Next Article in Journal
Geochemical Variations of Kerolite, Stevensite, and Saponite from the Pre-Salt Sag Interval of the Santos Basin: An Approach Using Electron Probe Microanalysis
Next Article in Special Issue
Zircon LA-ICP-MS Dating and Geochemical Characteristics of Rhyolites from the Qushi Area, Tengchong Terrane, Yunnan Province
Previous Article in Journal
Petrogenesis, Geochemistry, and Geological Significance of the Kongco Granitic Porphyry Dykes in the Northern Part of the Central Lhasa Microblock, Tibet
Previous Article in Special Issue
Mafic Intrusions in the Cuona Area, Eastern Tethyan Himalaya: Early Kerguelen Mantle Plume Activity and East Gondwana Rifting
 
 
Search for Articles:
Title / Keyword
Author / Affiliation / Email
Journal
Article Type
 
 
Advanced Search
 
Section
Special Issue
Volume
Issue
Number
Page
 
Journals
Minerals
Volume 15
Issue 3
10.3390/min15030284
minerals-logo
Submit to this Journal Review for this Journal Propose a Special Issue
► Article Menu

Article Menu

share Share announcement Help format_quote Cite question_answer Discuss in SciProfiles
first_page
settings
Order Article Reprints
Font Type:
Arial Georgia Verdana
Font Size:
Aa Aa Aa
Line Spacing:
Column Width:
Background:
Article

S-Type Granites from the Guomang-Co Area in Central Tibet: A Response to Early Paleozoic Andean-Type Orogeny Along the Northern Margin of East Gondwana

by
Yuhe Zhang
1,
Ming Wang
1,2,*,
Changsheng Yu
1 and
Zhenglong Li
1
1
College of Earth Sciences, Jilin University, Changchun 130061, China
2
Key Laboratory of Mineral Resources Evaluation in Northeast Asia, Ministry of Nature Resources, Changchun 130061, China
*
Author to whom correspondence should be addressed.
Minerals 2025, 15(3), 284; https://doi.org/10.3390/min15030284
Submission received: 13 January 2025 / Revised: 7 March 2025 / Accepted: 9 March 2025 / Published: 11 March 2025
(This article belongs to the Special Issue Tectonic Evolution of the Tethys Ocean in the Qinghai–Tibet Plateau)
Browse Figures
Versions Notes

Abstract

:
The Proto-Tethys Ocean existed between Gondwana and Laurussia during the late Neoproterozoic to Early Paleozoic. As part of the northern margin of East Gondwana, the Lhasa terrane records subduction-related processes of the Proto-Tethys Ocean. This study analyzes mylonitized granites from the Guomang-Co area in the central Lhasa terrane, focusing on their major and trace elements, U-Pb age values, and Sr-Nd-Pb-Hf isotopes. Geochemical and isotopic data consistently indicate S-type affinity derived from Paleoproterozoic metasedimentary sources, and likely formed in a syn-collisional setting. Combined with previous studies, the granites are interpreted as products of the Early Paleozoic Andean-type orogeny along the northern margin of East Gondwana, which indicate southward subduction of the Proto-Tethys Ocean during the Cambrian–Ordovician.

1. Introduction

The Proto-Tethys Ocean, which originated from the breakup of the Rodinia supercontinent during the late Neoproterozoic, existed between the northern margin of Gondwana and Laurussia from the late Neoproterozoic to the late Paleozoic. Its evolution profoundly influenced the global tectonic framework of the Early Paleozoic [1,2,3,4,5] and is closely linked to the early formation and evolution of the Tibetan Plateau.
The Proto-Tethys Ocean underwent a general evolution from extensional rifting and expansion during the late Neoproterozoic, to the initiation of subduction in the Early Paleozoic, and finally to the closure of the ocean basin by the late Silurian. However, extensive later magmatic activity and tectonic overprinting have left many issues concerning the Proto-Tethys Ocean unresolved, with the debate over its subduction polarity being one of them. Some researchers advocate a unidirectional northward subduction model [6,7,8,9], whereas others propose a bidirectional model involving both northward and southward subduction [10,11,12,13,14]. This debate is closely linked to whether the northern margin of Gondwana during the Early Paleozoic functioned as a passive continental margin or experienced Andean-type orogenesis.
In recent years, numerous Neoproterozoic and Early Paleozoic magmatic events along the northern margin of East Gondwana have been dated by researchers (Table 1). The relationship between these magmatic activities, the Pan-African orogeny, and Proto-Tethys subduction has become a focal point of debate. Currently, there are three prevailing viewpoints regarding these magmatic events:
(1)
The traditional perspective is on the basis of the understanding that the Pan-African orogeny occurred between 550~450 Ma [15]; it posits that the Early Paleozoic magmatism in the Tibetan Plateau is part of the Pan-African event; e.g., [16,17,18,19,20,21,22,23].
(2)
Another perspective posits that during the late Neoproterozoic, the northern margin of Gondwana functioned as a passive continental margin (e.g., [9,24,25,26,27]), and that Early Paleozoic magmatic rocks were generated in a post-collisional extensional setting following the Pan-African orogeny (e.g., [7,28,29,30,31,32,33]).
(3)
The third perspective argues that an Andean-type orogenic belt developed along the northern margin of Gondwana during the Early Paleozoic, and that these rocks were associated with subduction-related processes (e.g., [10,34,35,36,37,38]).
The primary reasons behind these debates are as follows: (1) Differences in understanding the spatiotemporal extent of the Pan-African orogeny. (2) These reports are colloreted to primarily acidic rocks, with few mafic rocks and fewer intermediate rocks reported, and records of Andean-type orogenic events on the northern margin of Australia are limited. (3) The northern margin of Gondwana is considered as a passive continental margin during the Neoproterozoic, the mechanism through which a passive continental margin transitioned into a subduction zone remains unclear.
Table 1. Early Paleozoic statistical age data reported along the northern margin of East Gondwana.
Table 1. Early Paleozoic statistical age data reported along the northern margin of East Gondwana.
LocationTerraneLithologyGenesis TypeMethodAgeRef.
MabjiaHimalayaGranitic gneiss\SIMS530[39]
KampaHimalayaGranitic gneiss\SHRIMP527, 506[40]
KangmarHimalayaGranitic gneiss\U-Pb508[41]
KangmarHimalayaGranitic gneiss\SHRIMP515[16]
KangmarHimalayaGranitic gneissS-typeLA-ICP-MS500~478[42]
KangmarHimalayaGraniteS-typeSHRIMP499~498[43]
GyirongHimalayaGranitic gneiss\SHRIMP514[16]
GyirongHimalayaGranitic gneiss\SHRIMP499[44]
GyirongHimalayaGranitic gneissS-typeLA-ICP-MS486~474[42]
GyirongHimalayaGraniteS-typeLA-ICP-MS486~429[43]
LaguigangriHimalayaGranitic gneissS-typeLA-ICP-MS514[29]
YadongHimalayaGranite\SHRIMP512[16]
YadongHimalayaGraniteS-typeSHRIMP508[43]
YadongHimalayaGraniteS-typeLA-ICP-MS499[45]
Namche BawaHimalayaGraniteS-typeSHRIMP506[43]
Namche BawaHimalayaGranitic gneissI-typeLA-ICP-MS503~490[46]
DinggyeHimalayaGranitic gneissS-typeSHRIMP504~482[47]
NielamuHimalayaGranitic gneiss\SHRIMP501[16]
YalaxiangboHimalayaGranitic gneissS-typeLA-ICP-MS496~488[42]
XiaruHimalayaGraniteS-typeMC-ICP-MS486~446[43]
XiaruHimalayaOthogneissI-type or S-typeSIMS480~470[48]
XiaruHimalayaGraniteS-typeLA-ICP-MS478, 475[49]
Kathmandu, DadeldhuraHimalayaGranite\MC-ICP-MS484~476[34,50]
KathmanduHimalayaGranite\LA-ICP-MS478, 477[10]
DadeldhuraHimalayaGranite\MC-ICP-MS482~474[51]
DadeldhuraHimalayaGranite\LA-ICP-MS478[52]
RupshuHimalayaGranitePeral. I-typeIDMS482[53]
Tso MorariHimalayaGranitic gneissS-typeIDMS479[53]
Lhagoi KangriHimalayaGraniteS-typeSHRIMP477[43]
MabjiaHimalayaGraniteS-typeSHRIMP475[43]
SimcharHimalayaGranite\LA-ICP-MS471[54]
DuguerSouth QiangtangGranitic gneissS-typeLA-ICP-MS502~492[55]
DuguerSouth QiangtangGranitic gneissS-typeMC-ICP-MS490~473[56]
DuguerSouth QiangtangGabbroE-MORBMC-ICP-MS490[57]
DuguerSouth QiangtangBasaltE-MORBMC-ICP-MS483[57]
DuguerSouth QiangtangAndesiteOIBMC-ICP-MS477~473[57]
DuguerSouth QiangtangGranitic gneiss\LA-ICP-MS476~471[58]
DuguerSouth QiangtangGranitic gneissA-typeMC-ICP-MS454[57]
Bensong-CoSouth QiangtangGranitic gneissS-typeLA-ICP-MS497, 496[59]
Bensong-CoSouth QiangtangGranitic gneissS-typeLA-ICP-MS486, 481[60]
GemuriSouth QiangtangGranite\MC-ICP-MS489, 480[61]
GemuriSouth QiangtangGraniteS-typeLA-ICP-MS486, 480[60]
GemuriSouth QiangtangGraniteS-typeMC-ICP-MS469~455[56]
GemuriSouth QiangtangGranite\MC-ICP-MS439[61]
EjiumaiSouth QiangtangGranite\SHRIMP476~463[62]
Moon-CoSouth QiangtangMetabasaltOIBLA-ICP-MS476[63]
Moon-CoSouth QiangtangMetarhyolite\LA-ICP-MS470, 461[63]
Moon-CoSouth QiangtangMetarhyolite\LA-ICP-MS458, 454[64]
HeibailingSouth QiangtangMetarhyolite\LA-ICP-MS467[63]
WugongshanSouth QiangtangGranitic gneiss\LA-ICP-MS465[19]
JitangSouth QiangtangGraniteS-typeLA-ICP-MS455[65]
Guomang-CoLhasaGraniteS-typeMC-ICP-MS530, 480this study
BangleiLhasaMetarhyolite\LA-ICP-MS536[28]
ZhaqianLhasaMetarhyoliteS-typeLA-ICP-MS525, 511[36]
ZhakangLhasaMetarhyolitePeral. A-typeMC-ICP-MS512[38]
ZhakangLhasaMetarhyoliteS-typeLA-ICP-MS510[36]
ZhakangLhasaMetarhyolite\LA-ICP-MS501[66]
XainzaLhasaGranite\LA-ICP-MS510[67]
TongkaLhasaGranite\SHRIMP507[18]
JiliLhasaGranitic gneissPeral. I-typeLA-ICP-MS504, 495[68]
MilinLhasaGraniteS-typeLA-ICP-MS501~496[69]
NyingchiLhasaGranitic gneiss\LA-ICP-MS496[70]
BangleiLhasaMetabasalt\LA-ICP-MS492[11]
BangleiLhasaMetarhyoliteS-typeLA-ICP-MS492[11]
AmdoAmdoGranitic gneiss\LA-ICP-MS532~483[71]
AmdoAmdoGranitic gneiss\U–Pb531[72]
AmdoAmdoGranitic gneissI-typeLA-ICP-MS517~505[37]
AmdoAmdoGranitic gneiss\SHRIMP502~483[46]
AmdoAmdoGranitic gneiss\LA-ICP-MS488[21]
The data are primarily concentrated between 530~460 Ma.
The Lhasa terrane, one of the principal tectonic blocks forming the Tibetan Plateau, is generally regarded as a microcontinent that developed along the northern margin of Gondwana (i.e., southern margin of the Proto-Tethys Ocean) during the Early Paleozoic [11,73]. This terrane holds significant importance for understanding the Early Paleozoic evolution of the northern Gondwana margin. In this study, we report a suite of Early Paleozoic mylonitized granites from the Guomang-Co area in Xainza County, Lhasa terrane. On the basis of geochemical data, U-Pb geochronological results, and Sr-Nd-Pb-Hf isotopic analyses, this paper investigates the petrogenesis and tectonic setting of these granites, providing new constraints on the Early Paleozoic evolution of the Proto-Tethys Ocean along the northern margin of Gondwana.

