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Xiujin Liu, Wei Liu. Re-Os Dating of the Suoerkuduke Cu (Mo) Deposit, Fuyun County, Xinjiang, and its Geodynamic Implications. Journal of Earth Science, 2013, 24(2): 188-202. doi: 10.1007/s12583-013-0322-5
Citation: Shenqiang Chen, Hanlin Chen. Late Cenozoic Activity of the Tashkurgan Normal Fault and Implications for the Origin of the Kongur Shan Extensional System, Eastern Pamir. Journal of Earth Science, 2020, 31(4): 723-734. doi: 10.1007/s12583-020-1282-1

Late Cenozoic Activity of the Tashkurgan Normal Fault and Implications for the Origin of the Kongur Shan Extensional System, Eastern Pamir

doi: 10.1007/s12583-020-1282-1
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  • Corresponding author: Shenqiang Chen, ORCID:0000-0002-2265-6313, shenqiang.chen@erdw.ethz.ch
  • Received Date: 26 Aug 2019
  • Accepted Date: 28 Nov 2019
  • Publish Date: 24 Aug 2020
  • In the northwest of the Himalayan-Tibetan Orogen, the ~250 km-long Kongur Shan extensional system in the eastern Pamir was formed during the convergence between the Indian and Asian plates. Tectonic activity of the Kongur Shan normal fault and the Tashkurgan normal fault can help to reveal the origin of east-west extension along the Kongur Shan extensional system. The Kongur Shan fault has been extensively studied, while the Tashkurgan fault calls for systemic research. In this study, low-temperature thermochronology including apatite fission track analysis and apatite and zircon (U-Th)/He analyses is applied to constrain the timing of activity of the Tashkurgan fault. Results indicate that the Tashkurgan fault initiated at 10-5 Ma, and most likely at 6-5 Ma. The footwall of the Tashkurgan fault has been exhumed at an average exhumation rate of 0.6-0.9 mm/a since the initiation of the Tashkurgan fault. Combined with previous research on the Kongur Shan fault, we believe that the origin of east-west extension along the Kongur Shan extensional system was driven by gravitational collapse of over-thickened Pamir crust.

     

  • In the forthcoming years, modelling of hydraulic fracture and flow of fluid and heat in fragmented material will play a vital role in the exploitation of geothermal energy. The deep geothermal energy extraction process involves drilling deep boreholes into hot rocks and injecting water under high pressure which decreases the effective friction on closed (impermeable) inter-meshing joint surfaces, causing them to "fracture" and slip in response to the existing tectonic pre-stress of the region. The fracture and slip of these joints creates high permeability pathways for fluid flow. The thermal energy trapped in the rocks within this region can then be extracted by circulating water between the injection and production wells through this permeable fracture system. Due to the high expense of drilling and inability to access underground wells, there are huge risks and uncertainties associated with this process. One of the challenges in geothermal energy extraction is how to stimulate and sustain the flow of water through the geothermal field and how to generate an efficient hydraulic subsurface heat exchange (fracture) system.

    A fully developed thermo-hydro-mechanical coupling model and code which includes the most important physical mechanisms would provide means to study the phenomena and meet this challenge with minimal cost and risk.

    Many approaches have been proposed for simulating fragmentation of solids using continuum methodology. While continuum based models can simulate discontinuities to an extent either replacing the discontinuities with material of a different rheology, or through special treatments of the discontinuity nodes, they cannot be used to study emergent behavior and probe the evolution of fracture systems which is a consequence of microscopic processes. Particle based models such as the discrete element method (DEM) and lattice solid model (LSM) naturally overcome such difficulties since displacements and detachment of solid fragments can be simulated.

    When modeling fluid flow, the classical continuum approach is based on the numerical solution of Navier-Stokes (N-S) equations (i.e., computational fluid dynamics). As in the case of solids, in addition to the continuum approach based on numerical solution of the N-S equations, there are also other microscopic and mesoscopic approaches, such as the molecular dynamics (MD) method, the lattice Boltzmann method (LBM), and the smoothed particle hydrodynamics (SPH) method (Gingold and Monaghan, 1977). The LBM method is based on kinetic gas theory and simulates fluid flows by tracking the evolution of the single fluid particle distributions. The LBM is a semi-microscopic approach that models particle distributions rather than individual particles. Some advantages of LBM over the classical N-S approach include its ease in implementation and parallelization, and its ability to handle boundary conditions of complicated geometries (Chen and Doolen, 1998).

    This paper introduces the coupled LSM/LBM, a new fully microscopic model based on coupling the LSM with the LBM thereby allowing simulations including solid-fluid coupling, fracture, and thermal fluid flow, and hence, to investigate the creation, evolution and efficiency of geothermal reservoir fracture systems as emergent phenomena.

    We believe that the coupled LSM/LBM is a natural and elegant approach from a conceptual and physical point of view for simulating complicated solid-fluid systems aimed at studies of emergent behaviour than any approach which involves coupling microscopic and macroscopic methods for solid dynamics and fluid flow.

    An interesting alternative to the coupled LSM/LBM is the coupled LSM/SPH (Komoróczi et al., 2013). While it has less conceptual and physical appeal in our view due to involving a coupling between a microscopic and macroscopic method, it is attractive for other reasons such as ease of implementation of the SPH within the LSM by making use of the LSM particle implementation as a basis for SPH nodal points, and possibly greater computational efficiency for some physical problems (although this is speculation at this stage).

