Figure
1.
Sketch geologiacal map of the Kekesentao area (modified from Wang et al., 2012).
| Citation: | Yu Shi, Yuwang Wang, Jingbin Wang, Lijuan Wang, Rufu Ding, Yanfei Chen. Zircon U-Pb Age, Geochemistry and Geological Implications of Granitoids in Tuerkubantao, Xinjiang. Journal of Earth Science, 2013, 24(4): 606-618. doi: 10.1007/s12583-013-0360-z
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It is generally accepted that the central Asian orogenic belt (CAOB), the world's largest accretinary orogen, was largely formed by subduction of the Paleo-Asian Ocean and accretion of oceanic seamounts and plateaus, ophiolites and collision of ancient microcontinents, arc terranes and successions of passive continental margins (Xiao et al., 2009, 2004; Jahn et al., 2004; Safonova et al., 2004; Sengör et al., 1993; Coleman, 1989; Feng et al., 1989).
The northwest margin of Junggar is south to Chinese Altay, and separated by Erqis fault, which marks the boundary between the Caledonian Altay orogenic belt to the north and the Hercynian Junggar terrane to the south (Coleman, 1989). The volcanic rocks and its intrusions in this terrane is characterized by high εNd(t) (up to +8.4), which is much higher than that of the terranes in Chinese Altay, and indicate the juvenile character of its basement (Wang et al., 2009; Zhang Z C et al., 2008, 2006). Therefore, the granites in this belt display chemical differences from the granites in Altay orogen. Two kinds of major orogenic granites have been recognized in the northwestern margin of Junggar. The first one is typical volcanic arc granites (VAG) (Wang et al., 2012; Zhang H X et al., 2008; Zhang Z C et al., 2006), some of which is adakite associated with copper porphyries deposit (Xue et al., 2010; Yang et al., 2005). The second one is A-type granite occurred in Buergen with composition similar to the A2-type granites formed in ridge subductionrelated extensional setting (Shen et al., 2011), rather than that formed in post-orogenic setting (Black and Liegeois, 1993). Therefore, the identification and study of granitoids in this area are of tectonic and economic significances.
During the recent field studies of the Kekesentao Mountains area located in the southwest of Buerjin Town, North Xinjiang, we sampled three types of granitoids. In this article, we present the geochemistry and zircon U-Pb ages of three types of granitoids and discuss their geological and geochemical data in the context of the convergence and collision in order to reconstruct the tectonic framework of the Altay orogen evolution.
The strata outcropping in Tuerkubantao district consist of Devonian to Carboniferous sedimentary sequence (Fig. 1). Middle Devonian Yundukala Formation (D2y) is the dominant outcrops in the studying area, and is divided into two sub-formations on lithology. The lower sub-formation (D2ya) is sandy slate interbeded with siliceous rock and tuffaceous siltstone, while the upper sub-formation (D2yb) is sandy slate interbeded with quartzite, limestone. In the south, there are outcrops of mudstones, siltstones and limestones of the Lower Carboniferous Nalinkala Formation (C1n), as well as calcareous sandstones and mudstones of the Upper Carboniferous Qiaqihai Formation (C2q). Yundukala Formation is intruded by Hercynian granitic batholith, which is dominated by porphyritic biotite granite. In the south, there are also outcrops of Hercynian granitic porphyry intrude the D2y Formation, occurred as apophyses and dikes.
The biotite granites were collected at 47º31.1'N, 86º53.6'E, while granites and rhyolites were collected at 47º30.7'N, 86º51.5'E and 47º31.7'N, 86º53.7'E, respectively (Fig. 1). The granite is grayish and possesses porphyritic texture. The mineral assemblages are dominated by quartz and plagioclase, with minor biotite and potassium feldspar (Fig. 2a). The rhyolite contains quartz and potassium feldspar as phenocryst, both of which vary in size (Fig. 2b). The biotite granite is medium to coarse grained with typical granitic texture and consists of quartz, plagioclase and biotite and accessory magnetite (Fig. 2c).
Three types of granitoids including granite, rhyolite and biotite granite were collected from Tuerkubantao area. After careful microscopically study, several representative samples were selected for major and trace elements analysis. Major and trace elements compositions were determined in the Analytical Laboratory of Beijing Research Institute of Uranium Geology, CNNC (China National Nuclear Corporation). Analyses of major element compositions were performed by X-ray fluorescence spectrometer, and ferrous iron was determined by a wet chemical method. Trace and rare earth elements compositions were determined using ICP-MS. The precision of the analyses was generally ~1% for major oxides, ~0.5% for SiO2, and 3%–7% for trace elements. Accuracy is monitored by repeated analyses of standard BHVO-1. The results are listed in Table 1.
