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ORIGINAL RESEARCH article

Front. Earth Sci., 12 January 2023
Sec. Structural Geology and Tectonics
This article is part of the Research Topic Sichuan-Tibet Traffic Corridor: Fundamental Geological Investigations and Resource Endowment View all 11 articles

In-situ boron isotope and chemical composition of tourmaline in the Gyirong pegmatite, southern Tibet: Implications for petrogenesis and magma source

  • 1Faculty of Geosciences and Environmental Engineering, Southwest Jiaotong University, Chengdu, China
  • 2Institute of Mountain Hazards and Environment, Chinese Academy of Sciences, Chengdu, China
  • 3Information Center, Ministry of Natural Resources of China, Beijing, China
  • 4Chengdu Center, China Geological Survey, Chengdu, China

Leucogranitic rocks, mainly including leucogranite-pegmatite systems, have been found to be widely distributed in the South Tibetan Himalaya, and they have received considerable interest because of their significance in crustal evolution and associated rare-metal mineralization. Although the nature and geodynamic setting of the Himalayan leucogranites have been well documented by numerous studies, the pegmatites spatially associated with these leucogranites are still poorly understood. Tourmaline is a ubiquitous phase from the leucogranite to the pegmatite. We have therefore conducted in situ major and trace element and boron isotope investigations of tourmaline from the Gyirong pegmatite, synthesizing published data on the Gyirong leucogranite, to document the origin of tourmaline and its genetic implications. Two types of tourmaline (Tur-Ⅰ & Tur-Ⅱ) have been identified in this contribution and they are enriched in Fe, Si and Al but depleted in Mg and Ca, with Mg/(Mg+Fe) ratios ranging from 0.22 to 0.45. Accordingly, the tourmalines belong to the alkali group and have schorl composition. Trace elements, such as Zn, Ga, V, Sc, Li, Sn, Sr, and Co in the tourmalines are relatively enriched, whereas, other trace elements record low concentrations less than 10 ppm. The trace element concentrations of tourmaline are mainly controlled by melt composition. Morphological and geochemical characteristics reflect that the tourmalines from the Gyirong pegmatite are magmatic in origin. The Gyirong pegmatitic tourmalines have S-type granitoids and pegmatites boron isotopic signatures with a tight range of δ11B values between −11.8 and −9.7‰, which is consistent with the magmatic tourmalines (Mg-poor) of the Gyirong leucogranite. This study suggests that the Gyirong pegmatite was the product of crustal anatexis and that the crustal metapelitic rocks within the Greater Himalayan Crystalline Complex were the most likely source components.

1 Introduction

The India-Asia collision since the Early Cenozoic formed the largest Himalayan-Tibetan orogenic system on Earth (Yin and Harrison, 2000; Najman et al., 2010; Hu et al., 2016; Xu et al., 2017). Meanwhile, the ongoing continental collision-convergence processes triggered large-scale anatexis of the crust during the Late Eocene to Miocene and eventually generated the world’s most famous voluminous leucogranite belt (Le Fort et al., 1987; Hou et al., 2012; Wu et al., 2015; Fan et al., 2021). As a probe, the Himalayan leucogranites carry ample information, such as their origin, age, emplacement mechanisms and related economic mineralization, which is critical for understanding the tectonic-magmatic-metamorphic evolution of the Himalayan orogeny (Searle et al., 2010; Liu et al., 2019; Wang et al., 2020; Wu et al., 2020; Tang et al., 2021; Xu et al., 2021; Cao H. et al., 2022). These leucogranitic rocks mainly include leucogranite-pegmatite systems, which are widely distributed in the South Tibetan Himalaya (Zhou et al., 2019). Considerable attention has been paid to the nature and geodynamic setting of the Himalayan leucogranites (Cao et al., 2022a and reference therein), while the pegmatites spatially associated with these leucogranites are still poorly understood.

Tourmaline, as a ubiquitous cyclosilicate mineral in rocks of the Earth’s crust, forms in a wide range of geological settings and is particularly prevalent in evolved granitic rocks (Trumbull et al., 2008; van Hinsberg et al., 2011; Wadoski et al., 2011; Čopjaková et al., 2021). The chemical compositions of tourmaline have negligible diffusion rates with wide temperature (150 °C–900 °C) and pressure (6 MPa to >6 GPa) stability ranges, making it an ideal petrogenetic indicator (Henry et al., 2011; Wei and Zhao, 2020). Importantly, tourmaline is the dominant boron-bearing mineral, and its boron isotopes show significant variations. Therefore, tourmaline boron isotope geochemistry has been widely applied to trace boron sources and magmatic-hydrothermal processes (Marschall and Jiang, 2011; Grew et al., 2016; Guo et al., 2021; Guo et al., 2022). In addition, tourmaline occurs widely in Himalayan leucogranites and associated pegmatites, and often has well-defined crystal faces with complex zonal structures (Yang et al., 2015; Zhou et al., 2019; Liu et al., 2022; Zhang et al., 2022). Such convoluted chemical zoning retains the history of physicochemical conditions of the melt or fluid from which it crystallized and provides major insights into petrologic processes (Hawthorne and Dirlam, 2011; Bosi, 2018; Liu and Jiang, 2021).