    The lattice solid model (LSM) was first developed by Peter Mora in 1992 at Institute de Physique du Globe (Mora and Place, 1993; Mora, 1992). The LSM was motivated by molecular dynamics principles with either particle interactions via Lennard-Jones potential functions or elastic-brittle bonds. The LSM shares similarities with the Discrete Element Mode (DEM) but involves a different computational approach that is based on the use of large-scale supercomputer simulation via domain decomposition and parallel programming. The model was initially developed to study fracture, friction, rock rheology, tectonic processes and earthquake dynamics (Mora and Place, 1994, 1993; Mora, 1992). As more physics was incorporated including heat flow, thermo-porous coupling, thermo-mechanical feedback, and additional degrees of freedom in 3D (tension, shear, torsion and bending) to ensure realistic fracturing behaviour, it became more powerful and was calibrated with laboratory experiments and used to study outstanding scientific research questions and the complex nonlinear behaviour of discontinuous solids including the heat flow paradox in geophysics (Place and Mora, 2000; Mora and Place, 1998). The LSM has since been developed as a parallel open-source C++ software system called ESyS_Particle. The initial team working on the LSM consisted of Peter Mora and David Place, but rapidly grew into a major particle research group at Earth Systems Science Computational Centre (ESSCC) that was directed by Peter Mora at the University of Queensland. Major contributors included Steffen Abe, Yucang Wang, Fernando Alonso-Marroquin, and Shane Latham, among others. The development of the ESyS-particle software infrastructure became funded by the Australian Computational Earth Systems Simulator Major National Research Facility (ACcESS MNRF) established by Peter Mora and a national group of solid earth systems simulation scientists. The ESyS-Particle software is available at: https://launchpad.net/esys-particle/ESyS-particle, which is a site maintained by Dion Weatherley with software developments contributed from around the world and by present and past ESSCC researchers.

    The initial particle simulation program of 1992 was written by Peter Mora in Connection Machine Fortran (CMF was a precursor to HPF and F90) at the IPG in Paris and was called LSMearth. David Place worked on an accurate way to simulate inter-particle friction (Place and Mora, 1999), and Peter Mora then added frictional heating and heat flow. Subsequently, Peter Mora, David Place and Steffen Abe added random particle sizes (Place and Mora, 2001), thermo-porous and thermo-mechanical coupling effects (Abe et al., 2000), and proposed an efficient scheme to model arbitrary shaped angular particles (Abe and Mora, 2003). LSMearth was redeveloped in C++ by David Place, and subsequently parallelised by Steffen Abe et al. (Abe et al., 2004) and Shane Latham et al. (Latham et al., 2005) using MPI into a highly efficient and usable tool, with various new micro-physics being added by a group of researchers and computational scientists under the direction of Peter Mora as part of the ACcESS MNRF. Around 20 researchers worldwide are currently contributing to ESyS-particle. Some of the most critical recent developments have been made by Yucang Wang and Fernando-Alonso Marroquin respectively to model the full set of degrees of freedom (six kinds of independent relative movements are transmitted between two 3-D interacting particles) needed to accurately simulate observed fracture patterns (Wang, 2009; Wang and Alonso-Marroquin, 2009; Wang and Mora, 2009, 2008b; Wang et al., 2006), and how to efficiently simulate complex particle shapes (Alonso-Marroquin and Wang, 2009; Alonso-Marroquin et al., 2007; Abe and Mora, 2003). One of the major advantages of the discrete (LSM) model over the continuum models is that the large deformation and dynamics process associated with fracture phenomena can be easily modelled. It has been successfully utilised to the study of physical process such as rock fracture (Wang and Alonso-Marroquin, 2009; Wang and Mora, 2008b; Place et al., 2002; Place and Mora, 2001; Mora and Place, 1993; Mora, 1992), the stick-slip frictional instability and earthquake dynamics (Mora and Place, 1999, 1993), the heat-flow paradox (Alonso-Marroquin et al., 2006; Mora and Place, 1999, 1998; Mora et al., 1997), accelerating acoustic emissions/energy release, load-unload-response-ratio and critical sensitivity prior to catastrophic failure and simulated earthquakes (Mora et al., 2002, 2000), earthquake physics and predictability (Mora and Place, 2002; Mora et al., 2000), localisation phenomena (Place and Mora, 2000; Mora and Place, 1999, 1998), fault gouge evolution (Mair and Abe, 2008; Alonso-Marroquin et al., 2007, 2006; Mora et al., 2000; Mora and Place, 1999) and comminution in shear cells (Mair and Abe, 2008).

    In order to simulate the creation, evolution, and long-term energy output of a deep geothermal reservoir system, one must be able to simulate complex nonlinear dynamical processes in complicated solid-fluid systems. An ideal simulation may involve first simulating the joint and fracture patterns in the region of interest by modelling the tectonic stress and thermal history of a region. Subsequently, one may simulate the drilling of boreholes into the rock, injection of water under high pressure, the ensuing hydraulic fracturing process, the subsequent long-term evolution of the fluid-flow pathways, and the overall energy output of the region before either the heat of the region is fully depleted, or no further energy can be produced due to blocking of flow pathways. Figure 1 depicts this simulation strategy.

