1. Introduction
Quartz is the most abundant rock-forming mineral of the continental crust, and its dynamic recrystallization processes greatly influence the rheological properties of crustal rocks. Lattice preferred orientation (LPO) of quartz has long been investigated to understand the regime and magnitude of strain along with mechanisms and temperature of deformation (e.g. Schmid & Casey, Reference Schmid, Casey, Hobbs and Heard1986; Law, Reference Law, Knipe and Rutter1990, Reference Law2014; Neumann, Reference Neumann2000; Trepmann & Stökhert, Reference Trepmann and Stöckhert2003; Heilbronner & Tullis, Reference Heilbronner and Tullis2006; Trepmann et al. Reference Trepmann, Stöckhert, Dorner, Moghadam, Küster and Röller2007; Thigpen et al. Reference Thigpen, Law, Lloyd and Brown2010; Faleiros et al. Reference Faleiros, Campanha, Pavan, Almeida, Rodrigues and Araújo2016, Cross et al. Reference Cross, Prior, Stipp and Kidder2017; Kilian & Heilbronner, Reference Kilian and Heilbronner2017). Electron backscatter diffraction (EBSD) is one of the most widely used methods for LPO analysis of common rock-forming minerals (Mainprice & Nicolas, Reference Mainprice and Nicolas1989; Prior et al. Reference Prior, Boyle, Brenker, Cheadle, Day, Lopez, Peruzzi, Potts, Reddy, Spiess, Timms, Trimby, Wheeler and Zetterstrom1999, Reference Prior, Mariani, Wheeler, Schwartz, Kumar, Adams and Field2009). Quartz LPO is developed due to dislocation creep mechanism. However, dynamic recrystallization and the development of LPO in quartz are intricately related as dynamic recrystallization can either destroy the pre-existing LPO or modify or mimic it or develop new LPO (Otani & Wallis, Reference Otani and Wallis2006; Vernooij et al. Reference Vernooij, den Brok and Kunze2006; Wightman et al. Reference Wightman, Prior and Little2006; Trepmann et al. Reference Trepmann, Hsu, Hentschel, Döhler, Schneider and Wichmann2017 and references therein). Dynamic recrystallization processes such as subgrain rotation (SGR) and grain boundary migration (GBM) can also be associated with Dauphiné Twin (Lloyd, Reference Lloyd, Alsop, Holdsworth, McCaffrey and Hand2004; Neumann, Reference Neumann2000; Piazolo et al. Reference Piazolo, Prior and Holness2005; Menegon et al. Reference Menegon, Piazolo and Pennacchioni2011; McGinn et al. Reference McGinn, Miranda and Hufford2020; Jaensch et al. Reference Jaensch, Lagoeiro, Fossen and Cavalcante2022). Therefore, the interpretation of strain regime and deformation mechanism in polydeformed crustal rocks are far from straightforward, as different recrystallization mechanisms may operate at different P-T conditions on the same rock along with the possible effect of fluid infiltration, grain boundary sliding, recovery processes and also Dauphiné Twin. In this context, the LPO of recrystallized quartz grains may provide more insights into the deformation conditions of the final stage of exhumation/evolution of polydeformed rocks (Kohlstedt & Weathers, Reference Kohlstedt and Weathers1980; Hacker et al. Reference Hacker, Yin, Christie and Davis1992; Cross et al. Reference Cross, Kidder and Prior2015).
The Tso Morari Crystalline Complex (TMCC) of trans-Himalaya, eastern Ladakh, lies to the southwest of the Indo-Eurasian collisional suture zone (Figure 1) and consists of quartz, feldspar and mica-rich gneisses, locally called as the Puga Gneiss, with enclaves of metabasic rocks that underwent high to ultra-high pressure metamorphism during subduction of the north Indian continental margin (Steck et al. Reference Steck, Epard, Vannay, Hunziker, Girard, Morard and Robyr1998; Guillot et al. Reference Guillot, Hattori and de Sigoyer2000; de Sigoyer et al. Reference de Sigoyer, Chavagnac, Blichert-Toft, Villa, Luais, Guillot, Cosca and Mascle2000; Leech et al. Reference Leech, Singh, Jain, Klemperer and Manickavasagam2005; Epard & Steck, Reference Epard and Steck2008). Quartz LPO of the Puga Gneiss (Long et al. Reference Long, Kohn, Kerswell, Starnes, Larson, Blackford and Soignard2020; Dutta & Mukherjee, Reference Dutta and Mukherjee2021) and omphacite and quartz from the metabasic enclaves (Dey et al. Reference Dey, Sen and Mamtani2022) have been extensively studied in the recent past to understand the strain regime that prevailed during various stages of the tectonic evolution of the TMCC.
(a) Geological map of Himalaya and trans-Himalaya. The yellow box represents the present study area. (b) Geological map of the TMCC, N-W India (after Epard & Steck, Reference Epard and Steck2008) showing major geological units and sample locations.
The objective of the present study is to understand the mechanism and regime of deformation that characterizes the retrogression stage and facilitates the final stage of exhumation of the TMCC (Puga Gneiss). In the present study, we have collected samples from the Puga Gneiss across the strike of the TMCC from the Zildat fault zone in the northeast to the Karzok fault zone to the southwest (Figure 1). For quartz LPO analysis by means of EBSD, we differentiated the relict quartz grains from the recrystallized ones of the Puga Gneiss on the basis of intragranular lattice distortion (Wheeler et al. Reference Wheeler, Mariani, Piazolo, Prior, Trimby and Drury2009; Wright et al. Reference Wright, Nowell and Field2011; Cross et al. Reference Cross, Prior, Stipp and Kidder2017) and carried out LPO and misorientation analysis for both the suites of grains. Our analysis shows that the relict grains, in general, show multiple <c> axis maxima owing to signatures of different deformation events that occurred during the complex metamorphic evolution of the TMCC. On the other hand, the recrystallized grains, especially in the proximity of the binding fault zones of the TMCC, reflect simple shear or non-coaxial deformation. Our study helps infer that the LPO of relict quartz grains, for most samples, bears ‘memory’ of earlier deformation events and is difficult to interpret in terms of tectonic evolution of the TMCC. Contrary to this, misorientation analysis of the recrystallized grains indicates presence of Dauphiné Twin along with prism and rhomb <a>slip during recrystallization and grain size reduction. Furthermore, LPO of recrystallized quartz grains suggests that the final exhumation of the TMCC took place in a simple shear regime aided by activity along its two binding fault zones.