2. Geological Setting and Samples

On the basis of the current plate tectonic model for the Tibetan Plateau and the Early Paleozoic tectonic framework [73,74], five major plate sutures with a nearly east-west orientation have been identified (Figure 1a). From north to south, these sutures are the Kunlun Mountain Suture Zone (KSZ), the Jinsha River Suture Zone (JSSZ), the Longmu Co-Shuanghu Suture Zone (LSSZ), the Bangong Lake-Nujiang Suture Zone (BNSZ), and the India-Yarlung Zangbo River Suture Zone (IYZSZ). The plates defined by these sutures are, in turn: the Bayan Har-Ganzi terrane, the North Qiangtang terrane, the South Qiangtang terrane, the Lhasa terrane, and the Himalaya terrane (Figure 1a).
The Lhasa terrane is situated between the Bangong Lake-Nujiang Suture Zone (BNSZ) and the Yarlung Zangbo River Suture Zone (IYZSZ), and exhibits characteristics akin to the northern margin of Gondwana. It can be further subdivided into three regions by the Shiquan River-Nam Co Mélange Zone (SNMZ) and Luobadui-Mila Moutain Fault (LMF)—northern, central, and southern regions. However, the formation of the northern and southern Lhasa terrane during the Meso-Cenozoic mainly occurred during the Mesozoic and Cenozoic, which has little relation to the Early Paleozoic evolutionary processes [74]. Therefore, for the purpose of this study, the Lhasa terrane is considered as a unified whole.
The granitic mylonite of Guomang-Co is exposed approximately 6 km east of Guomang Village in Xainza County, central Tibet (Figure 1b). Tectonically, it is situated near the Shiquanhe-Nam Co Ophiolitic Mélange Zone (SNMZ), within the central part of the Lhasa terrane. Mesozoic strata dominate to the north of Guomang-Co, while Paleozoic strata are predominantly exposed to the south (Figure 1b). In the Zhaqian area, about 12 km south of Guomang-Co, a well-preserved angular unconformity between Cambrian and Ordovician strata has been identified [76].
The coordinates of the Guomang-Co granite sampling site are E: 89°13′48.68″, N: 31°7′44.78″, and it is located within the Precambrian Nyainqengtanglha Group (AnZNq) previously defined by other researchers (Figure 1b). The Nyainqentanglha Group is distributed as a belt-like manner in the NWW direction in the area. It is a rock group with basement characteristics in Lhasa terrane, which is formed by the oldest sedimentary processes and generally has undergone metamorphism within the amphibolite facies-granulite facies. Its lithology includes biotite granodiorite gneiss, biotite plagiogneiss, greenstone plagioclase amphibolite, diopside marble, feldspar-quartzite, quartzite, quartz schist, granitic gneiss, slate, and phyllite [77,78]. Ji et al. [45] first identified an Early Cambrian rhyolite (501 Ma) separated from the Nyainqengtanglha Group in the Shenzha area and suggested that at least a portion of the upper strata belongs to the Cambrian. Subsequently, several Early Paleozoic reports have emerged from the originally defined Nyainqengtanglha Group region [11,28,36,38,69,70]. The Guomang-Co granite samples collected in this study are also part of the Nyainqengtanglha group.
The outcrop conditions at the sampling site are poor, and the contact relationship with adjacent rock bodies is unknown (Figure 2a). Field observations show that the Guomang-Co granite consists of a suite of dark-colored granitoid mylonite (Figure 2b,c), locally experiencing intense ductile deformation, with the development of sheath folds, stretching lineation, and shear bands (Figure 2b,c). Under the microscope, the samples are severely mylonitized, exhibiting a porphyroclastic texture and mylonitic structure (Figure 2d,e). The primary constituents are quartz and alkali feldspar; the porphyroblasts constitute about 50%, with 80% alkali feldspar and 20% quartz. The matrix shows a fine-grained granoblastic texture, making up about 47%, with a certain degree of preferred orientation (Figure 2f). White mica fills mineral gaps and constitutes about 3%, with mica fish structures formed due to ductile deformation (Figure 2f,g).

3. Materials and Methods

3.1. Whole-Rock Geochemical Data

Four fresh samples (Q22T4H1–Q22T4H4) were processed for geochemical characterization. The samples were crushed to a grain size <200 mesh at the Regional Geological Survey Center of Hebei Province, China. Major and trace element testing were conducted at the Key Laboratory of Mineral Resources Evaluation in Northeast Asia of Jilin University, Changchun, China. Major elements were analyzed with a Leeman Prodigy ICP-OES and Rigaku ZSX Primus II X-ray fluorescence spectrometer achieving analytical precision of 1%–3%. Trace elements were determined using an Agilent 7500a ICP-MS, with elemental uncertainties generally <5%. Loss on ignition (LOI) was measured by heating ~1 g powder at 1000 °C. Analytical protocols followed established procedures in references [79,80].

3.2. Zircon U-Pb Geochronological Investigations

Two samples (numbered Q22T4-1 and Q22T4-2) of Guomang-Co granite were selected for zircon U-Pb dating. Zircon grains were separated using conventional heavy liquid and magnetic techniques at the Regional Geological Survey Center of Hebei Province, China, with cathodoluminescence (CL) images taken in the same place. Zircon U-Pb dating was performed at the Key Laboratory of Mineral Resources Evaluation in Northeast Asia of Jilin University, Changchun, China, using an Agilent 7500a inductively coupled plasma mass spectrometer (ICP-MS) with 193 nm laser ablation system (UP193SS). In this study, 91,500 was used as the zircon standard [81]. NIST 610 was used as the external standard, and 29Si was used as the internal standard for trace element calculations, the GJ-1 reference zircon was analyzed as an unknown sample, yielding an average 206Pb/238U age of 609.5 ± 2.4 Ma, matching its certified value (608.5 ± 0.37 Ma) [82]. Methodology details can be founded in [83]. Data reduction utilized ICPMS Data Cal v10.2 [84] and Isoplot v4.15 [85].

3.3. Zircon Hf Isotope

In situ zircon Hf isotope analysis was conducted at Beijing Createch Testing Technology Co. Ltd., Beijing, China, by use of a Neptune Plus Multi-collector Inductively Coupled Plasma Mass Spectrometer (MC-ICP-MS) equipped with a New Wave 213 laser-ablation system (30 or 38 μm diameter laser beam). The laboratory temperature was maintained between 18 °C and 22 °C, with relative humidity kept below 65%. The laser ablation beam used for testing had an energy density of 6 J/cm2, a pulse frequency of 6 Hz, and a diameter of 55 μm. Signal acquisition time was approximately 1 min. The international zircon standard GJ-1 was used as the external standard during the analysis. The material produced by laser ablation was transported to the Neptune Plus MC-ICP-MS for analysis, with high-purity helium (He) used as the carrier gas. Hf isotope data were obtained in low-resolution static mode. Detailed analytical procedures and parameters can be found in [86]. The decay constant for 176Lu used to correct the results was 1.867 × 10−11 a−1, following [87]. Additionally, Hf model age values and εHf(t) values were calculated on the basis of the methods of [88,89].

3.4. Whole-Rock Sr-Nd-Pb Isotopes

Two samples were selected for Sr-Nd-Pb isotope analysis (numbered Q22T4H1 and Q22T4H2) at Beijing Createch Testing Technology Co., Ltd., by use of a Thermo Scientific Neptune Plus Multi-Collector Inductively Coupled Plasma Mass Spectrometer (MC-ICP-MS). The analytical procedure is briefly outlined as follows: first, the samples were digested by use of a mixture of nitric acid and HF acid in Teflon beakers, followed by separation and analysis by use of a dedicated cation exchange column. Detailed testing methods and related parameters can be found in [90]. Sr and Nd isotopes were normalized using 86Sr/88Sr = 0.7219 and 146Nd/144Nd = 0.7219, respectively. The international standards NBS 987 (87Sr/86Sr = 0.710248 ± 14 (2SD, n = 33)) and GSB Nd (143Nd/144Nd = 0.512190 ± 10 (2SD, n = 10)) were used for external calibration.

4. Results

4.1. Whole-Rock Geochemical Characteristics

The whole-rock major and trace elements of the samples show good consistency, and the analytical results are presented in Table S1. The mineral assemblage observed under the microscope shows orientation, indicating that the samples underwent late-stage deformation. However, no significant mineral phase transformations were observed (Figure 2d–g). The loss on ignition (LOI) of the samples has a range of 0.63%~0.80%, showing relatively low values and small variation. The K2O/Na2O ratios are stable (0.97~1.05), and no significant changes in Sr and Ba content were observed, suggesting that these elements did not experience significant loss or enrichment [91]. The high field strength elements (HFSEs) and rare earth elements (REEs) distribution patterns are consistent with those of granite rocks (Figure 3a,b) [92], indicating that the samples were not significantly affected by late-stage alteration. Therefore, the whole-rock major and trace element data of the samples are considered reliable for geochemical analysis.
The samples are rich in SiO2 (75.18%~75.76%) and Al2O3 (13.32%~13.63%), with a Na2O content range of 4.02%~4.15% and a K2O content range of 3.98%~4.23%. They are low in TiO2 (0.08%~0.09%), CaO (0.51%~0.59%), P2O5 (~0.17%), MgO (0.20%~0.25%), MnO (0.01%~0.03%), and FeOT (0.68%~0.79%), with Mg# values ranging within 38.5~39.7. In the TAS diagram, the samples fall within the granite field (Figure 4a) and belong to the high-potassium calc-alkaline series (Figure 4b). Mineral calculations using the CIPW norm [95] show that the samples primarily consist of quartz (34.4%~35.2%) and orthoclase (58.8%~59.5%), with minor amounts of plagioclase (1.4%~1.8%) and corundum (1.5%~2.0%). The QAP diagram places the samples in the orthoclase granite field (Figure 4c). The A/CNK values of the samples have a range of 1.09~1.13, classifying them as weakly peraluminous granites (Figure 4d). These geochemical features are consistent with those of S-type granites [96,97].
In the whole-rock REE chondrite-normalized diagram (Figure 3a), the samples exhibit a pronounced rightward inclination. These rocks have REE patterns characterized by flat to fractionated LREE [(La/Sm)N = (1.48~3.77)] and flat to depleted HREE [(Gd/Yb)N = 0.61~0.95], with moderate negative Eu anomalies (δEu = 0.61~0.72) and positive Ce anomalies (δCe = 1.07~1.80). The REE distribution pattern is similar to that of arc-related magmatic rocks [98]. Two of the samples exhibited a relatively pronounced tetrad effect, which is often observed in highly evolved peraluminous S-type granite rocks [99].
In the trace element primitive mantle-normalized diagram (Figure 3b), the samples display enrichment in large ion lithophile elements (LILEs) such as Rb, Th, U, and Pb, depletion in high field strength elements (HFSEs) such as Nb and Ti, and depletion in Sr and Ba. Compared with early Paleozoic granites reported from the Lhasa terrane, the Guomangcu granite exhibits overall lower elemental abundances (REE = 10.3~27.8 ppm) and a more pronounced depletion of heavy rare earth elements. This may be attributed to garnet-bearing residue, indicating the derivation from the lower crust and a higher degree of fractional crystallization [98].
Minerals 15 00284 g004
Figure 4. (a) TAS diagram [100]; (b) SiO2-K2O diagram [101]; (c) QAP diagram [102], mineral composition derived from the CIPW normative mineral calculation; (d) A/NK-A/CNK diagram [103].
Figure 4. (a) TAS diagram [100]; (b) SiO2-K2O diagram [101]; (c) QAP diagram [102], mineral composition derived from the CIPW normative mineral calculation; (d) A/NK-A/CNK diagram [103].
Minerals 15 00284 g004