    Figure  1.  Illustration of simulation based framework to study creation of fluid flow networks for viable deep geothermal energy. Upper left. creation of a pre-existing joint/fracture system via microscopic LS/LB simulation of tectonic stress and thermal history acting on a rock volume (left. real fracture systems; right. simulated fracture systems. The upper and lower images are at different scales). Upper right: Drilling, high pressure water injection, and hydraulic fracturing via microscopic LS/LB simulation. Lower left. microscopic LS/LB simulation to study the evolution of fractures and their effective permeability as they slip, grains rub off, fluids flow, and chemical processes occur over a long time scale. Lower right. macroscopic simulation to calculate the long-term energy output of the geothermal reservoir/fracture system predicted by the micro-scale simulation using the permeability evolution of fractures derived from micro-scale simulation (Xing and Mora, 2006).

    During the first stage of creating a fracture system, water is injected at the "injection wells" and this causes a decrease in the effective normal stress on the initially closed joint surfaces around these wells. This then allows these joints to slip and partially release the tectonic pre-stress in the region. This induced seismicity is used in the field to help map the fracture system which provides a pathway (or pathways) for fluid flow. However, it would be costly to vary the injection characteristics by trial and error in the field until a suitable fracture system with multiple fluid flow pathways could be developed. Multiple pathways are crucial for any given field to be fully produced, that is, to fully deplete the anomalously high heat for a given region such that the investment of the injection and production wells is has been fully covered and the field is economically viable.

    Simulations may provide a means to study how to vary injection characteristics such as depths and pressures, in order to create multiple fractures and hence, flow pathways between injection wells and production wells. However, such simulations would need to accurately simulate fracture and other emergent behavior in complicated solid-fluid models. Here, we propose use of the LSM for simulation of the solid dynamics due to its proven ability to accurately reproduce realistic fracture behavior as illustrated in the following sections.

    Figure 2 shows the 3D complex fracturing behaviour of a leftwards travelling impacting ball in a laboratory experiment (Khanal et al., 2008) compared to a numerical simulation using the LSM by Yucang Wang. Figure 3 shows a 3D simulation result of axial breakage compared to a laboratory experiment of axial breakage (see Wang and Alonso-Marroquin, 2009, 2008).

    Figure  2.  Laboratory result of an impacting ball by Khanal et al. (2008) (left) compared with numerical result using the LSM by Wang and Alonso-Marroquin (2008) (right).
    Figure  3.  Numerical simulation of axial breakage (top) compared to laboratory experiment (bottom).

    The additional examples shown in Fig. 4 of the simulation of the development of brittle fracture systems also exhibit a close match to the patterns observed in laboratory experiments (Wang and Mora, 2009, 2008b), and provides a further illustration that the lattice solid model and software system, ESyS-Particle, is capable of matching fracture patterns seen in laboratory experiments. Hence, implementation of the lattice solid model including thermo-porous flow, frictional heat generation and heat flow, thermo-mechanical coupling effects and realistic solid-fluid dynamics such as hydraulic fracturing, provides a unique platform for scientific breakthroughs on how to create and sustain the multiple fluid flow pathways required for proof of concept and development of the new geothermal green energy industry.

    Figure  4.  Brittle failure experiments—laboratory result versus simulation result.

    The accurate modelling of realistic fracturing behaviour that matches with experimental laboratory data was only possible by including rotational dynamics as new degrees of freedom (see Fig. 5). Details of the contact model are provided in the literature (Wang, 2009; Wang and Mora, 2009, 2008b).

    Figure  5.  The 6 degrees of freedom for 3D particle interaction. Fr is force in radial direction, Fs1 and Fs2 are shear forces, Mt is twisting torque, and Mb1, Mb2 are bending torques.

    Elastic properties in regular lattices have been derived in these cases (Wang and Mora, 2008a). As a test of fracture behaviour, we have accurately reproduced "wing cracks" (see Fig. 6) that are observed in the laboratory (Wang and Mora, 2008b). ESyS-Particle has unique capabilities to model such wing cracks as all six degrees of freedom per particle are modelled to include contact forces, bending and twisting moments (Wang, 2009; Wang and Mora, 2009). The 2D example of wing cracks to the right is from Wang and Mora (2008b).

    Figure  6.  Simulation of wing cracks.

    To model dynamics of fluids in the cracks and pore space, we use the thermal energy distribution type BGK thermal lattice Boltzmann method (Hung and Yang, 2011; Guo et al., 2007; He et al., 1998) which has been shown to yield the Navier-Stokes equations for fluid flow combined with heat flow. Namely, in one time step Δt, the mass density of particles moving in the α-direction of a regular lattice moving with velocity cα denoted fα is updated as

    fα(x,t+Δt)=fα(xΔxα,t)+ΔfCα(x,t+Δt)/τf (1)

    where the first term on the right denotes the streaming of particles moving one lattice spacing Δxα in the α-direction in one time step, and the second term on the right denotes the redistribution of mass density flow due to collisions where τf is the dimensionless relaxation time constant for the collision term which is related to kinematic viscosity via νf=(τf0.5)c2sΔt where cs is the speed of sound in the fluid. The collision term is calculated using

