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Article

Petrogenesis of Early Cretaceous High-Mg Adakitic Pluton in the North Lhasa Block, Tibet Plateau: Implications for the Tethyan Orogeny

by
Qian-Ru Xiao
1,
Yong-Feng Wei
1,2,*,
Zhong-Yuan Liu
1,
Fu-Hao Xiong
1,
Lei Fan
1,
Jian-Xin Wu
1 and
Han Zhao
1
1
College of Earth Sciences, Chengdu University of Technology, Chengdu 610059, China
2
Regional Geological Survey Team, Sichuan Geology and Mineral Bureau, Shuangliu 610213, China
*
Author to whom correspondence should be addressed.
Minerals 2022, 12(2), 213; https://doi.org/10.3390/min12020213
Submission received: 12 December 2021 / Revised: 2 February 2022 / Accepted: 3 February 2022 / Published: 7 February 2022
(This article belongs to the Special Issue Composition, Geochronology and Geodynamic Implications of Igneous Rock)
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Abstract

:
Late Mesozoic igneous rocks from the north Lhasa block record the Neo-Tethyan orogeny in the southern Tibet Plateau. This study presents geochronological and geochemical data of Bieruozecuo quartz diorite pluton in the northern margin of the Lhasa block to constrain its petrogenesis and tectonic implications. The LA–ICP–MS zircon U–Pb geochronology of quartz diorites shows that the emplacement occurs at ca. 114–116 Ma, belonging to the products of Early Cretaceous magmatic activities. The high concentrations of TiO2, MgO, and MnO, together with SiO2 vs. K2O and A/NK vs. A/CNK diagrams, all suggest that the Bieruozecuo quartz diorites are meta-aluminous and high-potassium calc-alkaline rocks. Their high Sr and low Y and Yb contents, as well as high Sr/Y and La/Yb ratios, are consistent with the typical adakitic rocks. The REE patterns show a large distribution of compositions, which have LREE, while HREE are buffered, along with large ratios of (La/Yb)N, as well as high values of K2O/Na2O, Mg#, Cr, and Ni, all of which imply the partial melting of a delaminated lower crust, without obvious fractional crystallization during the magma ascending and emplacement. This study suggests that, with the closure of the Bangonghu–Nujiang Tethys Ocean Basin, the post-collisional extension of the north Lhasa block will have started no later than ca. 114–116 Ma. Combined with the previous studies, our new data demonstrates that the partial melting of the delaminated lower crust, in a post-collisional setting, may be the main mechanism responsible for the ca. 116–82 Ma adakitic magmatism in the north Lhasa block.

1. Introduction

The Lhasa block in the southern Tibet Plateau is characterized by the presence of large-scale Late Mesozoic–Cenozoic magmatic rocks, which records the magmatic–tectonic evolution and geodynamic processes during the oceanic lithosphere subduction and collision/accretion of terranes [1,2,3,4,5,6]. Hence, unraveling their petrogenesis is the key to understanding the tectonic evolution and Neo-Tethyan orogeny. Despite many studies that have been carried out on the Late Mesozoic magmatic rocks in the Lhasa block, the models, proposed so far on their petrogenesis and dynamic background, are still controversial. Some studies propose that the Late Mesozoic magmatic activity in the Lhasa block was formed during the northward subduction of the southern Yarlung Zangbo Neo-Tethyan -oceanic slab [4,7,8]. In contrast, others believe that their petrogenesis is closely related to the southward oceanic lithosphere subduction or terrane collision during the Northern Bangong Hu-Nujiang Tethys orogeny [2,3,9,10]. Meanwhile, previously published studies on the magma source of Late Mesozoic magmatic rocks in the Lhasa block are not consistent, suggesting different models, including remelting of the thickened lower crust in a collisional setting [7] and partial melting of Neo-Tethyan oceanic crust [2]. Therefore, it is necessary to continue to study the petrogenesis and tectonic setting of the Late Mesozoic magmatic rocks in the Lhasa block, to get a better understanding the Neo-Tethyan orogeny.
In this contribution, we present studies on the petrology, petrography, LA–ICP–MS zircon U–Pb chronology, and whole-rock geochemistry of one Early Cretaceous quartz diorite pluton in the northern Lhasa block. Combined with published data of the other Late Mesozoic coeval magmatic rocks in northern and central Tibet, we discuss the melt sources and magmatic evolution processes, as well as their tectonic implications on the Neo-Tethyan orogeny in the Lhasa block, southern Tibet.

2. Geological Setting and Petrography

The Tibet Plateau, located in the eastern part of the Tethys tectonic domain, is a key area for studying the geodynamic processes of oceanic lithosphere subduction and collision of the Tethys terranes. Multiple Tethyan subductions and accretion orogenic processes occurred in Tibet Plateau, including the Early Paleozoic Proto-Tethys, Carboniferous–Triassic Paleo-Tethys, and Mesozoic–Cenozoic Neo-Tethys orogenies [11,12,13,14,15]. The Lhasa block is located in the southern Tibet Plateau, which is bound by the Yarlung Zangbo Neo-Tethyan Tethyan suture zone (IYZSZ) to the south and northern Bangonghu–Nujiang suture zone (BNSZ) to the north. Taking the Lobadui Milashan fault (LMF) and Shiquanhe-Namucuo ophiolite melange belt (SNMZ) as the boundaries, the Lhasa block is subdivided into the north Lhasa block (NL), central Lhasa block (CL), and south Lhasa block (SL) (Figure 1a). Mesozoic and Cenozoic magmatic rocks are the dominant rocks in the entire Lhasa block. Triassic–Cretaceous magmatic rocks, forming a large-scale Gandeses batholith belt, occur as the dominant rocks, only in the south Lhasa block, whereas the Late Jurassic/Early Cretaceous sedimentary strata, Zenong Group volcanic rocks, and Early Cretaceous intrusive rocks are widely exposed in the central and north Lhasa blocks [8,16,17] (Figure 1b).
The Bieruozecuo quartz diorite pluton is located in the transitional part of the central and north Lhasa blocks. This area is characterized by the development of Jurassic–Cretaceous volcanic sedimentary strata and a large number of intermediate-acid intrusive rocks (Figure 1b). The Early Cretaceous Bieruozecuo quartz diorite pluton is irregular or nearly oval in form, emplaced into the Early Cretaceous Shishenla and Duoni formations, with the acreage for a single mass rock of 10–25 km2. The investigated intrusion is about 19 km2. The petrographic observation of the outer rim of the pluton provides good evidence for the thermal contact metamorphism, including hornfelsification, silicification, and marbleization. The quartz diorite is a greyish–green color and displays a fine-grained texture. Plagioclase (~50%) is the most abundant mineral, followed by alkaline feldspar (~18%), quartz (~15%), hornblende (~9%), and biotite (~4%). The plagioclase group of minerals consists of oligoclase and andesine, in the form of subhedral crystals, with a diameter of 0.5–1.6 mm. The euhedral growth zoning was generally observed in andesine. The main variety of alkaline feldspar is orthoclase. Most of the orthoclase grains are subhedral to anhedral. The quartz is heteromorphic. Alkali feldspar has xenomorphic granular structure. Zircon, apatite, magnetite, and sphene are rare, and other minerals are present only in trace amounts (Figure 2). The alterations cannot be observed in the fresh, thin sections of the samples.

3. Samples and Methods

Two samples of the Bieruozecuo quartz diorite were collected for zircon geochronology analysis, and sample P11(20) was collected from the inner of the pluton (82°55′41″ E, 32°20′04″ N), while sample P11(46) was collected from the rim of the pluton (82°56′22″ E, 32°19′53″ N). Prior to LA–ICP–MS analyses, the samples were pretreated, crushed, and sorted at the Huayang Rock and Mineral Testing Center of Sichuan, China. Zircon concentrates were mounted in epoxy mounts, which were then carefully polished. All zircon grains were observed under a microscope, with transmitted and reflected light, as well as with cathodoluminescence (CL) imaging to confirm high transparency and avoid measuring spots with inclusions or/and cracks. Measurements of U and Pb isotopes were carried out using LA–ICP–MS, equipped with an ArF 193 nm UV excimer laser, at the State Key Laboratory of Dynamics, Northwestern University, China. The single pulse energy was set to 220 mJ, and the maximum laser repetition rate was 20 Hz. A fluence of 50 Jcm−2 was chosen, with a beam diameter of around 60 μm. The standard zircon 91500 was used as an external standard for the calibration of the Pb–U. For quality assurance, the standard was analyzed at the end of the analytical run, after the measurement of six samples. Further data evaluation has been performed by using ISOPLOT and SQUID software. More detailed analytical procedures are described by [23].
The bulk compositions (major, trace, and rare earth elements) of samples were performed using an Axios X-ray fluorescence spectrometer, X Series 2 plasma-mass spectrometer, IRIS Intripid2XSP ICP full spectrum direct-reading spectrometer, zeenit600 graphite furnace atomic absorption spectrometer, and AFS-230E atomic fluorescence spectrometer at Zhongnan Mineral Resources Supervision and Testing Center. The analytical uncertainties were less than 5%.