The Gyirong aera, located in the central Himalayan orogenic belt, contains the vital record of sedimentary sequence, drainage development and magmatic-tectonic events of the Himalaya (Shen et al., 2016; Dong et al., 2017). Previous studies mainly focused on climatic and tectonic uplift evolution (Hong et al., 2010; Shen et al., 2016; Wolff et al., 2022), paleoenvironmental analysis (Xu et al., 2012), gneiss dome and associated granitoids (Gao and Zeng, 2014; Dong et al., 2017; Gao et al., 2017; Wang et al., 2017) and potential rare metal mineralization (Wu et al., 2020). The geochemical variations in accessory minerals such as zircon, monazite, tourmaline and garnet from the leucogranites are also involved in the above investigations (Gao et al., 2017; Hu et al., 2022), whereas there is a lack of studies on tourmaline from the pegmatites therein. In this contribution, we present in situ major and trace elements and boron isotopes of tourmalines from the Gyirong pegmatite of southern Tibet. Our results, combined with the geochemical data of the tourmalines from other regions along the Himalayan leucogranite belt, allow us to document the geochemical behavior of tourmaline precipitation and its origin, and also contribute additional constraints on the genetic mechanisms of the Himalayan leucogranites as well as the architecture and evolution of the Himalayan orogen.

2 Geological setting and samples

The roughly east-west-trending Himalayan orogen (extending ∼2500 km long), bounded by the Indus-Yarlung Tsangpo suture to the north and the Main Front Thrust (MFT) to the south, is a classic example of collisional belts worldwide (Figure 1A) (Hodges, 2000; Zhao Z-b et al., 2021; Yu et al., 2021; Pan et al., 2022). It has experienced a prolonged and complicated history that included several periods of oceanic spreading, subduction and continental collision and eventually formed via the amalgamation of multiple terranes (Pan et al., 2012; Metcalfe, 2021; Xu et al., 2022). Tectonically, from north to south, four major lithotectonic units have been defined within this orogen: the Tethyan Himalayan Sequence (THS), the Greater Himalayan Crystalline Complex (GHC), the Lesser Himalayan Sequence (LHS) and the sub-Himalayan Sequence (SHS, or defined as the Siwalik Sequence), which are separated sequentially by the South Tibet Detachment System (STDS), the Main Central Thrust (MCT) and the Main Boundary Thrust (MBT) (Figure 1B) (Yin, 2006; Goscombe et al., 2018; Cao et al., 2020). The THS located in the northernmost part of the orogenic belt mainly exposed Early Paleozoic-Eocene clastic and carbonate rocks that experienced low-grade greenschist- and low amphibolite-facies metamorphism (Cao et al., 2018). A series of discontinuously distributed gneiss domes (e.g., the Malashan dome, Kawakami et al., 2007), belonging to the North Himalayan gneiss domes (NHGD) (Alsdorf et al., 1998; Fu et al., 2017; Ma et al., 2022), are recognized within the THS. The GHC consists of Proterozoic-Early Paleozoic high-grade metasediments, orthogneiss and magmatic rocks (Grujic et al., 2002; Gou et al., 2016; Gou et al., 2022; Ji et al., 2022), representing the core of the Himalayan orogenic belt. Further evidence suggests that it exhumed from the middle-lower crust to near the surface in the Cenozoic (Webb et al., 2017). The LHS principally comprises Paleoproterozoic to Early Paleozoic greenschist-to amphibolite-facies metasedimentary rocks, augen gneisses and metavolcanic rocks (Imayama et al., 2010; Martin, 2017). Two subparallel Cenozoic leucogranite belts with nearly east-west direction are discontinuously exposed along Himalayan orogen (Figure 1B): the northern belt occurs in the THS and NHGD, and the southern belt is distributed at the top of the GHC or involved in the shear zone beneath the STDS (Searle, 1999). Petrographically, the Himalayan leucogranites are generally equivalent to monzonite granites and dominated by two-mica (muscovite and biotite), biotite-, tourmaline- and garnet-bearing leucogranites (Wu et al., 2020). Their mineralogical composition includes quartz, euhedral plagioclase, perthitic potassic feldspar, muscovite, tourmaline, biotite and garnet (Guillot and Le Fort, 1995).

FIGURE 1
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FIGURE 1. (A) Geographical location of the Himalaya. (B) Simplified geological map of the Himalayan Orogen (modified after Cao et al., 2021).