2. Geology of the area
The trans-Himalaya of eastern Ladakh is characterized by the NW-SE striking Indus Suture Zone (ISZ) that separates the Ladakh Magmatic Arc and the Indus Foreland sediments in the east of the ISZ from the ophiolite (Nidar Ophiolite) and ophiolitic mélanges (Zildat Ophiolitic Mélange) of Tethyan oceanic origin in the west of the ISZ (Figure 1; Thakur & Mishra, 1984). The TMCC lies to the west of the Zildat Ophiolitic Mélange. The Puga Gneiss, or its orthogneissic part, has a Cambro-Ordovician age (Figure 2a, c, d) (∼479 Ma) (Girard & Bussy, Reference Girard and Bussy1999). The Zildat fault demarcates the boundary between the Zildat Ophiolitic Mélange and the TMCC (Figure 2b). In the western margin of the TMCC lies the Karzok fault, which separates the TMCC from the Paleozoic granites and Tethyan metasedimentary sequences (de Sigoyer et al. Reference de Sigoyer, Guillot, Lardeaux and Mascle1997; Hazarika et al. Reference Hazarika, Sen and Kumar2014, Reference Hazarika, Paul, Wadhawan, Kumar, Sen and Pant2017). de Sigoyer et al. (2004) identified three deformation episodes in the TMCC. D1 phase of deformation (∼55 Ma) is characterized by the formation of upright folds at eclogitic grade followed by the D2 deformation phase (∼47 Ma), in dominantly garnet-amphibolite grade, during rapid exhumation that formed NW-SE trending open anticlines. The final D3 stage (∼30 Ma) at the greenschist facies conditions is characterized by extensional movement along the Zildat and Karzok faults and is related to the final exhumation of the TMCC. Present-day movement along these two binding faults of the TMCC has also been observed through fault plane solutions of shallow crustal earthquakes of low to moderate magnitudes (Hazarika et al. Reference Hazarika, Paul, Wadhawan, Kumar, Sen and Pant2017). Metamorphic modelling carried out by various workers on the eclogitic enclaves of the TMCC (e.g. St-Onge et al. 2014; Palin et al. Reference Palin, Reuber, White, Kaus and Weller2017; review by O’Brien, Reference O’Brien, Zhang, Zhang, Schertl and Wei2019; Pan et al. Reference Pan, Macris and Menold2020) suggests peak metamorphism at a P-T condition of ≥ 2.8 GPa and 550°C–650°C followed by near isothermal decompression up to 1 GPa and a subsequent high-temperature overprint (0.7–0.8 GPa and 680°C–720°C). This was followed by a clockwise path towards garnet-amphibolite, and finally, greenschist conditions (Figure 3). Study of Quartz LPO from the Puga Gneiss suggests exhumation of the TMCC through a combination of pure and simple shear (Long et al. Reference Long, Kohn, Kerswell, Starnes, Larson, Blackford and Soignard2020; Dutta & Mukherjee, Reference Dutta and Mukherjee2021). EBSD analysis of omphacite and quartz carried out by Dey et al. (Reference Dey, Sen and Mamtani2022) on the eclogitic enclaves of TMCC also helped infer the transition from constrictional to plane strain during peak metamorphism to subsequent exhumation. Paul et al. (Reference Paul, Hazarika and Wadhawan2017) carried out crustal anisotropy analysis based on shear wave splitting of both S-wave emanating from local earthquakes and PS-converted phases of receiver function data. They observed fast polarizing direction parallel to the Zildat and Karzok faults of the TMCC.
(a) Outcrop of granitic gneiss locally called Puga Gneiss (Location 6A2). (b) Outcrop showing the Zildat fault in Sumdo. (c) Outcrop of Puga Gneiss showing presence of conjugate fractures (Location 3B1). (d) A hand specimen of granitic gneiss cut parallel to XZ section showing asymmetric quartz porphyroclast (Sample 3A2); foliation bands are well developed and are comprised of muscovite.
Diagram showing comparative P-T paths of Tso morari eclogite during its metamorphic evolution obtained by various workers (compiled and modified after Pan et al. Reference Pan, Macris and Menold2020). The P-T paths compared are of (K) = Konrad-Schmolke et al. (Reference Konrad-Schmolke, OʼBrien, de Capitani and Carswell2008); (St.) = St-Onge et al. (Reference St-Onge, Rayner, Palin, Searle and Waters2013); (de) = de Sigoyer et al. (Reference de Sigoyer, Chavagnac, Blichert-Toft, Villa, Luais, Guillot, Cosca and Mascle2000); (G) = Guillot et al. (Reference Guillot, De Sigoyer, Lardeaux and Mascle1997); (Wa)= Warren et al. (Reference Warren, Beaumont and Jamieson2008); (W) = Wilke et al. (Reference Wilke, OʼBrien, Schmidt and Ziemann2015); (Pa) = Pan et al. (Reference Pan, Macris and Menold2020); (P) = Palin et al. Reference Palin, Reuber, White, Kaus and Weller2017. Metamorphic facies boundaries are drawn after Gilotti (Reference Gilotti2013) and Hacker et al. (Reference Hacker, Gerya and Gilotti2013). Abbreviations of fields: Lws = Lawsonite; EC = Eclogite; Ep = Epidote; Amp = Amphibole; HGR = High-pressure Granulite; BS = Blueschist; GR = Granulite; EA = Epidote Amphibolite; AM = Amphibolite.
