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Article

Zircon U-Pb Geochronology, Geochemistry, and Sr-Nd-Hf Isotopic Composition of Ben Giang-Que Son Complex in the Southern Truong Son Belt: Implications for Permian–Triassic Tectonic Evolution

1
Vietnam Institute of Geosciences and Mineral Resources, Hanoi 100000, Vietnam
2
Faculty of Geology, University of Science, Ho Chi Minh City 700000, Vietnam
3
Vietnam National University, Ho Chi Minh City 700000, Vietnam
4
School of Earth Sciences and Engineering, Sun Yat-sen University, Guangzhou 510275, China
*
Authors to whom correspondence should be addressed.
Minerals 2024, 14(6), 569; https://doi.org/10.3390/min14060569
Submission received: 1 April 2024 / Revised: 22 May 2024 / Accepted: 23 May 2024 / Published: 29 May 2024
(This article belongs to the Special Issue Petrogenesis, Magmatism and Geodynamics of Orogenic Belts)

Abstract

:
The magmatic rocks of the Ben Giang-Que Son complex exposed in the southern part of the Truong Son belt have petrographic compositions including gabbro, gabbrodiorite, granodiorite, and granite. Geochemically, the magmatic rocks are of subalkaline affinity and belong to the high-K calc-alkaline series. All analyzed samples contain hornblende and biotite as mafic minerals and are defined as metaluminous with a aluminum saturation index of <1.1. Chondrite-normalized rare earth element diagrams are characterized by fractionation between light and heavy rare earth elements and show small to moderate negative Eu anomalies (Eu/Eu* = 0.81–0.44). Primitive mantle-normalized trace element patterns exhibit enrichment in LILEs such as Rb, K, U, and especially Pb and depletion of HFSEs (Nb, Ta, and Ti), indicating arc-magma. The BG-QS gabbro and gabbrodiorite have low Cr, Co, and Ni and display enrichment in 87Sr/86Sr (0.7084 to 0.7147), ꜪNd(t) (−0.5 to −1.9), and positive ꜪHf(t) (+2.4 to 4.5), suggesting generation from the enriched mantle source. The BG-QS diorite and granodiorite contain small mafic enclaves, have a wide range of SiO2 contents and enrichment in Sr-Nd isotopes (87Sr/86Sr = 0.7109–0.7178; ꜪNd(t) = −3.3 to −3.7), and display high Mg# (43–51). All these features indicate that they were formed by the mixing of magmas, which originated from an enriched mantle source and the pre-existing juvenile mafic lower crust. The whole-rock Nd and zircon Hf model ages are of 1160–760 Ma. The Ben Giang-Que Son complex yields LA-ICP-MS zircon U-Pb ages of 285 ± 3.1 and 278 ± 3.5 Ma that corresponds to the Cisuralian epoch (early Permian), which is linked to the subduction and amalgamation of the Indochina and South China blocks due to the closing a branch of the Paleotethys along the Song Ma suture.

1. Introduction

Many micro-continental fragments that were split off from northern Gondwanaland, including the Sibumasu, Simao, South China, and Indochina blocks, combined to form Southeast Asia [1,2]. Numerous studies [2,3,4,5,6,7] have linked the closure of the Paleotethys Ocean to the collision between the Indochina and South China blocks. This collision is considered to be the cause inducing the Permian–Triassic magmatic activities that are widely distributed along the Truong Son belt and the Song Ma suture zone (Figure 1a). Precise information about volcanic and plutonic rocks is key for understanding the geodynamic context and the tectono-magmatic evolution. According to current research, the Song Ma suture, which lies within Vietnamese territory, is the place where the Indochina and South China blocks met during the Late Permian to Early Triassic period [2,5,8,9]. The magmatic rocks along the SMSZ and the northern section of the Truong Son (TS) belt have been thoroughly investigated, meanwhile those in the southern part of the belt are poorly documented. The magmatic rock assemblage of the Ben Giang-Que Son (BG-QS) complex is distributed mainly in the southern part of the TSB. Previous studies have focused on petrographical and mineralogical characteristics of the rocks. Only several mineral K-Ar and/or Ar-Ar isotope ages have been reported for the BG-QS magmatic rocks so far [8]. In addition, key information, such as the geochemical and isotopic data of the rocks, necessary for identifying the type and source of the magmatic rocks is not available. Thus, knowledge regarding the genesis and exact emplacement age remains unclear. Furthermore, some BG-QS magmatic plutons in the southern TS belt were dated using the zircon U-Pb isotope, yielding a 206Pb/238U age of 460–470 Ma, instead of 258–260 Ma [10,11].
This paper presents the results of whole-rock geochemical and Sr-Nd isotopic data as well as zircon U-Pb geochronology and initial Hf isotopic analyses for the magmatic rocks of the BG-QS complex. Our U-Pb zircon age data represent the most important information necessary to better comprehension the tectono-magmatic evolution of central Vietnam, in particular, and the whole of Southeast Asia, in general.

2. Regional Geology and Petrography

Geologists from Vietnam and abroad argue that the Indochina block consists of three main structural zones on Vietnamese territory: the Kontum massif in central Vietnam, the Da Lat zone in the south, and the TS belt in the north [3,9,16,17,18] (Figure 1a). The Song Ma suture borders to the northern margin of the TS belt, which is located in north–central Vietnam [1,2,5,19,20,21,22]. The Tam Ky-Phuoc Son suture, which is also thought to be a boundary dividing the TS belt (TS terrane) from the Kontum massif, borders the TS belt to the south [23,24].
The TS belt exhibits several left-lateral, northwest–southeast faults, like the Song Ca and Khe Sanh-Da Nang faults, which are sub-parallel with the Song Ma suture [25]. According to stratigraphy, the TS belt displays prehistoric deposits, including Cambrian–Ordovician quartz–sericite schist and Neoproterozoic quartz schist, as well as common Permian–Triassic, volcanic–plutonic magmatic bodies; Triassic siltstone; and Jurassic sandstone sediments (Figure 1b). The majority of the TS belt is made up of plutonic and volcanic complexes, such as the Dien Bien, Song Ma, Phia Bioc, Ben Giang-Que Son (BG-QS), Hai Van, and Dong Trau formations, whose dates range from the Permian to the Triassic. The Permian–Triassic plutonic and volcanic complexes along the TS belt and the Song Ma suture zone are the result of three phases of amalgamation between the South China and Indochina blocks: subduction (290–250 Ma), syn-collision (250–240 Ma), and post-collision (240–210 Ma) [2,3,5,6,13,18,26,27]. Although there are many different views, but it is generally accepted that these three tectonic phases related to the collisional process occurred between the South China and Indochina plates during the Indosinian period.
In this study, the magmatic rock assemblage of the BG-QS complex is mainly distributed in the southern TS belt and north Kontum massif. Their distribution area includes many blocks from a few tens of km2 to hundreds of km2. They are mainly distributed in the western region of Quang Nam province, with an area of more than 60 km2 (Figure 1b). In the field, they intrude into eruptive sediments of the Cambrian–Ordovician A Vuong and the Long Dai Ordovician–Silurian Formations and are covered by the Nong Son sedimentary formation of Late Triassic age. Petrographically, the main rocks of the BG-QS complex are gabbrodiorite, diorite, granodiorite, and granite. They are medium-to-coarse-grained rocks and dark to dark-gray in color. The main rock-forming mineral assemblages are plagioclase (35–55%), potassium feldspar (2–15%), quartz (2–30%), biotite (0–15%), and hornblende (3–20%). Plagioclases exhibit slightly altered polysynthetic twins, and some show evidence of oscillatory zoning. Potassium feldspar is slightly sericitized or kaolinized, and its shape is indicative of an anhedral crystal. Quartz is interstitial and anhedral granular in shape. Biotite crystals are euhedral in shape and have undergone minor modifications, including chloritization and sericitization. Hornblende has a subhedral granular to prismatic shape, and some hornblendes show cleavages at 56 and 124 degrees. Typical accessory minerals are magnetite, sphene, zircon, and apatite (Figure 2).

