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Estimation of virgin state of stress and determination of final rock stress model
Published in Katsuhiko Sugawara, Yuzo Obara, Akira Sato, Rock Stress, 2020
Further, since rock masses are rarely homogeneous, isotropic and continuous, stresses are also expected to vary spatially in the rock mass. An obvious situation in which stresses are discontinuous is at contacts between rock masses of different lithology and where rocks are intersected by several sets of joints, faults and other structural features. Stresses not only vary in space but also with time. Geological processes like erosion, sedimentation, mountain building and other tectonic events act over millions of years. The stress related to each of the processes will adjust in space and time or continue to change with time in order to maintain equilibrium of the system.
Geomorphic mapping and analysis of neotectonic structures in the piedmont alluvial zone of Haryana state, NW-India: a remote-sensing and GPR based approach
Published in Geomatics, Natural Hazards and Risk, 2023
Harsh Kumar, R. S. Chatterjee, R. C. Patel, Abhishek Rawat, Somalin Nath
The rise of the Himalayan mountain belt is result of the collision of the Indian tectonic plate with Eurasia. The Indian plate has been under thrusting beneath Eurasia since the closing of the Tethys Sea in the early Tertiary, and the mountain-building deformation front has moved southward from the initial collision contact at the Indus-Tsangpo Suture Zone (ITSZ) by processes that transfer Indian crust to the overriding plate. The deformational front gradually shifted along the Main Central Thrust (MCT), Main Boundary Thrust (MBT) and at present it is along the Himalayan Frontal Thrust (HFT) and its surrounding region (Joshi and Patel 1997; Valdiya 2001; Champel et al. 2002; Patel and Kumar 2003; Pant and Paul 2007; Roy and Mondal 2012; Goswami and Deopa 2013). The active HFT marks the present day physiographic and tectonic boundary between the Himalayan mountain belt and the Indo-Gangetic plains (Thakur et al. 2010). It is postulated that the active deformation is propagating further south of the HFT to the 10–50 km wide piedmont zone of the Indo-Gangetic alluvial plains (Shukla and Bora 2003; Yeats and Thakur 2008).
A tectonic reconstruction model for Aotearoa-New Zealand from the mid-Late Cretaceous to the present day
Published in New Zealand Journal of Geology and Geophysics, 2023
Hannu Seebeck, Dominic P. Strogen, Andrew Nicol, Benjamin R. Hines, Kyle J. Bland
Plate tectonic reconstructions are key for understanding the evolution of plate boundary zones by providing a spatial and temporal context for geological and geophysical observations. Plate tectonic reconstructions help constrain the timing and mechanisms of subduction and continental break-up, the relationships between crustal and mantle processes, and provides the context for paleo-environmental interpretation along with the underlying mechanisms associated with plate boundary deformation, mountain building and basin formation (e.g. Seton et al. 2012; Reyners 2013; Müller et al. 2019; Hines et al. 2022; Strogen et al. 2022). In the Southwest Pacific, the continent of Zealandia has experienced a complex tectonic history since the Late Cretaceous, including the break-up of Gondwana, subduction initiation and reactivation, and formation of the Alpine Fault transform between the Australian and Pacific plates (King 2000; Sutherland et al. 2000; Schellart et al. 2006; Herzer et al. 2011; Lamb 2011; Bache et al. 2014; Matthews et al. 2015; Mortimer et al. 2017; Strogen et al. 2017; Sutherland et al. 2017). As a result of this deformation the lithosphere of Aotearoa-New Zealand (A-NZ) has accommodated significant strain since its formation.
Crustal evolution events in the Chinese continent: evidence from a zircon U-Pb database
Published in International Journal of Digital Earth, 2020
Yujing Wu, Xianjun Fang, Sisi Liao, Lizhi Xue, Zhe Chen, Jiangnan Yang, Yamin Lu, Kun Ling, Shengyi Hu, Shuyuan Kong, Yiwei Xiong, Huacheng Li, Xiuqi Shang, Rui Ji, Xueyun Lu, Biao Song, Lei Zhang, Jianqing Ji
Second-order zircon growth peaks (II): the duration of zircon growth is relatively short, i.e. the vertical axis intercept of the classification is smaller than 20 Ma. Such peaks are probably caused by short-term tectonic or climate events, including the Wutai orogeny, Caledonian orogeny, and a series of events around the Lvliang orogeny and Indosinian orogeny. The growth of the earth's crust results from the combination of internal and external dynamic. During the orogenic process, climatic factor could induce crustal decompression and metamorphism, with the growth of zircon. In the past 20 years, researches on young active orogeny, especially Himalayan orogeny, indicate that the dynamics of subduction and mountain-building can be controlled by the processes of erosion, and ultimately climate (Beaumont et al. 2001; Zeitler et al. 2001; Lamb and Davis 2003; Yu et al. 2011; Tu et al. 2015).