Our study area, which is located near the Gyirong County of southern Tibet, encompasses the Malashan-Paiku Co dome, the THS, the STDS, and the GHC from north to south (Figure 2). In addition, several Late Cenozoic fault basins, such as Gyirong and Oma, are also distributed in this area, which may be controlled by the north-south extension related to the STDS (Yang et al., 2009). The Malashan-Paiku Co dome acts as a segment of the NHGD and consists essentially of two-mica granite and Paiku composite leucogranite in the core and metamorphic rocks such as gneiss, schist and phyllite toward the margin (Wang et al., 2016; Gao et al., 2017), accompanied by multistage ductile deformation (Aoya et al., 2005). To the south, there is a set of Ordovician-Jurassic sedimentary rocks containing a small amount of Early Paleozoic and Mesozoic volcanic rocks. The cross-section of Gyirong area shows that folds and normal faults are developed in this set of strata. The STDS in the Gyirong area is a large ductile shear zone with a width of more than 10 km. It is mainly composed of Paleozoic granitic gneiss and Cenozoic foliated two-mica granites with syn-deformational features (Yang et al., 2009) and was emplaced by late undeformed leucogranites (∼17.7 Ma, Gao et al., 2016). The GHC in the study area exposes medium-grade metamorphic rocks mainly consisting of augen gneiss, amphibole-biotite gneiss, metapelite, meta-sandstone, plagioclase-amphibole gneiss and schist. Leucogranites occurring as sills, dikes, dykes, dendritic and lenticular shapes intruded into the metamorphic rocks within the GHC. These leucogranitic veins were emplaced at 22–16 Ma (Wang et al., 2013; Gao et al., 2016), which record a long duration of anatexis and a tectonic transformation.

FIGURE 2
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FIGURE 2. Geological map of the Malashan-Gyirong area (modified after Wang et al., 2017).

Two tourmaline-bearing samples (JL-4 and JL-5) were collected from the granitic pegmatites within the GHC (Figures 3A,B,D. Sample JL-4 is garnet tourmaline granitic pegmatite. Plagioclase, potassium feldspar, tourmaline, garnet, muscovite and biotite dominate sample JL-4 (Figure 3C). Some tourmaline occurs as rounded inclusions within garnet (Figure 3C). In contrast, sample JL-5 displays similar mineral assemblages (Figures 3D–F) but much less garnet, thus it can be defined as tourmaline granitic pegmatite. Tourmaline in two samples shows diverse colors (e.g., green, brownish, yellow, pale blue) and usually has a dark- or light-colored core surrounded by a zoned rim. These tourmaline grains commonly occur as large crystals and are predominantly prismatic or granular in shape with sizes mainly ranging from 0.1 to 4 cm (Figures 3C,E–H). In this study, we select large tourmaline grains with complex zoning (Tur-Ⅰ type) within sample JL-4 and granular tourmaline (Tur-Ⅱ type) in sample JL-5 for further chemical and B isotope investigation.

FIGURE 3
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FIGURE 3. Representative photographs of tourmalines in the Gyirong pegmatite. (A) Outcrops of the Gyirong pegmatite. (B) Hand specimen of garnet tourmaline granitic pegmatite. (C) Granular tourmalines as rounded inclusions within garnet and quartz. (D) Hand specimen of tourmaline granitic pegmatite. (E) Large columnar tourmalines showing diverse colors. (F) Tourmaline grains, K-feldspar, plagioclase, quartz, muscovite and biotite in pegmatite. (G) Large tourmaline with complex zoning (Tur-Ⅰ type). (H) Granular tourmaline (Tur-Ⅱ type). The red circles are the points of iin situmajor and trace elements and boron isotope analyses. Abbreviations: Bi, Biotite; Grt, Garnet; Kfs, K-feldspar; Mus, Muscovite; Pl, Plagioclase; Qtz, Quartz; Tur, Tourmaline.

3 Analytical techniques

Major element compositions of tourmaline were obtained from polished thin sections using an EMPA-1600 electron microprobe with wavelength dispersive spectrometry at the Chengdu Center of the Geological Survey of China. The operating conditions were at 15 kV acceleration potential, 20 nA beam current and a 20 μm defocused spot with counting times between 10 and 30 s.

The trace element concentrations of tourmaline in polished thin sections were determined using an Agilent 7700E inductively coupled plasma mass spectrometer (ICP-MS) equipped to a GeolasPro laser ablation (LA) system at Wuhan Sample Solution Analytical Technology Co., Ltd., Wuhan, China. In this experiment, the ablating diameter for the LA-ICP-MS trace element analysis was set at 35 μm on the equivalent locations where the EPMA had been conducted. The detailed testing procedures and conditions were similar to those described by Zheng and Chen (2021). Data processing was performed offline using ICPMSDataCal software (Liu et al., 2008).

In situ boron isotopic compositions of tourmaline were measured in polished thin sections by the RESOlution S-155 laser ablation system coupled to a Nu plasma II multi-collector ICP-MS (LA-MC-ICP-MS). Analyses were carried out with laser spot size of 50 μm, 10 Hz repetition rate, and energy of ∼5 J/cm2. Two Faraday cups were used to collect 11B/10B signals of tourmaline samples and various standards. The standard-sample-standard bracketing (SSB) method was adopted to calibrate the instrumental mass fractionation (IMF). The international tourmaline standard IAEA B4 from Tonarini et al. (2003) served as an external standard, whereas tourmaline reference material IMR RB1 was adopted as the monitoring standard. Replicate analyses of standard tourmaline IMR RB1 yielded an average δ11B of -13.3‰ (Supplementary Table S1), which is consistent with the reference value of −12.97‰ ± 0.97 (2σ; n = 57) obtained by LA-MC-ICP-MS (Hou et al., 2010). The external precision is estimated to be better than 0.5‰ (±2σ) based on the replicated analyses of reference tourmalines during the process of this study. The internal precision (1 SD) in per mil for individual analysis was calculated from approximately 100 cycles during each analysis (Zhao K-D. et al., 2021). Detailed analytical procedure broadly followed that presented in Yang and Jiang (2012).