3. Analytical Methods

3.1. Major and Trace Element Analyses

For determination of the major and trace elements, the fresh magmatic samples were crushed and then powdered in an agate mill to a grain size of <200 meshes. Before being weighed, the powdered samples were dried overnight at 110 °C. Measurement of the abundance of geochemical elements was performed at the Sun Yat-sen University (SYSU) of Zhuhai, China, using wavelength X-ray fluorescence (XRF) spectrometry and iCAP-RQ-ICP-MS. Loss-on-ignition of each sample was calculated after heating a 1 g powder sample at 1000 °C for one hour. The uncertainty of the analysis was less than 3% for major elements and from 8 to 12% for trace elements, depending on their concentration in the rocks. The details of the major- and trace-element analytical procedure are shown in [28]. The analytical results are given in Table 1.

3.2. Sr-Nd and Pb Isotopes

The isotopic ratios of Sr, Nd, and Pb were determined using about 100 mg of whole-rock powder. To assure the decomposition of refractory phases, the samples were decomposed for six days at 180 degrees Celsius in Teflon beakers containing steel-jacket bombs and a mixture of HF and HClO4. A Finnigan MAT-262 mass spectrometer was used to measure the isotopic compositions of Sr and Nd after they were separated using standard ion exchange techniques at the University of Science and Technology of China in Hefei. The isotopic ratios were corrected for mass fractionation via normalization to 146Nd/144Nd = 0.7219 and 86Sr/88Sr = 0.1194. The total procedure blanks for Sr and Nd were less than 200 pg and 50 pg, respectively. Throughout this investigation, a mean value of 87Sr/86Sr = 0.7102625 ± 15 was obtained from three analyses of standard NBS SRM-987. The Ames Nd standard measurements produced a mean value of 143Nd/144Nd = 0.512139 ± 12. Using diluted HBr, the traditional cation-exchange method was used to separate and purify Pb. Standard NBS SRM-981 was used throughout the examination process and yielded 206Pb/204Pb = 18.640 to 18.708, 207Pb/204Pb = 15.741 to 15.758, and 208Pb/204Pb = 39.160 to 39.336. The Sr-Nd isotope analytical results are summarized in Table 2. The analytical procedures are described in detail in [30,31].

3.3. Zircon U-Pb Data and Hf Isotopic Composition

We selected zircon grains in non-magnetic fractions to analyze their U-Pb isotopic compositions. Magnetic separation and heavy liquids were used to obtain zircon grains from the rock samples. Finally, under a binocular microscope, each zircon crystal was individually selected for age dating. It was then set in epoxy resin and polished until the center of the zircon grains was visible. The cathodoluminescence (CL) technique was used to study the internal structure of zircons. U-Th-Pb concentrations in zircons were measured using laser ablation inductively coupled plasma spectrometry (LA-ICP-MS). A laser spot size of 34 µm and laser repetition at 6 Hz were set for analyses. Using helium gas, the ablated samples were moved from the ablation cell to the ICP-MS torch. All these measurements were carried out at the State Key Laboratory of Geological Processes and Mineral Resources, China University of Geosciences in Wuhan, China. Zircon 91500 served as an external standard for U-Pb dating and was tested twice every five analyses. Analysis of zircon 91500 gave a concordant U-Pb age of 1064.9 ± 2.5 Ma, corresponding to the reported U-Pb age of 1065.4 ± 0.3 Ma obtained in different laboratories [32]. The ICPMSDataCal program described in [33] was used for quantitative calibration of the U-Pb dating technique. Ludwig’s (2003) [34] Isoplot Program was used to create Concordia diagrams and calculate weighted means. The uncertainties in ages are quoted as 95% confidence levels. The U-Pb isotope analytical results are summarized in Table 3. Uncertainties in each analysis were described at the 1 sigma level.

4. Analytical Results

4.1. Major and Trace Element Geochemistry

The studied samples were collected from the BG-QS complex including gabbrodiorite and granodiorite. Their geochemical results are presented in Table 1. The bulk-rock compositions of the gabbrodiorite are characterized by moderate TiO2 (1.01–1.07 wt%) and SiO2 contents range from 51.11 to 52.76 wt%, high Al2O3 of 18.02–18.31 wt%, and total alkali contents (K2O + Na2O) of 5.32–6.10 wt%) with a wide variation of K2O/Na2O ratios (0.35–0.41). The concentrations of MgO, Fe2O3t, and CaO oxides varied from 3.33 to 4.22 wt%, 7.73 to 8.67 wt%, and 7.70 to 8.41 wt%, respectively. The bulk-rock compositions of the granodiorite are characterized by low TiO2 (0.59–0.81 wt%) and moderate SiO2 contents of 61.51–64.11 wt%, Al2O3 of 15.61–16.29 wt%, and relatively high total alkali contents ((K2O + Na2O) of 6.92–7.85 wt%) with the wide variation of K2O/Na2O ratios (0.91–1.29). The concentrations of MgO, Fe2O3t, and CaO oxides vary from 1.65 to 2.83 wt%, 4.21 to 5.45 wt%, and 2.95 to 4.21 wt%, respectively.
The Harker diagrams show negative correlations between TiO2, Al2O3, Fe2O3, MgO, CaO, Na2O, and SiO2, whereas K2O increases with increasing SiO2 (Figure 3). In the TAS diagram, the investigated samples fall into the gabbrodiorite and granodiorite fields (Figure 4a), exhibit calc-alkaline affinity, and belong to the high-K series (Figure 4c). The Al2O3/(Na2O + K2O) vs. Al2O3/(CaO + Na2O + K2O) diagram defines all rocks as metaluminous with aluminum saturation indices (ASI = Al2O3(molar)/(CaO + Na2O + K2O(molar)) of 0.78–0.79 for gabbrodiorite and of 0.86–1.01 < 1.1 for granodiorite (Figure 4b), suggesting I-type granite. The diagrams of SiO2-P2O5 also support the I-type characteristic of the granodiorite. The trace element abundance exhibits significantly more scatter than the major elements. The Sr element shows a negative linear trend, while Rb defines a positive trend with increasing SiO2. Chondrite-normalized REE patterns are characterized by moderate fractionation between LREEs and HREEs ((La/Yb)n = 8.58–29.83) and show slightly negative Eu anomalies (Eu/Eu* = 0.44–0.81) (Figure 5a). Primitive mantle-normalized trace element patterns exhibit enrichment in LILEs such as Rb, K, U, and especially Pb and depletion in HFSEs (Nb, Ta, and Ti) (Figure 5b). On the classification diagram (Figure 6a-c), the samples mainly plot in the volcanic field and show a temperature range of ~750 °C–820 °C (Figure 6d).

