension (Fig. 12A); particularly, it accounts for the dextral transtensional component on the NNE–SSW striking normal faults of the Shanxi graben and of STLFZ. It is proposed that the maximum horizontal compression (σHmax) trends NNE–SSW in Southern Tibet where extension, due to the weight of the topography, trends ≈ WNW–ESE (Mercier et al., 1987; Tapponnier et al., 1981); northward, the compressional trajectory progressively curves toward the east (Mattauer and Mercier, 1980; Tapponnier et al., 1981; Wan, 2011; Xu, 1993a, 1993b, 1993c; Xu et al., 1992); it trends ≈ NE–SW in Northern Tibet where tectonics are compressional (σHmax = σ1) and in Eastern China where tectonics are extensional (σHmax = σ2); around the Ordos, extension may have been favoured by the effects of high topography (He et al., 2004) (Fig. 14F). From the analysis of SPOT images, we had estimated the sinistral slip-rate on the QLFZ at 7 ± 2 mm yr −1 during the Holocene–Mid.
Evolution of the Murphy synclinorium, southern Appalachian Blue Ridge, USA
2012, Journal of Structural GeologyCitation Excerpt :The strain data from the northern segment of the synclinorium, and those from the palinspastically rotated central and southern segments (Fig. 5), indicate regional northwest-southeast shortening (flattening) perpendicular to the axial surface, accommodated by orthogonal shallowly plunging (<20°) extension sub-parallel to the regional fold axes and mesoscopic lineations, i.e., lateral, sub-horizontal north northeast-south southwest extension (Figs. 3 and 5). Such parallelism between fold axes and stretching lineations (lineations parallel to the X-axis of the strain ellipsoid) has been noted as a common feature in parts of many orogenic belts (Cloos, 1946; Flinn, 1962; Milnes, 1968; Bryant and Reed, 1969; Borradaile, 1972; Escher and Watterson, 1974; Mattauer, 1975; Bell, 1978; Malavieille, 1987; Froitzheim, 1992; Grujic and Mancktelow, 1995), and this parallelism can result from several different deformational mechanisms (Carosi and Montomoli, 1999). Perhaps the most common explanation for extension-parallel folds is either 2-D or 3-D bulk compressional or transpressional crustal shortening resulting from regional-scale plate convergence, coupled with sub-horizontal crustal extension (Blake et al., 1981; Sanderson and Marchini, 1984; Mancktelow, 1992; Chauvet and Sérrane, 1994; Mattauer et al., 1996; Hartz and Andresen, 1997).