    Δfac=feqafa (2)

    where Δfcα is the velocity change due to collision, fαeq is the equilibrium distribution expressed in Eq. 3. In this work, we model the D2Q9 BGK model (the two-dimensional, nine speeds Bhatnagar-Gross-Krook model) so the particle distributions travel with speeds of cα=0 (α=0), cαxt (α=1, 2, 3, 4) particles moving in the ±x and ±y directions and cα=2Δx/Δt (α=5, 6, 7, 8) for particles travelling in the diagonal directions. The equilibrium distribution is calculated using

    feqα=ρwα[1+3cαu+92(cαu)232uu] (3)

    where the equilibrium distribution weights are wα=(49,19,19,19,19,136,136136136), ρ is density, u is the macroscopic velocity of the fluid. For this case, the RMS velocity, and hence, the speed of sound in the fluid is cs=13. The macroscopic density and momentum are calculated using ρ=αfα and ρu=αfαcα. In the thermal lattice Boltzmann method, a second distribution gα is introduced which relates to kinetic energy within the fluid and hence the heat. This is also modeled in the two steps of streaming and collision

    gα(x,t+Δt)=gα(xΔxα,t)+ΔgCα(x,t+Δt)/τg (4)

    where collision term is ΔgCα=gαeqgα and the equilibrium distribution for gα is calculated using

    geqα=12ρ(cαu)2wα[1+3cαu+92(cαu)232uu] (5)

    The macroscopic internal kinetic energy and temperature are calculated using ρE=αgα and E=DRT/2 where D=2 is the number of dimensions, R is the gas constant, and T is the temperature. In the above equations, the different relaxation time τg allows the thermal diffusivity of the fluid to be controlled.

    To implement mechanical coupling between the LSM and LBM, the following issues need to be considered: moving boundary conditions for a curved solid-fluid interface; momentum transfer between solid particles and the fluid; and force transfer between fluid nodes and solid particles. Here Yu's moving boundary condition is adopted (Yu et al., 2003). The lattice node on the fluid side of the boundary is denoted as xf and that on the solid side is denoted as xb (see Fig. 7). The particle momentum moving from xf to xb is eα and the revised momentum from xb to xf is e˜α=eα. Here, xw denotes the intersection of the wall with the lattice link. Due to the arbitrary position of the particles and the curved particle surface, the particle surface can intersect the link between two nodes at an arbitrary distance.

    Figure  7.  The moving curved wall boundary condition.

    To accurately capture the position of the particle surface, the fraction of an intersected link in the fluid region can be computed as (Fig. 6)

    δ=|xfxw||xfxb|[0,1] (6)

    The reflected distribution function at nodes can be calculated using an interpolation scheme

    f˜α(xf,t+Δt)=11+δ[(1δ)fα(xf,t+Δt)+δfα(xb,t+Δt)+δf˜α(xf2,t+Δt)6wαρweαuw/c2] (7)

    The fluid force acting on the particle surface can be obtained using

    fF=xb9α=1eα[fα(xb,t)+f˜α(xf,t+Δt)]Δx/Δt (8)

    where the first summation is taken over all fluid nodes at xb adjacent to the particle, and the second is taken over all possible lattice directions pointing towards a particle cell. This force is added to the particle force in LSM code.

    The thermal coupling between the lattice solid model and lattice Boltzmann method has the same issues as the mechanical coupling and can be achieved in the same way. However, because the thermal diffusion time scale is longer than the time scale of solid and fluid dynamical processes (e.g., fracture etc.—solid; turbulence etc.—fluid), it is less sensitive to the precision of the implementation. On the other hand, the thermal LBM can become unstable and care must be taken in the implementation, particularly when the fluid is undergoing rapid dynamical interaction with a solid and hence, may be far from equilibrium during such processes. We have implemented heat transfer within the Lattice Solid using the thermal LBM with a third distribution hα, and a different relaxation time τh which allows the solid to have a different thermal diffusivity than the fluid. This approach of modeling the heat flow in the moving lattice solid fragments (groups of bonded particles) consistently with the LBM leads to a stable approach for modeling heat in the solid-fluid system with the advantage of yielding relatively homogeneous numerical precision for the heat flow calculations within both solid and fluid regions (c.f., more heterogeneous precision had different methods been used for heat flow calculations within solid and fluid regions).

    We use the thermal-energy-distribution type BGK thermal lattice Boltzmann method that has been shown to yield the NS equations for fluid flow combined with heat flow. Key issues of the LSM-LBM coupling: moving boundary conditions for a curved solid-fluid interface; momentum transfer between solid particles and the fluid; and force transfer between fluid nodes and solid particles. Moving boundary condition is adopted. Verification of the model has been achieved using simulation of particles in fluids, see Fig. 8. The example simulates dragging of particles by the fluids, convective and diffusive heat flow, and turbulent flow for high Reynolds numbers where particle surfaces act as boundary conditions.

    Figure  8.  Snapshots of a coupled LSM-LBM simulation of initially hot particles in a cold fluid moving to the right through a channel. The colours represent temperature (left) and velocity (right). The dots within the flow are tracer particles to assist visualisation of the flow field. The edge of the circular particles are coloured dark blue on the left plot to assist in visualising the locations of the particles in the temperature field.

    Figure 9 shows a 2D simulation of hydraulic fracturing. In this test, rock is modeled as 1 026 bonded LSM particles with a hole in the middle representing a borehole in which pressurized water is injected. Particle sizes are variable and range from 0.1 to 1 units. Water is simulated using the LBM. The minimum particle size is 2 times of the LBM grid size of the fluid. Fluid pressure in the centre of the hole is increased slowly to model the injection of water. The pressure increase is modelled by addition of a source term on the right-hand side of the standard LBM scheme. The cracks start from the surface of the borehole and propagate inside the rock due to the pressure of the fluid. Tensile fractures are dominant in the beginning of the crack initiation. Our simulations include most of the mechanisms of the hydraulic fracturing process: (i) mechanical deformation and fracturing induced by the fluid pressure; (ii) flow of fluid within the fracture that was generated; and (iii) fracture propagation.