4. Results

4.1. U–Pb Zircon Age

U–Pb zircon data are shown in Table 1. Zircon grains from sample P11(20) and sample P11(46) are mostly euhedral to subhedral and 95 to 220 μm in length. The zircons in the two samples show similar zircon texture; both the inherited cores and magmatic rims of the zircons were observed in the two studied samples. Most zircon grains are transparent and show euhedral concentric zoning under CL images (Figure 3). A total of 48 analyses of zircon grains were obtained (Table 1). The concordance curves of the quartz diorite in sample P11(20) are shown in Figure 4a. The concordant age within analytical errors is 114.36.1 ± 0.43 Ma (MSWD = 0.44), yielding a weighted mean 206Pb/238U age of 114.52 ± 0.91 Ma (mean squared weighted deviation (MSWD) = 0.87). The concordance age of zircons in sample P11(46) is shown in Figure 4b, and its concordance age is 116.7 ± 0.70 Ma (MSWD =7.7), with a weighted mean 206Pb/238U age of 116.6 ± 1.4 Ma (MSWD = 0.95). Therefore, the crystallization age of the Bieruozecuo quartz diorite is 116 ~ 114 Ma (Early Cretaceous).

4.2. Bulk Geochemical Characteristics

The major and trace element compositions of the representative samples (N = 15) from the Bieruozecuo pluton are presented in Table 2. The studied samples have low contents of LOI, indicating that the samples are fresh, and the geochemical data can be used to efficiently constain their petregenesis. They contain higher Al2O3 (14.72–15.75 wt.%), and Na2O (3.27–4.02 wt.%), but the lower concentrations of MgO (1.60–2.67 wt.%) and TiO2 (0.45–0.71 wt.%). ALK, Na2O/K2O ratios, and A/CNK ratios are 6.50–7.26%, 0.95–1.49, 0.89–0.93, respectively. The studied rocks show high-K calc-alkaline affinity (Figure 5a) and fall into the meta-aluminous field in the A/NK–A/CNK diagram (Figure 5b). The Bieruozecuo quartz diorites show a narrow range in SiO2, from 64.07 to 68.32 wt.%, and all samples are plotted in the granodiorite field on the total alkalis-silica diagram (Figure 6a). The Th vs. Co diagram suggests that all samples are depleted in Co and Th and plot in the calc-alkaline field (Figure 6b).
The trace and REE composition of the Bieruozecuo quartz diorites are consistent with previously reported Cretaceous adakitic rocks in the Lhasa block (Figure 7), suggesting a possible genetic relationship. All the rocks are characterized by the enrichment of light rare earth elements (LREEs) and depletion of heavy rare earth elements (HREEs) [(La/Yb)N =9.08–22.99, Figure 7a]. The REE contents of the quartz monzonite are much lower than the mean value of the upper crust (210.10 ppm) [27] and display slightly negative Eu anomalies (Eu/Eu* = 0.66–0.94). All rocks exhibit overall enriched large ion lithophile elements (LILE, e.g., Rb and K) and LREE, and are depleted in high field strength elements (HFSE, e.g., Nb, Ti, and P; Figure 7b). The samples show marked Nb and Ti negative anomalies. Nb negative anomaly is a feature of the continental crust [28], indicating crustal materials are involved in the magmatic source [29] of the Bieruozecuo quartz diorites. These plutonic rocks also show high Sr content (296.00–574.00 ppm), high Sr/Y ratio (17.94–47.76), low Y content (9.85–17.60 ppm) and Yb content (0.98–2.19 ppm), which are comparable with adakitic composition (Figure 8).

5. Discussion

5.1. Geochemical Classification

The “adakite” was first proposed by [34], which is considered to be one type of intermediate-felsic igneous rock with special geochemical characteristics. These adakite rocks usually have the following characteristic: SiO2 > 56 wt.%, Al2O3 > 15 wt.%, MgO < 3 wt.%, Sr/Y ratio (>20, depleted in Y (<18 ppm) and HREE (Yb < 19 ppm), high Sr (>400 ppm or 300 ppm) (positive or without Eu), and Sr anomalies (depleted in high field strength elements) [33,35,36,37,38]. The generation of adakites was initially proposed to be related to the partial melting of the young and hot subducted oceanic lithosphere under eclogite facies condition [34,38], although their origin is much more complex. Many studies show that some igneous rocks with adakite-like geochemical affinities are actually unrelated to slab melting, and they proposed a broad definition of adakites, compassing a wide range of island arc magmatic rocks and collision-related rocks [36,39]. Thus, the term “adakitic” is proposed to distinguish rocks with adakite-like geochemical features to those rocks formed by slab melting [39,40,41]. At present, many rocks are classified as adakitic, and many studies show that adakitic rocks and typical adakites can be formed in several geodynamic settings, including oceanic subduction, syn-collision, post-collision extension, and within-plate rifting [35,36,37,38,39,40,41]; thus, adakitic rocks and typical adakites are one key probe to study the tectonic evolution of paleo-orogenic belt.
The studied Bieruozecuo quartz diorites samples have high contents of SiO2 (64.07–68.32 wt.%) and Al2O3 (14.72–15.75 wt.%), with high Sr/Y (21.18–47.76) and La/Yb (13.78–34.90), as well as low MgO (1.60–2.67 wt.%), Y (9.850–16.500 ppm), and Yb (0.980–2.190 ppm). The geochemical discrimination diagrams of (La/Yb)N vs. YbN and Sr/Y vs. Y show that the studied Bieruozecuo quartz diorites exhibits typical adakitic geochemical affinities (Figure 8). Previous studies have reported several ca. 90~82 Ma adakitic plutons in the north and central Lhasa blocks. The Bieruozecuo quartz diorites studied in this paper has similar geochemical composition and crystallization age to those reported adakitic plutons (Figure 5, Figure 6, Figure 7 and Figure 8), suggesting that the adakitic magmatic activity in the north and central Lhasa blocks may last from 116 Ma to 82 Ma.

5.2. Petrogenesis

Numerous studies show that the petrogenesis of intermediate igneous rocks is complex and various, including the mixing of mantle-derived mafic magma and granitic magma, partial melting of mafic crust, and AFC of mantle-derived magma [42,43,44]. The Early Cretaceous Bieruzecuo quartz diorites are meta-aluminous high-K calc-alkaline plutonic rock, with high K2O (average content of 3.13 wt.%) and low CaO (average content of 4.16 wt.%), indicating that the magma mainly originated from the partial melting of continental crust [45]. The trace elements of Cr (20.8–63.5 ppm, with an average of 40.9 ppm), Ni (10.4–32.0 ppm, with an average of 21.4 ppm), and Co (9.3–19.2 ppm, with an average of 16.1 ppm) are very close to the continental crust, and the La/Nb ratios (2.38–3.74) are significantly different from mantle-derived magma (La/Nb ≈ 0.96) [30]. Nb and Ta are stable in the process of erosion and metamorphism and have the characteristics of tracing magma origin [46,47]. The Nb/Ta ratios of the Late Early Cretaceous quartz diorite is 9.88–13.54, which is close to the average crustal value (12–13) but significantly lower than the mantle magma value (17 ± 1, [48]). The Nd/Th ratios (1.09–3.46) are consistent with the Nd/Th ratio for the crustal source (≈3) and significantly lower than that of the mantle source (>15) [49], suggesting that the magma may not derive from partial melting of mantle peridotite or separation and crystallization of basaltic magma [50], but from partial melting of continental crustal rocks [51]. The Ti/Zr ratios (21.23–86.26, average 44.97) and Ti/Y ratios (193.94–349.06, average 272.02) are slightly higher than those of continental crust rocks (Ti/Zr < 30, Ti/Y < 200) [52], which may be related to the presence of garnet residues in the source [53] and resemblance with the high La/Yb and Sr/Y ratios of rocks.
The Bieruzecuo quartz diorites have the geochemical characteristics of adakitic rocks. According to previous works, the genesis of adakitic rocks may be due to: (1) partial melting of young oceanic crust [34,40,54,55,56]; (2) fractional crystallization of primitive basaltic magma and assimilation with crustal materials, i.e., the AFC model [34,57]; (3) magma mixing between felsic and mafic magmas [58,59]; (4) partial melting of a thickened lower crust or delaminated lower crust under high-temperature conditions [38,60,61]; and (5) partial melting of subducted continental crust [38,61]. The Bieruzecuo adakitic rocks have high SiO2 content (65–69.32 wt.%); there is no obvious Eu anomaly in the REE patterns, and the rocks do not show assemblages of gabbro–diorite–granodiorite, which precludes the AFC model of the geochemical trends in Rb/Nd vs. Rb, and the La/Sm vs. Sm diagrams do not support the AFC model (Figure 9). As mentioned above, the Bieruzecuo quartz diorites are mainly derived from the partial melting of continental crust materials, which is consistent with their high ratios of K2O/Na2O (Figure 10A).
Based on the geochemical characteristics of the Bieruozecuo adakites, we propose that the studied adakites may be the product of partial melting of the delaminated lower crust. In general, the adakite formed by partial melting of the delaminated lower crust is easy to modify via the addition of mantle materials during magma ascending and emplacement, resulting in high MgO, Cr, and Ni contents in the rocks [21,40,64,65]. The studied adakites have high Mg#, Cr (20.80–63.50 ppm), and Ni (10.40–32.00 ppm), resembling the rocks that derived from the melting of the delaminated lower crust or subducted oceanic crust, but differ from the adakite formed by partial melting of the thickened lower crust (Figure 10). However, the geochemical features of the high ratios of K2O/Na2O and low ratios of CaO/Al2O3 strongly exclude the model of the melting of the subducted oceanic crust (Figure 10a). Thus, the melting of the delaminated continental lower crust is proposed to be the most possible model for the origin of the studied adakitic rocks in the northern Lhasa block.