4.2. Zircon U-Pb Geochronological Investigations

In this study, 30 zircon grains from samples Q22T41 and Q22T42 were selected for LA-ICP-MS dating. Under cathodoluminescence (CL) images (Figure 5), the zircon grains are transparent to semi-transparent and range in color from colorless to light brown, predominantly exhibiting sub-euhedral columnar or granular morphologies, with some grains showing damaged, incomplete crystal forms. The grain size has a range of 50~100 μm, and the length-to-width ratio is 1:1~1:2. The Th/U ratios of these zircon grains are significantly greater than 0.5, with a range of 1.22~2.38, which is consistent with a magmatic origin [104]. Given that these zircon grains possess clear cores and most exhibit distinct and regular oscillatory zoning, a feature not typical of hydrothermal zircons, the zircon grains’ cores are most likely of magmatic origin and can be used to constrain the formation age of the primary granite [105]. Moreover, the narrow widths of the oscillatory zones indicate relatively low crystallization temperatures, which concurs with the zircon saturation temperature calculations presented later [104].
The results of the zircon U-Pb geochronological investigations are shown in Table S1, and the concordia diagrams for the 21 zircon analysis points are presented in Figure 5. The 206Pb/238U ages of the nine analysis points from sample Q22T41 have a range of 528~531 Ma, with a weighted mean age of 529.4 ± 3.0 Ma (MSWD = 0.074, n = 9). The 206Pb/238U ages of the 12 analysis points from sample Q22T42 range of 478~482 Ma, with a weighted mean age of 479.8 ± 2.5 Ma (MSWD = 0.800, n = 12). Both samples exhibit good concordance and represent two distinct episodes of magmatic activity.

4.3. Zircon Hf Isotope

Zircon in situ Lu-Hf isotope analysis was performed on 19 concordant test points from the two samples (Figure 6), with the analytical data presented in Table S1. For sample Q22T41, the 176Yb/177Hf ratio has a range of 0.045832~0.093184, and the 176Lu/177Hf ratio has a range 0.001548~0.003017. The fLu/Hf values have a range of −0.91~−0.95, with an average value of −0.93. The εHf(t) values have a range of −4.10~−8.36, and the two-stage model age (TDM2) has a range of 1745~2010 Ma. For sample Q22T42, the 176Yb/177Hf ratio has a range of 0.044872~0.160229, and the 176Lu/177Hf ratio has a range of 0.001543~0.004988. The fLu/Hf values have a range of −0.85~−0.95, with an average value of −0.93. The εHf(t) values have a range of −2.20~−9.33, and the two-stage model age (TDM2) has a range of 1587~2033 Ma.

4.4. Whole-Rock Sr−Nd−Pb Isotopes

The Sr-Nd-Pb isotopic test results for the Guomang-Co granite samples Q22T41 and Q22T42 are shown in Table S1. The samples exhibit relatively high initial 87Sr/86Sr ratios (0.706955~0.707155) and modern values (0.744868~0.747049), indicating a crustal origin. The (143Nd/144Nd)t ratios have a range of 0.511896~0.511933, with negative εNd(t) values of −10.72 to −9.99 (Figure 7). The relatively low initial 143Nd/144Nd ratios (0.511406~0.511408) also suggest that their magma source region has undergone long-term radioactive decay. The Pb isotopic ratios are as follows: 206Pb/204Pb, 207Pb/204Pb, and 208Pb/204Pb with a range of 19.4131~19.4225, 15.8121~15.8164, and 39.9654~40.0308, respectively; (206Pb/204Pb)t, (207Pb/204Pb)t, and (208Pb/204Pb)t ratios with a range of 17.0398~17.1831, 15.6817~15.6821, and 39.3308~39.5131, respectively, all of which are consistent with a crustal source composition.

5. Discussion

5.1. Petrogenesis and Magma Source

The general granite classification scheme divides granites into four types: A-type (anorogenic), S-type (sedimentary source-modified), I-type (crust-mantle co-melting), and M-type (mantle source) [109].
The granite samples exhibit S-type granite characteristics, as evidenced by the following observations: (1) The samples possess high SiO2 and K2O contents and display peraluminous features, with CIPW normative mineral calculations indicating the presence of 1.5~2.0% corundum [96,97]. (2) The REE distribution pattern is analogous to that of arc-related magmatic rocks, with relatively low Sr and Ba contents implying dehydration melting of mica [110,111]. Furthermore, the samples exhibit low 10,000 Ga/Al and FeOT/MgO ratios and a depletion of HFSEs (Zr + Nb + Ce + Y), positioning them within the non-A-type granite field (Figure 8b,c) [84]. (3) Using the zircon saturation temperature formula TZr = 12,900/[2.95 + 0.85M + ln(496,000/Zrmelt)] [112], the formation temperature of the granite is calculated to the range of 653 °C~679 °C, consistent with the low formation temperature characteristic of S-type granites. (4) The samples exhibit relatively high initial 87Sr/86Sr ratios (0.706955~0.707155) and very low εNd(t) values (–10.72~–9.99), which effectively distinguish them from I-type granites [97]. Moreover, in the ACF diagram, the samples plot within the S-type granite field (Figure 8a).
S-type granites can originate either from the fractional crystallization of basaltic magmas or from the deep melting of metamorphosed sedimentary rocks in the crust [113,114]. During fractional crystallization, the isotopic composition of the magma remains constant in a closed system, meaning that acid rocks formed through crystallization differentiation would exhibit isotopic compositions similar to those of the mafic parent magma. However, the Hf isotopic signature of samples (εHf(t) = −9.3~−2.2) is significantly lower than that of nearly coeval Banglei metamorphic basalts from the adjacent area (ca. 492 Ma, εHf(t) = −0.7~+7.5) (Figure 6). Therefore, the most likely origin is the partial melting of metamorphosed sedimentary rocks in the crust.
Additionally, the εHf(t) values of the samples are significantly higher than those of the strongly peraluminous Early Jurassic granites from central Lhasa (εHf(t) = −20.5~−16.0) (Figure 6) [106], indicating the involvement of mantle-derived materials. Compared with other contemporaneous S-type granites (Figure 6), the Guomangcuo granite generally exhibits higher εHf(t) values than those in other regions, such as Banglei in the Lhasa terrane (ca. 492 Ma, 538 Ma; εHf(t) = −14.7~−4.6) [11], Kangmar in the Himalaya terrane (ca. 478~500 Ma, εHf(t) = −17.8~1.99) [42], and Gyirong (ca. 486~474 Ma, εHf(t) = −13.6~−4.6) [42], but lower than those of the adjacent Zhaqian area (ca. 515 Ma, εHf(t) = −4.89~−0.3) [36] (Figure 1b). It can be comparable to those of Gemuri and Bensong Co in the southern Qiangtang terrane (ca. 486 Ma, εHf(t) = −8.5~−4.0) [60]. The two-stage Hf isotopic model age values, with a range of 1587~2033 Ma, suggest that the samples were derived from the ancient Mesoproterozoic crust. Notably, the Hf isotopic composition of sample Q22T4-2 (ca. 480 Ma) is more variable and heterogeneous than that of sample Q22T4-1, which may be attributed to a greater contribution of mantle-derived components. In conjunction with Nd isotopic data, the samples exhibit relatively low εNd(t) values (−10.72~−9.99), consistent with a crustal origin, but slightly higher than those of the strongly peraluminous Early Jurassic granites in the Lhasa terrane (εNd(t) = −14.79~−12.57) (Figure 7), further supporting the involvement of mantle-derived materials. The samples also display relatively high lead isotope ratios, and when plotted on the 07Pb/204Pb-206Pb/204P diagram (Figure 9) [115], the data points fall near the lower crustal field, which can also be corroborated by their depleted REE distribution patterns (Figure 3a).
The aluminous S-type granites formed by the crustal partial melting of metasedimentary rocks can be identified by whole-rock Rb/Sr, Rb/Ba, and CaO/Na2O ratios, which reflect the characteristics of their source region. In the Rb/Sr-Rb/Ba diagram (Figure 10a), most of our samples fall into the source region of the clay-rich, plagioclase-poor mudstone-derived melt. The CaO/Na2O ratio in granites is primarily controlled by plagioclase to clay ratio in the source region. Strongly peraluminous granites derived from clay-rich rocks with low plagioclase content exhibit CaO/Na2O < 0.3, while peraluminous granites derived from sandstones exhibit CaO/Na2O > 0.3 [114,116]. The CaO/Na2O ratio of the Guomang-Co granites have a range of 0.12~0.15, significantly lower than 0.3, indicating that their protolith was a metamorphosed mudstone. In the A/MF-C/MF diagram (Figure 10b), samples match with the model of partial melting of metamorphosed mudstone as well.
In summary, the Guomangcuo granite was most likely derived from the partial melting of Mesoproterozoic lower crustal metapelitic rocks, with a certain degree of mantle-derived material involvement.
Minerals 15 00284 g009
Figure 9. The 207Pb/204Pb-206Pb/204Pb diagrams [115]. EMI, EMII, HIMU, earth isochrone, and north hemisphere reference line after [117]; lower crust, mature arc, and upper crust after [115]. The area within the dashed lines represents the region of data concentration in each area.
Figure 9. The 207Pb/204Pb-206Pb/204Pb diagrams [115]. EMI, EMII, HIMU, earth isochrone, and north hemisphere reference line after [117]; lower crust, mature arc, and upper crust after [115]. The area within the dashed lines represents the region of data concentration in each area.
Minerals 15 00284 g009
Minerals 15 00284 g010
Figure 10. Diagram for magma source region discrimination. (a) Rb/Sr-Rb/Ba diagram [114]; (b) A/MF-C/MF diagram [118].
Figure 10. Diagram for magma source region discrimination. (a) Rb/Sr-Rb/Ba diagram [114]; (b) A/MF-C/MF diagram [118].
Minerals 15 00284 g010