3. Petrography and microstructures
The samples of Puga Gneiss collected for this study consist mainly of quartz, plagioclase, K-feldspar, muscovite and biotite. The ten samples are divided into three zones on the basis of spatial distribution (Figure 1b). Samples 6A1, 6A2 and 6A5 are from the Karzok zone and are collected from the western part of the TMCC, near the Karzok fault. Samples 2B2, 2C1 and 2C2 are from the Kyeger Tso Lake region in the central part of the TMCC and samples 3A1, 3A2, 3B1 and 3B2 are from the eastern part of the TMCC or the Zildat fault zone. All the samples contain characteristic microstructures of both quartz and feldspar that develop at different ranges of temperature. Tectonic foliation in almost all the samples is defined by preferred orientation of muscovite and biotite. Quartz, along with feldspar, often shows a shape-preferred orientation parallel to this tectonic fabric. Samples from the Karzok zone show presence of plagioclase porphyroclasts surrounded by recrystallized quartzo-feldspathic aggregates (Figure 4a, b) forming ‘core and mantle’ microstructures, which is indicative of deformation at a relatively low temperature (Passchier & Trouw, Reference Passchier and Trouw2005). Alternate layers of coarse- and fine-grained quartzo-feldspathic aggregates can be observed parallel to a tectonic fabric defined by shape preferred orientation of muscovite (Figure 4c). The central part of the TMCC also shows signs of deformation at a low temperature in the form of warping of muscovite around plagioclase porphyroclasts (Figure 4d). The plagioclase porphyroclast shows splaying fractures at high angle to the external foliation defined by muscovite. Bulging of quartz grain boundary into adjacent grain can also be observed (Figure 4e) along with presence of deformation twins in plagioclase (Figure 4f). The former is evidence of bulging recrystallization (BLG) and both these features are indicative of deformation at a comparatively low temperature, i.e. greenschist facies conditions. ‘Pinning’ of quartz grain by muscovite is also observed indicating GBM at a high temperature (Figure 4g) (Jessell, Reference Jessell1987; Stipp et al. Reference Stipp, Stünitz, Heilbronner, Schmid, de Meer, Drury, de Bresser and Pennock2002a; Passchier & Trouw, Reference Passchier and Trouw2005). Prismatic subgrains with varying extinction angles were observed within single quartz grains (Figure 4h), indicating the activation of multiple slip systems during a recovery process or SGR. Quartz also shows presence of sutured grain boundaries and presence of small sub-rounded recrystallized grains (Figure 4g, h) indicating GBM. GBM is also observed in samples from the Zildat fault zone in the form of sutured grain boundaries in quartz having varied grain sizes (Figure 4i) along with presence of 120° triple junctions (Figure 4j). Overall, our microstructural observations suggest dynamic recovery and recrystallization at high temperature (> 550°C) (GBM of quartz; Stipp et al. Reference Stipp, Stünitz, Heilbronner, Schmid, de Meer, Drury, de Bresser and Pennock2002a, b; pinning and dragging microstructure) and medium to high temperature (400°C–550°C) as evidenced by presence of prismatic subgrains in quartz or SGR in quartz (Stipp et al. Reference Stipp, Stünitz, Heilbronner, Schmid, de Meer, Drury, de Bresser and Pennock2002a, b) and also by the presence of recrystallized grains and irregular grain boundaries of plagioclase and K-feldspar (Tullis & Yund, Reference Tullis and Yund1985, Reference Tullis and Yund1987). Microstructures developed at low temperatures (< 400°C) (BLG in quartz; Stipp et al. Reference Stipp, Stünitz, Heilbronner, Schmid, de Meer, Drury, de Bresser and Pennock2002a, b and deformation twin in plagioclase; Tullis & Yund, Reference Tullis and Yund1985) are also common.
Photomicrographs showing microstructural features from the Puga Gneiss (a) Twinned plagioclase porphyroclast surrounded by recrystallized quartzo-feldspathic aggregate forming ‘core and mantle’ structure. (b) Warping of thin film of white mica-rich aggregate around a plagioclase porphyroclast. Note presence of quartzo-feldspathic aggregate in the ‘pressure shadow’ zone and also strong tectonic foliation defined by preferred orientation of white mica. (c) Alternate layers of fine- and coarse-grained quartzo-feldspathic aggregates lying parallel to the tectonic foliation. (d) Warping of foliation defined by biotite and muscovite around a plagioclase porphyroclast. Note splaying microfractures (marked by red dotted lines) within the porphyroclast at a high angle to the external foliation. (e) Bulging of quartz grain boundary in the adjacent grain. (f) Deformation/tapered twins in plagioclase. Note evidence of GBM in plagioclase and quartz in the form of highly irregular grain boundaries and presence of sub-rounded recrystallized grains. (g) ‘Pinning’ of quartz grain by muscovite. (h) Prismatic subgrains of quartz lie concordant with the tectonic foliation defined by mica flakes. (i) Highly irregular/sutured grain boundaries in recrystallized quartz and K-feldspar suggesting grain boundary migration (GBM). (j) Formation of 120° triple junction in quartz owing to GBM. Mineral abbreviations: q = Quartz; Plg = Plagioclase; wm = Muscovite; Kfs = K-Feldspar.