4 Results

4.1 Tourmaline chemical compositions and classification

4.1.1 Major element crystal chemistry

Tourmaline has a fairly complicated crystal structure framework and varied constituents with empirical crystallochemical formula of XY3Z6 [T6O18][BO3]3V3W followed by (Hawthorne and Henry, 1999), where X = Na+, Ca2+, X[vacancy], K+, Pb2+; Y = Mg2+, Fe2+, Al3+, Li+, Ti4+, Mn2+, Fe3+, Zn2+; Z = Al3+, Cr3+, Fe3+, Mg2+, Fe2+; T = Si4+, B3+, Al3+; V = OH-, O2- ; and W = OH- , F- and O2-. Tourmaline formulas were calculated by normalizing to 15 cations apfu (atoms per formula unit) in the tetrahedral and octahedral sites (T+Y+Z) and assuming B=3 pfu following the procedure of (Henry and Dutrow, 1996). The calculation was undertaken with the WinTcac program of Yavuz et al. (2014) based on the EPMA data (Table 1). A complete list of the major element analyses can be found in Supplementary Table S2.

TABLE 1
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TABLE 1. Summary of EPMA results and calculated atoms per formula (apfu) for tourmalines from the Gyirong pegmatites.

Tourmalines from the Gyirong pegmatite show large variable contents of FeO (9.08–4.68 wt.%) and MgO (2.01–0.19 wt.%) but restricted ranges of SiO2 (33.09–34.65 wt.%), TiO2 (0.42–0.95 wt.%), Al2O3 (31.46–3.80 wt.%), CaO (0.60–0.95 wt.%), Na2O (1.76–0.08 wt.%) and K2O (0.06–0.11 wt.%), with low K2O (0.06–0.11 wt.%), MnO (0–0.22 wt.%) and F (0–0.06 wt.%). According to the X site classification of (Henry et al., 2011), all the tourmalines from the Gyirong pegmatite belong to the alkali group (Figure 4A). From the cores to the rims of Tur-Ⅰ, a trend of lower FeO (14.68–0.13 wt.%) and higher MgO (2.24–0.55 wt.%) were found during crystal growth, whereas the concentrations of other major elements did not show clear differences. For tourmaline of Tur-Ⅱ, its chemical composition is consistent with that of tourmaline rims of Tur-Ⅰ. Thus, tourmalines from the Gyirong pegmatite are distributed in two groups: group-Ⅰ of tourmaline cores of Tur-Ⅰ, and group-Ⅱ of tourmaline rims of Tur-Ⅰ & tourmaline of Tur-Ⅱ, with average Mg# (Mg#=Mg/(Mg+Fe)) ratios of 0.22 and 0.45, respectively. The variations in the Y site Mg# are shown in the plots of Mg/(Mg+Fe) versus the X-site occupancy (Xv/Xv+Na) (Figure 4B) and Mg/(Mg+Fe) vversusthe X-site occupancy (Na/Na+Ca) (Figure 4C). All the tourmaline samples exhibit small Na/Na+Ca and Xv/Xv+Na variations on the X-site, combined with Mg# ratios, classifying them as schorl type (Figures 4B,C). As illustrated in Al-Fe-Mg and Ca-Fe-Mg ternary diagrams (Figures 4D,E) (Henry and Guidotti, 1985), tourmaline cores of Tur-Ⅰ fall in field 2, equal to Li-poor granitoids and associated pegmatites and aplites. This is consistent with the negligible content of Li (less than 50 ppm) confirmed by the LA-ICP-MS analysis (see below). In contrast, some analyses of tourmalines from Tur-Ⅰ rims and Tur-Ⅱ fall in the range of Ca-poor metapelites, metapsammites and quartz-tourmaline rocks (field 10).

FIGURE 4
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FIGURE 4. Ternary and binary diagrams for tourmaline in the Gyirong pegmatite. (A) Principal groups of tourmalines based on X-site occupancy (Henry et al., 2011). Plots of Mg/(Mg + Fe) vs. Xv/(Xv + Na) (B) and Mg/(Mg + Fe) vs. Na/(Na+Ca) (C) of tourmalines (Henry et al., 2011). (D) Ternary Al-Fe-Mg (D) and Ca-Fe-Mg (E) diagrams for tourmalines (Henry and Guidotti, 1985). Data sources: Hu et al.,(2018); Hu et al. (2022) and references therein.