4.2. Nd-Sr Isotopic Composition

The isotopic compositions of Rb-Sr and Sm-Nd from four analyzed samples are presented in Table 2 and Figure 7. The initial isotopic compositions of Sr and Nd were calculated at an age of 280 Ma. The analyzed samples exhibit relatively high (87Sr/86Sr)i ratios (0.70849–0.71782) and negative ꜪNd(t) values (−3.7 to −0.5). The depleted mantle model ages (TDM2) vary from 1.0 to 1.2 Ga.

4.3. U-Pb Data

Representative cathodoluminescence (CL) images of specific zircons are presented in Figure 8. The zircon U-Pb data are presented in Table 3 and Figure 9. In general, the zircons separated from two samples, TS32 and TS26, were brown and white in color. They were transparent and contain less inclusion. The zircon grains ranged from 80 to 250 μm in length with length/width ratios of 2.5/1.5 to 1.2/1.0. The majority of the zircon grains exhibited oscillatory zoning and were euhedral, which suggests that they were formed by igneous processes (Figure 8). Inherited zircon with older age was not commonly observed. Only zircon grains with a concordance of 206Pb/238U ages greater than 95% were used for the weighted mean age calculation. Errors are quoted as one sigma.
Sample TS32 (gabbrodiorite): This sample was collected from a pluton in Nam Giang area, which is considered the reference pluton of the BG-QS complex [8]. Twenty individual zircon grains were selected and analyzed for their U-Pb isotopic compositions. This sample consisted of mainly of long, euhedral, prismatic, and transparent zircons. The zircon grains had U and Th concentrations of 220–580 ppm and 102–402 ppm, respectively, with values of Th/U ratios ranging from 0.51 to 0.84, indicating magmatic origin. Twenty data points obtained from this sample gave 206Pb/238U ages ranging from 270 to 298 Ma, but most ages were around 281 Ma. All of the data points were plotted on or nearly on the concordia curve and yielded a weighted mean 206Pb/238U age of 285 ± 3.1 Ma (MSWD = 2.4) (Figure 9a). When combined with CL images of zircons, the age of 285 Ma was interpreted as the sample’s emplacement age.
Sample TS26 (granodiorite): Zircon grains separated from this sample were brown and white in color. They were prismatic and transparent zircons. The analyzed zircon grains of the TS26 had U and Th concentrations of 250–615 ppm and 122–390 ppm, respectively. All analyzed zircons had Th/U ratios of 0.34–0.85, which were characterized by the crystallization of zircon from the melt. Twenty zircon grains were examined to determine the composition of U-Pb isotopes and yielded 206Pb/238U ages from 260 to 289 Ma, but most ages cluster around 276 Ma. Figure 9b shows that the analytical data were plotted on or nearly on the concordia curve and produced a weighted mean 206Pb/238U age of 278 ± 3.5 Ma (MSWD = 0.48), corresponding to the early Permian time. The age value of 278 Ma is the best estimate of the sample’s emplacement when combined with zircon CL images.
Zircon Lu-Hf isotope composition: Lu-Hf isotope ratios from zircon grains of the sample TS32 were determined on the same zircon spots where U-Pb dating had been carried out. Twenty analytical spots were located on twenty zircon grains of this sample, and the results are shown in Table 4. The 176Hf/177Hf and 176Lu/177Hf ratios vary from 0.282670 to 0.282738 and 0.000399 to 0.001618, respectively. An age of 280 Ma obtained from this sample was used to calculate the initial Hf isotope composition. All of the analyzed zircons indicate relatively uniform (176Hf/177Hf)i ratios (from 0.282665 to 0.282729), consistent with ꜪHf(t) values of +2.4 to +4.6 (weighted mean of 3.7 ± 1.1; Figure 10). The current values of 176Hf/177Hf (0.28325) and 176Lu/177Hf (0.0384) were applied to calculate single-stage Hf model ages [46]. The Hf model zircon ages (TDM1) were in the range of 738–818 Ma and (TDM2) were in the range of 1008–1153 Ma, respectively.

5. Discussion

5.1. Emplacement Age of the Ben Giang-Que Son Complex

The magmatic rocks of the BG-QS complex are distributed mainly in the south of Truong Son belt and north of the Kontum massif. In the field, they intrude into the metamorphic rocks of the A Vuong and Long Dai Formations. The formation age of the BG-QS complex was previously estimated based on geological relationships, and only some radiogenic ages obtained using biotite or/and amphibole K-Ar or Ar-Ar methods were reported. In our study, two samples of gabbrodiorite and granodiorite from the BG-QS complex in southern Truong Son zone were collected and dated using the zircon U-Pb method. All analytical data points yielded weighted mean 206Pb/238U ages of 285 and 278 Ma (Figure 9a,b). The fine zoning and prismatic shape of zircon grains extracted from these samples indicate that they originated from a magmatic source. Using the internal structure features of zircons and their high Th/U ratios >> 0.1 (Table 4), we concluded that the magmatic rocks of the BG-QS complex were emplaced between 285 and 278 Ma years ago, corresponding to the early Permian period. These ages are similar to those reported by [51] (in Vietnamese with an English Abstract) but show a narrow range and are relatively older than previously published geochronological data (242–266 ± 4.4 Ma by hornblende Ar-Ar, Hung 1999; 251–271 Ma by biotite K-Ar, Khai 1979; and 300 ± 16 Ma by biotite K-Ar, Bao 1979).