4. Analytical techniques
Measurement of quartz LPO was the critical analysis to be performed in this study. For this, SEM-EBSD analysis was done on Broad Ion Beam (BIB) polished rock thin sections. BIB polishing was done following the MFAL protocol of Mamtani et al. (Reference Mamtani, Chakraborty, Biswas, Suryawanshi, Goswami and Bhatt2020). Slides were initially polished with colloidal silica, followed by BIB polishing, consisting of two steps: 5 minutes of surface cleaning followed by 30 minutes of polishing. EBSD patterns were acquired at 30 kV accelerating voltage, 1.49 x 10−6 mbar system vacuum, and ∼15 mm working distance using Carl Zeiss Auriga Compact FEG-SEM fitted with NordlysMax2 EBSD detector (Oxford Instruments, UK) in Indian Institute of Technology Kharagpur (India). Thin sections were placed in the SEM sample chamber and tilted to 70º before the EBSD analyses. Data acquisition and indexing of EBSD patterns were carried out automatically using Aztec software (Oxford Instruments, UK), along with the elimination of wild spikes. Step size in the range of 6–7.5 µm was taken for EBSD mapping. Grain size distribution, grain-orientation spread (GOS) (Figure 5), distribution of misorientation angles of quartz and axis/angle misorientation distribution analyses were carried out using MTEX 5.7.0., an open-source MATLAB toolbox for quantitative texture analyses, available at http://mtex-toolbox.github.io (Hielscher & Schaeben, Reference Hielscher and Schaeben2008). A 10° threshold angle was used for grain segmentation, keeping only grains that are bigger than 5 µm in size (area of the grain) and have more than three orientation solutions. Grain boundaries are also smoothened. Halfwidth of 10° was kept. Pole figures were plotted using one point per grain to avoid oversampling bias of large porphyroclastic grains. Grains separated by 60±5° rotation around the <c> axis, or Dauphiné twin boundaries (Figure 6), were merged before pole figure analysis. The cylindricity index (B) (Vollmer, Reference Vollmer1990) was used to characterize the distribution of quartz c-axes. B ranges between 0 and 1, starting from completely random fabric to a completely nonrandom fabric. B represents the sum of the point (P) and girdle (G) end-member fabric components. Fabric strength of the indexed phases was calculated using the M-index (Skemer et al. Reference Skemer, Katayama and Karato2006). The M-index is defined as:
$${\rm{M}} = {1 \over {2{\rm{}}}}\int {\rm{I}}{{\rm{R}}^{\rm{T}}}\left( {\rm{\theta }} \right) - {{\rm{R}}^{0{\rm{\;}}}}\left( {\rm{\theta }} \right)|{\rm{d\theta }}$$
Grain orientation spread (GOS) map of quartz for all the samples. All grains < 100 µm in size and with < 2.5° GOS are recrystallized grains and rest are relict grains.
Quartz phase map showing presence of Dauphiné twin boundaries marked by magenta lines.
Where R T (θ) is the theoretical distribution of misorientation angle for a random fabric, and R 0(θ) is the distribution for observed misorientation angles. All the pole figures are plotted after determining the vorticity normal surface (VNS). A ratio of 1: 4 for magnitude of principal and secondary axes of each grain scale dispersion was kept as a threshold to ignore analyzed points with insignificant dispersion of lattice (https://github.com/zmichels/CVA). The VNS was determined using the crystallographic vorticity analysis (CVA) using MTEX, following the method of Michels et al. (Reference Michels, Kruckenberg, Davis and Tikoff2015) and Giorgis et al. (Reference Giorgis, Michels, Dair, Braudy and Tikoff2017).
Recrystallized and relict quartz grains were differentiated and treated separately for LPO analysis. The characterization of recrystallized and relict grains was carried out following the method outlined by Cross et al. (Reference Cross, Prior, Stipp and Kidder2017). This method distinguishes recrystallized grains on the basis of GOS that reflects intracrystalline lattice distortion. The GOS threshold (2.5°) for classification is determined by identifying the knee of the trade-off curve of GOS and cumulative grain counting of each dataset (Cross et al. Reference Cross, Prior, Stipp and Kidder2017). Differential flow stress was also calculated for all indexed quartz grains having a size < 100 µm using the quartz piezometer of Stipp & Tullis (Reference Stipp and Tullis2003). The mean grain size (area of the grain) values for the recrystallized grains are given as root mean square values of circle equivalent diameters (Cross et al. Reference Cross, Prior, Stipp and Kidder2017).
The piezometer relationship (Stipp & Tullis, Reference Stipp and Tullis2003) is:
D = 103.56±0.27 * σ−1.26±0.13
Where D is the mean diameter and σ is differential flow stress.
It may be noted that number of grains considered for differential stress analysis and LPO analysis are different, as for LPO analysis of recrystallized quartz grains, apart from having a size of < 100 µm, only grains having GOS < 2.5° and size > 5 µm are considered.
5. Results
5.1. Quartz grain size distribution and differential stress estimation
Quartz grain size distribution for both relict and recrystallized grains are shown in Figure 7 and Figure 8 and Table. 1. In the Karzok zone, mean relict grain size varies from 90.78 µm (Sample No. 6A2) to 109.48 µm (Sample No. 6A1). For recrystallized grains, the average size varies from 4.60 µm (Sample No. 6A2) to 6.51 µm (Sample No. 6A5). In the Central zone, the mean relict grain size varies from 101.01 µm (Sample No. 2B2) to 354 µm (Sample No.2C1). Mean recrystallized grain size varies from 3.29 µm (Sample No. 2C2) to 5.17 µm (Sample No. 2B2). In the Zildat zone, the mean relict grain size ranges from 280 µm (Sample No. 3A1) to 618.58 µm (Sample No. 3A2). The mean size of recrystallized grains from this zone varies from 3.03 µm (Sample No. 3B2) to 4.15 µm (Sample No. 3A1). Differential stress values obtained from the Karzok zone vary from 80.07 MPa (Sample No. 6A5) to 104.77 MPa (Sample No. 6A2). In the Central zone, it varies from 97.83 MPa (Sample No. 2C1) to 115.83 MPa (Sample No. 2C2). In the Zildat zone, the differential stress values are slightly higher with minimum value of 103.5 MPa (Sample No. 3A1) to 122.61 MPa (Sample No. 3B2). It may be noted that sample 3B2 lying closest to the Zildat fault shows recrystallized grains whose mean size indicates the highest value of differential stress. (Table. 1).
Histograms showing grain size distribution of relict quartz grains for all the samples. The X-axis varies according to the size of the largest grain and y-axis according to the number of grains of certain size.
Histograms showing grain size distribution of recrystallized quartz grains for all the samples. Y-axis varies according to the number of grains of certain size.