5.2. Tectonic Setting and Significance

In orogenic belts around the world, S-type granites are closely associated with the partial melting of the thickened crust [96]. They typically form during the continental–continental collision stage of mountain building, while they can also form in continental arcs, back arcs, and post-collision settings [113,114,119]. However, discussing tectonic settings must first focus on the regional geological context.
The samples have a high SiO2 content, exhibiting peraluminous characteristics, and belong to the typical high-potassium calc-alkaline series. It is enriched in LILEs, depleted in HFSEs and shows negative δEu. These geochemical features are consistent with granites from active continental margins [98,120]. In the granite tectonic discrimination diagrams related to Nb, Ta, Rb (Figure 11a–d), the Guomangcuo granite samples fall into the syn-collision region. Notably, the sample data also fall within the region of granites related to slab break off [121]. In the Hf-Rb-Ta diagram (Figure 11e), the sample data fall within the late-collision to post-collision tectonic setting. Similarly, in the R1–R2 diagram (Figure 11f), the sample data also fall near the syn-collision region, post-collision. Taken together, the formation of the Guomangcuo granite aligns with a syn-collision to post-collision tectonic background.
Collins and Pisarevsky [126] summarized the spatiotemporal distribution patterns of the Pan-African orogeny on the East Gondwana continent, dividing it into two tectonic events. The early orogenic event occurred only in the eastern part of Africa and is referred to as the East African Orogeny (650~620 Ma), while the later orogenic event had a broader influence and is known as the Pan-African Orogeny. The latter includes the Kuunga Orogen (570~500 Ma) between southeast Antarctica and India, and the Malagasy Orogen (550~520 Ma) between East and West Gondwana. Subsequently, more researchers have supported this view, asserting that the Pan-African orogeny refers to a series of collisional orogenic events between different continental blocks within the Gondwana continent, with a timeframe concentrated at 570~520 Ma [10,31,33,35,36,127]. In contrast, the various blocks of the Tibetan Plateau and its surrounding regions (such as the Himalayan terrane, Lhasa terrane, and South Qiangtang terrane) were located along the northern margin of the Gondwana during the Early Paleozoic. Through our statistics of Early Paleozoic age from these regions (Table 1), it is not hard to find out that the tectonic movements mainly occurred at 530~460 Ma, which is generally 40~60 Ma later than the timing of the Pan-African orogeny. Therefore, we do not consider these magmatic events to be part of the Pan-African orogeny. It is worth noting that most of the granites reported in these records are S-type granites. Although an extensional setting can also produce S-type granites, it does not provide the geological conditions for the formation of large-scale S-type granites.
On the basis of the principle of global volume balance, Cawood et al. [10] proposed that after the end of the Pan-African orogeny, a new subduction zone formed along the northern margin of the East Gondwana, leading to Andean-type accretionary orogeny. This viewpoint fully considers the global tectonic evolution and the delayed tectonic movements in the Early Paleozoic of the Tibetan Plateau and its surrounding regions, and may be consistent with the Ediacaran-Cambrian Cadomian orogeny on the northern margin of West Gondwana [128,129,130]. It has since been widely accepted by many scholars [11,12,35,36,49,131]. The Early Paleozoic magmatic rocks are believed to be related to the subduction and consumption of oceanic crust [36,38], and micro-continental block collisions occurred at the edge of the Andes magmatic arc [11,44].
Through the study of the Early Paleozoic bimodal magmatism in the Lhasa terrane, Zhu et al. [11] proposed an Andean-type subduction-slab break-off evolution model. According to this model, magmatic activity at the margin of the Gondwana continent has exsited around 536 Ma. As the subduction depth of the Proto-Tethys oceanic crust increased, the oceanic plate sank under gravity. Around 510 Ma, the slab began to retreat, and subsequently, the back-arc basin underwent extension, accompanied by asthenosphere upwelling, triggering deep melting of the continental crust and resulting in extensive magmatic activity. Around 492 Ma, slab break-off occurred, and the upwelling asthenosphere initiated large-scale magmatic activity, which also marked the onset of post-collision orogeny.
The Guomangcuo granite supports the hypothesis of Andean-type subduction, aligning well with the aforementioned evolutionary model. Notably, in the adjacent Zhaqian area (Figure 1b), a Cambrian–Ordovician angular unconformity is present. The overlying undeformed Lower Ordovician strata are nearly orthogonal (~90°) to the underlying strongly deformed Cambrian strata [76]. A volcanic interlayer within the underlying sequence has yielded an age of ca. 501 Ma, thereby constraining the termination of the collisional event to after this time. Thus, the syn-collisional phase likely occurred during the Cambrian, corresponding to the ca. 530 Ma age of the samples. By the early Ordovician (ca. 480 Ma), slab break-off triggered partial melting of the mantle, which in turn facilitated deep crustal anatexis. Some mantle-derived material mixed with the metasedimentary-derived melts, modifying the isotopic composition of the magma (Figure 12). This transition marked the shift of the Andean-type orogenic process into its post-orogenic stage, which also explains why the sample data plot near the post-orogenic field in tectonic discrimination diagrams (Figure 11c,e,f).
Our research provides new constraints for the study of the Early Paleozoic evolution of the Proto-Tethys Ocean and supplements the Early Paleozoic data of the Lhasa terrane.

6. Conclusions

The Guomang-Co granites are a set of dark mylonitized granite newly defined from the originally defined Nyainqengtanglha Group (AnZNq). Its main components are quartz and alkaline feldspar, with no significant mineralogical phase changes. The protolith is considered to be an alkaline granite.
The zircon U-Pb age results for the two samples of Guomangcuo granite are 529.4 ± 3.0 Ma and 479.8 ± 2.5 Ma, corresponding to the Early Cambrian and Early Ordovician, respectively, indicating two magmatic events during the Early Paleozoic in this region.
The Guomang-Co granites exhibit classic S-type geochemical signatures, including peraluminous composition (A/CNK = 1.09~1.13), high-potassium calc-alkaline, negative Nd, Hf systematics (εNd(t) = −10.72~−9.99, εHf(t) = −2.20~−9.33). It may originate from partial melting of lower crustal Paleo-Proterozoic mudstone influenced by mantle-derived components, likely a product of the Andean-type orogeny along the northern margin of Gondwana in the Early Paleozoic, indicating the existence of the Proto-Tethys Ocean’s southward subduction during the Cambrian–Ordovician period.

Supplementary Materials

The following supporting information can be downloaded at https://www.mdpi.com/article/10.3390/min15030284/s1; Table S1: Geochemistry and Sr-Nd-Pb-Hf isotope data of Guomang-Co granite samples.

Author Contributions

Conceptualization, Y.Z.; formal analysis, Y.Z.; investigation, Z.L.; writing—original draft preparation, Y.Z.; writing—review and editing, M.W. and C.Y.; supervision, M.W.; funding acquisition, M.W. and C.Y. All authors have read and agreed to the published version of the manuscript.

Funding

This work was supported by the Deep Earth Probe and Mineral Resources Exploration-National Science and Technology Major Project (Grant No.2024ZD1000100), the National Key R&D Program of China (Grant No. 2022YFC3080200), the Scientific Research Project of the Education Department of Jilin Province (Grant No. JJKH20241254KJ), and Graduate Innovation Fund of Jilin University (Grant No. 2024CX102).

Data Availability Statement

The data presented in this study are available in this paper.

Acknowledgments

We acknowledge anonymous reviewers of their constructive reviews and valuable suggestions that led to great improvement in the presentation of the paper. We also thank Teng Wang for his help in data collection in this paper.

Conflicts of Interest

The authors declare that they have no competing interests.