5.3. Tectonic Setting and Geological Significance

Previous studies show that the Tethyan ophiolites, along the BNSZ, are overlain unconformably by clastic sequences of the Lower Cretaceous Dongqiao Formation (ca. 130−118 Ma) [7,9,14]. This relationship suggests that the BNSZ ocean basin was closed in the Early Cretaceous, and collision between north Lhasa and Qiangtang blocks occurred at the Early Cretaceous [69]. However, the transition from syn-collision to post-collisional extension is still unclear, resulting in the discussion of the geodynamic setting of the Cretaceous magmatism in the Lhasa block.
As shown in Figure 1, the Early Cretaceous is an important magmatic activity period in the Lhasa block, which occurs almost simultaneously in the south (ca. 100–137 Ma), the central (ca. 95–145 Ma), and north Lhasa blocks (ca. 110–133 Ma). The peak period of magmatic activity is concentrated in ca. 120–110 Ma [2,70], and the Bieruozecuo adakitic quartz diorite is the product of this peak magmatism. Recent studies have shown that the collision between the Lhasa and Qiangtang blocks in Early Cretaceous may result in the thickening of the continental crust of the north Lhasa block [7,69]. As shown in Figure 11, The Bieruzecuo quartz diorites mostly fall in the field of volcanic arc granites (VAG). The ca. 116–114 Ma Bieruozecuo quartz diorite has the geochemical characteristics identical to magmas originating from delaminated crust, which indicates, once again, that the large-scale adakitic magmatism in the northern and central Lhasa blocks is the response to the delamination of continental lower crust, as well as the tectonic transition from syn-collision to post-collisional extension, occurring at ca. 120–110 Ma.
Therefore, we propose that the Bieruzecuo pluton is the product of post-collisional extension and derived from the partial melting of the delaminated continental lower crust. Continental crust delamination may be responsible for the post-collisional extension, which is an important mechanism to the ca. 120–110 Ma adakitic magmatism flare-up event in the Lhasa block (Figure 12).

6. Conclusions

(1) LA–ICP–MS zircon U–Pb geochronology shows that the Bieruozecuo quartz diorite from north Lhasa block crystallized at ca. 116–114 Ma (Early Cretaceous magmatic event).
(2) The Bieruozecuo quartz diorite was enriched in Al2O3 and Na2O, but relatively depleted in TiO2, MgO, and MnO, which may be included in the quasi-alumina high-K calc-alkaline series. They display the geochemical characteristics typical of adakitic rocks, with high Sr, low Y and Yb, as well as high Sr/Y and La/Yb ratios. The high Mg#, K2O/Na2O ratios, Cr, and Ni contents indicate that these adaktic rocks probably derived from the partial melting of the delaminated continental crust, without obvious fractional crystallization during magma ascending and emplacement.
(3) The Early Cretaceous flare-up event of adaktic magmatism of the Lhasa block is a response to the delamination of continental crust, as well as the transition from syn-collision to post-collisional extension at ca. 120–110 Ma.

Author Contributions

Conceptualization, Q.-R.X. and Y.-F.W.; methodology, F.-H.X.; software, Z.-Y.L.; formal analysis, Q.-R.X., Y.-F.W., and Z.-Y.L.; investigation, Y.-F.W. and Z.-Y.L.; resources, Y.-F.W.; data curation, Q.-R.X. and J.-X.W.; writing—original draft preparation, Q.-R.X.; writing—review and editing, F.-H.X. and L.F.; visualization, Q.-R.X., L.F., and H.Z.; project administration, Y.-F.W.; funding acquisition, Y.-F.W. All authors have read and agreed to the published version of the manuscript.

Funding

This work was supported by the project, named Geological and Mineral Survey, of Gzezao Bieruozuo, 1:50,000, in Tibet (I44E022020, I44E022021, I44E023020, I44E023021).

Data Availability Statement

The data supporting reported results can be found in the text.

Acknowledgments

We gratefully acknowledge the research members, who are Zeng Wei, Shao Zhiwei, Yu Xuhui, Tang Guangcheng, Zhu Guobao, etc., for their cooperation and help.

Conflicts of Interest

The authors declare no conflict of interest.