Table showing total number of relict and recrystallized quartz and also number of recrystallized grains used for LPO analysis
B and M index for relict and recrystallized grains for all the samples are also shown. Note that the number of recrystallized grains shown for differential stress estimation and pole figure analysis are different as for the former all grains having grain size < 100 µ and GOS< 2.5° are considered while for pole figure analysis using CVA grains < 5 µ and GOS< 1° are also excluded. Similarly, the number of relict grains shown in histogram in Figure 7 and those used for pole figure analysis are different as all relict grains having GOS > 2.5° are considered for histogram but only grains bigger than 5 µ are considered for pole figure analysis. Apart from that, for pole figure analysis of both relict and recrystallized grains, a ratio of 1:4 for magnitude of principal and secondary axes of each grain scale dispersion was kept as a threshold for CVA analysis.
5.2. LPO of Quartz
As evident from past metamorphic modelling studies (Figure 3), the TMCC has experienced a complex metamorphic history and it is likely that its quartz grains have experienced multiple deformations starting from peak metamorphism to exhumation to high-temperature overprint and finally retrogression till greenschist facies conditions. This implies that the analyzed samples may show LPO patterns regarding different P-T conditions by the activation of different slip systems. Therefore, relict (GOS > 2.5°) and recrystallized (GOS < 2.5°) grains are treated separately to infer any meaningful LPO and active slip systems during the late retrogression or the final exhumation stage of these rocks. Keeping this in mind, pole figures were prepared separately for relict and recrystallized grains for all ten samples. The M and B indices for the relict grains vary from 0.0336 to 0.1525 and 0.1950 to 0.6653, respectively (Table 1). For the recrystallized grains, these indices are much lower, and they vary respectively from 0.0110 to 0.0933 and 0.1927 to 0.5533 (Table 1). Maximum values multiple uniform distribution were calculated based on one point per grain of the <c> axis and it varies from zero to six for relict grains and from zero to five for recrystallized grains. All other crystallographic axes and planes have maxima lower than that of the <c> axis.
5.2.1. Karzok zone
<c> axis plot of relict grains from sample 6A1 shows one strong maxima lying in the NE quadrant of the pole figure and two weaker maxima showing a polar distribution in the NW and SE quadrant lying oblique to the XZ plane (Figure 9a, b). Apart from the <c> axis, only the negative rhomb z {01-11} shows partial girdle distribution parallel to the foliation plane for this sample. 6A2 shows a strong <c> axis maxima at ∼10° anticlockwise from the Y-axis in the southern quadrant. A weaker maxima showing polar distribution at opposite quadrants can also be seen lying ∼20° anticlockwise from the lineation (Figure 9c). 6A5 also shows multiple <c> axis maxima with the strongest lying in the NW quadrant and defining a polar distribution at ∼10° anticlockwise from the Y-axis. Other maxima can also be observed at the southern quadrant (Figure 9d). The recrystallized grains show a more regular pattern of <c> axis distribution in the pole Figure 6A1 shows single girdle distribution ∼10° counterclockwise from the XZ plane (Figure 10a). Both 6A2 and 6A5 show strong maxima at ∼10° clockwise from the Y-axis (Figure 10b, c). The a-axis <11–20> shows weak girdle distribution along the foliation plane for sample 6A5 (Figure 10c).
(a) Cartoon showing plotting conventions for inferences of quartz slip systems (after Neumann, Reference Neumann2000). (b–k) Quartz LPOs shown in lower hemisphere equal-area projections (halfwidth = 10°) for relict quartz grains for all the samples. Shear senses are marked for samples having asymmetric single girdle or polar distribution oblique to foliation for the <c> axis.
(a–j) Quartz LPOs shown in lower hemisphere equal-area projections (halfwidth = 10°) for recrystallized quartz grains for all the samples. Shear senses are marked for samples having asymmetric single girdle or polar distribution oblique to foliation for the <c> axis.
5.2.2. Central zone
Relict grains from both samples 2B2 and 2C1 show irregular distribution with multiple maxima for <c> axis (Figure 9e, f). Only sample 2C2 shows strong polar distribution of <c> axis along the Y-axis and one secondary maxima lying on the Z-axis (Figure 9g). Recrystallized grains from 2B2 and 2C2 show <c> axis maxima lying sub-horizontally ∼5° anticlockwise from the XZ plane (Figure 10d, f). 2C1 shows strong <c> axis maxima lying on the z-axis (Figure 10e) indicating prism <a> slip.
5.2.3. Zildat zone
In this zone, relict grains from sample 3A1 show <c> axis maxima at the southern quadrant lying ∼10° clockwise from the Y-axis. A weak girdle parallel to the XZ plane can also be observed (Figure 9h). Samples 3A2 and 3B2 show strong <c> axis maxima defining an asymmetric single girdle at a high angle to the foliation plane (Figure 9i, k). On the other hand, 3B1 shows strong <c> axis maxima lying on the Z-axis and a weaker maxima defining weak girdle distribution along the Y-axis (Figure 9j) indicating both prism and rhomb <a> slip components. Recrystallized quartz grains of 3A1 show <c> axis point maxima lying at opposite quadrants at ∼45° anticlockwise from the XZ plane (Figure 10g). 3A2 has <c> axis point maxima slightly off centre to the Z-axis and defines a weak girdle ∼45° anticlockwise from the XZ plane (Figure 10h). 3B1, on the other hand, shows <c> axis maxima lying subparallel to the XZ plane defining a girdle distribution (Figure 10i). For sample 3B2, the <c> axis has a single asymmetric girdle distribution lying ∼5° anticlockwise from the Y-axis (Figure 10j).