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The samples were processed involving crushing and initial heavy liquid and subsequent magnetic separation. Zircon grains form the > 25 μm nonmagnetic fractions were hand-picked and mounted on adhesive tape, enclosed in epoxy resin and then polished to about half of their size and photographed under reflected and transmitted light. Cathodoluminescence (CL) imaging of zircon grains was carried out using a Mono CL3 detector attached to an electron microprobe at the Key Laboratory of Mineral Resources of Institute of Geology and Geophysics, Chinese Academy of Sciences. LA-ICP-MS analyses were made on the exposed zircon surface using a 213 laser ablation system coupled with Agilent 7500a quadrupole ICP-MS at the Key Laboratory of Orogenic Belt and Crustal Evolution, Beijing University. The instrumental performance and detailed analytical procedures and parameters followed Xia et al. (2004). In our analysis, zircon standard PLE was used as a calibration standard, while zircon standard QH was used as a supplementary calibration standard. The laser beam of 32–60 μm in diameter depending on the sample grain size, 5 Hz and 12 J/cm2 was limited to an analytical cycle of 0.2 s. All analyses in this study yielded a 204Pb intensity lower than the limitation of detection, typically < 20 counts per second, and thus no common lead correction was necessary. Since the fractionation of 206Pb/238U was linear during the time of acquisition, the intercept method was used to correct for the laser induced Pb/U fractionation (Sylvester and Ghaderi, 1997). Ages have been calculated from the U and Th decay constants recommended by Steiger and Jäger (1977). All data were processed using Glitter 4.4 soft ware, and reported ages were calculated using IsoplotEx 4.96. The results of U-Pb zircon dating age are listed in Table 2 and illustrated in Fig. 3, in which errors are ±1σ, whereas error for weighted mean ages of samples is quoted at ±2σ.
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Granites (K-3, K-4) are scattered in the TAS (total alkali-silica) diagram (not shown) and in the SiO2 vs. K2O diagram (not shown) for its high amount of LOI (loss on ignition) ranging from 1.6 to 2.6. All the granite samples have molar ratios of Al2O3/(Na2O+K2O) ranging from 1.09 to 1.52 and are metaluminous with aluminous indices (A/CNK) ranging from 0.85 to 0.95.
The rhyolites (K-5, K-5b, and K-5c) are classified as alkaline rhyolite or trachy-dacite, and belong to the shoshonite series. All the samples are characterised by low amount of Al2O3 (13.26 wt.% to 16.46 wt.%), high amount of total alkaline (9.60 wt.% to 11.19 wt.%). The ratio of K2O/Na2O ranges from 0.9 to 1.9 mainly more than 1, which indicate the host lava is high-potassium rock.
Biotite granites (K-7, K-8, and K-9) are classified as granodiorites in composition in the TAS diagram (not shown). The freshest sample (K-9) belongs to the high-K calc-alkaline series, while the rest samples (K-7, K-8) are a little scattered due to its high value of LOI (up to 2.27 wt.%). All the biotite granites are peraluminous with A/CNK and A/NK ranging from 1.10 to 1.29 and 1.71 to 2.11, respectively, and have K2O/Na2O lower than 1.
The granites have lower REE and incompatible element contents but similar normalized REE and incompatible element patterns with that of granite porphyries in Xilekuduke (Figs. 3a, 3b). The ΣREE of the rhyolites (58 ppm–147 ppm) is lower than the other two types of granitoids in this article. The granites are enriched in LREE ((La/Sm)N=2.46–3.29, (La/Yb)N=3.16–5.77), and depleted in Eu (δEu=0.29–0.53). In the spider diagram (Fig. 3b), the rhyolites are characterized by the depletion of Sr, Nb, Ta, Ti, P, and enrichment of LREE, large iron lithophile elements (LILE).
The rhyolites have lower contents of REE, LILE, and HFSE compared with A-type granites in Qiaqihai and Kuoyitasi, however, they share a same shape of normalized REE and incompatible elements patterns (Figs. 3c, 3d). The rhyolites, with ΣREE ranges from 161 ppm to 317 ppm, display significant LREE enrichment ((La/Sm)N=3.24–3.92, (La/Yb)N=7.31–2.08), and show slightly negative Eu anomalies (δEu=0.52–0.58). In the spider diagram (Fig. 3d), the rhyolites depleted in Nb, Ta, Ti and P, while enriched Rb, Ba, Th, U, K, Zr and Hf, which could be compared with A-type granites in Qiaqihai.