5.2. Petrogenesis of the Ben Giang-Que Son Complex

The magmatic rocks of the BG-QS Son complex have a petrographic composition ranging from gabbro, to gabbro-diorite, to granodiorite, to less granite. They have calc-alkaline affinity and belong to the high-K series (Figure 4c). The A/CNK and A/NK diagram [53] defines the rock as metaluminous with aluminum saturation indices (ASI) <1.1. The negative correlations between major and trace elements, including TiO2, Al2O3, Fe2O3, MgO, CaO, Na2O, and Sr vs. SiO2, and positive trends between K2O, Rb, and SiO2 indicate that the fractional crystallization of magma played a main role in its petrogenesis (Figure 3). Primitive-mantle-normalized trace element patterns show distinct positive anomalies for large ion lithosphere elements including Rb, K, and La as well as depletion in Nb, Ti, and Ta elements. Magmatic rocks with this feature imply that they were formed in a subduction-related tectonic setting. Negative anomalies of Sr and Ba elements as well as slightly negative Eu/Eu* (0.44 to 0.81) indicate the crystallization of plagioclase (Figure 5a,b). The major elemental composition of the analyzed granodiorites in this study is close to Permian I-type granite and differs greatly from Triassic S-type granite (Figure 3 and Figure 4; Table S1). However, the K2O + Na2O content is higher than that of Permian I-type granite (Figure 4a,c).
All the studied samples in this study have relatively high initial 87Sr/86 Sr ratios of 0.70849 to 0.71782 and negative ꜪNd(t) values of −3.7 to −0.5 with Nd model ages (TDM2) of 1.0 to 1.2 Ga; all zircon ꜪHf values obtained from the gabbrodiorite sample TS32 ranged from +2.4 to +4.6 (an average of +3.7) with TDM1 of 738 to 818 Ma, which reflects the duration of extracting the source materials from the depleted mantle (Figure 7 and Figure 10). The magmatic rocks’ isotope characteristics, in conjunction with the geochemical features mentioned above, may suggest an origin from (1) partial melting of mafic rocks in the lower continental crust (e.g., [54,55,56]); (2) an enriched mantle source region (e.g., [57,58]); and (3) mixing between the mantle-originated magmas with crustal melts (e.g., [59]). The first model is unlikely, because many experimental data have reported that melting of crustal rocks in the hydrous condition, regardless of the melting degrees, would produce magmatic rocks with a low magnesium number (Mg# < 40) (e.g., [60,61]). Meanwhile, all the analyzed samples have Mg# > 41. The magma-mixing model with felsic crust is also impossible because all of the investigated samples did not contain felsic enclaves. In general, the BG-QS magmatic rocks had a wide range of SiO2 content, from gabbro to granite, and high Mg# (43.68 to 50.70), indicating a mantle-derived generation rather than a pure crustal source rocks. Furthermore, zircons from the two dated samples did not contain inherited zircons, which reflect the age of continental crust. The mantel origin is also supported by the positive zircon ꜪHf(t) values obtained from the gabbrodiorite sample TS32 [28,62,63]. However, the studied samples have low contents of Cr and Ni elements, negative whole-rock ꜪNd(t), and relatively high initial 87Sr/86Sr ratios (>0.708), indicating that the mantle source region, where the magma originated, was not primitive mantle. In Figure 7, all analyzed samples are plotted into enriched mantle type I (EM I). Therefore, we prefer an enriched mantle origin. The spider diagrams also show positive anomalies and high whole-rock isotope ratios of lead, supporting an enrichment of mantle source (Figure 7 and Table 2). However, some granodiorite of the BG-QS complex contain small mafic enclaves, which exhibit an igneous texture and have mineral assemblages, as well as an age similar to the host hornblende granodiorite. These features, together with geochemical and isotope studies, indicate that BG-QS granodiorite generated from the mixing of magmas derived from the enriched mantle and pre-existing juvenile mafic lower crust. Trace element and whole-rock Sr-Nd isotopic compositions show that BG-QS granodiorite is quite close to Permian I-type granite (Figure 5 and Figure 6, Table S1). Meanwhile, they are different from Triassic S-type granite (Figure 5 and Figure 6; Tables S1 and S2).
The mantle was probably enriched due to metasomatism triggered by subduction-related fluid/melt that took place in the past. The two-stage Hf model (TDM2) ages (1008 Ma to 1153 Ma) of the analyzed zircons are significantly older than their crystallized ages (283 Ma to 275 Ma); along with geochemical features of the rocks, this suggesting that the lithospheric mantle wedge, where BG-QS magma originated, was transformed during the Meso- to Neoproterozoic period via ancient subduction, as proposed by Wang et al. (2022) [28]. The whole-rock Nd TDM age, from 990 to 1160 Ma, also reflects the time of metasomatism of the lithosphyric mantle wedge. The mantle enrichment was probably caused by slap-derived fluid/melts. The analyzed samples have very low (Hf/Sm)PM and (Ta/La)PM ratios of 0.01 to 2.98 and 0.17 to 0.75, respectively, which may suggest slap-derived fluids. The (Hf/Sm)PM vs. (Ta/La)PM figure illustrates that gabbrodiorite samples plot on the fluid-related subduction metasomatism field, meanwhile most of the granodiorite samples fall close to the border between fluid- and melt-related subduction metasomatism fields (Figure 11). In brief, we infer that BG-QS gabbro and gabbrodiorites likely generated from an enriched mantle source, which was modified by subduction-related fluids during the Meso- and Neoproterozoic period, while the magma mixing process had an important role in the genesis of the BG-QS hornblende granodiorites. Two end-member magmas were engaged as follows: one derived from an enriched mantle source region and the other from a pre-existing juvenile mafic lower crust.