5.3. Quartz misorientation
Misorientation angle distribution for the relict and recrystallized quartz grains are shown in Figure 11 and Figure 12. Both the correlated (misorientation between neighbouring grains) and uncorrelated (misorientation between random grains far from each other) are shown. It can be observed that in case of the relict grains from majority of the samples, the misorientation angle frequency varies from the theoretical uniform distribution (green curve). On the other hand, in case of the recrystallized grains, frequency of misorientation and the theoretical uniform distribution curve match almost perfectly. For the relict grains of samples 6A1 and 6A5, a misorientation angle frequency peak can be observed at 60° (Figure 11a, c). The misorientation axis/angle pair inverse pole figures shown in crystal coordinates reveal that this misorientation angle frequency lies parallel to the <c> axis (Figure 12b, d). In fact, integration of the misorientation angle distribution with the corresponding axis/angle pair inverse pole figure reveals that the frequency of misorientation angle observed at 60° interval lies invariably parallel to the <c> axis for all the samples (Figure 11 and Figure 13). The high-angle misorientations (≥70°) are generally parallel to the <z> and <r> plane with sample 6A2 showing high-angle misorientation parallel to the <a> axis (Figure 13). Relict grains from all the samples except 2C1 show low-angle (≤15°) misorientation parallel to the <c> axis. 2C1 shows low-angle misorientation parallel to the <a> axis. For the intermediate ranges of misorientation angles (15° to 55°), the axis/angle pair inverse pole figures show multiple point maxima that indicate activation of multiple slip systems (Figure 13). Only sample 2C1 shows misorientation angles in the range of 15° to 35° and 35° to 55° lying parallel to the <a> and <c> axes, respectively. For the recrystallized grains, both the low angle (≤15°) and 60±5° misorientation angles lie parallel to the <c> axis (Figure 12 and Figure 14). In the recrystallized grains, misorientation around 60° is the only major frequency peak observed (Figure 12).
Histogram showing quartz misorientation angle distribution for relict grains.
Histogram showing quartz misorientation angle distribution for recrystallized grains.
(a) Slip system conventions according to misorientation (after Neumann, Reference Neumann2000). (b–k) Misorientation axis/angle pairs for quartz displayed in crystal coordinates (relict grains, inverse pole figure).
Misorientation axis/angle pairs for quartz displayed in crystal coordinates (recrystallized grains, inverse pole figure).
6. Discussion
Before we interpret the petrographic and EBSD results obtained from both relict and recrystallized quartz grains, it is necessary to understand the conditions at which the microstructures and LPO of quartz may have developed. As mentioned earlier, the TMCC has a complex metamorphic history (Figure 3), and it is very likely that the relict quartz grains, in particular, may reflect microstructures developed during UHP, decompression or high-temperature overprint episodes of metamorphism (Figure 3). Our petrographic observations (Figure 4) suggest that the Puga Gneiss bears signature of recovery and recrystallization at a high temperature (GBM at > 500°C) in the form of ‘pinning’ (Figure 4g) and GBM microstructures (Figure 4i), 120° triple junctions and irregular grain boundaries in quartz (Figure 4j) along with evidences of SGR including prismatic subgrains in quartz (Figure 4h) indicating recovery and recrystallization in a temperature range of 400°C–550°C (Stipp et al. Reference Stipp, Stünitz, Heilbronner and Schmid2002b). Furthermore, BLG in quartz (Figure 4e), deformed twins in plagioclase (Figure 4f) and presence of fine-grained quartzo-feldspathic aggregate parallel to the tectonic foliation (Figure 4c) may have developed at a lower temperature range of 270°C–400°C (Tullis & Yund, Reference Tullis and Yund1985; Stipp et al. Reference Stipp, Stünitz, Heilbronner, Schmid, de Meer, Drury, de Bresser and Pennock2002a, b; Passchier & Trouw, Reference Passchier and Trouw2005). These observations would suggest that the Puga Gneiss developed microstructure and LPO during the clockwise P-T evolution (Figure 3) of the TMCC with continued exhumation, retrogression and progressive lowering of temperature. Dutta & Mukherjee (Reference Dutta and Mukherjee2021) carried out detailed microstructural analysis of the Puga Gneiss and inferred a deformation temperature range starting from < 400°C to > 600°C. The study by Long et al. (Reference Long, Kohn, Kerswell, Starnes, Larson, Blackford and Soignard2020) on the Puga Gneiss suggests deformation temperature ranging from 330°C to 600°C. Our temperature estimates, based on published pseudosection modelling (Figure 3) and our microstructural observations, have a similar range of temperature. However, we infer a temperature range of ∼270°C to ≥ 550°C for deformation and development of microstructures (BLG to GBM regime of dynamic recovery and recrystallization of quartz).
It may be noted that, apart from quartz, plagioclase and muscovite are the two major constituent minerals observed in the studied samples. The relationship between these rheologically different minerals with quartz, in terms of deformation, needs to be taken into account to understand the microstructural evolution of the studied rocks. As described earlier, both plagioclase and quartz show characteristic recovery and recrystallization microstructures developed at high temperature and at intermediate temperature to low-temperature conditions. However, some amount of strain partitioning can be envisaged between these two phases, as some of the plagioclase porphyroclasts are not completely disaggregated and retain their lens-like shape (Figure 4d) and even subhedral shape (Figure 4f). This indicates rheological competence of plagioclase in comparison to quartz. It can be argued that presence of rheologically stronger feldspar and weaker quartz may have caused strain partitioning with the non-coaxial strain accommodated by the weaker phase in the matrix, i.e. quartz-rich fine-grained layers, and coaxial shear partitioned in the more competent feldspar porphyroclasts (Lister & Williams, Reference Lister and Williams1983). Presence of splaying microfractures within the plagioclase porphyroclasts, lying at a high angle to the external foliation (Figure 4d), can be inferred to be a result of partitioning of strain in coaxial shear component within the porphyroclast and non-coaxial shear component within the external foliation. Experimental study by Holyoke & Tullis (Reference Holyoke and Tullis2006) suggests that muscovite is a much weaker phase than quartz and plagioclase. In the Puga Gneiss, muscovite generally defines the tectonic foliation by preferred orientation and, sometimes, shows monoclinic shape (Figure 4g–j). Muscovite, apart from developing ‘pinning’ microstructures at relatively higher temperature (Figure 4g), generally recorded the latest deformation episode at a relatively low temperature that coincides with the timing of development of strong tectonic fabric, along which they are usually aligned. However, presence of ‘pinning’ of quartz indicates that GBM of quartz has been controlled by mica to some extent.