    Figure  9.  From top to bottom: snapshots of hydraulic fracture; fracturing event distribution, with blue for tensile fractures and red for shear fracture; velocity vector field of fluid flow during hydraulic fracturing; and fluid pressure during hydraulic fracturing (in this case dark green means higher fluid pressure).

    We digitised a 2D porous sandstone to generate the lattice representing the rock. The digitised grains were shrunk to generate permeability that would be present in 3D, and were then initialised with a uniform high temperature. Space between grains was filled with a cold fluid with a velocity u=(0.1cs, 0). Left and right boundary conditions imposed continued flow to the right and upper and lower boundaries were non-slip. Figure 10 depicts a snapshot of the temperature and velocity fields at t=700 time-steps of a simulation. The results illustrate the ability of the coupled lattice solid/lattice Boltzmann model to simulate the combined fluid/heat flow within a complex solid-fluid system.

    Figure  10.  Temperature T (left) and fluid velocity magnitude |u| (right) at t=700 time steps in a simulation of an initially cold fluid with high thermal diffusivity, through a hot solid porous and permeable 2D sandstone matrix with low thermal diffusivity. Colours are red=hot/fast, blue=cold/slow. Lines are tracer particles that started as vertical columns. These allow fluid flow to be visualised simultaneously with temperature.

    The lattice solid model particle based method has the ability to provide breakthroughs in the understanding of the mechanical properties of hot rocks, their efficient fracturing, and the ability to produce sustained fluid pathways through the induced fracture network. In situ measurements to assess the fracture of rocks require theoretical interpretation of the energy budget and fracture propagation. These theories can be incorporated into a continuum model by interconnecting the length scales of fragmentation. Here particle-based models can be used to extract data of fracture creation that are subsequently passed to the continuum models (i.e., using up-scaling). This ab-initio approach has the potential to exploit a model of large-scale fragmentation based on processes at the smallest scale which represents an independent source of data more closely related to the complexity of fragmentation.

    The examples shown in this paper illustrate the potential, when fully developed, of the coupled lattice solid/lattice Boltzmann model to simulate the creation, dynamics, evolution and energy yield of realistic deep geothermal reservoir systems as emergent phenomena. Additional physical processes that may need to be incorporated include chemical reactions and precipitation since these may affect the viability of flow pathways. Carefully controlled laboratory tests can be used to validate the model. Also, if the temperature data and seismicity data are obtained in the real bores, the model results can be compared to experiments. Triggered seismicity can be modeled, with the potential energy in the bonds corresponding to the seismic energy released, and Richter scale can be defined accordingly by analyzing the frequency of the events. If enough real seismic data are obtained, the simulation results can be used to compare with the real data. Currently the simulations presented in this paper are just qualitative and stay at rudimental stages. More detailed and comprehensive work need to be done to produce more reasonable/realistic results.

    Further development and application of the thermo- and hydro-mechanically coupled ESyS_Particle simulation software system will benefit geothermal exploitation, by delivering new multi-scale, numerical capabilities to model fracturing, heat flow, and solid-fluid coupling; and hence, to model the generation and sustainability of the hot-fractured rock geothermal energy fracture systems required to exploit this new green-energy resource. This may prove to be the key to realise sustainable green geothermal energy to contribute to power the world.