5.3. Implications for the Permian–Triassic Magmatism and Tectonic Setting

Prior research on magmatic activity associated with the subduction and closure of the Paleotethys Ocean in Vietnamese territory during the Late Permian–Early Triassic period has essentially offered a comprehensive understanding of the formation time, origin, and tectonic settings of these formations (Tables S1 and S4, Figure 12 and Figure 13) [2,3,4,5,13,21,23,26,49,50,51,52,64,65,66,67]. The extensive dispersion of granitic magmatism throughout the Late Permian–Early Triassic period in Vietnam is illustrated in Figure 12, which can be divided into three main geological regions, with the Northwest–Southeast belonging to two tectonic settings (intracontinental rift and subduction): (1) Song Da rift, Tu Le basin, and Phan Si Pan zone, (2) North TS belt and Song Ma suture, and (3) South TS and North Kontum massif. Permian–Triassic formations of the TS zone in this study belong to the region of the South TS belt and North Kontum massif. The North TS belt and the Song Ma suture zone (Figure 13a) are mainly composed of I-type granites (Chieng Khuong, Dien Bien, and Song Ma bodies), which are products of the Paleotethys subduction process. Indochina blocks along the Song Ma suture during the Late Permian–Early Triassic period (section AB, Figure 13b) [4,5,26,52,64]. In the South TS and North Kontum massif, Central Vietnam (Figure 13c), previous studies have suggested that the BG-QS magmatic rocks were formed due to the subduction of the Paleotethys Ocean beneath the Indochina blocks (section CD, Figure 13c) [3,23,67,68]. The abundance of Late Permian–Early Triassic granitic formations in the Kontum massif is evidence for the Paleotethys Ocean subduction process (e.g., 250 Ma [42] and 257–244 Ma [23]).
However, there are different interpretations of the magmatic activity and metamorphic events that occurred during the Indosinian stage. This Indosinian orogeny stage was previously thought to be related to the subduction–closure process of the Paleotethys ocean, leading to widespread development of Permian–Triassic thermo-tectonic events and metamorphism [1,9,22,64,69]. The subduction and closure of the Song Ma Paleotethys Ocean branch and the subsequent collision and amalgamation of the Indosinian and South China blocks resulted in the formation of the TS tectono-magmatic belt in the northeast part of the Indochina; this TS belt is the most important poly-mineralization belt in Southeast Asia [23,70,71]. Some other authors have argued that the Permian–Triassic felsic volcanic rocks in the Kontum massif have genetic links to the Emeishan mantle plume. The mantle plume could cause large-scale magmatic intrusion in the Kontum terrane and supply a heat source that would cause partial melting and high-grade metamorphism of the lower crust [42,44,72,73].
Some geologists believe that the poly-mineralization in the TS belt is related to formation of large-scale Permian–Triassic granites [74]. Existing studies have identified a large number of late Paleozoic (306~260 Ma) island arc magmatic rocks that related to the subduction of the ocean basin in the Song Ma area in Laos and northern Vietnam in the Truong Son zone (Table S4; [4,7,23,26]). In addition, many studies on Late Permian–Triassic magmatism and metamorphic events have been conducted on this belt and its surrounding areas, such as MuongLat granite in the Song Ma zone, northern Vietnam (251~235 Ma [2]); LatBoua granite (255~245 Ma), Kham granite (253~234 Ma), Phon Thong granite (250~245 Ma), and Lua granite (239~234 Ma) and Na The granite [52]; granite in the Dien Bien area of northwest Vietnam (242~225 Ma [4,6,66]); and Hai Van granite in Central Vietnam (242~224 Ma [13]).
Metamorphic research also shows that the metamorphic process of the TS belt and surrounding areas mainly occurred after the Early Triassic stage. The evidence for this is the deformation age of mylonite in the Nam Co and the Song Ma formation in Northern Vietnam around ~250~240 Ma [75]. Zircon and monazite separated from eclogite of the Song Ma suture zone gave U-Pb ages of 230 ± 8 Ma and 243 ± 4 Ma, respectively. In addition, the progressive metamorphic age of clay grains and the thermo-tectonic age of the orogeny period are identified at 233 ± 5 Ma and 251~229 Ma, respectively [9,21,25,76,77,78]. Important Triassic geological events were also recorded in the Kontum massif in Central Vietnam—for example, thermal metamorphic events took place mainly from 251 to 222 Ma [27,42,44,62,64,75,79,80]; syn-tectonic granites have formation ages of 251~229 Ma [47,81].
B.A. Barbarin [82], who used the Wilson cycle to classify granitoids, proposed that the origin and two major tectonic settings are associated with the formation mechanism that initiates metaluminous I-type affinity magmatism: (1) magmatism associated with an Andean-type continental arc, and (2) post-orogenic lithospheric extension. The magmatic rocks of the Ben Giang-Que Son complex in this study are metaluminous I-granite and are linked to magmatism related to subduction (Figure 3, Figure 4, Figure 5 and Figure 6; Table S1). The BG-QS complex in the southern TS belt and I-type granites in the northern TS belt (Figure 12a) [83] have U-Pb isotopic ages of 283–275 Ma, which coincide with widespread magmatism along the Trans Vietnam Orogenic Belt (Figure 12a) [73]. These granites also cluster along a Permian–Triassic magmatic arc. This Permian–Triassic magmatic arc includes the magmatic rocks of the BG-QS complex, which is part of the built-up southern portion of the Trans Vietnam Orogenic Belt. Given all of the aforementioned original features and the period of their creation, it is likely that they formed during the Paleotethys Ocean’s subduction stage (290–250 Ma), beneath the Indochina block along the Song Ma suture (Figure 13).
Figure 12. (a) Tectonic map of Asia’s east and center regions (modified after [12,73]) and (b) geological map of the Indochina block that is simplified and displays the emplacement ages of Permian–Triassic rocks (modified after [12]). Comparison data are from [2,3,4,5,12,13,18,21,23,26,49,50,51,52,64,65,66].
Figure 12. (a) Tectonic map of Asia’s east and center regions (modified after [12,73]) and (b) geological map of the Indochina block that is simplified and displays the emplacement ages of Permian–Triassic rocks (modified after [12]). Comparison data are from [2,3,4,5,12,13,18,21,23,26,49,50,51,52,64,65,66].
Minerals 14 00569 g012
Figure 13. Tectonic reconstruction of the Indochina block and adjacent territories in the Permian–Triassic with modifications from [12,83] (a). Tectonic setting for the BG-QS magmatic rocks and other Permian–Triassic magmas in Vietnam, modified from [2,12] (b,c).
Figure 13. Tectonic reconstruction of the Indochina block and adjacent territories in the Permian–Triassic with modifications from [12,83] (a). Tectonic setting for the BG-QS magmatic rocks and other Permian–Triassic magmas in Vietnam, modified from [2,12] (b,c).
Minerals 14 00569 g013

6. Conclusions

The main conclusions drawn from the above observations and discussion include the following:
  • The Ben Giang-Que Son complex consists of gabbro, gabbrodiorite, quartz diorite, granodiorite, and less granite. They display typical features of I-type granite and belong to the high-K calc-alkaline series.
  • The geochemical and whole-rock Nd-Sr (ꜪNd(t) = −3.7 to −0.5) and zircon Hf (ꜪHf(t) = +2.4 to +4.6) isotopic characteristics indicated that the BG-QS gabbro and gabbrodiorite were generated from partial melting of an enriched mantle source. The hornblende diorite and granodiorite were generated from a mixing process of two magmas deriving from the enriched mantle and pre-existing juvenile lower crust. The mantle enrichment was triggered by subduction-related fluids and took place in the past.
  • LA-ICP-MS zircon U-Pb dating of BG-QS magmatic rocks provides the first reliable emplacement age of the BG-QS complex from 283–275 Ma. These ages indicate the existence of an Indosinian tectonic–thermal event in the study area, which is linked to the oceanic subduction of Paleotethys leading to the amalgamation of the Indochina and South China blocks.

Supplementary Materials

The following supporting information can be downloaded at: https://www.mdpi.com/article/10.3390/min14060569/s1, Table S1: Major and trace element contents of Permian-Triassic plutonic rocks in the Truong Son belt; Table S2: Whole-rock Sr–Nd isotope results in the Truong Son belt, Dalat zone and Kontum massif; Table S3: Initial ꜪHf values and Hf model ages on Permian-Triassic zircons from from the this study; Table S4: Ages of Permo-Triassic volcanic and plutonic in Viet Nam. Locations are shown in Figure 11b.