Dauphiné twinning reverses the positive and negative crystallographic forms of α-quartz through a 60° rotation around the <c> axis. It exchanges the positive and negative rhombs and <a> directions without changing the <c> axis (Thomas & Wooster, Reference Thomas and Wooster1951; Tullis & Tullis, Reference Tullis, Tullis, Heard, Borg, Carter and Raleigh1972; Rahl et al. Reference Rahl, McGrew, Fox, Latham and Gabrielson2018). With the advent of EBSD, Dauphiné twinning has been recognized in various geological conditions in quartz-bearing metamorphic rocks (Menegon et al. Reference Menegon, Piazolo and Pennacchioni2011 and references therein). Studies have shown that Dauphiné twinning plays an important role in intracrystalline plastic deformation in quartz (Menegon et al. Reference Menegon, Piazolo and Pennacchioni2011) and there is an intricate relationship between Dauphiné twinning, microstructural modifications and development of shear bands in quartz-bearing rocks (Neumann, Reference Neumann2000; Lloyd, Reference Lloyd, Alsop, Holdsworth, McCaffrey and Hand2004; Piazolo et al. Reference Piazolo, Prior and Holness2005; Menegon et al. Reference Menegon, Piazolo and Pennacchioni2011; Morales et al. Reference Morales, Mainprice, Lloyd and Law2011; McGinn et al. Reference McGinn, Miranda and Hufford2020; Jaensch et al. Reference Jaensch, Lagoeiro, Fossen and Cavalcante2022). According to Lloyd (Reference Lloyd, Alsop, Holdsworth, McCaffrey and Hand2004), Dauphiné twinning assists in progressive grain size reduction along with formation of new grains and subgrain boundaries. According to Stipp & Kunze (Reference Stipp and Kunze2008), Dauphiné twins are preferred sites for dynamic recrystallization. Recent studies by McGinn et al. (Reference McGinn, Miranda and Hufford2020) and Jaensch et al. (Reference Jaensch, Lagoeiro, Fossen and Cavalcante2022) also highlighted the importance of Dauphiné twinning in accommodation and localization of strain. Dauphiné twinning reduces the stiffness of the quartz crystal and converts it into a more deformable object (Tullis, Reference Tullis1970). Experimental study carried out by Wenk et al. (Reference Wenk, Bortolotti, Barton, Oliver and Brown2007) suggests that a minimum temperature of 300°C–400°C is required for Dauphiné twins to occur with a differential stress of at least ∼ 100 MPa. Past studies have reported occurrence of Dauphiné twins in SGR regime (Lloyd, Reference Lloyd, Alsop, Holdsworth, McCaffrey and Hand2004; Menegon et al. Reference Menegon, Piazolo and Pennacchioni2011; Morales et al. Reference Morales, Mainprice, Lloyd and Law2011) as well as in GBM regime (Neumann, Reference Neumann2000; Piazolo et al. Reference Piazolo, Prior and Holness2005; McGinn et al. Reference McGinn, Miranda and Hufford2020). Piazolo et al. (Reference Piazolo, Prior and Holness2005) reported Dauphiné twins related to α-β transition in quartz, which occurs at granulite-grade temperatures. On the other hand, Jaensch et al. (Reference Jaensch, Lagoeiro, Fossen and Cavalcante2022) have reported Dauphiné twins in folded conglomerate deformed in greenschist facies conditions. This suggests that Dauphiné twinning in quartz can occur at wide ranges of metamorphic conditions.
Twin boundaries that are at 60° angle to the <c> axis are plotted on the quartz phase map that reveals presence of Dauphiné twins (Figure 6). Misorientation analysis of relict quartz grains from all samples, except 2C2 and 3B1, shows a prominent frequency peak at 60°, which is the highest for samples 6A1 and 6A5 (Figure 11). This may suggest presence of Dauphiné twins. However, frequency distribution of misorientation angles should not be the only criteria to identify Dauphiné twin. The misorientation angle, in case of a Dauphiné twin, must be aligned with misorientation axis parallel to the <c> axis (Lloyd, Reference Lloyd, Alsop, Holdsworth, McCaffrey and Hand2004). Misorientation axis/angle pair analysis (Figure 12) clearly shows that the dominant 60° misorientation angle is parallel to the <c> axis. In brief, for the relict quartz grains, the misorientation axis/angle analysis shows that the low angle (2° to 15°) and for angles around 60°, the misorientation angle is aligned parallel to the <c> axis. The preferred alignment in case of 60°±5° confirms the presence of Dauphiné twins. On the other hand, recrystallized grains from all the samples show a prominent frequency peak at 60° (Figure 12), which lies parallel to the <c> axis (Figure 14) and indicates presence of Dauphiné twins. Our misorientation analysis (Figure 11–14) shows that except for relict grains from sample 3B2, low-angle (< 15°) misorientation is not prominent in the Puga Gneiss. This would mean that formation of subgrains through recovery was not dominant (Lloyd, Reference Lloyd, Alsop, Holdsworth, McCaffrey and Hand2004). Similarly, GBM, which operates at higher temperatures, can also be ruled out as regime where majority of Dauphiné twins have developed as the TMCC was undergoing exhumation and, therefore, experienced continuous deformation in progressively lower temperature. Therefore, signature of GBM is more likely to be largely obliterated in the recrystallized set of quartz grains. Although Dauphiné twinning in the relict grains at higher metamorphic grade cannot be ruled out, it can be argued that Dauphiné twins in the recrystallized suites of quartz grains in the Puga Gneiss developed at relatively low temperature of greenschist facies conditions during retrogression of the TMCC. It may also be noted that the differential stress estimated from the recrystallized grains (Table. 1) is similar to the magnitude expected for mechanical Dauphiné twinning (Wenk et al. Reference Wenk, Bortolotti, Barton, Oliver and Brown2007; Menegon et al. Reference Menegon, Piazolo and Pennacchioni2011).