References

  1. Mo, X.X.; Dong, G.C.; Zhao, Z.D.; Zhou, S.; Wang, L.L.; Qiu, R.Z.; Zhang, F.Q. Spatial and Temporal Distribution and Characteristics of Granitoids in the Gangdese, Tibet and Implication for Crustal Growth and Evolution. Geol. J. China Univ. 2005, 11, 281–290. [Google Scholar]
  2. Zhu, D.C.; Pan, G.T.; Mo, X.X.; Wang, L.Q.; Liao, Z.L.; Zhao, Z.D.; Dong, G.C.; Zhou, C.Y. Late Jurassic-Early Cretaceous geodynamic setting in middle-northern Gandese: New insights from volcanic rocks. Acta Petrol. Sin. 2006, 22, 534–546. [Google Scholar]
  3. Zhu, D.C.; Pan, G.T.; Wang, L.Q.; Mo, X.X.; Zhao, Z.D.; Zhou, C.Y.; Liao, Z.L.; Dong, G.C.; Yuan, S.H. Spatial-temporal distribution and tectonic setting of Jurassic magmatism in the Gangdise belt, Tibet, China. Geol. Bull. China 2008, 4, 458–468. [Google Scholar]
  4. Ma, G.L.; Yue, Y.H. Cretaceous volcanic rocks in northern Lhasa block: Constraints on the tectonic evolution of the Gangdese arc. Acta Petrol. Mineral. 2010, 29, 525–538. (In Chinese) [Google Scholar]
  5. Wu, Z.H.; Wu, X.W.; Zhao, Z.; Lu, L.; Ye, P.S.; Zhang, Y.L. Shrimp U-Pb isotopic dating of the Late Cretaceous volcanic rocks and its chronological constraint on the red-beds in southern Qiangtang Block. Acta Geosci. Sin. 2014, 35, 567–572. (In Chinese) [Google Scholar]
  6. Zhang, S.; Shi, H.F.; Hao, H.J.; Li, D.W.; Lin, Y.; Feng, M.X. Geochronology, geochemistry and tectonic significance of Late Cretaceous adakites in Bangong Lake, Tibet. Earth Sci. (J. China Univ. Geosci.) 2014, 39, 509–524, (In Chinese with English abstract). [Google Scholar]
  7. Kapp, P.; DeCelles, P.G.; Gehrels, G.E.; Heizier, M.; Ding, L. Geological records of the Lhasa-Qiangtang and Indo-Asian collisions in the Nima area of central Tibet. Geol. Soc. Am. Bull. 2007, 119, 917–933. [Google Scholar] [CrossRef]
  8. Wen, D.R.; Liu, D.Y.; Chung, S.L.; Chu, M.F.; Ji, J.Q.; Zhang, Q.; Song, B.; Lee, T.Y.; Yeh, M.W.; Lo, C.H. Zircon SHRIMP U-Pb ages of the Gangdese Batholith and implications for Neotethyan subduction in southern Tibet. Chem. Geol. 2008, 252, 191–201. [Google Scholar] [CrossRef]
  9. Zhu, D.C.; Mo, X.X.; Niu, Y.L.; Zhao, Z.D.; Wang, L.Q.; Liu, Y.S.; Wu, F.Y. Geochemical investigation of Early Cretaceous igneous rocks along an east−west traverse throughout the central Lhasa Terrane, Tibet. Chem. Geol. 2009, 268, 298–312. [Google Scholar] [CrossRef]
  10. Zhu, D.C.; Zhao, Z.D.; Niu, Y.L.; Mo, X.X.; Chung, S.L.; Hou, Z.Q.; Wu, F.Y. The Lhasa Terrane: Record of a microcontinent and its histories of drift and growth. Earth Planet. Sci. Lett. 2011, 301, 241–255. [Google Scholar] [CrossRef]
  11. Powell, C.M.; Conaghan, P.J. Plate tectonics and the Himalayas. Earth Planetaru Sci. Lett. 1973, 20, 1–12. [Google Scholar] [CrossRef]
  12. Molnar, P.; Tapponnier, P. Cenozoic tectonice of Asia: Effects of a continental collision: Features of recent continental tectonics in Asia can be interpreted as results of the India-Eurasia collision. Science 1975, 189, 419–426. [Google Scholar] [CrossRef] [PubMed]
  13. Pan, G.T.; Chen, Z.L.; Li, X.Z.; Yan, Y.J.; Xu, X.S.; Xu, Q.; Jiang, X.S.; Wu, Y.L.; Luo, J.N.; Zhu, T.X.; et al. Geological-Tectonic Evolution in the Eastern Tethys; Grological Publishing House: Beijing, China, 1997; pp. 1–218. (In Chinese) [Google Scholar]
  14. Yin, A.; Harrison, T.M. Geologic evolution of the Himalayan-Tibetan Orogen. Annu. Rev. Earth Planet. Sci. 2000, 28, 211–280. [Google Scholar] [CrossRef] [Green Version]
  15. Xu, Z.Q.; Yang, J.S.; Li, W.C.; Li, H.Q.; Cai, Z.H.; Yan, Z.; Ma, C.Q. Paleo- Tethys system and accretionary orogeny in the Tibet Plateau. Acta Petrol. Sin. 2013, 29, 1847–1860, (In Chinese with English abstract). [Google Scholar]
  16. Mo, X.X.; Niu, Y.L.; Dong, G.C.; Zhao, Z.D.; Hou, Z.Q.; Zhou, S.; Ke, S. Contribution of syncollisional felsic magmatism to continental crus growth: A case study of the Paleogene Linzizong volcanic succession in southern Tibet. Chem. Geol. 2008, 250, 49–67. [Google Scholar] [CrossRef]
  17. Wang, Z.Z.; Liu, D.; Zhao, Z.D.; Yan, J.J.; Shi, Q.S.; Mo, X.X. The Sangri highly fractionated I-type granites in southern Gangdese: Petrogenesis and dynamic implication. Acta Petrol. Sin. 2017, 22, 2479–2493. (In Chinese) [Google Scholar]
  18. Wu, F.Y.; Ji, W.Q.; Liu, C.Z.; Chung, S.L. Detrital zircon UePb and Hf isotopicdata from the Xigaze fore-arc basin: Constraints on Transhimalayan. Chem. Geol. 2010, 271, 13–25. [Google Scholar] [CrossRef]
  19. Huang, S.H.; Chen, J.L.; Zen, Y.C.; Tan, R.Y.; Huang, T.T.; Liu, X.J. Geochemical characteristics of Early Cretaceous magmatic rocks in the northwestern part of the Lhasa Block and indications of early crustal growth of the southern plateau. Geochimica 2020, 49, 21–35. [Google Scholar]
  20. Sun, G.Y.; Hu, X.M.; Zhu, D.C.; Hong, W.T.; Wang, J.G.; Wang, Q. Thickened juvenile lower crust-derived ~90 Ma adakitic rocks in the central Lhasa terrane, Tibet. Lithos 2015, 224, 225–239. [Google Scholar] [CrossRef]
  21. Yu, H.X.; Chen, J.L.; Xu, J.F.; Wang, B.D.; Wu, J.B.; Liang, H.Y. Geochemistry and origin of Late Cretaceous(~90 Ma) ore-bearing porphyry of Balazha in mid-northern Lhasa terrane, Tibet. Acta Petrol. Sin. 2011, 27, 2011–2022, (In Chinese with English abstract). [Google Scholar]
  22. Dong, Y.C.; Wang, M.; Xie, C.M.; Yu, Y.P.; Hao, Y.J. Genesis and tectonic indication of the Late Cretaceous adakite rocks in the Lamunale area, Nima County, Tibet. Acta Petrol. Sin. 2020, 36, 426–442. [Google Scholar]
  23. Hou, K.J.; Li, Y.H.; Tian, Y.R. In situ U-Pb zircon dating using laser ablation-multi ion counting-ICP-MS. Miner. Depos. 2009, 28, 481–492. [Google Scholar]
  24. Zhang, X.F.; Li, Y.G.; Cao, X.M.; Qu, X.M.; Xin, H.B.; Wang, J.; Du, D.D. LA-ICP-MS zircon U-Pb age and geochemical characteristics of the acid intrusive rocks in the western part of Bangong Lake-Nujiang River suture zone. Geol. Bull. CHN. 2014, 33, 984–994, (In Chinese with English abstract). [Google Scholar]
  25. Middlemost, E.A.K. Naming materials in the magma/igneous rock system. Earth-Sci. Rev. 1994, 37, 215–224. [Google Scholar] [CrossRef]
  26. Hastie, A.R.; Kerr, A.C.; Pearce, J.A.; Mitchell, S.F. Classification of altered volcanic island arc rocks using immobile trace elements: Development of the Th-Co discrimination diagram. J. Petrol. 2007, 48, 2341–2357. [Google Scholar] [CrossRef] [Green Version]
  27. Maniar, P.D.; Piccoli, P.M. Tectonic discrimination of granitoids. Geol. Soc. Am. Bull. 1989, 101, 635–643. [Google Scholar] [CrossRef]
  28. Jiang, Y.H.; Yang, W.Z. Geochemistry of early Yanshanian granitoids and its tectonic significance in the western Qinghai-Tibet plateau. Mineral. Petrol. 2000, 20, 74–79. [Google Scholar]
  29. Zhong, H.M.; Tong, J.S.; Lu, R.K.; Xia, J. Geochemical characteristics and tectonic setting of peraluminous granite in the Songxi area, Rutog County, Tibet, China. Geol. Bull. China 2006, 25, 183–188. [Google Scholar]
  30. Sun, S.S.; McDonough, W.F. Chemical and isotopic systematics of oceanic basalts: Implications for mantle composition and processes. In Magmatism in Occean Basins; Sander, A.D., Norry, M.H., Eds.; Geological Society of London Special Publications: London, UK, 1989; Volume 42, pp. 313–345. [Google Scholar]
  31. Taylor, S.R.; McLennan, S.M. The Continental Crust: Its Composition and Evolution; U.S. Department of Energy: Washington, DC, USA, 1985. [Google Scholar]
  32. Drummond, M.S.; Defant, M.J. A model for trondhjemite–tonalite–dacite genesis and crustal growth via slab melting: Archaean to modern comparisons. J. Geophys. Res. 1990, 95, 21503–21521. [Google Scholar] [CrossRef]
  33. Martin, H. Adakitic magmas: Modern analogues of Archaean granitoids. Lithos 1999, 46, 411–429. [Google Scholar] [CrossRef]
  34. Defant, M.J.; Drummond, M.S. Derivation of some modern are magmas by melting of young subducted lithosphere. Nature 1990, 327, 662–665. [Google Scholar] [CrossRef]
  35. Clemens, J. D S-type granitic magmas: Petrgenetic issues, models and evidene. Earth-Sci. Rev. 2003, 61, 1–18. [Google Scholar] [CrossRef]
  36. Castillo, P.R. An overview of adakite petrogenesis. Chin. Sci. Bull. 2006, 51, 257–268. [Google Scholar] [CrossRef]
  37. Castillo, P.R. Adakite petrogenesis. Lithos 2012, 134,135, 304–316. [Google Scholar] [CrossRef]
  38. Wang, Q.; Xu, J.F.; Zhao, Z.H.; Zi, F.; Tang, G.J.; Jia, X.H.; Jiang, Z.Q. Tectonic setting and associated rock suites of adakitc rocks. Bull. Mineral. Petrol. Geochem. 2008, 27, 344–350. (In Chinese) [Google Scholar]
