Late Permian tectonic evolution at the southeastern margin of the Songnen–Zhangguangcai Range Massif, NE China: Constraints from geochronology and geochemistry of granitoids

Gondwana Research 24 (2013) 635–647

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Late Permian tectonic evolution at the southeastern margin of the Songnen–Zhangguangcai Range Massif, NE China: Constraints from geochronology and geochemistry of granitoids Jiejiang Yu ⁎, Feng Wang, Wenliang Xu, Fuhong Gao, Jie Tang College of Earth Sciences, Jilin University, Changchun 130061, China

a r t i c l e

i n f o

Article history: Received 7 October 2012 Received in revised form 28 November 2012 Accepted 30 November 2012 Available online 18 January 2013 Handling Editor: G.C. Zhao Keywords: Songnen–Zhangguangcai Range Massif Late Permian Granitic magmatism Geochronology Central Asian Orogenic Belt

a b s t r a c t This paper reports the LA-ICP-MS U–Pb zircon dating and geochemical data for the Huangqigou, Xiaobeihu and Lalagou granitic plutons at the southeastern margin of the Songnen–Zhangguangcai Range Massif, which will not only place important constraints on the rock-forming ages, source characteristics and tectonic setting of these granitic plutons, but will also provide insights into understanding the tectonic evolution of the eastern segment of the Central Asian Orogenic Belt. Zircons from three plutons have distinct oscillatory zoning structures in their cathodoluminescene (CL) images, which, combined with the Th/U ratios of 0.28–1.06, indicate their magmatic origins. Zircon U–Pb dating results for these granitic plutons indicate that the granitic magmatism occurred mainly in the late Permian (256–252 Ma). The granites have SiO2 of 58.0–74.3%, Na2O of 2.74–3.76%, K2O of 2.75–3.95%, Na2O/K2O of 0.77–1.13, Mg# [100(Mg/(Mg+Fe2+)] of 21.8–39.9, and A/CNK of 0.88–1.08, with REE patterns characterized by LREE/HREE=7.75–12.82, (La/Yb)N =7.88–14.9 and δEu=0.56– 0.87. The trace element spider diagrams indicate that these granites are enriched in large ion lithosphile elements (Rb, Ba, Th, U, etc.) and relatively depleted in high field-strength elements (Ti, Nb, Ta), with Sr and Pb ranging from 205 to 350 ppm and from 2.02 to 3.60 ppm, respectively. The in-situ Hf isotope analysis reveals that εHf(t) values range from −2.22 to +11.65, and the two-stage Hf model ages (TDM2) range between 641 and 1274 Ma. These geochemical characteristics indicate that the late Permian granitic plutons at the SE margin of the Songnen– Zhangguangcai Range Massif can be assigned to metaluminous and weakly peraluminous high potassium calc-alkaline I-type granites with low-Sr and high-Yb features, and that the magmas to have formed these granites were originated from the partial melting of mafic igneous rocks in the lower crust. The source rocks are composed mainly of the juvenile crust with small contributions of ancient continental crust. Considering the existence of coeval mafic intrusive rocks and sedimentary basins, we propose that the Late Permian magmatism in the study area occurred in a post-collisional extensional setting following the collision of the Xingkai Block and the united Jiamusi and Songnen–Zhangguangcai Range Massifs. © 2013 International Association for Gondwana Research. Published by Elsevier B.V. All rights reserved.

1. Introduction As the largest accretionary orogenic belt in the world, the Central Asian Orogenic Belt (CAOB) has attracted extensive attention of the international geological community. In the last decade, researchers from different countries have carried out extensive and intensive investigations on this belt and produced a large amount of new data and competing interpretations (Dobretsov et al., 2003, 2006; Xiao et al., 2003, 2004, 2008, 2009, 2010a,b, 2011, 2013; Buslov et al., 2004; Klemd et al., 2005; Charvet et al., 2007, 2011; Windley et al., 2007; Gao et al., 2009; Han B.F. et al., 2010; Han C.M. et al., 2010; Kröner et al., 2010, 2012; Lehmann et al., 2010; Buslov, 2011; Han et al., 2011; Turkina et al., 2012; Xu et al., 2012; Tang et al., 2013). However, ⁎ Corresponding author at: College of Earth Sciences, Jilin University, No. 2199 Jianshe Street, Changchun, 130061, China. Tel.: +86 431 88502278; fax: +86 431 88584422. E-mail address: [email protected] (J. Yu).