  • Angiolini, L., Zanchi, A., Zanchetta, S., et al., 2013. The Cimmerian Geopuzzle:New Data from South Pamir. Terra Nova, 25(5):352-360. https://doi.org/10.1111/ter.12042
    Arnaud, N. O., Brunel, M., Cantagrel, J. M., et al., 1993. High Cooling and Denudation Rates at Kongur Shan, Eastern Pamir (Xinjiang, China) Revealed by 40Ar/39Ar Alkali Feldspar Thermochronology. Tectonics, 12(6):1335-1346. https://doi.org/10.1029/93tc00767
    Bershaw, J., Garzione, C. N., Schoenbohm, L., et al., 2012. Cenozoic Evolution of the Pamir Plateau Based on Stratigraphy, Zircon Provenance, and Stable Isotopes of Foreland Basin Sediments at Oytag (Wuyitake) in the Tarim Basin (west China). Journal of Asian Earth Sciences, 44:136-148. https://doi.org/10.1016/j.jseaes.2011.04.020
    Brunel, M., Arnaud, N., Tapponnier, P., et al., 1994. Kongur Shan Normal Fault:Type Example of Mountain Building Assisted by Extension (Karakoram Fault, Eastern Pamir). Geology, 22(8):707-710. https://doi.org/10.1130/0091-7613(1994)022<0707:ksnfte>2.3.co; 2 doi: 10.1130/0091-7613(1994)022<0707:ksnfte>2.3.co;2
    Burtman, V. S., Molnar, P. H., 1993. Geological and Geophysical Evidence for Deep Subduction of Continental Crust beneath the Pamir. Geological Society of America Bulletin, 281:1-76. https://doi.org/10.1130/spe281-p1
    Cai, Z. H., Xu, Z. Q., Cao, H., et al., 2017. Miocene Exhumation of Northeast Pamir:Deformation and Geo/thermochronological Evidence from Western Muztaghata Shear zone and Kuke Ductile Shear Zone. Journal of Structural Geology, 102:130-146. https://doi.org/10.1016/j.jsg.2017.07.010
    Cao, K., Wang, G. C., van der Beek, P., et al., 2013a. Cenozoic Thermo-Tectonic Evolution of the Northeastern Pamir Revealed by Zircon and Apatite Fission-Track Thermochronology. Tectonophysics, 589:17-32. https://doi.org/10.1016/j.tecto.2012.12.038
    Cao, K., Bernet, M., Wang, G. C., et al., 2013b. Focused Pliocene-Quaternary Exhumation of the Eastern Pamir Domes, Western China. Earth and Planetary Science Letters, 363:16-26. https://doi.org/10.1016/j.epsl.2012.12.023
    Chapman, J. B., Scoggin, S. H., Kapp, P., et al., 2018. Mesozoic to Cenozoic Magmatic History of the Pamir. Earth and Planetary Science Letters, 482:181-192. https://doi.org/10.1016/j.epsl.2017.10.041
    Chen, X. W., Chen, H. L., Lin, X. B., et al., 2018. Arcuate Pamir in the Paleogene? Insights from a Review of Stratigraphy and Sedimentology of the Basin Fills in the Foreland of NE Chinese Pamir, Western Tarim Basin. Earth-Science Reviews, 180:1-16. https://doi.org/10.1016/j.earscirev.2018.03.003
    Cheng, X. G., Chen, H. L., Lin, X. B., et al., 2016. Deformation Geometry and Timing of TheWupoer Thrust Belt in the NE Pamir and Its Tectonic Implications. Frontiers of Earth Science, 10(4):751-760. https://doi.org/10.1007/s11707-016-0606-z
    Cowgill, E., 2010. Cenozoic Right-Slip Faulting along the Eastern Margin of the Pamir Salient, Northwestern China. Geological Society of America Bulletin, 122(1/2):145-161. https://doi.org/10.1130/b26520.1
    Farley, K. A., 2000. Helium Diffusion from Apatite:General Behavior as Illustrated by Durango Fluorapatite. Journal of Geophysical Research:Solid Earth, 105(B2):2903-2914. https://doi.org/10.1029/1999jb900348
    Flowers, R. M., Ketcham, R. A., Shuster, D. L., et al., 2009. Apatite (U-Th)/He Thermochronometry Using a Radiation Damage Accumulation and Annealing Model. Geochimica et Cosmochimica Acta, 73(8):2347-2365. https://doi.org/10.1016/j.gca.2009.01.015
    Galbraith, R. F., 1981. On Statistical Models for Fission Track Counts:Reply. Journal of the International Association for Mathematical Geology, 13(6):485-488. https://doi.org/10.1007/bf01034500
    Guenthner, W. R., Reiners, P. W., Ketcham, R. A., et al., 2013. Helium Diffusion in Natural Zircon:Radiation Damage, Anisotropy, and the Interpretation of Zircon (U-Th)/He Thermochronology. American Journal of Science, 313(3):145-198. https://doi.org/10.2475/03.2013.01
    Hacker, B. R., Ratschbacher, L., Rutte, D., et al., 2017. Building the Pamir-Tibet Plateau-Crustal Stacking, Extensional Collapse, and Lateral Extrusion in the Pamir:3. Thermobarometry and Petrochronology of Deep Asian Crust. Tectonics, 36(9):1743-1766. https://doi.org/10.1002/2017tc004488
    Hurford, A. J., Green, P. F., 1983. The Zeta Age Calibration of Fission-Track Dating. Chemical Geology, 41:285-317. https://doi.org/10.1016/s0009-2541(83)80026-6
    Imrecke, D. B., ,., Robinson, A. C., et al., 2019. Mesozoic Evolution of the Eastern Pamir. Lithosphere, 11(4):560-580. https://doi.org/10.1130/l1017.1
    Jiang, Y. H., Liu, Z., Jia, R. Y., et al., 2012. Miocene Potassic Granite-Syenite Association in Western Tibetan Plateau:Implications for Shoshonitic and High Ba-Sr Granite Genesis. Lithos, 134/135:146-162. https://doi.org/10.1016/j.lithos.2011.12.012