  39. Moyen, J.F. High Sr/Y and La/Yb ratios: The meaning of the “adakitic signature”. Lithos 2009, 112, 556–574. [Google Scholar] [CrossRef]
  40. Martin, H.; Smithies, R.H.; Rapp, R.; Moyen, J.F.; Champion, D. An overview of adakite, tonalite-trondhjemite-granodiorite(TTG), and sanukitoid: Relationships and some implications for crustal evolution. Lithos 2005, 79, 1–24. [Google Scholar] [CrossRef]
  41. Xu, J.F.; Wu, J.B.; Wang, Q.; Chen, J.L.; Cao, K. Research advances of adakites and adakitic rocks in China. Bull. Mineral. Petrol. Geochem. 2014, 33, 6–13, (In Chinese with English abstract). [Google Scholar]
  42. Arnaud, N.O.; Vidal, P.H.; Tapponnier, P.; Matte, P.H.; Deng, W.M. The high K2O volcanism of northwestern Tibet: Geochemistry and tectonic implications. Earth Planet. Sci. Lett. 1992, 111, 351–367. [Google Scholar] [CrossRef]
  43. Thompson, A.B. Fertility of crusta1 rocks during anatexis. Trans. R. Soc. Edinburgh Earth Sci. 1996, 87, 1–10. [Google Scholar]
  44. Wang, Y.J.; Fan, W.M.; Guo, F. Geochemistry of early Mesozoic potassium-rich diorites-granodiorites in southeastern Hunan Province, South China: Petrogenesis and tectonic implications. Geochem. J. 2003, 37, 427–448. [Google Scholar] [CrossRef]
  45. Xiao, Q.H.; Deng, J.F.; Ma, D.Q.; Hong, D.W.; Mo, X.X.; Lu, X.X.; Li, Z.C.; Wang, X.W.; Ma, C.Q.; Wu, F.Y.; et al. Thinking and Method of Granite Research; Geological Publishing House: Beijing, China, 2002; pp. 12–20. [Google Scholar]
  46. Barth, M.G.; McDonough, W.; Rudnick, R. Tracking the budget of Nb and Ta in the continental crust. Chem. Geol. 2000, 165, 197–213. [Google Scholar] [CrossRef]
  47. Pfänder, J.A.; Münker, C.; Stracke, A.; Mezger, K. Nb/Ta and Zr/Hf in ocean island basalts - implications for crust-mantle differentiation and the fate of Niobium. Earth Planet. Sci. Lett. 2007, 254, 158–172. [Google Scholar] [CrossRef]
  48. Green, T.H. Significance of Nb/Ta as an indicator of geochemical processes in the crust-mantle system. Chem. Geol. 1995, 120, 347–359. [Google Scholar] [CrossRef]
  49. Bea, F.; Arzamastsev, A.; Montero, P.; Arzamastseva, L. Aonmalous alkaline rocks of Soustov, Kola:evidence of mantle-derived matasomatic fluids affecting crustal materials. Contrib. Min. Pet. 2001, 140, 554–566. [Google Scholar] [CrossRef]
  50. Li, S.G.; Nie, Y.H.; Zhen, S.G. Interaction between subducted continental crust and upper mantle—I. Geochemistry of major elements and trace elements in the synchromatic mafic-ultramafic rocks in Dabieshan. China Sci. 1997, 27, 488–493. [Google Scholar]
  51. Xie, L.; Dun, D.; Zhu, L.D.; Ni, M.C.; Yang, W.G.; Tao, G.; Li, C.; He, B.; He, Y. Zircon U-Pb geochronology, geochemistry and geological significance of the Zhaduding A-type granites in northern Gangdise, Tibet. Geol. China 2015, 42, 1214–1227. [Google Scholar]
  52. Wedepohl, K.H. The composition of the continental crust. Geochim. Cosmochim. Acta 1995, 59, 1217–1232. [Google Scholar] [CrossRef]
  53. Zhang, Z.Z.; Gu, L.X.; Wu, C.Z.; Zhai, J.P.; Wang, C.S.; Tang, J.H.; Xiao, E. Early-Middle Indosinian Weiya Quartz Diorite, Eastern Segment of the Middle Tianshan Mountains, NW China: Implications for Intra-Continent Subduction and Partial Melting of Juvenile Lower Crust. Acta Geol. Sin. 2011, 85, 1420–1434. [Google Scholar]
  54. Rapp, R.P.; Shimizu, N.; Norman, M.D.; Applegate, G.S. Reaction between slab-derived melts and peridotite in the mantle wedge: Experimental constraints at 3.8GPa. Chem. Geol. 1999, 160, 335–356. [Google Scholar] [CrossRef]
  55. Zhang, Z.M.; Zhao, G.C.; Santosh, M.; Wang, J.L.; Dong, X.; Shen, K. Late Cretaceous charnockite with adakitic affinities from the Gangdese batholith, shoutheastern Tibet: Evidence for Neo-Tethyan mid-ocean ridge subdution? Gondwana Res. 2010, 17, 615–631. [Google Scholar] [CrossRef]
  56. Eyuboglu, Y.; Chung, S.L.; Santosh, M.; Dudas, F.O.; Akaryali, E. Transition from shoshonitic to adakitic magmatism in the eastern Pontides, NE Turkey: Implications for slab window melting. Gondwana Res. 2011, 19, 413–429. [Google Scholar] [CrossRef]
  57. Kang, Z.Q.; Xu, J.F.; Wang, B.D.; Dong, Y.H.; Wang, S.Q.; Chen, J.L. Geochemistry of Cretaceous volcanic rocks of Duoni Formation in northern Lhasa Block: Discussion of tectonic setting. Earth Sci. (J. China Univ. Geosci.) 2009, 34, 89–104. (In Chinese) [Google Scholar]
  58. Guo, F.; Nakamuru, E.; Fan, W.; Kobayoshi, K.; Li, C. Generation of Palaeocene adakitic andesites by magma mixing in Yanji Area, NE China. J. Petrol. 2007, 48, 661–692. [Google Scholar] [CrossRef]
  59. Streck, M.J.; Leeman, W.P.; Chesley, J. High-magnesian andesite from Mount Shasta: A product of magma mixing and contamination, not a primitive mantle melt. Geology 2007, 35, 351–354. [Google Scholar] [CrossRef]
  60. Wang, Q.; McDermott, F.; Xu, J.F.; Bellon, H.; Zhu, Y.T. Cenozoic K-rich adakitic volcanic rocks in the Hohxil area, northern Tibet: Lower-crustal melting in an intracontinental setting. Geology 2005, 33, 465–468. [Google Scholar] [CrossRef] [Green Version]
  61. Lai, S.C.; Qin, J.F. Adakitic rocks derived from the partial melting of subducted continental crust: Evidence from the Eocene volcanic rocks in the northern Qiangtang block. Gondwana Res. 2013, 23, 812–824. [Google Scholar] [CrossRef]
  62. Schiano, P.; Monzier, M.; Eissen, J.P.; Martin, H.; Koga, K.T. Simple mixing as the major control of the evolution of volcanic suites in the Ecuadorian Andes. Contrib. Mineral. Petrol. 2010, 160, 297–312. [Google Scholar] [CrossRef]
  63. Wu, H.; Li, C.; Xu, M.J.; Li, X.K. Early cretaceous adakitic magmatism in the Dachagou Area, northern Ihasa terrane, Tibet: Implications for slab roll-back and subsequent slab break-off of the lithosphere of the Bangong-Nujiang Occan. J. Asian Earth Sci. 2015, 97, 51–66. [Google Scholar] [CrossRef]
  64. Smithies, R.H. The Archaean tonalite-tonalite-trondhjemite-granodiorite (TTG) series is ont an analogue of Cenozoic adakite. Earth Planetaru Sci. Lett. 2000, 182, 115–125. [Google Scholar] [CrossRef]
  65. Prouteau, G.; Scaillet, B.; Pichabant, M.; Maury, R. Evidence for mantle metasomatism by hydrous silicic melts derived from subducted oceanic crust. Nature 2001, 410, 197–200. [Google Scholar] [CrossRef] [PubMed] [Green Version]
  66. Chen, J.; Wei, J.; Fu, L.; Li, H.; Zhou, H.; Zhao, X.; Zhan, X.; Tan, J. Multiple sources of the Early Mesozoic Gouli batholith, Eastern Kunlun Orogenic Belt, northern Tibetan Plateau: Linking continental crustal growth with oceanic subduction. Lithos 2017, 292–293, 161–178. [Google Scholar] [CrossRef] [Green Version]
  67. Wang, Q.; Wyman, D.A.; Xu, J.F.; Zhao, Z.H.; Jian, P.; Xiong, X.L.; Bao, Z.W.; Li, C.F.; Bai, Z.H. Petrogenesis of Cretaceous adakitic and shoshonitic igneous rocks in the Luzong area, Anhui Province (eastern China): Implications for geodynamics and Cu-Au mineralization. Lithos 2006, 89, 424–446. [Google Scholar] [CrossRef]
  68. Huang, X.L.; Xu, Y.G.; Lan, J.B.; Yang, Q.J.; Luo, Z.Y. Neoproterozoic adakitic rocks from Mopanshan in the western Yangtze Craton: Partial melts of a thickened lower cnust. Lithos 2009, 1, 367–381. [Google Scholar] [CrossRef]
  69. Zhu, D.C.; Li, S.M.; Cawood, P.A.; Wang, Q.; Zhao, Z.D.; Liu, S.A.; Wang, L.Q. Assembly of the Lhasa and QIangtang terranes in central Tibet by divergent double subduction. Lithos 2016, 245, 7–17. [Google Scholar] [CrossRef] [Green Version]
  70. Zhu, D.C.; Pan, G.T.; Wang, L.Q.; Mo, X.X.; Zhao, Z.D.; Zhou, C.Y.; Liao, Z.L.; Dong, G.C.; Yuan, S.H. Tempo-spatial variations of Mesozoic magmatic rocks in the Gangdise belt, Tibet, China, with a discussion of geodynamic setting-related issues. Geol. Bull. China 2008, 27, 1535–1550. [Google Scholar]
  71. Pearce, J.A.; Harris, N.B.W.; Tindle, A.G. Trace-element discrimination diagrams for the tectonic interpretation of granitic-rocks. J. Petrol. 1984, 25, 956–983. [Google Scholar] [CrossRef] [Green Version]
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Figure 1. (a) Schematic tectonic framework of the Tibetan Plateau (modified from [18]); (b) tectonic framework of the Lhasa terrane, showing major tectonic subdivisions (modified from [19]; the correlation data are from [6,20,21,22]); (c) simplified geological map showing sample locations.
Figure 1. (a) Schematic tectonic framework of the Tibetan Plateau (modified from [18]); (b) tectonic framework of the Lhasa terrane, showing major tectonic subdivisions (modified from [19]; the correlation data are from [6,20,21,22]); (c) simplified geological map showing sample locations.
