Zircon U-Pb SHRIMP Ages from the Late Paleozoic Turpan-Hami Basin, NW China

Home , Hami, Turpan Depression

Journal of Earth Science, Vol. 25, No. 5, p. 924–931, October 2014 ISSN 1674-487X Printed in China DOI: 10.1007/s12583-014-0484-9

Xiang Mao*1, 2, Jianghai Li1, 2, Huatian Zhang1, 2 1. The Key Laboratory of Orogenic Belts and Crustal Evolution, Ministry of Education, School of Earth and Space Sciences, Peking University, Beijing 100871, China 2. Institute of Oil and Gas, Peking University, Beijing 100871, China

ABSTRACT: Permian volcanic rocks are widely distributed in the Turpan-Hami Basin, which is part of the Central Asian orogenic belt. Here we present SHRIMP zircon data for the rhyolite in Well Baocan 1, one of the deepest wells in the basin. The 283.9±2.7 Ma reported in our study provides the best precise age determination for the Yierxitu Formation, the oldest Permian layer of Hami Depression, one of the three substructural units of the Turpan-Hami Basin, and a potential hydrocarbon reservoir in this basin. Our data refines earlier imprecise 39Ar-40Ar ages and shows that the volcanic rocks both inside the Turpan-Hami Basin and along its margin are almost coeval. We delineate a collisional orogenesis, and the new age of 283.9±2.7 Ma may limit the latest time of the collision orogenesis. KEY WORDS: SHRIMP U-Pb zircon geochronology, Turpan-Hami Basin, Permian, Yierxitu Forma- tion, Central Asian orogenic belt.

0 INTRODUCTION the 1980s, with a number of reports on the sedimentological During Late Paleozoic, the Central Asian orogenic belt and tectonic evolution (Wu et al., 2009; Greene et al., 2001; (CAOB) was in a transitional period with complex crust-mantle Shao et al., 1999; Shao, 1996; Zhao et al., 1992; Allen et al., material exchange and formation of transitional crust as evi- 1991; Windley et al., 1990; Zhu and Yang, 1988; Zhu and Chen, denced from the Xinjiang region (Xiao et al., 2006). As a result, 1980). In addition, as one of the three biggest basins in large scale Paleozoic volcanic activity occurred throughout the Xinjiang, the Turpan-Hami Basin is currently a focus for min- Junggar and Turpan-Hami basins. However, compared with the eral and energy resource exploration. Several literatures about large database accumulated in recent studies from the Junggar the oil, natural gas, coal, porphyry copper, and the large-scale Basin, there are only limited studies on the Paleozoic volcanic regional uranium anomalies has been published recently (Wang rocks from the Turpan-Hami Basin primarily because the sur- et al., 2011; Wu et al., 2009; Tang et al., 2007; Han et al., 2006; face of the basin is covered mostly by desert, and the only ex- Chen et al., 2001). Since exploration in the volcanic reservoirs posures are limited to the margin of the basin. For instance, Li in the adjacent Junggar and Santanghu basins has been suc- et al. (2006) studied the Permian mafic-ultramafic complexes cessfully carried out, the prospects for hydrocarbon exploration on the southern margin of the Turpan-Hami Basin; Ren et al. in the volcanic reservoirs in the Turpan-Hami Basin are also (2006) dated the east Caixiashan quartz diorite stock in the fairly good. southern margin of the basin, and Li et al. (2011) investigated In this study, we report a zircon U-Pb SHRIMP age of the the petrology, isotope chronology, and geochemical features of rhyolite from the core of Well Baocan 1, one of the deepest Carboniferous volcanic rocks in eastern Tianshan, bounded to wells in the Turpan-Hami Basin, in the eastern part of the basin. the south of the Turpan-Hami Basin. There are also some re- Our study provides important new constraints on the timing of ports on 39Ar-40Ar dating of the volcanic rocks from the core the Paleozoic volcanic activity in the Turpan-Hami Basin and samples from inside the basin (Liu et al., 2006; Zhou et al., shows the contrasting evolution between the margin and the 2006), but the imprecise age range is much wider than the basin. range of the volcanic rocks in the margin. In addition, the characteristics of Paleozoic volcanic rocks buried inside the basin 1 GEOLOGICAL SETTING AND SAMPLING are still poorly understood. The Turpan-Hami Basin (also called Tuha Basin, Fig. 1), The Turpan-Hami Basin has been intensively studied since is located in the eastern side of the Xinjiang Uygur Autonom- ous region in Northwest China. It covers an area of approx- *Corresponding author: [email protected] imately 5.35×104 km2, and most of the basin consists of desert © China University of Geosciences and Springer-Verlag Berlin or regolith sediments (Wang et al., 2011; Chen et al., 2001). Heidelberg 2014 Aiding Lake, located in the southwestern part of the basin, is the lowest land surface in China, lying 154 m below sea level; Manuscript received October 18, 2013. it is also the second lowest continental point in the world Manuscript accepted April 15, 2014. (Wang et al., 2011; Wu et al., 2009; Pirajno et al., 2008;