    Jiang, Y. H., Liu, Z., Jia, R. Y., et al., 2013. Origin of Early Cretaceous High-K Calc-Alkaline Granitoids, Western Tibet:Implications for the Evolution of the Tethys in NW China. International Geology Review, 56(1):88-103. https://doi.org/10.1080/01431161.2013.819963
    Ke, S., Luo, Z., Mo, X., et al., 2008. The Geochronology of Taxkorgan Alkalic Complex, Pamir Syntax. Acta Petrologica Sinica, 24(2):315-324 (in Chinese with English Abstract) http://www.wanfangdata.com.cn/details/detail.do?_type=perio&id=ysxb98200802011
    Ketcham, R. A., Donelick, R. A., Carlson, W. D., 1999. Variability of Apatite Fission-Track Annealing Kinetics; Ⅲ, Extrapolation to Geological Time Scales. American Mineralogist, 84(9):1235-1255. https://doi.org/10.2138/am-1999-0903
    Ketcham, R. A., Gautheron, C., Tassan-Got, L., 2011. Accounting for Long Alpha-Particle Stopping Distances in (U-Th-Sm)/He Geochronology:Refinement of the Baseline Case. Geochimica et Cosmochimica Acta, 75(24):7779-7791. https://doi.org/10.1016/j.gca.2011.10.011
    Lee, J. K. W., Williams, I. S., Ellis, D. J., 1997. Pb, U and Th Diffusion in Natural Zircon. Nature, 390(6656):159-162. https://doi.org/10.1038/36554
    Liu, X., Fan, H. R., Evans, N. J., et al., 2014. Cooling and Exhumation of the Mid-Jurassic Porphyry Copper Systems in Dexing City, SE China:Insights from Geo-and Thermochronology. Mineralium Deposita, 49(7):809-819. https://doi.org/10.1007/s00126-014-0536-1
    Mechie, J., Yuan, X., Schurr, B., et al., 2012. Crustal and Uppermost Mantle Velocity Structure along a Profile Across the Pamir and Southern Tien Shan as Derived from Project TIPAGE Wide-Angle Seismic Data. Geophysical Journal International, 188(2):385-407. https://doi.org/10.1111/j.1365-246x.2011.05278.x
    Murphy, M. A., An, Y., Kapp, P., et al., 2000. Southward Propagation of the Karakoram Fault System, Southwest Tibet:Timing and Magnitude of Slip. Geology, 28(5):451. https://doi.org/10.1130/0091-7613(2000)28<451:spotkf>2.0.co; 2 doi: 10.1130/0091-7613(2000)28<451:spotkf>2.0.co;2
    Owen, L. A., Chen, J., Hedrick, K. A., et al., 2012. Quaternary Glaciation of the Tashkurgan Valley, Southeast Pamir. Quaternary Science Reviews, 47:56-72. https://doi.org/10.1016/j.quascirev.2012.04.027
    Reiners, P. W., Spell, T. L., Nicolescu, S., et al., 2004. Zircon (U-Th)/He Thermochronometry:He Diffusion and Comparisons with 40Ar/39Ar Dating. Geochimica et Cosmochimica Acta, 68(8):1857-1887. https://doi.org/10.1016/j.gca.2003.10.021
    Reiners, P. W., Brandon, M. T., 2006. Using Thermochronology to Understand Orogenic Erosion. Annual Review of Earth and Planetary Sciences, 34(1):419-466. https://doi.org/10.1146/annurev.earth. 34.031405.125202 doi: 10.1146/annurev.earth.34.031405.125202
    RGSRTK (Regional Geological Survey Report of the People's Republic of China, 2004. 1: 250 000 Tashkurgan County J43C003003. China Geological Survey (in Chinese)
    Robinson, A. C., Yin, A., Manning, C. E., et al., 2004. Tectonic Evolution of the Northeastern Pamir:Constraints from the Northern Portion of the Cenozoic Kongur Shan Extensional System, Western China. Geological Society of America Bulletin, 116(7/8):953-973. https://doi.org/10.1130/b25375.1
    Robinson, A. C., Yin, A., Manning, C. E., et al., 2007. Cenozoic Evolution of the Eastern Pamir:Implications for Strain-Accommodation Mechanisms at the Western End of the Himalayan-Tibetan Orogen. Geological Society of America Bulletin, 119(7/8):882-896. https://doi.org/10.1130/b25981.1
    Robinson, A. C., Yin, A., Lovera, O. M., 2010. The Role of Footwall Deformation and Denudation in Controlling Cooling Age Patterns of Detachment Systems:An Application to the Kongur Shan Extensional System in the Eastern Pamir, China. Tectonophysics, 496(1/2/3/4):28-43. https://doi.org/10.1016/j.tecto.2010.10.003
    Robinson, A. C., 2015. Mesozoic Tectonics of the Gondwanan Terranes of the Pamir Plateau. Journal of Asian Earth Sciences, 102:170-179. https://doi.org/10.1016/j.jseaes.2014.09.012
    Rutte, D., Ratschbacher, L., Schneider, S., et al., 2017a. Building the Pamir-Tibetan Plateau-Crustal Stacking, Extensional Collapse, and Lateral Extrusion in the Central Pamir:1. Geometry and Kinematics. Tectonics, 36(3):342-384. https://doi.org/10.1002/2016tc004293
    Rutte, D., Ratschbacher, L., Khan, J., et al., 2017b. Building the Pamir-Tibetan Plateau-Crustal Stacking, Extensional Collapse, and Lateral Extrusion in the Central Pamir:2. Timing and Rates. Tectonics, 36(3):385-419. https://doi.org/10.1002/2016tc004294
    Schmalholz, M., 2004. The Amalgamation of the Pamirs and Their Subsequent Evolution in the Far Field of the India-Asia Collision: [Dissertation]. Universitat Tubingen, Tubingen. 1-103
    Schmidt, J., Hacker, B. R., Ratschbacher, L., et al., 2011. Cenozoic Deep Crust in the Pamir. Earth and Planetary Science Letters, 312(3/4):411-421. https://doi.org/10.1016/j.epsl.2011.10.034