The biotite granites share a common shape of normalized REE and incompatible elements patterns with the gneissic granites in Tuerkubantao ophiolitic mélange, at the same time, the contents of incompatible elements of these two kinds of granitoids are comparable (Figs. 3e, 3f). The biotite granites have REE abundances of 100 ppm–139 ppm, display the least enrichment of LREE ((La/Sm)N=2.46–3.29, (La/Yb)N=3.16–5.77), and slightly depletion in Eu (δEu=0.67–0.82). In the spider diagram (Fig. 3f), the biotite granites enriched of Rb, Ba, Th, K, and LREE, and depleted of Nb, Ta, Ti and P.
Sample K-3, granite, composed of K-feldspar, plagioclase and quartz, and 10 zircon grains were selected from it to analyze. Most of the 10 zircon grains are colorless, transparent, and display oscillatory zoning (Fig. 4a). However, all of the zircon grains in granite are small in size. At the same time, all the samples have high Th/U ratios ranging from 0.50 to 0.99 indicating their magmatic origin. In the concordia diagram (Fig. 4b), all of the analyses are normally discordant and intercept with the concordia curve with the weighted lower intercept 206Pb/238U age of 324.4±7.3 Ma.
Sample K-5b, rhyolite, composed of quartz and K-feldspar, from which 22 zircon grains were selected for analyzing. All of the 22 zircon grains are colorless, transparent, well-shaped, and have oscillatory zoning (Fig. 4c). The Th/U ratio ranges from 0.44–0.98, with an average of 0.80, higher than 0.4, at the same time, the contents of Th and U are well correlated suggesting their magmatic origin (Vavra et al., 1999, 1996). Twenty-two analyses are obtained from 22 zircon grains. All analyses from one coherent group and tightly cluster on concordia diagram (Fig. 4d), yielding a concordia age of 295.9±1.4 Ma.
Sample K-9, biotite granite, composed of biotite, K-feldspar, plagioclase and quartz, and 15 zircon grains were selected from it to analyze. Two separate parts of the zircon are recognized on CL image: one part is the core with oscillatory zoning patterns; the other is the overgrowth rim with dark CL images. The core is colorless and transparent, and the analyzed spots are labeled after K-9-1 to K-9-7 (Fig. 4e). The overgrowth rim of the zircon grains display the characteristics of hydrothermal zircon (Zhu and Song, 2006), and the analyzed spots are labeled after K-9-8 to K-9-15 (Fig. 4g). Two groups of concordia age were obtained. The first group analyses of zircon concentrate on the concordia age of 383.8±2.5 Ma (Fig. 4f), while the second group of age cluster tightly on 356.2±6.4 Ma (Fig. 4h).
Since the bulk rock of the granite and the biotite granite are both altered severely, the granitoids in adjacent area with the same age are taken into consideration to discuss the tectonic framework of northwest margin of Junggar Block.
The texture of the zircon grains in the biotite granite indicate that its zircon grains had experienced at least two stages of growth. The core of the zircon grains in the biotite granite display the characteristics of magmatic zircon (Pei et al., 2009), and its concordia age implies that the biotite granite crystallized in magma in Middle Devonian. This age could be linked to the episode producing adakites in Xileketehalasu (381±6 Ma, Zhang et al., 2006) and in Kalasai (376±10 Ma, Zhang et al., 2006), both of which are typical volcanic arc granite (VAG) produced by subduction of oceanic slab (Zhang et al., 2006). The rims of zircon grains are gray in color and similar to the hydrothermal zircon (Zhu and Song, 2006). The concordia age of the hydrothermal zircon rims (356.2±6.4 Ma) is very close to the crystallization age of gneissic granites (355.4±6.9 Ma, Wang et al., 2012) in the ophiolitic mélange, which also occur in Tuerkubantao area. Then, it is reasonable to suggest that the recrystallization of the hydrothermal zircon rim is possibly induced by intrusion of another magmatism producing the gneissic granites in the Tuerkubantao ophiolitic mélange. Although the biotite granites are slightly altered, the immobile elements chondrite and primitive mantle normalized patterns display the characteristics of volcanic arc granite, which is characterised by the enrichment of LILE and LREE and depletion of HFSE including Nb, Ta, Zr, Hf (Fig. 2f). Therefore, it could be concluded that the northwestern margin of the Junggar terrane had been in the process of oceanic subduction from Middle Devonian to Late Devonian.