References

  1. Stampfli, G.M.; Borel, G.D. A plate tectonic model for the Paleozoic and Mesozoic constrained by dynamic plate boundaries and restored synthetic oceanic isochrons. Earth Planet. Sci. Lett. 2002, 196, 17–33. [Google Scholar] [CrossRef]
  2. Stampfli, G.M.; Hochard, C.; Vérard, C. The formation of Pangea. Tectonophysics 2013, 593, 1–19. [Google Scholar] [CrossRef]
  3. Cocks, L.R.M.; Torsvik, T.H. The Palaeozoic geography of Laurentia and western Laurussia: A stable craton with mobile margins. Earth Sci. Rev. 2011, 106, 1–51. [Google Scholar] [CrossRef]
  4. Wu, F.-Y.; Wan, B.; Zhao, L.; Xiao, W.-J.; Zhu, R.-X. Tethyan geodynamics. Acta Petrol. Sin. 2020, 36, 1627–1674. [Google Scholar]
  5. Zhao, G.-C.; Wang, Y.-J.; Huang, B.-C.; Dong, Y.-P.; Li, S.-Z.; Zhang, G.-W.; Yu, S. Geological reconstructions of the East Asian blocks: From the breakup of Rodinia to the assembly of Pangea. Earth Sci. Rev. 2018, 186, 262–286. [Google Scholar] [CrossRef]
  6. Wilhem, C.; Windley, B.F.; Stampfli, G.M. The Altaids of Central Asia: A tectonic and evolutionary innovative review. Earth Sci. Rev. 2012, 113, 303–341. [Google Scholar] [CrossRef]
  7. Miller, C.; Thöni, M.; Frank, W. The early Palaeozoic magmatic event in the Northwest Himalaya, India: Source, tectonic setting and age of emplacement. Geol. Mag. 2001, 138, 237–251. [Google Scholar] [CrossRef]
  8. Ji, W.-Q.; Wu, F.-Y.; Chung, S.-L. Zircon U–Pb geochronology and Hf isotopic constraints on petrogenesis of the Gangdese batholith, southern Tibet. Chem. Geol. 2009, 262, 229–245. [Google Scholar] [CrossRef]
  9. Pan, G.-T.; Wang, L.-Q.; Zhang, W.-P.; Wang, B.-D.; Pan, G.T.; Wang, L.Q.; Li, R.S.; Yuan, S.H.; Ji, W.H.; Yin, F.G.; et al. Tectonic evolution of the Qinghai-Tibet plateau. Asian Earth Sci. 2012, 53, 314. [Google Scholar] [CrossRef]
  10. Cawood, P.A.; Johnson, M.R.W.; Nemchin, A.A. Early Palaeozoic orogenesis along the Indian margin of Gondwana: Tectonic response to Gondwana assembly. Earth Planet. Sci. Lett. 2007, 255, 70–84. [Google Scholar] [CrossRef]
  11. Zhu, D.-C.; Zhao, Z.-D.; Niu, Y.-L.; Dilek, Y.; Wang, Q.; Ji, W.-H.; Dong, G.-C.; Sui, Q.-L.; Liu, Y.-S.; Yuan, H.-L.; et al. Cambrian bimodal volcanism in the Lhasa Terrane, southern Tibet: Record of an early Paleozoic Andean-type magmatic arc in the Australian proto-Tethyan margin. Chem. Geol. 2012, 328, 290–308. [Google Scholar] [CrossRef]
  12. Wang, Y.-J.; Xing, X.-W.; Cawood, P.A.; Lai, S.-C.; Xia, X.-P.; Fan, W.-M.; Liu, H.-C.; Zhang, F.-F. Petrogenesis of early Paleozoic peraluminous granite in the Sibumasu Block of SW Yunnan and diachronous accretionary orogenesis along the northern margin of Gondwana. Lithos 2013, 182–183, 67–85. [Google Scholar] [CrossRef]
  13. Liu, G.-C. Petrology Component and Geochronology of Early Paleozoic Proto-Tethys Ophiolitemélange in SW Yunnan. Ph.D. Thesis, China University of Geosciences, Wuhan, China, 2020. [Google Scholar]
  14. Liu, G.-C.; Zi, J.-W.; Nie, X.-M.; Santosh, M.; Zhu, C.; Wang, W.; Zhao, T.-Y.; Chen, G.-Y.; Feng, Q.-L. Late Cambrian Magmatic Events in SW Yunnan and Implications for the Tectonic Reconstruction of Northern Gondwana. J. Earth Sci. 2024, 35, 1407–1425. [Google Scholar] [CrossRef]
  15. Kennedy, W.Q. The structural differentiation of Africa in the Pan-Africa (±500 my) tectonic episode. Univ. Leeds Res. Inst. Afr. Geol. Ann. Rept. 1964, 8, 48–49. [Google Scholar]
  16. Xu, Z.-Q.; Yang, J.-S.; Liang, F.-H.; Qi, X.-X.; Liu, F.-C.; Zeng, L.-S.; Liu, M.-Y.; Li, H.-B.; Wu, C.-L.; Shi, R.-D.; et al. Pan-African and Early Paleozoic orogenic events in the Himalaya terrane: Inference from SHRlMP U-Ph zircon ages. Acta Petrol. 2005, 21, 3–14. [Google Scholar]
  17. Liu, W.-C.; Zhou, Z.-G.; Zhang, X.-X.; Zhao, X.-G. SHRIMP zircon geochronological constraints on a Pan-African orogeny in the Yadong Area, Southern Tibet. Geochim. Cosmochim. Acta Suppl. 2006, 70, A365. [Google Scholar] [CrossRef]
  18. Li, C.; Xie, Y.-W.; Sha, S.-L.; Dong, Y.-S. SHRIMP U-Pb zircon dating of the Pan-African granite in Baxoi County, eastern Tibet, China. Geol. Bull. China 2008, 27, 64–68. [Google Scholar]
  19. Hu, P.-Y.; Li, C.; Su, L.; Li, C.-B.; Yu, H. Zircon U-Pb dating of granitic gneiss in Wugong Mountain area, central Qiangtang, Qinghai-Tibet Plateau: Age records of Pan-African movement and Indo-China movement. Geol. China 2010, 37, 1050–1061. [Google Scholar]
  20. Xie, C.-M.; Li, C.; Su, L.; Wu, Y.-W.; Wang, M.; Yu, H. LA-ICP-MS U-Pb dating of zircon from granite-gneiss in the Amdo area, northern Tibet, China. Geol. Bull. China 2010, 29, 1737–1744. [Google Scholar]
  21. Liu, Q.-S.; Ye, P.-S.; Wu, Z.-H. SHRIMP zircon U-Pb dating and petrogeochemistry of Ordovician granite bodies in the southern segment of Gaoligong Mountain, western Yunnan Province. Geol. Bull. China 2012, 31, 250–257. [Google Scholar]
  22. Lin, S.-L.; Cong, F.; Gao, Y.-J.; Zou, G.-F. LA-ICP-MS zircon U-Pb age of gneiss from Gaoligong Mountain Group on the southeastern margin of Tengchong block in western Yunnan Province. Geol. Bull. China 2012, 31, 258–263. [Google Scholar]
  23. Wang, Y.-W.; Zhou, Q.; Xie, Q.-X.; Sun, P.; Zhang, J.-R.; Wang, H.; Xiao, L. Pan-African and Early Paleozoic Geological Orogenic Events in the Tethyan Himalaya: From Chronological Evidence of Gneissic Monzonitic Granite, Kangma, Tibet. Bull. Geol. Sci. Technol. 2016, 35, 30. [Google Scholar]
  24. Murphy, J.B.; Nance, R.D. Supercontinent model for the contrasting character of Late Proterozoic orogenic belts. Geology 1991, 19, 469–472. [Google Scholar] [CrossRef]
  25. Brookfield, M.E. The Himalayan passive margin from Precambrian to Cretaceous times. Sediment. Geol. 1993, 84, 1–35. [Google Scholar] [CrossRef]
  26. Wang, M.; Li, C.; Fan, J.-J. Geochronology and geochemistry of the Dabure basalts, central Qiangtang, Tibet: Evidence for~550 Ma rifting of Gondwana. Int. Geol. Rev. 2015, 57, 1791–1805. [Google Scholar] [CrossRef]
  27. Wang, M.; Li, C.; Xie, C.-M. Dating of detrital zircons from the Dabure clastic rocks: The discovery of Neoproterozoic strata in southern Qiangtang, Tibet. Int. Geol. Rev. 2016, 58, 216–227. [Google Scholar] [CrossRef]
  28. Pan, X.-P.; Li, R.-S.; Wang, C.; Yu, P.-S.; Gu, P.-Y.; Zha, X.-F. Geochemical characteristics of the Cambrian volcanic rocks in Banglecun area on the northern margin of Gangdise, Nyima County, Tibet. Geol. Bull. China 2012, 31, 63–74. [Google Scholar]
  29. Gu, P.-Y.; He, S.-P.; Li, R.-S.; Shi, C.; Dong, Z.-C.; Zha, X.-F.; Wu, J.-L.; Wang, Y. Geochemical features and tectonic significance of granitic gneiss of Laguigangri metamorphic core complexes in southern Tibet. Acta Petrolog. Sin. 2013, 29, 756–768. [Google Scholar]
  30. Yang, X.-J.; Jia, X.-C.; Xiong, C.-L.; Bai, X.-Z.; Huang, B.-X.; Luo, G.; Yang, C.-B. LA-ICP-MS zircon U-Pb age of metamorphic basic volcanic rock in Gongyanghe Group of southern Gaoligong Mountain, western Yunnan Province, and its geological significance. Geol. Bull. China 2012, 31, 264–276. [Google Scholar]
  31. Liu, Y.-M. Magmatism at 550~450 Ma Within the SouthQiangtang-Baoshan Plate of the Tibetan Plateau: Constraintson the Tectonic Evolution of the Basement of the northernGondwana Margin. Ph.D. Thesis, Jinlin University, Changchun, China, 2017. [Google Scholar]
  32. Lv, P.-R.; Zhang, H.-D.; Luo, Y.-J.; Yao, W.-G. LA-ICP-MS Zircon U-Pb Dating of Granitic Gneiss from Yadong Area in South Tibet and Its Geochemical Characteristics. Earth Sci. 2018, 43, 4459–4474. [Google Scholar]
  33. Zhang, T.-Y. Early Paleozoic Tectonic Movement on the Tibetan Plateauand Its Adjacent Areas: A Case Study of Cambrian-Ordovician Unconformity. Ph.D. Thesis, Jinlin University, Changchun, China, 2018. [Google Scholar]
  34. Gehrels, G.E.; DeCelles, P.G.; Martin, A.; Ojha, T.P.; Pinhassi, G. Initiation of the Himalayan orogen as an early Paleozoic thin-skinned thrust belt. GSA Today 2003, 13, 4–9. [Google Scholar] [CrossRef]
  35. Zhang, Z.-M.; Wang, J.-L.; Shen, K.; Shi, C. Paleozoic circum-Gondwana orogens: Petrology and geochronology of the Namche Barwa Complex in the eastern Himalayan syntaxis, Tibet. Acta Petrolog. Sin. 2008, 24, 1627–1637. [Google Scholar]
  36. Hu, P.-Y.; Li, C.; Wang, M.; Xie, C.-M.; Wu, Y.-W. Cambrian volcanism in the Lhasa terrane, southern Tibet: Record of an early Paleozoic Andean-type magmatic arc along the Gondwana proto-Tethyan margin. J. Asian Earth Sci. 2013, 77, 91–107. [Google Scholar] [CrossRef]
  37. Xie, C.-M.; Li, C.; Su, L.; Wu, Y.-W.; Xie, Y.-W. Pan-African and early Paleozoic tectonothermal events in the Nyainrong microcontinent: Constraints from geochronology and geochemistry. Sci. China Earth Sci. 2014, 56, 2066–2079. [Google Scholar] [CrossRef]
  38. Ding, H.-X.; Zhang, Z.-M.; Dong, X.; Yan, R.; Lin, Y.-H.; Jiang, H.-Y. Cambrian ultrapotassic rhyolites from the Lhasa terrane, south Tibet: Evidence for Andean-type magmatism along the northern active margin of Gondwana. Gondwana Res. 2014, 27, 1616–1629. [Google Scholar] [CrossRef]
  39. Lee, J.; Whitehouse, M.J. Onset of mid-crustal extensional flow in southern Tibet: Evidence from U/Pb zircon ages. Geology 2007, 35, 45–48. [Google Scholar] [CrossRef]
  40. Quigley, M.C.; Liangjun, Y.; Gregory, C.; Corvino, A.; Sandiford, M.; Wilson, C.J.L.; Xiaohan, L. U–Pb SHRIMP zircon geochronology and T–t–d history of the Kampa Dome, southern Tibet. Tectonophysics 2008, 446, 97–113. [Google Scholar] [CrossRef]
  41. Lee, J.; Hacker, B.R.; Dinklage, W.S.; Wang, Y.; Gans, P.; Calvert, A.; Wan, J.-L.; Chen, W.-J.; Blythe, A.E.; McClelland, W. Evolution of the Kangmar Dome, southern Tibet: Structural, petrologic, and thermochronologic constraints. Tectonics 2000, 19, 872–895. [Google Scholar] [CrossRef]
  42. Wang, X.-X.; Zhang, J.-J.; Santosh, M.; Liu, J.; Yan, S.-Y.; Lei, G. Andean-type orogeny in the Himalayas of south Tibet: Implications for early Paleozoic tectonics along the Indian margin of Gondwana. Lithos 2012, 154, 248–262. [Google Scholar] [CrossRef]
  43. Gao, L.-E.; Zeng, L.-S.; Hu, G.-Y.; Wang, Y.-Y.; Wang, Q.; Guo, C.-L.; Hou, K.-J. Early Paleozoic magmatism along the northern margin of East Gondwana (Review). Lithos 2019, 334–335, 25–41. [Google Scholar] [CrossRef]
  44. Wang, X.-X.; Zhang, J.-J.; Yang, X.-Y.; Zhang, B. Zircon SHRIMP U-Pb ages, Hf isotopie features and their geologicalsiqnificance of the Greater Himalayan Crystalline Complex augen qneiss in Gyirong Area, south Tibet. Earth Sci. Front. 2011, 18, 127–139. [Google Scholar]
  45. Shi, C.; Li, R.-S.; He, S.-P.; Wang, C.; Pan, S.-J.; Liu, Y.; Gu, P.-Y. LA-ICP-MS zircon U-Pb dating for gneissic garnet-bearing bi otite granodiorite in the Yadong area, southern Tibet, China and its geological significance. Geol. Bull. China 2010, 29, 1745–1753. [Google Scholar]
  46. Zhang, Z.-M.; Dong, X.; Santosh, M.; Liu, F.; Wang, W.; Yiu, F.; He, Z.-Y.; Shen, K. Petrology and geochronology of the Namche Barwa Complex in the eastern Himalayan syntaxis, Tibet: Constraints on the origin and evolution of the north-eastern margin of the Indian Craton. Gondwana Res. 2012, 21, 123–137. [Google Scholar] [CrossRef]
  47. Yang, D.-T. Geochronology, Geochemistry and Tectonic Implication of EarlyPaleozoic Granitic Gneisses in the Dinggyê Area, Southern Tibet. Master’s Thesis, Chinese Academy of Geological Science, Beijing, China, 2015. [Google Scholar]
  48. Liu, Z.-C.; Wu, F.-Y.; Ding, L.; Liu, X.-C.; Wang, J.-G.; Ji, W.-Q. Highly fractionated Late Eocene (~35 Ma) leucogranite in the Xiaru Dome, Tethyan Himalaya, South Tibet. Lithos 2016, 240–243, 337–354. [Google Scholar] [CrossRef]
  49. Zhang, S.-Z.; Li, F.-Q.; Li, Y.; Liu, W.; Qin, Y.-D. Early Ordovician strongly peraluminous granite in the middle section of the Yarlung Zangbo junction zone and its geological significance. Sci. China Earth Sci. 2014, 57, 630–643. [Google Scholar] [CrossRef]