4.1.2 Trace element contents

The trace element compositions analyzed by LA-ICP-MS are summarized in Table 2, and the whole data set can be found in Supplementary Table S2. All types of tourmalines in the Gyirong pegmatite contain low contents of rare earth elements (REEs), with the majority of analyses yielding concentrations below 1 ppm. The total contents of REEs range from 13.3 to 23.9 ppm. Tourmalines of Tur-Ⅰ and Tur-Ⅱ from the Gyirong pegmatite share similar chondrite-normalized REE patterns (Figure 5), which are characterized by marked light REE enrichment with positive Eu anomalies and weak to negligible Ce anomalies. The concentrations of most trace elements except REEs vary from 0.1 to tens of parts per million (ppm) (Figure 6). Tourmalines are relatively enriched in Zn (195.56–333.63 ppm), Ga (79.92–7.50 ppm), V (15.30–14.60 ppm), Sc (18.06–3.38 ppm), Li (16.05–4.95 ppm), Sn (17.19–4.25 ppm), Sr (15.71–6.43 ppm) and Co (9.49–9.75 ppm). Whereas, trace elements such as Be, Ni, Rb, Y, Sb and Pb show concentrations less than 10 ppm. A few elements exhibit large variations in tourmaline of different types. Tourmalines in group-Ⅰ display higher Li, Sc, Zn, Sn, and Pb contents than those in group-Ⅱ. In contrast, elements such as V, Co, Ni and Sr are highly enriched in group-Ⅱ.

TABLE 2
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TABLE 2. Representative LA-ICP-MS trace element analyses of tourmaline from the Gyirong pegmatite (in ppm)

FIGURE 5
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FIGURE 5. Chondrite-normalized REE diagrams of tourmalines in the Gyirong pegmatite.

FIGURE 6
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FIGURE 6. (A–L) Correlation diagrams between selected trace elements (Li, Be, Sc, Sr, Ga, V, Co, Ni, Pb, Zn, Sn, and REE) and Mg/(Mg + Fe) ratios in tourmalines from the Gyirong pegmatite.

4.2 Boron isotopic composition of tourmaline

The LA-MC-ICP-MS analytical results of boron isotopic compositions of tourmalines from the Gyirong pegmatite are available in Table 3 and Figure 7A. The tourmalines show a tight range of δ11B values between -11.8 and -9.7‰. There seem to be no obvious differences in B-isotope compositions between the two types of tourmalines. More specifically, the δ11B values of Tur-Ⅰ from sample JL-4 and Tur-Ⅱ from sample JL-5 are concentrated from −11.8 to −9.9‰ (mean −10.4‰) and from −11.8 to −9.7‰ (mean −11.1‰), respectively. With regard to compositional zonation, Tur-Ⅰ shows slight core-rim variation, with mean δ11B values ranging from −10.6‰ (core) to −10.2‰ (rim).

TABLE 3
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TABLE 3. LA-MC-ICP-MS boron isotope analyses for tourmaline from the Gyirong granitic pegmatite

FIGURE 7
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FIGURE 7. Histograms representing the δ11B values of (A) tourmalines from the Gyirong leucogranite and pegmatite; and (B) magmatic tourmalines from Himalayan leucogranite and pegmatite. (C) Summary of boron isotope compositions for marine and crustal rocks and for tourmaline from the Gyirong and Malashan areas. Date sources: tourmalines from the Gyirong leucogranite (Hu et al., 2022), tourmalines from Himalayan leucogranites and pegmatites (Supplementary Table S3), average continental crust (Marschall and Jiang, 2011), and other boron reservoirs (Trumbull et al., 2020 and references therein). Abbreviations: Tur: tourmaline, M-Tur: magmatic tourmaline.

5 Discussion

5.1 Formation of tourmaline in the Gyirong pegmatite

Tourmaline is a common accessory mineral in many evolved granitic rocks (Trumbull and Chaussidon, 1999; uriánek and Novák, 2007; Yang and Jiang, 2012), especially peraluminous leucogranites and related pegmatites, which widely exist in continental collision zones such as the Himalayan orogenic belt (Le Fort et al., 1987; Guillot and Le Fort, 1995; Wu et al., 2020; Liu et al., 2022). Abundant boron in melt-fluid system is the main factor for the crystallization of tourmaline (Wolf and London, 1997; London, 2011). Due to the incompatibility of boron and the crystallization of boron-poor materials (e.g., feldspar and quartz) during magma evolution, boron-rich magma may have been produced at late stage, causing tourmaline to crystallize (Pesquera et al., 2013). However, in the magmatic-hydrothermal stage, boron is preferentially partitioned into the fluid phase (London, 1999), and boron-rich fluid reacted with crystallized minerals and residual melts to form tourmaline nodules accordingly (Trumbull et al., 2008; Balen and Broska, 2011). Thus, tourmaline in the granite-pegmatite system could be magmatic in origin as documented by prior studies (Trumbull and Chaussidon, 1999; Chakraborty, 2021). Alternatively, it could also be generated from the reaction between boron-rich fluid with crystallized granite at shallow levels, as proven by field investigations and experimental works (Morgan and London, 1989; Cheng et al., 2019). Moreover, there are also examples of tourmaline in the pegmatite reported to be of magmatic-hydrothermal origin at the late magmatic stage (e.g., Gou et al., 2017). Accordingly, tourmaline in the pegmatite could potentially crystallize from a melt or (magmatic-) hydrothermal fluid, which requires comprehensive information to distinguish.