The significant depletion of Eu and Sr of the bulk rocks implies the large amount of plagioclase fraction had taken place in the magmatic process. At the same time, the granites have high amount of LOI and lower content of incompatible elements compared with the granitoids in Xilekuduke, both of which imply that the granites had suffered severe alteration. All of the analyses of the zircon grains are normally discordant and the zircon grains appear to have suffered significantly Pb loss. This could be coursed either by its small size or the severe alteration of the bulk rock, both of which could induce the effect of Pb loss (Silver and Deustch, 1963). The granite has a lower intercept age of 324.4±7.3 Ma, which is in accordance with the crystallized age of the granite in Xilekuduke (329.6±4.1 Ma, Long et al., 2009) in the range of error. The granite's incompatible element patterns are similar to that of the granitoids in Xilekuduke, at the same time, both Tuerkubantao and Xilekuduke districts locate on the eastern margin of the Junggar terrane, then, the magmatism occurred in the same period could be attributed to the same tectonic event. Then, bulk rock geochemistry of the granitoids in Xilekuduke is used to discuss the episode that toke place in the Early Carboniferous for the severe alteration of the Tuerkubantao granite in this study. Two groups of granitoids in Xilekuduke including granodiorite porphyries and granite porphyries are recognized, both of which originated from the same source, and are products in different evolution stages (Long et al., 2009). In the R1 vs. R2 diagram (Fig. 5a), the granite porphyries in Xilekuduke fall in the area of syn-collision, while the granodiorites porphyry in Xilekuduke plot in the area of post-collision uplift. The trend of the magmatic rock in Xilekuduke evolves from the field 6 (syn-collision field) to field 3 (post-collision uplift) is very similar to the evolve trend of syn-collisional I-type porphyritic granites in the central Ribeira belt in Brazil (Mendes et al., 2006). Therefore, the suit of granitic rocks in Xilekuduke is likely formed during syn-collision to post-collision process. To sum up, we suggest that both the granites in Tuerkubantao and granitoids in Xilekuduke are formed in syn-collisional tectonic setting.
The rhyolite with crystallization age of 295.9±1.4 Ma formed nearly at the same period with the typical A-type granites in Qiaqihai and Kuoyitasi (290.7±9.3 and 297.9±4.6 Ma, respectively, Zhou et al., 2006) in the error range, both of which formed in post-orogenic tectonic setting. In the R1 vs. R2 discriminating diagram (Fig. 5a), the samples of Qiaqihai and Kuoyitasi plot in the late orogenic area and post-orogenic area respectively, and the rhyolite mainly plot in the post-orogenic area. The rhyolites are plot in the WPG area (Figs. 5b, 5c, 5d) and classified as A-type granitoids in the discriminating diagram of Zr+Nb+Ce+Y vs. FeO(T)/MgO (Fig. 5e) together with the A-type granites in Qiaqihai and Kuoyitasi, and recognized as A2 type granitoids in the discriminating diagram of Nb-Y-Ce (Fig. 5f). Therefore, the rhyolite belongs to the A-type granitoids and formed in post-orogenic tectonic setting.
Three types of granitoids including biotite granite, granite, and rhyolite occur in the Tuerkubantao district of the Kekesentao area, northern Xinjiang. The geochemistry and geochronology of three types of granitoids in Tuerkubantao have recorded the tectonic evolution the North Junggar. Based on the geochemistry of the three types of granitic rocks and it's implication on their tectonic setting, we use the zircon U-Pb chronology to reconstruct the tectonic framework of orogen evolution between Kazakhstan and Siberia continents. From Middle to Late Devonian, the northwestern margin of Junggar has been in the stage of convergence, with large scale magmatism induced by the subduction of oceanic slabs. The area of northwestern margin of Junggar terrane had been in syn-collisional setting in Early Carboniferous, and stepped into post-orogenic setting in the Early Permian.
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Yu Shi, Yuwang Wang, Jingbin Wang, Lijuan Wang, Rufu Ding, Yanfei Chen. Zircon U-Pb Age, Geochemistry and Geological Implications of Granitoids in Tuerkubantao, Xinjiang. Journal of Earth Science, 2013, 24(4): 606-618. doi: 10.1007/s12583-013-0360-z
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