Mao, X., Li, J. H., Zhang, H. T., 2014. Zircon U-Pb SHRIMP Ages from the Late Paleozoic Turpan-Hami Basin, NW China. Journal of Earth Science, 25(5): 924–931. doi:10.1007/s12583-014-0484-9 Zircon U-Pb SHRIMP Ages from the Late Paleozoic Turpan-Hami Basin, NW China 925

Figure 1. Simplified geological map of the Turpan-Hami Basin in northwest China showing distribution of granitic rocks, mafic-ultramafic intrusions and intraplate mafic volcanics. Modified after Geng et al. (2011), Pirajno et al. (2008) and Chen et al. (2001).

Min et al., 2005; Shao et al., 1999). Bounded by the Bogda 2001). In the Hami Depression, the Yierxitu Formation is the Mountains to the north, Jueluotage Mountains to the south, first cap rock with an angular unconformity above the Carbo- Haerlike Mountain to the east, and Kalawucheng Mountain to niferous basement (Gao et al., 2004; Zhang et al., 1997). It is the west (Wu et al., 2009; Chen et al., 2001; Shao et al., 1999; comprised of volcanic rocks (mainly andesite, tuff and volcanic Fig. 1), the Turpan-Hami Basin is positioned between the breccia) and clastic rocks, with a total thickness ranging from Junggar Basin to the northwest and the Tarim Basin to the 355 to 1 215 m. southwest, being surrounded on all sides by the Tian Shan fold In this work, samples were collected from Well Baocan 1 belts (Pirajno et al., 2008; Ge et al., 1997; Fig. 1). The basin in the Hami Depression. Well Baocan 1 was drilled on Sep- can be subdivided into three sub-basins: the Turpan Depression tember 8th, 2009 and was the deepest well in the Turpan-Hami in the west, the Liaodun Uplift in the mid-section, and the Ha- Basin (with a designed depth of 5 600 m) at that time. Volcanic mi Depression in the east (Chen et al., 2001; Fig. 1). rocks of the Yierxitu Formation (mainly brownish red andesite) Windley et al. (1990) and Allen et al. (1991) proposed that were obtained below 4 240 m. From the rhyolite (Fig. 2; red, the Turpan-Hami Basin was formed as a foreland basin during with obvious fluxion structure in hand specimen and highly the Palaeozoic collisions that formed the Tian Shan orogenic directional quartz in microsection) from the 1/2 of the fourth belts, and Hou (1995) proposed that the collision occurred dur- core barrel (4 854.4 m), Sample T79 was selected for SHRIMP ing the Late Carboniferous–Early Permian. However, there are U-Pb zircon analyses. also alternate views on its tectonic evolution, such as Ge et al. (1997) who held that the Turpan-Hami Basin is a piggyback on 2 ANALYTICAL METHOD AND RESULT the Bogda nappe. Sample T79 was processed by crushing and initial heavy The basement rocks of the Turpan-Hami Basin are Prote- liquid and subsequent magnetic separation. Together with sev- rozoic metasedimentary units and Carboniferous inter- eral grains of standard zircon TEMORA, the zircons extracted mediate-acidic volcanic and volcaniclastic rocks (Min et al., from the sample were handpicked and mounted in epoxy, which 2005). The Permo-Carboniferous strata in the Turpan-Hami was then polished to section the crystals for analysis. All zir- Basin consist primarily of marine carbonate rocks, volcanic cons were then studied under transmitted and reflected light as rocks, and pyroclastic rock assemblages. The Upper Permian is well as cathodoluminescence (CL) to identify their internal a lacustrine sequence whereas the Triassic rocks are composed structures and to ensure that analytical sites did not transgress of moderately deep to shallow lake and fluvial deposits. Above internal boundaries. The mount was vacuum-coated with the Triassic, the dominant rocks are Jurassic conglomerate, high-purity gold. sandstone, shale and coal, Cretaceous red conglomerate and U-Th-Pb analyses of the zircons were performed on the sandstone, Tertiary red conglomerate, sandstone and shale, and SHRIMP II in the Beijing SHRIMP Center, Institute of Geology, Quaternary gravel, sand and clays (Min et al., 2005; Chen et al., Chinese Academy of Geological Sciences. Analytical