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Figure 2. (a) Field photograph showing the outcrops of Bieruozecuo quartz diorite adakitic rocks; (b) Microphotograph of the adakitic rock (sample P10-19); (c) Microphotograph of the adakitic rock (sample P11-6). Qtz = quartz; Pl = plagioclase; Afs = alkali feldspar; Bt = biotite; Hbl = hornblende; Mag = magnetite; Ap = apatite; Zrn = zircon; Chl = chlorite; Spn = sphene.
Figure 2. (a) Field photograph showing the outcrops of Bieruozecuo quartz diorite adakitic rocks; (b) Microphotograph of the adakitic rock (sample P10-19); (c) Microphotograph of the adakitic rock (sample P11-6). Qtz = quartz; Pl = plagioclase; Afs = alkali feldspar; Bt = biotite; Hbl = hornblende; Mag = magnetite; Ap = apatite; Zrn = zircon; Chl = chlorite; Spn = sphene.
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Figure 3. Representative cathodoluminescence images of zircon grains, analyzed from (a) sample 11(20) and (b) sample 11(46).
Figure 3. Representative cathodoluminescence images of zircon grains, analyzed from (a) sample 11(20) and (b) sample 11(46).
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Figure 4. Concordia diagram for zircons from the samples; the circles indicate the locations of LA–ICP–MS U–Pb dating spot analyses. (a) P11(20); (b) P11(46).
Figure 4. Concordia diagram for zircons from the samples; the circles indicate the locations of LA–ICP–MS U–Pb dating spot analyses. (a) P11(20); (b) P11(46).
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Figure 5. Diagram showing the variations in SiO2 and K2O concentrations of the Bieruozecuo quartz diorites and other Late Cretaceous igneous rocks within the central and northern Lhasa blocks, as well as the Miocene adakitic rocks in the southern Lhasa block. Data sources: ore-bearing porphyry in Balazha, [21]; adakitic rocks in Rutog, [24]; adakitic rocks in Azhang, [20]; adakitic rocks in Lamunale, [22].
Figure 5. Diagram showing the variations in SiO2 and K2O concentrations of the Bieruozecuo quartz diorites and other Late Cretaceous igneous rocks within the central and northern Lhasa blocks, as well as the Miocene adakitic rocks in the southern Lhasa block. Data sources: ore-bearing porphyry in Balazha, [21]; adakitic rocks in Rutog, [24]; adakitic rocks in Azhang, [20]; adakitic rocks in Lamunale, [22].
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Figure 6. (a) TAS classification and nomenclature diagram [25]; (b) Th–Co diagram showing sample compositional variations, after [26].
Figure 6. (a) TAS classification and nomenclature diagram [25]; (b) Th–Co diagram showing sample compositional variations, after [26].
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Figure 7. (a) Primitive mantle-normalized trace element spider diagrams (normalization values, after [30]); (b) chondrite-normalized REE patterns (normalization values, after [31]).
Figure 7. (a) Primitive mantle-normalized trace element spider diagrams (normalization values, after [30]); (b) chondrite-normalized REE patterns (normalization values, after [31]).
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Figure 8. (a) (La/Yb) N vs. YbN [32,33] and (b) plots of Sr/Y vs. Y [34].
Figure 8. (a) (La/Yb) N vs. YbN [32,33] and (b) plots of Sr/Y vs. Y [34].
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Figure 9. Discrimination diagrams of petrogenetic processes of the Bieruozecuo quartz diorites. (a) Rb/Nd s. Rb (after [62]); (b) La/Sm s. La (after [63]).
Figure 9. Discrimination diagrams of petrogenetic processes of the Bieruozecuo quartz diorites. (a) Rb/Nd s. Rb (after [62]); (b) La/Sm s. La (after [63]).
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Figure 10. Relationship diagram of geochemical characteristics of the major elements for the Bieruozecuo adakitic rocks. Diagram (a) after [66]; (b) after [67]; (c) after [68]; (d) after [68].
Figure 10. Relationship diagram of geochemical characteristics of the major elements for the Bieruozecuo adakitic rocks. Diagram (a) after [66]; (b) after [67]; (c) after [68]; (d) after [68].
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Figure 11. Bulk geochemical data for the Bieruozecuo adakitic rock from the Lhasa block, Tibet, plotted on the Pearce diagram [71].
Figure 11. Bulk geochemical data for the Bieruozecuo adakitic rock from the Lhasa block, Tibet, plotted on the Pearce diagram [71].
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Figure 12. Schematic illustration showing the geodynamic evolution of the central–northern Lhasa subterrane, at ca. 120–110 Ma. BNSZ = Bangong–Nujiang suture zone; SNMZ = Shiquan River–Nam Tso mélange zone; UC= upper crust; LC = lower crust; and SCLM = sub-continental lithospheric mantle.
Figure 12. Schematic illustration showing the geodynamic evolution of the central–northern Lhasa subterrane, at ca. 120–110 Ma. BNSZ = Bangong–Nujiang suture zone; SNMZ = Shiquan River–Nam Tso mélange zone; UC= upper crust; LC = lower crust; and SCLM = sub-continental lithospheric mantle.
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Table
Table 1. LA–ICP–MS zircon U–Pb ages for samples from the Bieruozecuo pluton in the Lhasa block, southern Tibet.
Table 1. LA–ICP–MS zircon U–Pb ages for samples from the Bieruozecuo pluton in the Lhasa block, southern Tibet.
Sample
Mark		Isotope RatioAge (Ma)
207Pb/206Pb207Pb/235U206Pb/238U208Pb/232Th207Pb/206Pb207Pb/235U206Pb/238U208Pb/232Th
Ratio1σRatio1σRatio1σRatio1σAge1σAge1σAge1σAge1σ
P11(20)-010.047 090.003 660.117 230.008 380.018 050.000 330.005 580.000 2153.3176.17112.67.62115.32.11112.44.28
P11(20)-020.054 600.003 840.136 790.008 670.018 160.000 330.006 130.000 25395.9150.5130.27.751162.11123.54.95
P11(20)-030.046 150.002 950.112 350.006 340.017 650.000 300.005 620.000 175.7146.94108.15.79112.81.88113.33.48
P11(20)-040.050 720.003 130.126 030.006 820.018 020.000 310.005 620.000 18228.3136.7120.56.15115.11.95113.33.66
P11(20)-050.050 270.003 950.123 740.008 950.017 850.000 340.005 720.000 23207.3172.58118.58.091142.13115.34.53
P11(20)-060.050 350.003 540.126 340.008 000.018 190.000 330.005 800.000 21211.2154.95120.87.21116.22.091174.12
P11(20)-070.049 350.004 740.123 990.011 230.018 220.000 390.006 140.000 28164.5210.23118.710.15116.42.44123.75.67
P11(20)-080.047 210.003 480.113 800.007 640.017 480.000 320.005 840.000 1959.5167.44109.46.97111.72.02117.73.88
P11(20)-090.045 390.002 650.112 800.005 680.018 020.000 290.005 790.000 140.1101.05108.55.18115.11.83116.72.84
P11(20)-100.040 630.004 970.099 350.011 720.017 730.000 380.005 530.000 280.1096.210.83113.32.4111.55.68
P11(20)-110.045 520.004 490.110 210.010 280.017 560.000 360.005 600.000 250.1194.99106.29.4112.22.31112.94.95
P11(20)-120.050 940.003 090.126 260.006 670.017 970.000 300.006 000.000 16237.9134.15120.76.02114.81.921213.16
P11(20)-130.052 850.005 320.133 820.012 750.018 360.000 400.006 240.000 31322.4213.24127.511.42117.32.52125.76.26
P11(20)-140.053 410.003 640.133 110.008 100.018 070.000 330.006 160.000 20346.1146.56126.97.26115.52.08124.23.93
P11(20)-150.058 740.004 540.145 320.010 280.017 940.000 350.006 720.000 26557.4160.27137.89.11114.62.24135.45.28
P11(20)-160.044 400.004 300.110 740.010 150.018 090.000 360.006 040.000 260.1133.26106.69.28115.62.31121.85.31
P11(20)-170.047 580.003 480.118 390.007 870.018 040.000 320.005 920.000 1877.7165.72113.67.15115.32.03119.33.7
P11(20)-180.049 510.003 060.126 830.006 860.018 570.000 310.006 110.000 17172.2138.15121.26.18118.61.971233.5
P11(20)-190.051 660.004 690.128 320.010 890.018 010.000 380.006 020.000 26270.5194.89122.69.8115.12.38121.35.24
P11(20)-200.049 220.002 840.118 160.005 860.017 410.000 280.005 840.000 14158.5129.68113.45.32111.21.77117.62.82
P11(20)-210.063 050.004 170.156 740.009 170.018 030.000 340.006 210.000 23709.8134.61147.88.05115.22.13125.14.61
P11(20)-220.047 640.003 130.117 600.006 880.017 900.000 310.005 940.000 1980.8149.81112.96.25114.41.93119.73.73
P11(20)-230.049 290.004 500.119 040.010 180.017 510.000 360.005 840.000 25161.7200.42114.29.24111.92.29117.64.99
P11(20)-240.050 000.003 520.122 780.007 810.017 800.000 320.005 950.000 21195.2155.96117.67.06113.82119.94.16
P11(46)-010.050 930.007 320.147 500.020 370.021 000.000 670.007 450.000 52237.5300.97139.718.021344.25149.910.35
P11(46)-020.050 780.003 630.132 110.008 440.018 870.000 330.006 600.000 21230.9157.241267.57120.52.08132.94.21