Tourmalines in the Gyirong pegmatite mainly act as isolated grains or long columnar coexisting with the major rock-forming minerals (quartz, plagioclase, K-feldspar, muscovite, etc.) with planar and arc-shaped contacts (Figures 3B,C,F–I). Furthermore, tourmaline crystals are found enveloped by quartz, feldspar and garnet grains (Figures 3B,C,F–I), suggesting that these tourmalines occurred early in the crystallization sequence. There is no textural evidence to show that pegmatite has undergone hydrothermal alteration. Geochemically, all the tourmaline samples reflect relatively homogeneous compositions and are characterized by low Mg# (0.20∼0.50) and CaO (0.60–0.95 wt.%), high Al2O3 (31.46–3.80 wt.%) and FeO (9.08–4.68 wt.%), and high Al contents at the Y-site (0.19–40 apfu). All tourmalines belong to the alkali group (Figure 4A) and plot in the schorl (Fe-rich) field (Figures 4B,C). In the ternary diagrams of Al-Al50Fe50-Al50Mg50 (Figure 4D) and Ca-Fe-Mg (Figure 4E), tourmalines plot mostly in the magmatic range, whereas few analyses of Tur-Ⅰ rims and Tur-Ⅱ lie across field 2 (Li-poor granitoids and associated pegmatites and aplites) to field 10 (Ca-poor metapelites, metapsammites and quartz-tourmaline rocks). All tourmaline analyses from the Gyirong pegmatite display high Zn concentrations (195.56–33.63 ppm), which indicate that they were crystallized from hydrous borosilicate melts (Veksler and Thomas, 2002; Hazarika et al., 2017). The above morphology and geochemistry of the tourmaline in the Gyirong pegmatite indicate that they are magmatic in nature (London and Manning, 1995), which is clearly different in composition from tourmaline of hydrothermal origin (Yang et al., 2015; Zhao H-D. et al., 2021; Liu et al., 2022). These features are consistent with those of magmatic tourmaline reported in other Himalayan leucogranites (Yang et al., 2015; Dai et al., 2019; Zhou et al., 2019; Cheng et al., 2021; Liu et al., 2022).

It is noteworthy that the Tur-Ⅰ rims and Tur-Ⅱ show slightly Mg (Ca)-rich and Fe-poor signatures compared to the Tur-Ⅰ cores. The common explanation for the significant increase in Mg# from the core to rim of tourmaline is magma mixing and input of external (Mg-rich) fluid (Jiang et al., 2008; Cheng et al., 2021). However, there is no field evidence, such as the presence of secondary tourmaline veins. Besides, the uniform B-isotope compositions (Tur-Ⅰ & Tur-Ⅱ) also argue against magma mixing or the involvement of external fluids (Palmer and Swihart, 1996; Albert et al., 2018; Qiu et al., 2021). Alternatively, considering that the composition of magmatic tourmaline depends on the nature of the melt (Liu and Jiang, 2021), the insignificant variations (e.g., Fe, Mg, Ca) in core-rim compositions of tourmaline might suggest that slight assimilation and contamination by wall rocks have occurred (Liu and Jiang, 2021; Qiu et al., 2021). The high-grade metamorphosed rocks with high-Mg/low-Fe compositions in the GHC have the potential to supply magnesium (Harris and Massey, 1994; Yin, 2006). The increase in V, Co and Ni and the decrease in Li with Mg/(Mg + Fe) from the Tur-Ⅰ cores to the Tur-Ⅰ rims and Tur-Ⅱ is consistent with contamination by the surrounding strata. This hypothesis is also supported by the distinct chemical variations in tourmalines in different lithologic units within the Gyirong area (Hu et al., 2022). Similarly, a transition trend recorded in elemental and Sr-Nd isotopic compositions of granitic dikes through Bendui intrusion to Himalayan leucogranites within the THS by a case study by Ji et al. (2020) also supports this scenario. It is worth noting that even if contamination by wall rocks might have occurred, the tourmaline composition only changes slightly (e.g., Mg# does not exceed 0.5). In this case, their boron isotopes can still represent the original B isotopic composition of the source (Hu et al., 2018).

The trace elements of tourmaline could record the compositional signature of its host melt (e.g., van Hinsberg, 2011). According to the correlation diagrams of trace elements versus Mg/(Mg + Fe), only V, Ni and Co (not obvious) are positively correlated with Mg/(Mg + Fe) (Figure 6), which may be related to the potential crystal chemical effects on their incorporation (Zhao et al., 2019). Most trace elements did not show apparent correlations with Mg/(Mg+Fe), which indicates that the trace element concentrations of tourmaline are mainly controlled by melt composition. This supports the scenario that tourmalines in the Gyirong pegmatite were crystallized directly from melt. In summary, we suggest that the tourmalines from the Gyirong pegmatite are of magmatic origin and are a product of direct crystallization from a boron-rich pegmatitic magma.