926 Xiang Mao, Jianghai Li and Huatian Zhang

Figure 2. Photograph and Photomicrographs of Sample T79. (a) Image of Sample T79, with obvious fluxion structure; (b) spherolitic structure; (c) carlsbad twin; (d) highly directional quartz. procedures followed those of Williams (1998), and data were ppm). The two older 206Pb-238U ages may indicate inheritance, processed using the Excel-based Squid and Isoplot programs but no interpretation could be made based on one spot. Reject- (Ludwig, 2003, 2001). Mass resolution during the analytical ing these two spots, the remaining 16 analyses give a weighted sessions was ~5 000 (1% definition). Spot sizes were approx- mean 206Pb-238U age of 283.9±2.7 Ma (data-point error symbols imately 30 μm, and the intensity of the primary O2 ion beam are 1σ, MSWD=0.54), which is interpreted as the eruption age was 4–6 nA. Each spot was rastered for 208 s prior to analysis. for the Sample T79. Based on the age, the timing of the vol- Data were determined by taking 5 scans on 90Zr2 16O+, 204Pb+, canic event which represents the time of the Yierxitu Formation background, 206Pb+, 207Pb+, 208Pb+, 238U+, 232Th16O+, 238U16O+. is confirmed to be 283.9±2.7 Ma. Common Pb corrections were made using the measured 204Pb. Uncertainties for each individual analysis are reported at a 1σ 3 DISCUSSION AND CONCLUSIONS level, whereas weighted mean ages of individual samples are Permian volcanic rocks are widespread in the Turpan- quoted at the 95% confidence level (2σ). All analytical results Hami Basin and its margins (Li X N et al., 2008; Han et al., are listed in Table 1. 2006; Liu et al., 2006, 2001; Chen et al., 2001; Li M W et al., Zircons from Sample T79 are mostly euhedral, transparent, 2001). Earlier studies showed that the ages of the Permian vol- colorless or brown, and range from 80 to 150 μm in length, canic rocks in the margin of the Turpan-Hami Basin range with length to width ratios between 1.5 : 1 and 2.5 : 1 (Fig. 3). mainly from about 266 to 292 Ma (Tang et al., 2011; Li et al., The CL images show that most zircons have a concentrically 2006; Liu et al., 2006; Ren et al., 2006; Zhou et al., 2006). oscillatory zoning core (Fig. 3), typical of magmatic origin. A However, the age range reported for the volcanic rocks from total of 18 analyses were performed on 18 zircon grains. inside the basin is much larger (Fig. 5), from approximately 206Pb/238U age is the common choice for rocks that are 260 to 305 Ma (Liu et al., 2006; Zhou et al., 2006). These re- younger than 800 Ma (Ireland and Gibson, 1998). In this study, sults provide a confusing scenario because most of the volcanic 16 data-points, both on the oscillatory zoning cores and on layers occur both along the margin and in the interior of the narrow nebulously zoned rims, are discordant and show similar basin. apparent 206Pb/238U ages ranging from 278.3 to 290.8 Ma (Ta- Zhou et al. (2006) dated the concentrations of major and ble 1 and Fig. 4). The spot 5 and spot 12 have much older trace elements for the Permian basaltic samples, from both the 206Pb-238U ages (321.4±5.4 and 308.8±7.9 Ma, 1σ), with high well cores inside the Turpan-Hami Basin and the margins of the common 206Pb percent (1.75% and 6.72%), low Pb content basin. All samples show similar major element compositions. (308 ppm and 252 ppm), and low Th content (112 ppm and 152 The low Mg# content (ranging from 0.36 to 0.58), as well

Zircon U-Pb SHRIMP Ages from the Late Paleozoic Turpan-Hami Basin, NW China 927

928 Xiang Mao, Jianghai Li and Huatian Zhang

Figure 3. Cathodoluminescence (CL) images of representative zircons from Sample T79. The ellipses on the analysed zircon grains show the positions of U-Pb analytical sites. as the low Cr, Co, and Ni content, show a non-initial magmatic For these reasons, considering the fact that the ages from property (Zhou et al., 2006). All the samples from basin inte- samples located inside the basin reported in earlier studies are riors and margins display similar REE pattern with E-MORB all 39Ar-40Ar ages (Fig. 5), the difference in ages between two (Fig. 6a), suggesting a partial melting origin, possibly from locations may be an artifact of the methodology. Therefore, the enriched mantle. The higher REE concentration than MORB new Zircon SHRIMP U-Pb age, 283.9±2.7 Ma, which is also in may be the result of lower extent of partial melting. However, the age range of the marginal volcanic rocks, provides an they show stronger HREE depletion compared with E-MORB. This can be illustrated by the existence of garnet in the mantle source, indicating a deep origin of magmas. To further constrain the tectonic setting, the geochemical data of the basalts from Zhou et al. (2006) were plotted on two kinds of discriminant diagrams, Zr/Y-Zr and Ti-Z-Y diagrams. Zr, Y, and Ti are immobile and incompatible elements in the evolution of magma, except for the affinity of Y in garnet and Ti in magnetite. On the Zr/Y-Zr plot (Fig. 6b1; Pearce and Norry, 1979), all the samples plot in the within-plate basalts field except one sample from Well Ya-1 which plots in the isl- and arc basalts field. Similarly, on the Ti-Zr-Y triangular plot (Fig. 6b2; Pearce and Cann, 1973), all of the samples also plot in the within-plate basalts field except the same sample from Well Ya 1. The depletion of Y compared with Zr and Ti (Fig. 6b) suggests that garnet exits as a stable phase and notably retains Y and HREE in the mantle source, resulting in high Ti/Y ratio