Author Contributions

Conceptualization, T.T.B.N. and P.T.H.; methodology, writing—original draft preparation, P.M.; data treatment and curation, T.T.B.N., P.T.H., Q.X., B.T.A., N.T.X., P.M. and H.T.T.; writing—review and editing, T.T.B.N. and P.T.H. All authors have read and agreed to the published version of the manuscript.

Funding

This study was financially supported by the National Foundation for Sciences and Technology Development of Vietnam (NAFOSTED) for the project 105.01-2018.320.

Data Availability Statement

The data are contained within the article.

Acknowledgments

We are deeply grateful to Pham Binh for guiding fieldwork and thin section preparation. We also acknowledge and thank Pham Thi Dung for guiding zircon separation.

Conflicts of Interest

The authors declare no conflicts of interest.

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Figure 1. (a) The geological tectonic framework of Southeast Asia, together with three main structural zones of the Indochina block (modified after [12,13]). (b) Geological map showing the distribution of different rock types in the study area (modified after [8,14]). The U-Pb zircon ages are compiled from [12,15] and data obtained in this study.
Figure 1. (a) The geological tectonic framework of Southeast Asia, together with three main structural zones of the Indochina block (modified after [12,13]). (b) Geological map showing the distribution of different rock types in the study area (modified after [8,14]). The U-Pb zircon ages are compiled from [12,15] and data obtained in this study.
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Figure 2. Petrography and mineralogy of the BG-QS complex: (a) representative field photos of the BG-QS studied samples; (b) medium–coarse-grained granodiorite; (c) medium–coarse-grained gabbrodiorite; (d,e) microphotographs of TS32 gabbrodiorite, and (f) microphotograph of TS26 granodiorite. Abbreviations: Pl = plagioclase, Bt = biotite, Hbl = hornblende, Qtz = quartz, and Kfs = K-feldspar.
Figure 2. Petrography and mineralogy of the BG-QS complex: (a) representative field photos of the BG-QS studied samples; (b) medium–coarse-grained granodiorite; (c) medium–coarse-grained gabbrodiorite; (d,e) microphotographs of TS32 gabbrodiorite, and (f) microphotograph of TS26 granodiorite. Abbreviations: Pl = plagioclase, Bt = biotite, Hbl = hornblende, Qtz = quartz, and Kfs = K-feldspar.
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Figure 3. (ai) Harker diagrams of major elements for the magmatic rocks of the BG-QS complex. The I- and S-type trends are from [6]. Comparison data are from [4,12,13].
Figure 3. (ai) Harker diagrams of major elements for the magmatic rocks of the BG-QS complex. The I- and S-type trends are from [6]. Comparison data are from [4,12,13].
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Figure 4. Geochemical characteristics of the BG-QS magmatic rock: (a) a plot of the SiO2 vs. K2O + Na2O [35]; (b) A/NK vs. A/CNK diagram [36], (c) SiO2 vs. K2O (wt%) showing high-K fields [37]; and (d) AFM diagram [38]. Comparison data are from [4,12,13].
Figure 4. Geochemical characteristics of the BG-QS magmatic rock: (a) a plot of the SiO2 vs. K2O + Na2O [35]; (b) A/NK vs. A/CNK diagram [36], (c) SiO2 vs. K2O (wt%) showing high-K fields [37]; and (d) AFM diagram [38]. Comparison data are from [4,12,13].
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Figure 5. Concentrations of the rare elements in the magmatic rocks of the BG-QS complex: (a) chondrite-normalized REE patterns and (b) primitive-mantle-normalized trace element distribution spidergrams. The normalized values are from [39]. Comparison data are from [4,12,13].
Figure 5. Concentrations of the rare elements in the magmatic rocks of the BG-QS complex: (a) chondrite-normalized REE patterns and (b) primitive-mantle-normalized trace element distribution spidergrams. The normalized values are from [39]. Comparison data are from [4,12,13].
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Figure 6. Discrimination diagram for the magmatic rocks of the BG-QS complex (ac) and zircon temperature (d) [29]. WPG = within-plate granite, VAG = volcanic-arc granite, Syn-COLG = syn-collisional granite, Post-COLG = post-collisional granite, ORG = ocean-ridge granite [40]. Comparison data are from [4,12,13].
Figure 6. Discrimination diagram for the magmatic rocks of the BG-QS complex (ac) and zircon temperature (d) [29]. WPG = within-plate granite, VAG = volcanic-arc granite, Syn-COLG = syn-collisional granite, Post-COLG = post-collisional granite, ORG = ocean-ridge granite [40]. Comparison data are from [4,12,13].
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Figure 7. Initial 87Sr/86Sr vs. ꜪNd diagram for the magmatic rocks of the BG-QS complex. Comparison data are from [12,41,42,43,44,45].
Figure 7. Initial 87Sr/86Sr vs. ꜪNd diagram for the magmatic rocks of the BG-QS complex. Comparison data are from [12,41,42,43,44,45].
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Figure 8. Cathodoluminescence (CL) images of representative zircon grains separated from the BG-QS magmatic rock. The zircon grains are ca. 80–250 μm long and 70–100 μm wide. Prismatic morphology and oscillatory zoning are characteristic of almost all zircon grains, suggesting a magmatic origin.
Figure 8. Cathodoluminescence (CL) images of representative zircon grains separated from the BG-QS magmatic rock. The zircon grains are ca. 80–250 μm long and 70–100 μm wide. Prismatic morphology and oscillatory zoning are characteristic of almost all zircon grains, suggesting a magmatic origin.
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Figure 9. Concordia diagrams showing LA-ICP-MS U-Pb ages of zircons separated from two representative magmatic samples of the BG-QS complex.
Figure 9. Concordia diagrams showing LA-ICP-MS U-Pb ages of zircons separated from two representative magmatic samples of the BG-QS complex.
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Figure 10. Characteristics of BG-QS magmatic rocks based on zircon isotope data. Histograms of zircon ꜪHf(t) values (a); Hf model age (TDM2) from the BG-QS magmatic rocks (b); and initial ꜪHf values and Hf model ages of zircons (c,d) from this study, Vietnam (modified after [2]). Comparison data are from [2,5,6,7,12,13,47,48,49,50,51,52].
Figure 10. Characteristics of BG-QS magmatic rocks based on zircon isotope data. Histograms of zircon ꜪHf(t) values (a); Hf model age (TDM2) from the BG-QS magmatic rocks (b); and initial ꜪHf values and Hf model ages of zircons (c,d) from this study, Vietnam (modified after [2]). Comparison data are from [2,5,6,7,12,13,47,48,49,50,51,52].
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Figure 11. Petrogenesis of the BG-QS complex: (Ta/La)PM vs. (Hf/Sm)PM for BG-QS magmatic rocks. Comparison data are from [4,12,13].
Figure 11. Petrogenesis of the BG-QS complex: (Ta/La)PM vs. (Hf/Sm)PM for BG-QS magmatic rocks. Comparison data are from [4,12,13].
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Table 1. Major and trace element compositions of the magmatic rocks of the BG-QS complex.
Table 1. Major and trace element compositions of the magmatic rocks of the BG-QS complex.
SampleTS24TS25TS26TS29TS30TS32TS32/1
LithologyGranodioriteGranodioriteGranodioriteGranodioriteGranodioriteGabbrodioriteGabbrodiorite
Latitude15°26′03.8″ N15°24′33.6″ N15°39′26.3″ N 15°36′03.6″ N15°38′49.6″ N15°41′33.5″ N15°41′33.5″ N
Longitude107°41′32.8″ E107°40′20.8″ E108°08′04.8″ E107°50′10.4″ E107°48′57.3″ E107°46′00.3″ E107°46′00.3″ E
SiO2 (wt%)64.1162.0262.7063.2861.5151.1152.76
TiO20.650.710.690.590.811.071.01
Al2O315.6515.9115.6115.7416.2918.3118.02
Fe2O3t4.214.524.514.245.458.677.73
MnO0.110.010.090.090.050.180.22
MgO1.652.112.211.962.834.223.33
CaO2.954.024.013.614.218.417.70
Na2O3.323.824.103.583.413.954.34
K2O4.294.013.753.893.511.371.76
P2O50.290.300.250.280.460.310.35