most of these investigations are concentrated on the middle and western segments of the belt (Sun et al., 2008, 2009; Geng et al., 2009, 2011; Cai et al., 2010, 2011a,b, 2012a,b; Han B.F. et al., 2010; Han C.M. et al., 2010; Long et al., 2010; Wong et al., 2010; Yuan et al., 2010, 2011; Jiang et al., 2011a,b, 2012; Zhang et al., 2011), and few studies have been done on the eastern sector of the belt (e.g. Wu et al., 2007a; Li et al., 2009; Xu et al., 2009; Zhou et al., 2009, 2011; Meng et al., 2010, 2011; Wilde et al., 2010; Lei et al., 2011; Choulet et al., 2012; Long et al., 2012; Wang et al., 2012a,b; Yang G.X. et al., 2012; Yang W.B. et al., 2012), which has significantly hampered further understanding of the formation and evolution of the belt. The eastern sector of the Central Asian Orogenic Belt includes Northeast China and adjacent regions of the Russian Far East and is characterized by the collision of micro-continental blocks during the Phanerozoic time. Two major tectonic domains have been distinguished in Northeast China: the western and eastern domains (Figs. 1 and 2; Sengör et al., 1993; Li et al., 2009), of which the former includes the Erguna, Xing'an,

1342-937X/$ – see front matter © 2013 International Association for Gondwana Research. Published by Elsevier B.V. All rights reserved. http://dx.doi.org/10.1016/j.gr.2012.11.015

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Songnen–Zhangguangcai Range, Jiamusi, and Khanka massifs, which together form part of the Central Asian Orogenic Belt (CAOB), marking the broad collision zone between the North China and Siberian cratons. The domain is dominated by mélanges, syn-collisional granitoids and post-orogenic A-type granites of Paleozoic age (Sengör and Natal'in, 1996; Wu et al., 2002). The eastern domain, which includes the Nadanhada and Sikhote-Alin terranes of the Russian Far East (Fig. 2a), is considered to be part of the Pacific margin, and characterized by Late Jurassic to Early Cretaceous subduction complexes, large-scale NE-trending granites, volcanic rock belts, and wrench fault systems (Xu et al., 1987; Faure and Natal'in, 1992; Faure et al., 1995; Maruyama et al., 1997). Intervening between the western and eastern domains is the composite Jiamusi–Khanka–Bureya Block, whose tectonic affinity still remains unknown or controversial (Zhou et al., 2009, 2010a,b,c). Northeast China contains voluminous granitic rocks, forming the Xiaoxing'anling–Zhangguangcailing granite belt, which is located in the Songnen–Zhangguangcai Range Massif and constitutes the major body of the voluminous granitic rocks in Northeast China (Wilde et al., 2010; Wu et al., 2011). The granitic rocks in this belt were traditionally considered to be the products of the Hercynian (or Variscan) orogeny (Huang, 1945; Huang et al., 1977; JBGMR, 1988; HBGMR, 1993). However, recent age data obtained by microanalysis dating techniques (SHRIMP and LA-ICP-MS) have revealed that most of these granitic rocks were emplaced during late Triassic–Jurassic and Cretaceous times, and only a small amount of granitic rocks formed during Caledonian and Hercynian times (Li et al., 1999; Sun et al., 2000, 2001, 2004a,b, 2005; Wu et al., 2002, 2003, 2011; Liu S. et al., 2010; Wang et al., 2012a). The granitic rocks in this area mainly occur as large batholiths, in which different rock associations and rock types are exposed. It still remains unknown whether these granites resulted from a single magmatic event or from multiphase magmatism. In the last few years, although

extensive investigations have been carried out on these granites (e.g. Wu et al., 2002, 2003, 2011; Sun et al., 2004a,b, 2005), there are many unresolved issues related to the timing and tectonic nature of these granites, including those of whether there are any Hercynian granites at the SE margin of the Songnen–Zhangguangcai Range Massif and if any, what are their spatial distribution, rock associations and tectonic settings. These issues form the justification for this study, in which we carried out detailed LA-ICP-MS U–Pb zircon dating, zircon Hf isotopic study and geochemical analysis on the Late Permian granitic rocks at the SE margin of the Songnen–Zhangguangcai Range Massif. The results will not only provide important insights into understanding the petrogenesis and tectonic nature of these granites, but will also place rigorous constraints on the tectonic evolution of the eastern segment of the Central Asian Orogenic Belt. 2. Geological background and sample descriptions Located to the east of the Song Liao Basin, the study area is part of the Songnen–Zhangguangcai Range Massif in the eastern sector of the Central Asian Orogenic Belt (Fig. 1; Wu et al., 2011; Zhou et al., 2011). The S–N extending Mudanjiang Fault lies in the east of the study area, separating the area from the Jiamusi Block (Fig. 1). The oldest Precambrian strata in the study are named the Neoproterozoic Zhangguangcai Range Group, which, together with a small amount of Neoproterozoic strata (the Dongfengshan Group) exposed in the Tangyuan and Yichun areas in the north, constitutes the crystalline basement of the Songnen– Zhangguangcai Range Massif (HBGMR, 1993; Zhou et al., 2009, 2011; Meng et al., 2010, 2011; Wilde et al., 2010; Wu et al., 2011; Wang et al., 2012a,b; Gao et al., in press). In addition, Paleozoic to Cenozoic terrigenous clastic rocks, carbonatites and pyroclastic rocks are sporadically distributed in the study area (JBGMR, 1988; HBGMR, 1993; Meng et al., 2010, 2011; Wang et al., 2012a,b). However, the sedimentary strata