(Fig. 6b) and HREE depletion (Fig. 6a). The garnet-bearing mantle source, as well as HREE depletion, indicated a deep Figure 4. U-Pb concordia diagram showing SHRIMP ana- origin of the magmas. Deep melting and enriched mantle origin lytical data for zircons from the rhyolite (Sample T79, the characterize a intraplate setting, suggesting that during Permian, Yierxitu Formation) from Well Baocan 1, in the Turpan- the volcanic activity both inside the Turpan- Hami Basin and in Hami Basin (place see Fig. 1). Data-point error symbols are its margins had the same magma source and similar tectonic σ. environment (intraplate setting).

Figure 5. Age distribution of the late Paleozoic volcanic rocks in the Turpan-Hami Basin and its margins (except for the age of this study, ages from Li et al., 2006; Liu et al., 2006; Ren et al., 2006; Zhou et al., 2006).

Zircon U-Pb SHRIMP Ages from the Late Paleozoic Turpan-Hami Basin, NW China 929

Figure 6. Normalized patterns and tectonic setting discrimination diagrams for the basaltic samples from Turpan-Hami Basin. (a1) & (a2) Chondrite-normalized patterns and E-MORB-normalized trace-element patterns for basaltic samples from both the well cores and surrounding outcrop areas, Turpan-Hami Basin (normalizing values from Sun and McDonough, 1989); (b1) Zr/Y vs. Zr diagram (after Pearce and Norry, 1979); (b2) Ti/100-Zr-Y×3 diagram (after Pearce and Cann, 1973). Data from Zhou et al. (2006) and Li et al. (2011). accurate reference for rocks occurring inside the basin. REFERENCES CITED As the first Permian cover layer, the Yierxitu Formation is Allen, M. B., Windley, B. F., Zhang, C., et al., 1991. Basin characterized by the coexistence of bimodal volcanic rocks (Lu, Evolution within and Adjacent to the Tien Shan Range, 2007) and sedimentary rocks (mainly black mudstone and silty NW China. Journal of the Geological Society, London, mudstones). The basaltic samples of the bimodal volcanic rocks 148: 369–378 display intraplate geochemical characters, indicating a conti- Charvet, J., Shu, L. S., Laurent-Charvet, S., 2007. Paleozoic nental rifting environment. It is consistent with the shallow Structural and Geodynamic Evolution of Eastern Tianshan water sedimentary environment, as revealed by low Sr/Ba val- (NW China): Welding of the Tarim and Junggar Plates. ues of sedimentary rocks (Miao et al., 2005). As indicated by Episodes, 30(3): 162–186 the Harlike and Dananhu arc, Turpan-Hami Basin was under Chen, J. P., Qin, Y., Huffe, B. G., et al., 2001. Geochemical subducting setting in Early Carboniferous (Xiao et al., 2013, Evidence for Mudstone as the Possible Major Oil Source 2004; Charvet et al., 2007). Therefore, the unconformity be- Rock in the Jurassic Turpan Basin, Northwest China. Or- tween the Yierxitu Formation and the Carboniferous strata ganic Geochemistry, 32: 1103–1125 probably records the transform stage (i.e., collision) between Gao, J. H., Wang, X. L., Fu, G. B., et al., 2004. The Influence subduction in Early Carboniferous and post-collision rifting in of Relative Sea Level Changes to the Replacement of Early Permian. Our new age of 283.9±2.7 Ma reported in this Brachiopods Communities: A Case Study of Taoxigou study limits the latest time of the eastern part of North Carboniferous Section of the North Margin of Turpan- Tianshan-Junggar collision. Hami Basin. Geoscience, 18(3): 290–296 (in Chinese with English Abstract) ACKNOWLEDGMENTS Ge, X. H., Wang, X. K., Zan, S. Q., et al., 1997. On the The authors thank Prof. M. Santosh, Prof. Y. Q. Liu and Dr. Turpan-Hami Shear-Piggyback Type Basin. Geological G. B. Fu for their help. Thanks to all reviewers for their care- Review, 43(6): 561–568 (in Chinese with English Ab- fully and patiently review. This study was supported by the stract) Chinese MOST 973 Program (No. 2009CB219302). Geng, H. Y., Sun, M., Yuan, C., et al., 2011. Geochemical and

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