LOI2.132.241.212.481.202.152.10
Total99.3799.6799.1399.7399.7399.7599.32
Mg#43.6848.0449.2547.8050.7049.0846.04
A/CNK1.010.890.860.940.950.790.78
A/NK1.551.501.441.561.732.291.99
Sc (ppm)11.537.8516.7712.756.0613.5020.75
V53.5893.0072.1951.1843.18164.00176.65
Cr9.1936.8018.4015.1411.8028.9026.60
Ni7.0517.2016.8811.918.2419.4041.38
Cu9.7360.2023.823.4917.2212.605.81
Zn30.9066.5071.0346.26118.77121.0094.02
Ga20.7418.3024.2220.1218.6222.4021.74
Rb89.0679.0040.5971.31114.9237.6087.66
Sr414.49550.00335.65479.09414.88739.00592.23
Zr207.38201.14199.92186.19298.10188.00178.07
Nb22.1117.4034.8920.5422.5510.2030.48
Cs1.881.313.082.981.733.411.45
Ba1367.88717.00133.211787.291094.33407.00399.00
Hf5.639.339.655.259.454.544.50
Ta1.671.371.900.812.170.540.52
Pb19.47272.0011.0623.3045.1914.5214.52
Th7.241.873.652.979.628.218.21
U51.0015.1136.4937.3462.8044.3544.35
La84.5430.7093.4981.3883.5322.0025.11
Ce150.7162.60173.70146.93148.9449.4050.60
Pr16.167.0120.1416.2616.456.397.02
Nd51.6625.1071.0159.8845.6056.9126.11
Sm7.454.5013.056.447.988.315.69
Eu1.370.981.851.521.451.341.33
Gd7.283.4212.467.697.644.334.40
Tb0.900.501.811.011.010.640.59
Dy4.552.749.844.944.953.503.48
Ho0.780.581.890.850.910.700.69
Er2.321.655.382.482.761.901.88
Tm0.340.270.740.320.380.290.31
Yb2.031.844.592.052.381.841.85
Lu0.310.300.680.300.370.280.25
Y22.7716.8046.8621.5923.9619.9021.10
Li6.555.5924.1810.367.2327.9015.02
Be3.244.263.852.782.761.423.30
10,000Ga/Al2.502.172.932.412.162.312.28
ToZircon793.91769.06765.35774.10811.77715.99716.56
Eu/Eu*0.570.760.440.660.570.680.81
∑LREE311.89130.89373.23312.41303.95144.35115.86
∑HREE18.5211.3037.3919.6520.4113.4813.45
∑REE330.41142.19410.62332.06324.36157.83129.31
(La/Yb)n29.8311.9714.6228.4225.198.589.74
(Tb/Yb)n2.021.241.792.241.931.591.45
(La/Nd)n3.222.412.592.683.610.761.89
Ybn11.9610.8226.9812.0813.9910.8210.88
Q (CIPW)18.3111.9111.8915.6413.17
C0.90 0.33
Or26.0724.3222.6323.6421.058.3010.70
Ab28.8933.1835.4331.1129.2934.2437.77
An13.1014.8013.3915.8518.1528.8825.19
Di(FS) 1.512.150.30 4.935.23
Di(MS) 1.532.220.29 4.884.58
Hy(MS)4.234.694.594.887.151.952.66
Hy(FS)5.915.295.105.867.422.263.49
Ol(MS) 4.602.63
Ol(FS) 5.873.79
Mt0.630.670.670.630.801.291.16
Il1.271.391.341.151.562.081.97
Ap0.690.710.590.661.080.740.83
A/CNK value: molar Al2O3/(CaO + Na2O + K2O); A/NK value: molar Al2O3/(Na2O + K2O). ToZircon (oC) = 12,900/(2.95 + 0.85 × ((Na + K + 2 × Ca)/(AlxSi)) + lnDZr,zircon/melt) [29].
Table 2. Whole-rock Sr-Nd isotopic composition of the Ben Giang-Que Son complex.
Table 2. Whole-rock Sr-Nd isotopic composition of the Ben Giang-Que Son complex.
SampleRbSr87Rb/86Sr(87Sr/86Sr)m(87Sr/86Sr)iSmNd147Sm/144Nd(143Nd/144Nd)m(143Nd/144Nd)iNd(t)TDM2
(ppm)(ppm)(±2σ)(ppm)(ppm)(±2σ)(Ga)
TS2540.6 335.7 0.35030.717963 ± 50.717828.562.10.1053 0.512279 ± 11 0.512086−3.71.16
TS26141.0 550.0 0.74240.711280 ± 80.710984.525.10.1084 0.512286 ± 60.512087−3.3 0.99
TS3237.6 739.0 0.14730.709079 ± 80.708498.353.90.0923 0.512411 ± 140.512132−0.51.03
TS32/171.3 479.1 0.43100.714958 ± 50.714795.126.00.1177 0.512396 ± 50.512181−1.91.13
m: measured isotopic ratios; i: initial isotopic ratios; t = 280 Ma is used for calculation of initial ratios.
Table 3. U-Pb zircon ages of the Ben Giang-Que Son complex.
Table 3. U-Pb zircon ages of the Ben Giang-Que Son complex.
SampleTh/UIsotopic Ratios Age (Ma)
207Pb/206Pb207Pb/235U206Pb/238U206Pb/238U207Pb/235UConc%
TS32 15°41′33.5″ N, 107°46′00.3″ E
−10.60.0523900.0007300.3289600.0048900.0455400.0004302873289499
−20.80.0521300.0007000.3071400.0050500.0427300.0005202703272499
−30.70.0525300.0007400.3270100.0052500.0451300.0004902853287499
−40.60.0523000.0007700.3181600.0061400.0440600.0005702784280599
−50.60.0515600.0007800.3046900.0052500.0429400.00062027142704100
−60.50.0548000.0009400.3301400.0075000.0435300.0005902754290695
−70.70.0519300.0007500.3058000.0055900.0427200.00062027042714100
−80.50.0512500.0009700.3168800.0063700.0448800.00060028342795101
−90.60.0524200.0007100.3252700.0053600.0449300.0005602833286499
−100.70.0520600.0007800.3087500.0045600.0430700.00054027232734100
−110.70.0520000.0007300.3083000.0051100.0429500.0005602713273499
−120.80.0516000.0006400.3201900.0055900.0448800.00065028342824100
−130.60.0517700.0010100.3155200.0069500.0442500.00077027952785100
−140.50.0519900.0008400.3225500.0064700.0449100.00066028342845100
−150.60.0515500.0010000.3183500.0072300.0448100.00072028342816101
−160.90.0522500.0006500.3302300.0045300.0457700.0004902883290399
−170.60.0522700.0007800.3299100.0058200.0456300.00045028832894100
−180.50.0524700.0011500.3415900.0075200.0472500.00054029832986100
−190.60.0526900.0007200.3428300.0048000.0471700.0004802973299499
−200.60.0525500.0011020.3428410.0123700.0448400.0006602825300694
TS26 15°39′26.3″ N, 108°08′04.8″ E
−10.60.0547200.0019600.3326600.0157100.0441900.002020279122921296
−20.60.0592800.0026600.3564800.0192600.0435100.00202027593101489
−30.50.0583900.0026300.3487700.0185400.0436400.00200027553041490
−40.80.0521600.0020400.3061700.0153200.0429300.0019602711227112100
−50.50.0583700.0018800.3547100.0161500.0440300.002000278123081290
−61.30.0547400.0019100.3296600.0152700.0436300.001980275122891295
−70.90.0548900.0018000.3438400.0155000.0458600.002090289133001296
−80.70.0590700.0026650.3385340.0163780.0416390.00053826442961289
−90.60.0536100.0017300.3308400.0151700.0445300.002030281132901297
−100.80.0608200.0024400.3756800.0195600.0446600.002060282133241487
−110.50.0610000.0017900.3863700.0173000.0458300.002110289133321387
−121.30.0658600.0020840.4060580.0139650.0440200.00057627843461080
−130.60.0668200.0018700.3913720.0153300.0424900.00066026873351180
−140.50.0523400.0027200.2933500.0177100.0412100.0019102601226114100
−150.90.0684700.0034900.4225800.0263100.0456500.002100288133581980
−161.20.0711400.0019900.4292700.0173200.0433800.00063027173631275
−171.90.0640000.0016900.3678100.0144800.0418600.00064026473181183
−180.90.0555500.0015200.3428400.0137000.0449400.00066028342991095
−190.40.0676000.0029400.4030500.0250000.0442900.00097027963441881
−200.70.0637400.0019100.3780100.0165900.0436600.001990275123261284
Conc.% = ((206Pb/238U)/(207Pb/235U)) × 100.
Table 4. Zircon Lu-Hf isotope composition and model age of the Ben Giang-Que Son complex.
Table 4. Zircon Lu-Hf isotope composition and model age of the Ben Giang-Que Son complex.
Sample176Yb/177Hf176Lu/177Hf176Hf/177Hf±2σ176Hf/177HfεHf(t)±2σTDM1TDM2
(t)(Ma)(Ma)
TS32 15°41′33.5″ N, 107°46′00.3″ E
TS32-010.0470770.0010760.282733130.2827264.50.57401016
TS32-020.0674070.0016180.282730130.2827194.30.57561030
TS32-030.0398870.0010480.282710130.2827033.70.57721068
TS32-040.0395900.0010040.282703130.2826963.50.57821083
TS32-050.0428730.0010910.282716130.2827093.90.57641054
TS32-060.0207240.0005010.282708130.2827033.70.57641066
TS32-070.0165870.0003990.282688130.2826843.00.57901110
TS32-080.0203010.0005050.282670130.2826652.40.58181153
TS32-090.0302480.0007380.282712110.2827063.80.47641061
TS32-100.0597720.0015000.282730130.2827204.30.57541029
TS32-110.0232930.0005690.282713120.2827083.90.47591056
TS32-120.0364730.0008800.282723130.2827174.20.57501036
TS32-130.0364180.0008860.282721130.2827144.10.57541042
TS32-140.0254580.0006400.282679130.2826732.70.58081134
TS32-150.0395560.0009910.282723130.2827164.20.57531038
TS32-160.0211920.0005560.282691120.2826873.10.47881104
TS32-170.0494430.0013030.282738130.2827294.60.57381008
TS32-180.0482060.0012000.282737130.2827294.60.57381009
TS32-190.0264040.0006860.282689150.2826843.00.57941110
TS32-200.0261300.0006650.282699130.2826943.40.57791087
t = 280 Ma for sample TS32.
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Nguyen, T.T.B.; Hieu, P.T.; Xin, Q.; Anh, B.T.; Xuan, N.T.; Minh, P.; Thu, H.T. Zircon U-Pb Geochronology, Geochemistry, and Sr-Nd-Hf Isotopic Composition of Ben Giang-Que Son Complex in the Southern Truong Son Belt: Implications for Permian–Triassic Tectonic Evolution. Minerals 2024, 14, 569. https://doi.org/10.3390/min14060569