One important effect of Dauphiné twinning is localization of dynamic recrystallization in the r-twin bands (Menegon et al. Reference Menegon, Piazolo and Pennacchioni2011). This effect of strain localization due to Dauphiné twinning in GBM or SGR regimes has been documented in the past (Lloyd, Reference Lloyd, Alsop, Holdsworth, McCaffrey and Hand2004; Menegon et al. Reference Menegon, Piazolo and Pennacchioni2011; Morales et al. Reference Morales, Mainprice, Lloyd and Law2011; McGinn et al. Reference McGinn, Miranda and Hufford2020). These studies have highlighted the importance of Dauphiné twins in strain localization in mid-crustal shear zones. Our study shows ubiquitous presence of Dauphiné twins in both the relict and recrystallized suites of grains. Therefore, we suggest that Dauphiné twins in the relict quartz grains may have developed at any, if not multiple, stages of the complex metamorphic history of the TMCC. As a result, attributing Dauphiné twins in the relict quartz grains of the Puga Gneiss to a particular dynamic recrystallization regime or strain localization is not possible. However, our petrographic observations reveal presence of alternate bands of coarse and fine-grained quartz-rich aggregates that lie parallel to the tectonic foliation defined by muscovite and biotite (Figures 4c, 6a, g, j). These bands are evidence of grain size reduction and strain localization. Abundance of Dauphiné twins in recrystallized quartz grains (Figure 12) indicates that Dauphiné twinning played an important role in grain size reduction and dynamic recovery and recrystallization of quartz aggregate during retrogression/late-stage exhumation of the TMCC. It also emphasizes the role of mechanical twinning in quartz in the overall rheological behaviour of the crust in a collisional zone.
Quartz LPO analysis for relict quartz grains shows that all samples from Karzok zone, two from Central zone (2B2, 2C1) and one sample from the Zildat zone (3A1) have multiple <c> axis maxima that don’t provide any meaningful tectonic interpretation (Figure 9). It can be argued that relict quartz grains from these six samples have multiple/mixed slip system activations that have developed during different stages of deformation/metamorphism. Sample 3B1 has symmetric single girdle and a point maxima around z-axis suggesting activation of both rhomb and prism <a-slip> that may have developed at a temperature of ≤ 500°C (Stipp et al. Reference Stipp, Stünitz, Heilbronner, Schmid, de Meer, Drury, de Bresser and Pennock2002a). However, three samples from the Zildat zone and sample 2C2 from the Central zone show asymmetric single girdle distribution of the <c> axis (Figure 9), which is indicative of non-coaxial or simple shear (Schmid & Casey, Reference Schmid, Casey, Hobbs and Heard1986; Thigpen et al. Reference Thigpen, Law, Lloyd and Brown2010). This distribution is also suggestive of rhomb <a> slip, which once again indicates that this simple shear environment is prevailed at a lower (≤ 500°C) temperature and at a later part of metamorphic evolution of the TMCC. In case of recrystallized grains, this asymmetric single girdle distribution of the <c> axis is more pronounced in the Karzok zone (Figure 10) and samples 3A1 and 3B2 of Zildat zone (Figure 10). This pattern of <c> axis distribution of recrystallized quartz grains, in proximity of the two binding fault zones, helps envisage a simple shear environment in the marginal parts of the TMCC during retrogression and final stage of exhumation.
As mentioned earlier, quartz microstructures and LPO patterns have been studied extensively in the recent past from both the Puga Gneiss (Long et al. Reference Long, Kohn, Kerswell, Starnes, Larson, Blackford and Soignard2020; Dutta & Mukherjee, Reference Dutta and Mukherjee2021) as well as the eclogitic enclaves embedded within the Puga Gneiss (Dey et al. Reference Dey, Sen and Mamtani2022). Long et al. (Reference Long, Kohn, Kerswell, Starnes, Larson, Blackford and Soignard2020) carried out finite strain analysis of quartz from the Puga Gneiss. They envisaged a protracted exhumation facilitated by shearing perpendicular to India-Asia convergence that resulted from strain partitioning due to oblique convergence. Dutta & Mukherjee (Reference Dutta and Mukherjee2021) also suggested transpressional tectonics during India-Asia convergence that helped the TMCC to exhume through a combination of mid-crustal channel flow and wedge extrusion mechanism. Dey et al. (Reference Dey, Sen and Mamtani2022) focused on the high-pressure eclogitic enclaves and suggested that subduction/peak metamorphism of the TMCC took place in a constrictional strain regime that changed to plane strain during exhumation. Our study suggests that the Zildat and the Karzok faults played an important role during final stage of exhumation of the TMCC and a simple shear environment persisted during its final clockwise retrograde P-T evolution at a temperature ≤ 500°C.
7. Conclusions
Based on the results obtained in the present study, the following conclusions can be drawn:
The relict quartz grains of the Puga gneiss developed deformational microstructures at various stages of metamorphism of the TMCC at a temperature range of 270°C–600°C.
Dauphiné twinning played an important role in progressive grain size reduction and overall deformation of the Puga Gneiss quartz.
Asymmetric single girdle distribution in LPO of recrystallized quartz <c> axis suggests a simple shear environment during final stages of exhumation of the TMCC aided by its two binding fault zones, i.e. the Karzok and the Zildat faults.
Acknowledgement
Director of WIHG is thanked for their encouragement and support. We gratefully acknowledge research grant provided by Ministry of Earth Sciences, Govt. of India (MoES/P.O./Geo/96/2017) for this study. Niloy Bhowmik is thanked for carrying out the EBSD analyses at IIT Kharagpur. Shubham Choudhary is thanked for his help during fieldwork. C. P. Dorje provided logistic support for fieldwork in Ladakh. Tim Johnson is thanked for editorial handling. Critical reviews provided by two anonymous reviewers are gratefully acknowledged. This work is part of the 1st authorʼs ongoing doctoral research work on the TMCC.
Financial support
Ministry of Earth Sciences, Govt. of India (MoES/P.O./Geo/96/2017).
Competing interests
All the authors declare no competing interests.
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