  50. Gehrels, G.E.; DeCelles, P.G.; Ojha, T.P.; Upreti, B.N. Geologic and U-Th-Pb geochronologic evidence for early Paleozoic tectonism in the Kathmandu thrust sheet, central Nepal Himalaya. Geol. Soc. Am. Bull. 2006, 118, 185–198. [Google Scholar] [CrossRef]
  51. Gehrels, G.E.; DeCelles, P.G.; Ojha, T.P.; Upreti, B.N. Geologic and U–Pb geochronologic evidence for early Paleozoic tectonism in the Dadeldhura thrust sheet, far-west Nepal Himalaya. J. Asian Earth Sci. 2006, 28, 385–408. [Google Scholar] [CrossRef]
  52. DeCelles, P.G.; Gehrels, G.E.; Quade, J.; LaReau, B.; Spurlin, M. Tectonic implications of U-Pb zircon ages of the Himalayan Orogenic Belt in Nepal. Science 2000, 288, 497–499. [Google Scholar] [CrossRef]
  53. Girard, M.; Bussy, F. Late Pan-African magmatism in the Himalaya: New geochronological and geochemical data from the Ordovician Tso Morari metagranites (Ladakh, NW India). Schweiz. Mineral. Petrogr. Mitt. 1999, 79, 399–418. [Google Scholar]
  54. Johnson, M.R.W.; Oliver, G.J.H.; Parrish, R.R.; Johnson, S.P. Synthrusting metamor phism, cooling and erosion of the Himalayan Kathmandu complex, Nepal. Tectonics 2001, 20, 394–415. [Google Scholar] [CrossRef]
  55. Liu, Y.-M.; Li, C.; Xie, C.-M.; Fan, J.-J.; Wu, H.; Jiang, Q.-Y.; Li, X. Cambrian granitic gneiss within the central Qiangtang terrane, Tibetan Plateau: Implications for the early Palaeozoic tectonic evolution of the Gondwanan margin. Int. Geol. Rev. 2016, 58, 1043–1063. [Google Scholar] [CrossRef]
  56. Wang, H.-T.; Zhai, Q.-G.; Hu, P.-Y.; Zeng, L.-S.; Tang, Y.; Zhu, Z.-C. Early Paleozoic granitic rocks of the South Qiangtang Terrane, northern Tibetan Plateau: Implications for subduction of the Proto- (Paleo-) Tethys Ocean. J. Asian Earth Sci. 2020, 204, 104579. [Google Scholar] [CrossRef]
  57. Liu, Y.-M.; Xie, C.-M.; Li, C.; Li, S.-Z.; Santosh, M.; Wang, M.; Fan, J.-J. Breakup of the northern margin of Gondwana through lithospheric delamination: Evidence from the Tibetan Plateau. Geol. Soc. Am. Bull. 2019, 131, 675–694. [Google Scholar] [CrossRef]
  58. Pullen, A.; Kapp, P.; Gehrels, G.E.; Ding, L.; Zhang, Q. Metamorphic rocks in central Tibet: Lateral variations and implications for crustal structure. Bulletin 2011, 123, 585–600. [Google Scholar] [CrossRef]
  59. Peng, Z.M.; Geng, Q.R.; Wang, L.Q.; Zhang, Z.; Guan, J.L.; Cong, F.; Liu, S.S. Zircon U-Pb ages and Hf isotopic characteristics of granitic gneiss from Bunsumco, central Qiangtang, Qinghai-Tibet Plateau. Chin. Sci. Bull. 2014, 59, 2621–2629. (In Chinese) [Google Scholar]
  60. Hu, P.-Y.; Zhai, Q.-G.; Jahn, B. Early Ordovician granites from the South Qiangtang terrane, northern Tibet: Implications for the early Paleozoic tectonic evolution along the Gondwanan proto-Tethyan margin. Lithos 2015, 220, 318–338. [Google Scholar] [CrossRef]
  61. Wang, H.-T.; Zhai, Q.-G.; Hu, P.-Y.; Zeng, L.-S.; Tang, Y.; Zhu, Z.-C. Late Cambrian to Early Silurian Granitic Rocks of the Gemuri Area, Central Qiangtang, North Tibet: New Constraints on the Tectonic Evolution of the Northern Margin of Gondwana. Acta Geol. Sin. 2020, 94, 1007–1019. [Google Scholar] [CrossRef]
  62. Zheng, Y.-L.; Wang, G.-H.; Guo, Z.-W.; Liang, X.; Yuan, G.-L.; Wang, H.-D.; Huang, B.; He, Y.-D. The record of the Pan African and the Indosinian tectono-thermal event in Qiangtang terrane, northern Tibet: Evidence from geochemical characteristics and U-Pb geochronology of the metamorphic complex in Ejiumai area. Acta Petrol. Sin. 2015, 31, 1137–1152. [Google Scholar]
  63. Xie, C.-M.; Li, C.; Fan, J.-J.; Su, L. Ordovician sedimentation and bimodal volcanism in the Southern Qiangtang terrane of northern Tibet: Implications for the evolution of the northern Gondwana margin. Int. Geol. Rev. 2017, 59, 2078–2105. [Google Scholar] [CrossRef]
  64. Xie, C.-M.; Li, C.; Fan, J.-J.; Wang, M.; Liu, Y.-M.; Zhang, H.-Y. Establishment of Middle-Upper Ordovician Dawashan Formationin central Oiangtang, Tibetan Plateau, and its significance. Geol. Bull. China 2015, 34, 1812–1820. [Google Scholar]
  65. Ren, F.; Yin, F.-G.; Xu, B.; Liu, H.-L.; Fan, B.-L.; Xu, C.-H.; Bai, J.-G. Zircon U-Pb age and Hf isotope of Early Paleozoic granite from the Jitang area in eastern Tibet and its insight into the evolution of the Proto-Tethys Ocean. Geol. Bull. China 2021, 40, 1865–1876. [Google Scholar]
  66. Ji, W.-H.; Chen, S.-J.; Zhao, Z.-M.; Li, R.-S.; He, S.-P.; Wang, C. Discovery of the Cambiran volcanic rocks in the Xainza area, Gangdese orogenic belt, Tibet, China and its significance. Geol. Bull. China 2009, 28, 1350–1354. [Google Scholar]
  67. Gehrels, G.; Kapp, P.; DeCelles, P.; Pullen, A.; Blakey, R.; Weislogel, A.; Ding, L.; Guynn, J.; Martin, A.; McQuarrie, N.; et al. Detrital zircon geochronology of pre-Tertiary strata in the Tibetan-Himalayan orogen. Tectonics 2011, 30, TC5016. [Google Scholar] [CrossRef]
  68. Kang, C.; Dai, K.; Li, H.; Liang, C.; Chen, X.; Zha, X.; Wang, T.; Li, J. The Cambrian metamorphic granites in the Jili area, Baxoi, Xizang: U-Pb dating, geochemical signatures and geological significance. Sediment. Geol. 2019, 39, 1–13. [Google Scholar]
  69. Dong, X.; Zhang, Z.-M. Cambrian granitoids from the southeastern Tibetan Plateau: Research on petrology and zircon Hf isotope. Acta Petrolog. Sin. 2015, 31, 1183–1199. [Google Scholar]
  70. Dong, X.; Zhang, Z.-M.; Wang, J.-L.; Zhao, G.-C.; Liu, F.; Wang, W.; Yu, F. Provenance and formation age of the Nyingchi Group in the southern Lhasa terrane, Tibetan Plateau: Petrology and zircon U-Pb geochronology. Acta Petrolog. Sin. 2009, 25, 1678–1694. [Google Scholar]
  71. Guynn, J.; Kapp, P.; Gehrels, G.E.; Ding, L. U-Pb geochronology of basement rocks in central Tibet and paleogeographic implications. J. Asian Earth Sci. 2012, 43, 23–50. [Google Scholar] [CrossRef]
  72. Xu, R.-H.; Schärer, U.; Claude, J. Allègre.Magmatism and Metamorphism in the Lhasa Block (Tibet): A Geochronological Study. J. Geol. 1985, 93, 41–57. [Google Scholar] [CrossRef]
  73. Li, C.; Huang, X.-P.; Zhai, Q.-G.; Zhu, T.-X.; Yu, Y.-S.; Wang, G.-H.; Zeng, Q.-G. The Longmu Co-Shuanghu-Jitang plate suture andthe northern boundary of Gondwanaland in the Qinghai-Tibet plateau. Earth Sci. Front. 2006, 13, 136–147. [Google Scholar]
  74. Zhu, D.-C.; Zhao, Z.-D.; Niu, Y.-L.; Wang, Q.; Dilek, Y.; Dong, G.-C.; Mo, X.-X. Origin and Paleozoic Tectonic Evolution of the Lhasa Terrane. Geol. J. China Univ. 2012, 18, 1–15. [Google Scholar]
  75. Xu, M.-J.; Li, C.; Wu, Y.-W.; Xie, C.-M. Geochemical characteristics and sedimentary environments of siliceous rocks in Guomang-Co ophiolitic mélange of Tibet. Geol. Bull. China 2014, 33, 1061–1066. [Google Scholar]
  76. Li, C.; Wu, Y.-W.; Wang, M.; Yang, H.-T. Significant progress on Pan-African and Early Paleozoic orogenic events in Qinghai-Tibet Plateau—Discovery of Pan-African orogenic unconformity and Cambrian System in the Gangdise area, Tibet, China. Geol. Bull. China 2010, 29, 1733–1736. [Google Scholar]
  77. Hu, D.; Wu, Z.; Jiang, W.; Shi, Y.; Ye, P.; Liu, Q. SHRIMP zircon U-Pb age and Nd isotope study of the Nianqing Tanggula Group in Tibet. Sci. China Ser. D Earth Sci. 2005, 48, 1377–1386. [Google Scholar] [CrossRef]
  78. Wu, Y.; Ma, X.-X.; Zhsng, Z.-P.; Jiao, S.-W.; Duan, K.; Dong, H.; Wang, X.-W.; Ma, T.; Li, P.-J.; Liang, Z.-Y.; et al. Geochemical Features of the Nyainqentanglha Group in the Western Lhasa Terrane, Western Tibet and Their Tectonic Significance. Acta Geol. Sin. 2016, 90, 3081–3098. [Google Scholar]
  79. Yu, H. Mineral Geochemical Characteristics and Genetic Mechanism of Olivine Rocks in Shangnan, Shanxi. Master’s Thesis, China University of Geosciences, Beijing, China, 2011. [Google Scholar]
  80. Li, W.-Q. Testing accuracy of 10 major elements in diabase by borate melting sample preparation method. World Geol. 2019, 38, 843–851. [Google Scholar]
  81. Wiedenbeck, M.; Alle, P.; Corfu, F.Y. Three natural zircon standards for U-Th-Pb, Lu-Hf, trace element and REE analyses. Geostand. Newslett. 1995, 19, 1–23. [Google Scholar] [CrossRef]
  82. Jackson, S.E.; Pearson, N.J.; Griffin, W.L. The application of laser ablation-inductively coupled plasma-mass spectrometry to in situ U–Pb zircon geochronology. Chem. Geol. 2004, 211, 47–69. [Google Scholar] [CrossRef]
  83. Hao, Y.-J.; Ren, Y.-S.; Zhao, H.-L.; Lai, K.; Zhao, X.; Ma, Y.-P. Metallogenic mechanism and tectonic setting of tungsten mineralization in the Yangbishan deposit in northeastern China. Acta Geol. Sin. 2018, 92, 241–267. [Google Scholar] [CrossRef]
  84. Liu, J.-F.; Chi, X.G.; Dong, C.-Y.; Zhao, Z.-L.; Guan, R.; Zhao, Y.-D. Discovery of Early Paleozoic granites in the eastern Xiao Hinggan Mountains, northeastern China and their tectonic significance. Geol. Bull. China 2008, 27, 534–544. [Google Scholar]
  85. Ludwig, K.R. Isoplot version 4.15: A geochronological toolkit for microsoft Excel; Berkeley Geochronology Center, Special Publication: Berkeley, CA, USA, 2008; Volume 4, pp. 247–270. [Google Scholar]
  86. Hou, K.-J. Laser ablation-MC-ICP-MS technique for Hf isotope microanalysis of zircon and its geological applications. Acta Petrol. Sin. 2007, 23, 2595–2604. [Google Scholar]
  87. Söderlund, U.; Patchett, P.J.; Vervoort, J.D. The 176Lu decay constant determined by Lu–Hf and U–Pb isotope systematics of Precambrian mafic intrusions. Earth Planet. Sci. Lett. 2004, 219, 311–324. [Google Scholar] [CrossRef]
  88. Bouvier, A.; Vervoort, J.D.; Patchett, P.J. The Lu–Hf and Sm–Nd isotopic composition of CHUR: Constraints from unequilibrated chondrites and implications for the bulk composition of terrestrial planets. Earth Planet. Sci. Lett. 2008, 273, 48–57. [Google Scholar] [CrossRef]
  89. Griffin, W.L.; Wang, X.; Jackson, S.E. Zircon chemistry and magma mixing, SE China: In-situ analysis of Hf isotopes, Tonglu and Pingtan igneous complexes. Lithos 2002, 61, 237–269. [Google Scholar] [CrossRef]
  90. Liang, X.-R. Precise measurement of 143Nd/144Nd and Sm/Na ratios using multiple collectors-inductively coupled plasma mass spectrometer (MC-ICPMS). Geochimica 2003, 32, 91–96. [Google Scholar]
  91. Rollinson, H.R. Using Geochemical Data: Evaluation, Presentation, Interpretation; Routledge: London, UK, 2014. [Google Scholar]
  92. Taylor, S.R.; McLennan, S.M. The Continental Crust: Its Composition and Evolution. 1985. Available online: https://www.osti.gov/biblio/6582885 (accessed on 3 January 2025).
  93. Sun, S.S.; McDonough, W.F. Chemical and isotopic systematics of oceanic basalt: Implication for mantle composition and processes. Geol. Soc. Lond. Spec. Publ. 1989, 42, 313–345. [Google Scholar] [CrossRef]
  94. Rudnick, R.L.; Fountain, D.M. Nature and composition of the continental crust: A lower crustal perspective. Rev. Geophys. 1995, 33, 267–309. [Google Scholar] [CrossRef]
  95. Kelsey, C.H. Calculation of the CIPW norm. Mineral. Mag. 1965, 34, 276–282. [Google Scholar]
  96. Chappell, B.W.; White, A.J.R. I-and S-type granites in the Lachlan Fold Belt. Earth Environ. Sci. Trans. R. Soc. Edinb. 1992, 83, 1–26. [Google Scholar]
  97. Chappell, B.W.; White, A.J. Two contrasting granite types: 25 years later. Aust. J. Earth Sci. 2001, 48, 489–499. [Google Scholar] [CrossRef]
  98. Hou, Q.-L. Advanced Structural Geology; Science Press: Beijing, China, 2018; Volume 1. [Google Scholar]
  99. Irber, W. The lanthanide tetrad effect and its correlation with K/Rb, Eu/Eu∗, Sr/Eu, Y/Ho, and Zr/Hf of evolving peraluminous granite suites. Geochim. Cosmochim. Acta 1999, 63, 489–508. [Google Scholar] [CrossRef]
  100. Middlemost, E.A.K. Naming materials in the magma/igneous rock system. Earth Sci. Rev. 1994, 37, 215–224. [Google Scholar] [CrossRef]