5.2 Boron isotope variation and genetic implications

We compiled a total of 394 boron isotopic analyses (Supplementary Table S3) on magmatic tourmalines (free of hydrothermal effects) from Himalayan leucogranites and pegmatites reported in the literature (Figure 7B, Chaussidon and Albarède, 1992; Yang et al., 2015; Gou et al., 2017; Hu et al., 2018; Dai et al., 2019; Zhou et al., 2019; Han et al., 2020; Cheng et al., 2021; Hu et al., 2022; Liu et al., 2022), which define an ample range of δ11B values from −18.9 to −5.8. The large boron isotopic compositional variations in tourmalines in the Himalaya may result from heterogeneous melt sources (magma mixing) or fractions of boron isotopes during magma evolution (Trumbull et al., 2013; Kawakami et al., 2019; Xiang et al., 2020).

The measured tourmaline boron isotopes from the Gyirong pegmatite define a narrow range of −11.8 to −9.7 ‰ (concentrated at approximately −10 ‰) with negligible boron isotopic zonation within tourmalines, which indicates that no significant isotopic fractionation has occurred. Similarly, magmatic tourmalines (Mg-poor) of the Gyirong leucogranite have δ11B values of −12.1 to −11.2 ‰ (Hu et al., 2022). Note that minimal boron isotope fractionation occurs between boric granitic or pegmatitic melt and tourmaline at common anatectic temperatures (Palmer and Swihart 1996; Smith and Yardley, 1996; Meyer et al., 2008). In this case, the boron isotopes of magmatic tourmaline should approximate that of the primary δ11B value of the parental magma. The light boron isotopic compositions of magmatic tourmalines in the Gyirong leucogranite and pegmatite are consistent with the global database of average continental crust (−10 ± 3‰), S-type granitoids and pegmatites (Figure 7C), reflecting a continental source of boron (Trumbull et al., 2020).

As addressed by numerous studies (e.g., Gao and Zeng, 2014; Gou et al., 2017; Fan et al., 2021), the Himalayan leucogranites were mainly generated by metapelite dehydration melting or fluid-present melting. The Gyirong leucogranite shows high (87Sr/86Sr)i ratios (0.7548–7586), high Rb contents, and low Sr and Ba contents (Gao et al., 2017; Wang et al., 2017), which can be ascribed to fluid-absent melting of muscovite in metasedimentary sources. This interpretation is also supported by recent Mg-Fe-Sr-Nd isotope studies (e.g., Tian et al., 2020; Shi et al., 2021). Note that some authors found that the Himalayan leucogranites do not record any mantle material contribution to the sources (Inger and Harris, 1993; opkinson et al., 2017). In addition, some studies emphasized the contribution from the LHS fluids with regard to the anatectic sources of the Greater Himalayan leucagranites (Guo and Wilson, 2012; Liu et al., 2022). In contrast, there are also recent studies arguing that the contribution of the LHS is unnecessary (e.g., Ji et al., 2022). In our case, homogeneous tourmaline δ11B values are consistent with the average crust and S-type granite, likely supporting the latter hypothesis in the Gyirong area. Hence, the crustal metapelitic rocks within the GHC were the most likely source components for the Gyirong pegmatite, which is consistent with most Himalayan leucogranites (Inger and Harris, 1993; Gao et al., 2017; Xie et al., 2018; Khanal et al., 2020; Hu et al., 2022; Ji et al., 2022).

Considering the close spatial and temporal relationship between the Gyirong leucogranite and pegmatite, it is easy to assume that the pegmatite originated from the highly differentiated evolution of granites. However, if this happened, the tourmaline in pegmatite could display lighter δ11B values than that in leucogranite since the crystallization of tourmalines would result in depletion of 11B in the residual melt (Chakraborty, 2021). As the melt cools, B-rich fluid exsolution from the magma often occurs in the granite-pegmatite systems (e.g., Thomas et al., 2003). Accordingly, tourmaline crystallized from the residual melt to show a lower δ11B value (Liu et al., 2022). We have no conclusive evidence to confirm or deny the existence of hydrothermal tourmaline in the Gyirong pegmatite, which requires further investigation. In the present case, our measured boron isotope compositions of pegmatite (δ11B of −11.8 to −9.7‰) show slightly higher values than those of the leucogranite (δ11B of −12.1 to −11.2‰), which preclude the possibility of fractional crystallization (e.g., Rayleigh fractionation) as well as fluid exsolution (Ghosh et al., 2021). Such overlapping or similar B isotopic compositions in the granite-pegmatite system favor a genetic relationship between the Gyirong leucogranite and pegmatite (Montenegro et al., 2021). The Gyirong pegmatite displays high 87Sr/86Sr16Ma (∼0.762), 208Pb/204Pb16Ma (∼39.72), 207Pb/204Pb16Ma (∼15.79) and 206Pb/204Pb16Ma (∼19.6), and low εNd16Ma value of −16.0 (authors’ unpublished data). Their Sr-Nd-Pb isotopic signatures are consistent with those of the Gyirong leucogranite, suggesting that they have similar origins. Furthermore, the whole-rock geochemical data (authors’ unpublished data) indicate that the Gyirong pegmatite did not experience a high degree of differentiation. Combined with the typical peraluminous mineral assemblage (e.g., tourmaline, muscovite and garnet) of the Gyirong pegmatite, we thus propose that the Gyirong pegmatite was the product of crustal anatexis rather than formed vviathe highly differentiated evolution of the granite. The anatectic metamorphism was linked to crustal thinning (28–5 a) caused by the STDS within the Himalayan orogen (Harris and Massey, 1994; Wang et al., 2017; Ding et al., 2021; Ji et al., 2022).