P11(46)-030.051 300.003580.138 460.008 610.019 570.000 320.006 730.000 22254.2152.94131.77.681252.05135.54.49
P11(46)-040.051 820.003520.131 820.007 930.018 450.000 310.006 490.000 21277.4148.45125.77.11117.81.96130.84.18
P11(46)-050.049 360.012510.124 030.030 650.018 220.000 990.008 500.000 90164.7504.78118.727.69116.46.2617117.94
P11(46)-060.052 300.009070.134 260.022 510.018 610.000 720.006 210.000 57298.7353.77127.920.15118.94.53125.111.44
P11(46)-070.047 860.006840.102 520.014 190.015 530.000 370.005 290.000 3391.2308.9399.113.0799.42.36106.76.7
P11(46)-080.049 220.003390.118 910.007 280.017 520.000 280.005 740.000 19158.2153.49114.16.61121.8115.63.78
P11(46)-090.049 350.013750.108 520.029 540.015 940.000 910.005 960.000 62164.4547.07104.627.061025.77120.112.4
P11(46)-100.051 100.004040.128 080.009 250.018 180.000 330.006 270.000 24245.2172.54122.48.33116.12.11126.24.86
P11(46)-110.049 240.006430.128 540.016 040.018 930.000 550.006 000.000 41159.2279.47122.814.43120.93.5120.98.28
P11(46)-120.050 220.005280.120 700.011 980.017 430.000 400.006 350.000 31205226.96115.710.86111.42.531286.28
P11(46)-130.146 930.006070.285 550.007 940.014 090.000 200.009 600.000 172310.569.22255.16.2790.21.3193.13.47
P11(46)-140.053 170.016130.125 220.037 020.017 080.001 170.006 530.001 06336571.83119.833.41109.17.43131.521.25
P11(46)-150.051 180.013020.135 070.033 480.019 140.001 070.009 300.001 09248.8499.44128.629.95122.26.79187.121.76
P11(46)-160.052 420.003850.123 600.008 190.017 100.000 300.005 500.000 16303.7158.38118.37.4109.31.88110.93.27
P11(46)-170.050 340.003420.129 040.007 800.018 590.000 300.006 820.000 21210.9150.2123.27.02118.71.9137.44.25
P11(46)-180.051 450.006440.129 660.015 460.018 270.000 520.007 330.000 44261.1264.1123.813.9116.73.31147.78.92
P11(46)-190.052 680.006210.134 720.015 080.018 540.000 520.006 120.000 40315248.02128.313.49118.43.27123.47.95
P11(46)-200.053 050.007720.130 470.018 240.017 830.000 600.007 220.000 52330.8300.38124.516.381143.77145.410.49
P11(46)-210.052 130.003770.132 380.008 590.018 410.000 330.005 790.000 19291.2156.78126.27.7117.62.11116.73.81
P11(46)-220.052 020.004250.131 050.009 820.018 270.000 360.005 970.000 21286.3176.061258.82116.72.3120.34.19
P11(46)-230.050 780.006020.124 970.014 080.017 850.000 490.005 760.000 30230.7252.21119.612.711143.08116.16.1
P11(46)-240.051 740.004630.133 140.011 100.018 660.000 370.006 270.000 24274.1192.25126.99.95119.22.32126.44.89
Table
Table 2. Major elements (wt%), trace elements (ppm) and REE (ppm) analyses of the Bieruozecuo quartz diorites.
Table 2. Major elements (wt%), trace elements (ppm) and REE (ppm) analyses of the Bieruozecuo quartz diorites.
SamplesP10(19)P10(88)P10(130)P10(161)P10(xx1)P10(xx2)P10(xx3)P10(xx4)P10(xx5)P11(6)P11(8)P11(18)P11(20)P11(34)P11(41)
LithologyQuartz Diorite
SiO265.64064.84064.50068.32064.43064.91064.07064.28065.73065.17066.41065.65065.98066.48066.280
Al2O315.69015.44015.44014.72015.32015.47015.71015.75015.46015.41015.09014.94015.34015.04014.920
Fe2O31.7901.8601.8901.2602.1101.9802.0502.1001.8201.4101.1401.3801.1701.8301.290
FeO1.9402.2802.0801.5902.3302.3002.2702.1501.9502.9702.8902.8302.6102.3302.800
CaO4.1304.3404.2103.6204.3204.1204.6604.6604.0604.4603.8904.1504.0303.9003.790
MgO2.1402.5302.4001.6002.6702.4402.5402.4302.1402.0601.8401.9901.7601.8301.830
K2O2.7002.8303.0803.6202.9003.0402.7902.7102.9403.1603.4703.4203.4303.4303.460
Na2O4.0203.7003.6503.6403.6703.7003.7903.7903.7303.3903.2803.2703.3403.2903.270
TiO20.5650.6620.6170.4500.7130.6900.6540.6300.5800.5870.5600.5950.5110.5690.552
P2O50.1890.2350.2280.1600.2530.2390.2640.2660.2380.1150.1120.1290.1020.1150.123
MnO0.0640.0630.0690.0580.0730.0660.0670.0620.0590.0750.0730.0720.0730.0730.078
LOI0.7670.7871.4400.6530.7770.6030.6970.7470.8320.7120.7651.0401.2200.7131.160
Total100.46299.71499.75899.89699.78899.82699.80299.67899.74099.98299.82399.93999.635100.01699.873
Mg#51.79253.28653.08751.15152.95351.58852.39051.74451.53346.41845.58146.55846.13645.06445.163
σ1.9901.9302.0902.0701.9902.0502.0301.9601.9401.9201.9301.9501.9701.9101.920
A/CNK0.9210.9060.9090.8930.9000.9170.8860.8930.9260.9010.9300.8990.9280.9270.932
A/NK1.6451.6871.6531.4861.6691.6501.6971.7181.6591.7131.6491.6451.6661.6481.635
CaO + Na2O8.1138.0637.8797.2688.0077.8348.4678.4777.8107.8517.1837.4257.3977.1897.069
Cu9.32022.00027.0006.36018.80044.50019.60025.60029.40033.40029.80022.20024.90029.00029.900
Pb9.28018.80014.50013.60022.30029.30022.10019.50022.00013.90015.30015.8007.04014.20020.700
Zn53.00067.70061.70046.00071.80071.60071.40061.20063.50069.20053.60049.60049.20050.70069.200
Cr44.40063.50050.20032.50059.20050.90057.50056.30048.10032.80020.80027.00023.80022.80023.100
Ni22.40035.50028.20020.40032.00029.50030.30028.40025.40013.50010.80012.20010.40011.00011.300
Co13.70019.20017.2009.27019.10017.30016.60017.00016.50018.40017.00016.60012.50015.50016.200
Rb65.000107.00085.200111.000114.000131.00098.90095.300112.000125.000129.000132.000124.000129.000139.000
Cs5.7604.7106.5006.1006.6708.9805.3305.3505.5303.3404.1105.5404.0004.1004.620
W47.50082.60074.20027.70079.20060.20058.10070.80077.00076.20083.30065.40030.80060.40071.200
Sb0.2700.4500.2600.2200.6601.2400.4100.8500.5401.2401.1800.4400.2000.5602.070
Bi0.0810.1200.1700.0890.2900.2000.1400.2700.2000.0620.0410.0880.0790.0360.220
Sr458.000554.000496.000427.000540.000513.000574.000574.000533.000327.000324.000326.000307.000323.000296.000
Ba352.000543.000395.000384.000478.000543.000444.000465.000501.000473.000501.000506.000368.000481.000445.000
V69.10080.70078.80051.80082.30078.30087.00087.90074.600101.00084.20089.40079.60088.30092.800
Nb9.88010.7009.7709.74011.40011.00011.10010.80011.20010.50010.80011.4008.79011.50013.100
Ta0.8200.7900.9200.9800.8000.8200.9200.8700.9600.9100.9200.9400.8901.0001.190
Zr98.00044.40092.200118.00065.00049.90065.30075.00069.90098.90092.500104.00087.800155.00094.600
Hf3.2301.4203.0703.7001.9201.6702.0602.3502.0003.5002.8203.3703.3605.5903.190
Sn1.8902.2502.0101.9202.5002.1703.4702.5702.4201.6601.6002.1001.7501.8202.250
Au1.0801.3900.7200.2501.7002.0200.5100.8801.7001.1301.7601.3800.3800.7600.510
Ag0.0180.0330.0390.0140.0280.0720.0400.0420.0440.0480.0580.0560.0460.0450.086
U1.3201.7101.6001.7201.8402.0501.7201.9801.5402.2402.0102.3204.6003.0103.160
Th7.7709.66011.20012.00015.40011.9009.22012.50012.40011.70012.80013.90016.20020.10017.400
Ti0.3390.3830.3700.2700.4130.3990.3790.3650.3360.3400.3240.3440.3060.3290.320
La33.20038.40032.20035.60039.00035.80036.10040.40037.00024.80027.60034.20029.90029.60031.200
Ce55.40062.30055.20061.00063.50059.80061.30067.20061.80041.90044.80053.40049.00047.10051.000
Pr6.4608.3706.5807.2508.1207.6708.1708.6708.0405.3505.7307.0005.6505.9906.700
Nd23.50030.60024.30026.20031.20028.90031.90033.40030.10019.70021.40025.20020.10021.90024.400
Sm3.8705.1404.1104.3605.2404.9905.5005.6205.0603.6604.0804.7803.5903.9404.610
Eu1.1001.3001.0701.0801.2901.3001.3501.4101.2800.9800.9501.0700.9400.9200.950
Gd3.2304.3403.3003.5504.3404.2004.6004.7204.1503.3803.6604.3103.1703.4504.040
Tb0.4300.5600.4400.4600.5600.5200.6200.6100.5300.4900.5500.6200.4700.5000.570
Dy2.2302.6502.3802.3202.7402.7103.0802.9402.6602.9603.2303.5802.7002.8503.340
Ho0.4200.4900.4300.4400.5200.4800.5700.5400.4800.5800.6200.7000.5600.5700.650
Er1.1001.3101.1401.1401.3001.3401.5001.4001.2401.5801.6701.9401.5601.5901.820
Tm0.1600.1900.1700.1600.1900.1800.2100.2000.1800.2400.2600.3100.2400.2700.310
Yb0.9801.1501.0801.0201.2801.2201.4201.3601.1801.8001.9202.1101.6001.7602.190
Lu0.1300.1500.1500.1400.1600.1600.1900.1700.1500.2400.2400.2800.2300.2500.300
Y9.85011.60010.60010.60012.40011.90013.80012.80011.60014.40015.30017.60014.10014.30016.500
La/Yb33.87833.39129.81534.90230.46929.34425.42329.70631.35613.77814.37516.20918.68816.81814.247
Sr / Y46.49747.75946.79240.28343.54843.10941.59444.84445.94822.70821.17618.52321.77322.58717.939
∑REE132.210156.950132.550144.720159.440149.270156.510168.640153.850107.660116.710139.500119.710120.690132.080
δEu0.9340.8270.8680.8210.8110.8530.8060.8220.8360.8450.7440.7130.8410.7530.664
(La/Yb)N22.31621.99619.64022.99120.07119.33016.74719.56820.6559.0769.46910.67712.31011.0799.385
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Xiao, Q.-R.; Wei, Y.-F.; Liu, Z.-Y.; Xiong, F.-H.; Fan, L.; Wu, J.-X.; Zhao, H. Petrogenesis of Early Cretaceous High-Mg Adakitic Pluton in the North Lhasa Block, Tibet Plateau: Implications for the Tethyan Orogeny. Minerals 2022, 12, 213. https://doi.org/10.3390/min12020213