AMA Style

Nguyen TTB, Hieu PT, Xin Q, Anh BT, Xuan NT, Minh P, Thu HT. Zircon U-Pb Geochronology, Geochemistry, and Sr-Nd-Hf Isotopic Composition of Ben Giang-Que Son Complex in the Southern Truong Son Belt: Implications for Permian–Triassic Tectonic Evolution. Minerals. 2024; 14(6):569. https://doi.org/10.3390/min14060569

Chicago/Turabian Style

Nguyen, Thuy Thi Bich, Pham Trung Hieu, Qian Xin, Bui The Anh, Nguyen Thi Xuan, Pham Minh, and Ho Thi Thu. 2024. "Zircon U-Pb Geochronology, Geochemistry, and Sr-Nd-Hf Isotopic Composition of Ben Giang-Que Son Complex in the Southern Truong Son Belt: Implications for Permian–Triassic Tectonic Evolution" Minerals 14, no. 6: 569. https://doi.org/10.3390/min14060569

APA Style

Nguyen, T. T. B., Hieu, P. T., Xin, Q., Anh, B. T., Xuan, N. T., Minh, P., & Thu, H. T. (2024). Zircon U-Pb Geochronology, Geochemistry, and Sr-Nd-Hf Isotopic Composition of Ben Giang-Que Son Complex in the Southern Truong Son Belt: Implications for Permian–Triassic Tectonic Evolution. Minerals, 14(6), 569. https://doi.org/10.3390/min14060569

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