  101. Rickwood, P.C. Boundary lines within petrologic diagrams which use oxides of major and minor elements. Lithos 1989, 22, 247–263. [Google Scholar] [CrossRef]
  102. Maniar, P.D.; Piccoli, P.M. Tectonic discrimination of granitoids. Geol. Soc. Am. Bull. 1989, 101, 635–643. [Google Scholar] [CrossRef]
  103. Streckeisen, A.L. Classification of the common igneous rocks by means of their chemical composition: A provisional attempt. N. Jb. Miner. Mon. 1976, 1, 1–15. [Google Scholar]
  104. Hoskin, P.W.; Schaltegger, U. The composition of zircon and igneous and metamorphic petrogenesis. Rev. Mineral. Geochem. 2003, 53, 27–62. [Google Scholar] [CrossRef]
  105. Vavra, G.; Schmid, R.; Gebauer, D. Internal morphology, habit and U-Th-Pb microanalysis of amphibolite-to-granulite facies zircons: Geochronology of the Ivrea Zone (Southern Alps). Contrib. Mineral. Petrol. 1999, 134, 380–404. [Google Scholar] [CrossRef]
  106. Zhu, D.-C.; Zhao, Z.-D.; Niu, Y.; Mo, X.-X.; Chung, S.-L.; Hou, Z.-Q.; Wang, L.-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]
  107. Hu, P.-Y.; Zhai, Q.-G.; Wang, J.; Tang, Y.; Wang, H.-T.; Zhu, Z.-C.; Wu, H. Middle Neoproterozoic (ca. 760 Ma) arc and back-arc system in the North Lhasa terrane, Tibet, inferred from coeval N-MORB-and arc-type gabbros. Precambrian Res. 2018, 316, 275–290. [Google Scholar] [CrossRef]
  108. Liu, Q.-S.; Jiang, W.; Jian, P.; Ye, P.-S.; Wu, Z.-H.; Hu, D.-G. Zircon SHRIMP U-Pb age and petrochemical and geochemicalfeatures of Mesozoic muscovite monzonitic granite at Ningzhong, Tibet. Acta Petrol. Sin. 2006, 22, 643–652. [Google Scholar]
  109. Whalen, J.B.; Currie, K.L.; Chappell, B.W. A-type granites: Geochemical characteristics, discrimination and petrogenesis. Contrib. Mineral. Petrol. 1987, 95, 407–419. [Google Scholar] [CrossRef]
  110. Inger, S.; Harris, N. Geochemical constraints on leucogranite magmatism in the Langtang Valley, Nepal Himalaya. J. Petrol. 1993, 34, 345–368. [Google Scholar] [CrossRef]
  111. Zhang, Z.-M.; Kang, D.-Y.; Ding, H.-X.; Tian, Z.-L.; Dong, X.; Qin, S.-K.; Mu, H.-C.; Li, M.-M. Partial meltig of Himalayan Orogen and formation mechanism of leucogranites. Earth Sci. 2018, 43, 82–98. [Google Scholar]
  112. Watson, E.B.; Harrison, T.M. Zircon saturation revisited: Temperature and composition effects in a variety of crustal magma types. Earth Planet. Sci. Lett. 1983, 64, 295–304. [Google Scholar] [CrossRef]
  113. Clemens, J.D. S-type granitic magmas–petrogenetic issues, models and evidence. Earth Sci. Rev. 2003, 61, 1–18. [Google Scholar] [CrossRef]
  114. Sylvester, P.J. Post-collisional strongly peraluminous granites. Lithos 1998, 45, 29–44. [Google Scholar] [CrossRef]
  115. Zartman, R.E.; Doe, B.R. Plumbotectonics—The model. Tectonophysics 1981, 75, 135–162. [Google Scholar] [CrossRef]
  116. Zindler, A.; Hart, S.R. Chemical geodynamics. Annu. Rev. Earth Planet. Sci. 1986, 14, 493–571. [Google Scholar] [CrossRef]
  117. Patiño Douce, A.E.; Johnston, A.D. Phase equilibria and melt productivity in the pelitic system: Implications for the origin of peraluminous granitoids and aluminous granulites. Contrib. Mineral. Petrol. 1991, 107, 202–218. [Google Scholar] [CrossRef]
  118. Altherr, R.; Holl, A.; Hegner, E.; Langer, C.; Kreuzer, H. High-potassium, calc-alkaline I-type plutonism in the European Variscides: Northern Vosges (France) and northern Schwarzwald (Germany). Lithos 2000, 50, 51–73. [Google Scholar] [CrossRef]
  119. Collins, W.J.; Richards, S.W. Geodynamic significance of S-type granites in circum-Pacific orogens. Geology 2008, 36, 559–562. [Google Scholar] [CrossRef]
  120. Barbarin, B. A review of the relationships between granitoid types, their origins and their geodynamic environments. Lithos 1999, 46, 605–626. [Google Scholar] [CrossRef]
  121. Whalen, J.B.; Hildebrand, R.S. Trace element discrimination of arc, slab failure, and A-type granitic rocks. Lithos 2019, 348, 105–179. [Google Scholar]
  122. Pearce, J.A.; Harris, N.B.W.; Tindle, A.G. Trace element discrimination diagrams for the tectonic interp retation of granitic rocks. J. Petrol. 1984, 25, 956–983. [Google Scholar] [CrossRef]
  123. Pearce, J. Sources and settings of granitic rocks. Episodes 1996, 19, 120–125. [Google Scholar] [CrossRef]
  124. Harris, N.B.W.; Pearce, J.A.; Tindle, A.G. Geochemical characteristics of collision-zone magmatism. Geol. Soc. Lond. Spec. Publ. 1986, 19, 67–81. [Google Scholar] [CrossRef]
  125. Batchelor, R.A.; Bowden, P. Petrogenetic interpretation of granitoid rock series using multicationic parameters. Chem. Geol. 1985, 48, 43–55. [Google Scholar] [CrossRef]
  126. Collins, A.S.; Pisarevsky, S.A. Amalgamating eastern Gondwana: The evolution of the Circum-Indian Orogen. Earth Sci. Rev. 2005, 71, 229–270. [Google Scholar] [CrossRef]
  127. Zhang, Z.-M.; Wang, J.-L.; Zhao, G.-C.; Shi, C. Geochronology and Precambrian tectonic evolution of the Namche Barwacomplex from the eastern Himalayan syntaxis, Tibet. Acta Petrolog. Sin. 2008, 24, 1477–1487. [Google Scholar]
  128. Rojo-Pérez, E.; Fuenlabrada, J.M.; Díez Fernández, R.; Arenas, R. Origin and evolution of Cadomian magmatism in SW Iberia: From subduction onset and arc building to a tectonic switching. Int. Geol. Rev. 2024, 66, 1885–1909. [Google Scholar] [CrossRef]
  129. Moreno-Martín, D.; Fernández, R.D.; Albert, R.; Martínez, S.S.; Rojo-Pérez, E.; Gerdes, A.; Arenas, R. Cuartel Ophiolite: Structure, timing and exhumation mechanisms for a Cadomian suture zone in the peri-Gondwanan Realm (SW Iberia). Gondwana Res. 2025, 137, 255–273. [Google Scholar] [CrossRef]
  130. Fuenlabrada, J.M.; Arenas, R.; Martínez, S.S.; Fernández, R.D.; Pieren, A.P.; Pereira, M.F.; Chichorro, M.; Silva, J.B. Geochemical and isotopic (Sm-Nd) provenance of Ediacaran-Cambrian metasedimentary series from the Iberian Massif. Paleoreconstruction of the North Gondwana margin. Earth-Sci. Rev. 2020, 201, 103079. [Google Scholar] [CrossRef]
  131. Cai, Z.-H.; Xu, Z.-Q.; Duan, X.-D.; Li, H.-Q.; Cao, H.; Huang, X.-M. Early stage of Farly Paleozoie orogenic event in western Yunnan Province, south eastern margin of Tibet Plateau. Acta Petrol. Sin. 2013, 29, 2123–2140. [Google Scholar]
Minerals 15 00284 g001
Figure 1. (a) Geotectonic map of Tibetan Plateau (revised by [73,74]); (b) geological map of Guomang-Co area (revised by [36,75]). 1: Kunlun Mountain Suture Zone (KSZ); 2: Jinsha River Suture Zone (JSSZ); 3: Longmu Co-Shuanghu Suture Zone (LSSZ); 4: Bangong Lake-Nujiang Suture Zone (BNSZ); 5: India-Yarlung Zangbo River Suture Zone (IYZSZ); 6: Shiquanhe-Nam Co Ophiolitic Mélange Zone (SNMZ); 7: Luobadui-Mila Mountain Fault (LMF).
Figure 1. (a) Geotectonic map of Tibetan Plateau (revised by [73,74]); (b) geological map of Guomang-Co area (revised by [36,75]). 1: Kunlun Mountain Suture Zone (KSZ); 2: Jinsha River Suture Zone (JSSZ); 3: Longmu Co-Shuanghu Suture Zone (LSSZ); 4: Bangong Lake-Nujiang Suture Zone (BNSZ); 5: India-Yarlung Zangbo River Suture Zone (IYZSZ); 6: Shiquanhe-Nam Co Ophiolitic Mélange Zone (SNMZ); 7: Luobadui-Mila Mountain Fault (LMF).
Minerals 15 00284 g001
Minerals 15 00284 g002
Figure 2. (a) Outcrop of map of mylonitized granites from Guomang-Co area in central Lhasa terrane. (b,c) Field features of the sample of Guomang-Co mylonitized granites. (d–g) Photomicrographs of mylonitized granites from Guomang-Co. Qzt—quart; Kfs—K-feldspar; Mus—muscovite.
Figure 2. (a) Outcrop of map of mylonitized granites from Guomang-Co area in central Lhasa terrane. (b,c) Field features of the sample of Guomang-Co mylonitized granites. (d–g) Photomicrographs of mylonitized granites from Guomang-Co. Qzt—quart; Kfs—K-feldspar; Mus—muscovite.
Minerals 15 00284 g002
Minerals 15 00284 g003
Figure 3. (a) Chondrite-normalized REE patterns of the Guomang-Co granites. (b) Primitive mantle-normalized trace elements spider diagrams of the Guomang-Co granites. Coeval granites data of Lhasa terrane are from [11,28,36,38,66,68]. Normalizing values are from [93]. The REE and trace element contents for the upper, middle, and lower crust are from [94].
Figure 3. (a) Chondrite-normalized REE patterns of the Guomang-Co granites. (b) Primitive mantle-normalized trace elements spider diagrams of the Guomang-Co granites. Coeval granites data of Lhasa terrane are from [11,28,36,38,66,68]. Normalizing values are from [93]. The REE and trace element contents for the upper, middle, and lower crust are from [94].
Minerals 15 00284 g003
Minerals 15 00284 g005
Figure 5. Cathodoluminescence (CL) images of representative zircon grains and concordia diagrams of the Early Paleozoic granites from Guomang-Co.
Figure 5. Cathodoluminescence (CL) images of representative zircon grains and concordia diagrams of the Early Paleozoic granites from Guomang-Co.
Minerals 15 00284 g005
Minerals 15 00284 g006
Figure 6. εHf(t)-t diagram and εHf(t) histogram for zircon grains from the Guomang-Co granites. Data of Banglei metabasalts and metarhyolites [11], Early Jurassic strongly peraluminous granitoids [106], Zhaqian metarhyolites [36] in the Lhasa terrane, Gemuri and Bensong Co granites [60] in the South Qiangtang terrane, Kangmar and Gyirong Granitic Gneiss [42] in the Himalaya terrane are shown for comparison.
Figure 6. εHf(t)-t diagram and εHf(t) histogram for zircon grains from the Guomang-Co granites. Data of Banglei metabasalts and metarhyolites [11], Early Jurassic strongly peraluminous granitoids [106], Zhaqian metarhyolites [36] in the Lhasa terrane, Gemuri and Bensong Co granites [60] in the South Qiangtang terrane, Kangmar and Gyirong Granitic Gneiss [42] in the Himalaya terrane are shown for comparison.
Minerals 15 00284 g006
Minerals 15 00284 g007
Figure 7. Initial Sr-Nd isotopic composition of Guomang-Co granites. Data of Cambrian metabasalts [28] and metarhyolites [11], Neoproterozoic N-MORB gabbros [107], Jurrassic strongly peraluminous [108] in the Lhasa terrane terrane are shown for comparison.
Figure 7. Initial Sr-Nd isotopic composition of Guomang-Co granites. Data of Cambrian metabasalts [28] and metarhyolites [11], Neoproterozoic N-MORB gabbros [107], Jurrassic strongly peraluminous [108] in the Lhasa terrane terrane are shown for comparison.
Minerals 15 00284 g007
Minerals 15 00284 g008
Figure 8. (a) CaO-FeOT + MgO-Al2O3-(Na2O + K2O) diagram [96]; (b) FeOT/MgO-10,000 Ga/Al diagram [109]; (c) 10,000Ga/Al-(Zr + Nb + Ce + Y) diagram [109].
Figure 8. (a) CaO-FeOT + MgO-Al2O3-(Na2O + K2O) diagram [96]; (b) FeOT/MgO-10,000 Ga/Al diagram [109]; (c) 10,000Ga/Al-(Zr + Nb + Ce + Y) diagram [109].
Minerals 15 00284 g008
Minerals 15 00284 g011
Figure 11. Granite tectonic discrimination diagrams. (a–d) Nb, Ta, Rb revalant diagrams [122,123]; (e) Hf-Rb-Ta diagram [124]; (f) R1-R2 dagram [125]. R1 = 4Si − 11(Na + K) − 2(Fe + Ti), R2 = 6Ca + 2Mg + Al. The granite data area related to slab break off comes from [121].
Figure 11. Granite tectonic discrimination diagrams. (a–d) Nb, Ta, Rb revalant diagrams [122,123]; (e) Hf-Rb-Ta diagram [124]; (f) R1-R2 dagram [125]. R1 = 4Si − 11(Na + K) − 2(Fe + Ti), R2 = 6Ca + 2Mg + Al. The granite data area related to slab break off comes from [121].
Minerals 15 00284 g011
Minerals 15 00284 g012
Figure 12. Schematic diagram of the Early Paleozoic tectonic evolution of the Lhasa terrane. (revised by [11]).
Figure 12. Schematic diagram of the Early Paleozoic tectonic evolution of the Lhasa terrane. (revised by [11]).
Minerals 15 00284 g012
Disclaimer/Publisher’s Note: The statements, opinions and data contained in all publications are solely those of the individual author(s) and contributor(s) and not of MDPI and/or the editor(s). MDPI and/or the editor(s) disclaim responsibility for any injury to people or property resulting from any ideas, methods, instructions or products referred to in the content.