6 Conclusion

Based on petrographic and geochemical studies conducted on tourmaline from the Gyirong pegmatite within the South Tibet Himalaya, we reached the following conclusions.

1) Mineralogical characteristics show that Gyirong pegmatite belongs to the peraluminous S-type pegmatite and contains abundant tourmaline. Two types of tourmalines (Tur-Ⅰ & Tur-Ⅱ) were identified in this contribution and they are all Fe-rich schorl with low Mg# ratios (0.22 –.45). The trace element concentrations of tourmaline are mainly controlled by melt composition.

2) Morphological and geochemical characteristics indicate that the tourmalines from the Gyirong pegmatite are magmatic in origin. Insignificant variations in tourmaline boron isotopic composition from −11.8 to −9.7‰ indicate that the Gyirong pegmatite was derived from the continental crust. And the crustal metapelitic rocks within the GHC were the most likely source components for the Gyirong pegmatite.

3) We hypothesize that the Gyirong pegmatite was the product of crustal anatexis rather than formed viathe highly differentiated evolution of the Gyirong leucogranite.

Data availability statement

The original contributions presented in the study are included in the article/supplementary material, further inquiries can be directed to the corresponding author.

Author contributions

QP and HC designed the project and helped to supervise this study. QP, FL, YZ, and YX conducted field investigations. QP, SM, and CL carried out EMPA and LA-ICP-MS analysis for major and trace element compositions. SM, CL, and SW are responsible for iin situboron isotope analysis. FL and JW assisted in data collection and analysis. All authors listed participated in the discussion and contributed to the writing of the manuscript.

Funding

This research received funding from the Second Tibetan Plateau Scientific Expedition and Research (SQ2019QZKK2203), the Key subject of Science and Technology Projects of Chinese Academy of Sciences (XDA19030303-02), the Sichuan Natural Science Foundation (2022NSFSC0410) and the National Natural Science Foundation of China (41802095).

Acknowledgments

We thank Kuidong Zhao for assistance in tourmaline boron isotope analysis. We also greatly appreciate the constructive comments and suggestions from the editor and three reviewers, which helped us considerably improve the paper.

Conflict of interest

The authors declare that the research was conducted in the absence of any commercial or financial relationships that could be construed as a potential conflict of interest.

Publisher’s Note

All claims expressed in this article are solely those of the authors and do not necessarily represent those of their affiliated organizations, or those of the publisher, the editors and the reviewers. Any product that may be evaluated in this article, or claim that may be made by its manufacturer, is not guaranteed or endorsed by the publisher.

Supplementary material

The Supplementary Material for this article can be found online at: https://www.frontiersin.org/articles/10.3389/feart.2022.1037727/full#supplementary-material

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Keywords: tourmaline, boron isotope, leucogranite, pegmatite, Tibet

Citation: Pei Q, Ma S, Li C, Liu F, Zhang Y, Xiao Y, Wang S, Wu J and Cao H (2023) In-situ boron isotope and chemical composition of tourmaline in the Gyirong pegmatite, southern Tibet: Implications for petrogenesis and magma source. Front. Earth Sci. 10:1037727. doi: 10.3389/feart.2022.1037727

Received: 06 September 2022; Accepted: 01 November 2022;
Published: 12 January 2023.

Edited by:

Stanislaw Mazur, Institute of Geological Sciences, Polish Academy of Sciences, Poland

Reviewed by:

Wang Fangyue, Hefei University of Technology, China
Yi-Xiang Chen, University of Science and Technology of China, China
Yongsheng He, China University of Geosciences, China

Copyright © 2023 Pei, Ma, Li, Liu, Zhang, Xiao, Wang, Wu and Cao. This is an open-access article distributed under the terms of the Creative Commons Attribution License (CC BY). The use, distribution or reproduction in other forums is permitted, provided the original author(s) and the copyright owner(s) are credited and that the original publication in this journal is cited, in accordance with accepted academic practice. No use, distribution or reproduction is permitted which does not comply with these terms.

*Correspondence: Huawen Cao, Y2FvaHVhd2VuMTk4OEAxMjYuY29t

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