    Schneider, F. M., Yuan, X., Schurr, B., et al., 2013. Seismic Imaging of Subducting Continental Lower Crust beneath the Pamir. Earth and Planetary Science Letters, 375:101-112. https://doi.org/10.1016/j.epsl.2013.05.015
    Schneider, F. M., Yuan, X., Schurr, B., et al., 2019. The Crust in the Pamir:Insights from Receiver Functions. Journal of Geophysical Research:Solid Earth, 124(8):9313-9331. https://doi.org/10.1029/2019jb017765
    Schwab, M., Ratschbacher, L., Siebel, W., et al., 2004. Assembly of the Pamirs:Age and Origin of Magmatic Belts from the Southern Tien Shan to the Southern Pamirs and Their Relation to Tibet. Tectonics, 23(4):TC4002. https://doi.org/10.1029/2003tc001583
    Shaffer, M., Hacker, B. R., Ratschbacher, L., et al., 2017. Foundering Triggered by the Collision of India and Asia Captured in Xenoliths. Tectonics, 36(10):1913-1933. https://doi.org/10.1002/2017tc004704
    Shuster, D. L., Flowers, R. M., Farley, K. A., 2006. The Influence of Natural Radiation Damage on Helium Diffusion Kinetics in Apatite. Earth and Planetary Science Letters, 249(3/4):148-161. https://doi.org/10.1016/j.epsl.2006.07.028
    Smit, M. A., Ratschbacher, L., Kooijman, E., et al., 2014. Early Evolution of the Pamir Deep Crust from Lu-Hf and U-Pb Geochronology and Garnet Thermometry. Geology, 42(12):1047-1050. https://doi.org/10.1130/g35878.1
    Sobel, E. R., Dumitru, T. A., 1997. Thrusting and Exhumation around the Margins of the Western Tarim Basin during the India-Asia Collision. Journal of Geophysical Research:Solid Earth, 102(B3):5043-5063. https://doi.org/10.1029/96jb03267
    Sobel, E. R., Schoenbohm, L. M., Chen, J., et al., 2011. Late Miocene-Pliocene Deceleration of Dextral Slip between Pamir and Tarim:Implications for Pamir Orogenesis. Earth and Planetary Science Letters, 304(3/4):369-378. https://doi.org/10.1016/j.epsl.2011.02.012
    Sobel, E. R., Chen, J., Schoenbohm, L. M., et al., 2013. Oceanic-Style Subduction Controls Late Cenozoic Deformation of the Northern Pamir Orogen. Earth and Planetary Science Letters, 363:204-218. https://doi.org/10.1016/j.epsl.2012.12.009
    Stearns, M. A., Hacker, B. R., Ratschbacher, L., et al., 2013. Synchronous Oligocene-Miocene Metamorphism of the Pamir and the North Himalaya Driven by Plate-Scale Dynamics. Geology, 41(10):1071-1074. https://doi.org/10.1130/g34451.1
    Stearns, M. A., Hacker, B. R., Ratschbacher, L., et al., 2015. Titanite Petrochronology of the Pamir Gneiss Domes:Implications for Middle to Deep Crust Exhumation and Titanite Closure to Pb and Zr Diffusion. Tectonics, 34(4):784-802. https://doi.org/10.1002/2014tc003774
    Strecker, M. R., Frisch, W., Hamburger, M. W., et al., 1995. Quaternary Deformation in the Eastern Pamirs, Tadzhikistan and Kyrgyzstan. Tectonics, 14(5):1061-1079. https://doi.org/10.1029/95tc00927
    Stübner, K., Ratschbacher, L., Rutte, D., et al., 2013a. The Giant Shakhdara Migmatitic Gneiss Dome, Pamir, India-Asia Collision Zone:1. Geometry and Kinematics. Tectonics, 32(4):948-979. https://doi.org/10.1002/tect.20057
    Stübner, K., Ratschbacher, L., Weise, C., et al., 2013b. The Giant Shakhdara Migmatitic Gneiss Dome, Pamir, India-Asia Collision Zone:2. Timing of Dome Formation. Tectonics, 32(5):1404-1431. https://doi.org/10.1002/tect.20059
    Thiede, R. C., Sobel, E. R., Chen, J., et al., 2013. Late Cenozoic Extension and Crustal Doming in the India-Eurasia Collision Zone:New Thermochronologic Constraints from the NE Chinese Pamir. Tectonics, 32(3):763-779. https://doi.org/10.1002/tect.20050
    Weather China, 2016. Climatic Data for Tashkurgan County (1971-2000). (2020-1-20). http://www.weather.com.cn/cityintro/101130903.shtml
    Willett, S. D., Brandon, M. T., 2013. Some Analytical Methods for Converting Thermochronometric Age to Erosion Rate. Geochemistry, Geophysics, Geosystems, 14(1):209-222. https://doi.org/10.1029/2012gc004279
    Worthington, J. R., Ratschbacher, L., Stübner, K., et al., 2019. The Alichur Dome, South Pamir, Western India-Asia Collisional Zone:Detailing the Neogene Shakhdara-Alichur Syn-Collisional Gneiss-Dome Complex and Connection to Lithospheric Processes. Tectonics, 39(1):e2019TC005735. https://doi.org/10.1029/2019tc005735
    Yin, A., Robinson, A., Manning, C. E., 2001. Oroclinal Bending and Slab-Break-off Causing Coeval East-West Extension and East-West Contraction in the Pamir-Nanga Parbat Syntaxis in the Past 10 m.y.. American Geophysical Union, 82(47):F1124 https://ui.adsabs.harvard.edu/abs/2001AGUFM.T12F..03Y/abstract
    Yuan, W. M., Carter, A., Dong, J. Q., et al., 2006. Mesozoic-Tertiary Exhumation History of the Altai Mountains, Northern Xinjiang, China:New Constraints from Apatite Fission Track Data. Tectonophysics, 412(3/4):183-193. https://doi.org/10.1016/j.tecto.2005.09.007
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