AMA Style

Xiao Q-R, Wei Y-F, Liu Z-Y, Xiong F-H, Fan L, Wu J-X, Zhao H. Petrogenesis of Early Cretaceous High-Mg Adakitic Pluton in the North Lhasa Block, Tibet Plateau: Implications for the Tethyan Orogeny. Minerals. 2022; 12(2):213. https://doi.org/10.3390/min12020213

Chicago/Turabian Style

Xiao, Qian-Ru, Yong-Feng Wei, Zhong-Yuan Liu, Fu-Hao Xiong, Lei Fan, Jian-Xin Wu, and Han Zhao. 2022. "Petrogenesis of Early Cretaceous High-Mg Adakitic Pluton in the North Lhasa Block, Tibet Plateau: Implications for the Tethyan Orogeny" Minerals 12, no. 2: 213. https://doi.org/10.3390/min12020213

APA Style

Xiao, Q. -R., Wei, Y. -F., Liu, Z. -Y., Xiong, F. -H., Fan, L., Wu, J. -X., & Zhao, H. (2022). Petrogenesis of Early Cretaceous High-Mg Adakitic Pluton in the North Lhasa Block, Tibet Plateau: Implications for the Tethyan Orogeny. Minerals, 12(2), 213. https://doi.org/10.3390/min12020213

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