Share and Cite

MDPI and ACS Style

Zhang, Y.; Wang, M.; Yu, C.; Li, Z. S-Type Granites from the Guomang-Co Area in Central Tibet: A Response to Early Paleozoic Andean-Type Orogeny Along the Northern Margin of East Gondwana. Minerals 2025, 15, 284. https://doi.org/10.3390/min15030284

AMA Style

Zhang Y, Wang M, Yu C, Li Z. S-Type Granites from the Guomang-Co Area in Central Tibet: A Response to Early Paleozoic Andean-Type Orogeny Along the Northern Margin of East Gondwana. Minerals. 2025; 15(3):284. https://doi.org/10.3390/min15030284

Chicago/Turabian Style

Zhang, Yuhe, Ming Wang, Changsheng Yu, and Zhenglong Li. 2025. "S-Type Granites from the Guomang-Co Area in Central Tibet: A Response to Early Paleozoic Andean-Type Orogeny Along the Northern Margin of East Gondwana" Minerals 15, no. 3: 284. https://doi.org/10.3390/min15030284

APA Style

Zhang, Y., Wang, M., Yu, C., & Li, Z. (2025). S-Type Granites from the Guomang-Co Area in Central Tibet: A Response to Early Paleozoic Andean-Type Orogeny Along the Northern Margin of East Gondwana. Minerals, 15(3), 284. https://doi.org/10.3390/min15030284

Note that from the first issue of 2016, this journal uses article numbers instead of page numbers. See further details here.

Article Metrics

Back to TopTop