Fig. 1. A sketch map of NE China, modified after Wu et al. (2007a). The inset shows the tectonic outlines of NE China. A and M represent the Altaids and Manchrides, respectively, of Sengör and Natal'in (1996). (I) Hegenshan–Heihe suture zone, (II) Mongolia–Okhotsk suture zone, (III) Solonker–Xar Moron–Changchun suture zone, and (IV) Middle Sikhote suture zone. ①: Xiguitu–Tayuan Fault; ②: Hegenshan–Heihe Fault; ③: Solonker–Xar Moron–Changchun suture; ④: Jiayin–Mudanjiang Fault; ⑤: Yitong–Yilan Fault; and ⑥: Dunhua–Mishan Fault. The location of Fig. 2a is outlined by a rectangle.

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Fig. 2. (a) Distribution of the Late Permian granitic rocks in the study area and adjacent areas; (b) generalized geological map of the Huangqigou pluton (based on the data from HBGMR, 1993); (c) generalized geological map of the Xiaobeihu pluton; and (d) generalized geological map of the Lalagou pluton.

in the study area are in volume much less compared with the granitic rocks that were emplaced in different stages. The granitic plutons exposed in this area and adjacent areas were previously attributed to the composite products of the Pre-Paleozoic, Early Paleozoic, Late Paleozoic and Mesozoic magmatic events based on their field contact relationship, lithological correlations and limited chronological data (JBGMR, 1988; HBGMR, 1993). The Huangqigou, Xiaobeihu and Lalagou granitic plutons, on which are focused by this contribution, are located at the SE margin of the Songnen–Zhangguangcai Range Massif (Fig. 2a). Previously regarded as a Neoproterozoic pluton (HBGMR, 1993), the Huangqigou granitic pluton is located in the northwest of Ning'an, extending along an irregular NE belt (Fig. 2b). It is intruded by an Early Yanshanian granite in the northwest, covered by the Cenozoic sediments in the east, and unconformably overlain by the lower Cretaceous Hailang Group in the north and south. The granitic pluton is dominated by porphyritic quartz diorite and porphyritic granodiorite enclosing minor fine-grained dioritic enclaves, whose long axis is always parallel to the direction of regional gneissosity. A representative sample (11HNA1-1) for this pluton collected from a roadside (44°23′01.9″N, 129°26′19.1″E) 5 km west of Ning'an City is porphyritic biotite–amphibole quartz diorite (Fig. 3a, b). The quartz diorite displays a porphyritic texture with alkali feldspars as phenocrysts, which are

commonly subeuhedral tabular microcline crystals, with a maximum length up to 6 cm. These often contain inclusions of hornblende, biotite and opaque minerals. The groundmass is composed predominantly of plagioclase (50%), hornblende (15–20%), biotite (10–15%) and quartz (10%), and accessory minerals are sphene, apatite and zircon. Biotite and amphibole in the rock are often distributed on parallel planes, constituting a gneissose structure. Also previously considered as a Neoproterozoic pluton (HBGMR, 1993), the Xiaobeihu granitic pluton is located in an area around Shanlanzhan Town, occurring as an irregular stock. It is composed mainly of monzogranite, with fine-grained dioritic enclaves (Fig. 2c). The pluton is in intrusive contact with the Yanshanian and Hercynian granites in the north and northwest, respectively, and encloses some Paleozoic strata that are dispersed as xenoliths in the pluton. The pluton is overlain by Cenozoic (Quaternary) sediments on its west and south sides. Sample 11HNA4-1 collected from a roadside west of Xiaobeihu (44°06′16.1″N; 128°43′18.9″E) is biotite–hornblende monzogranite, with an inequigranular subhedral texture and a weak gneissose structure (Fig. 3c, d). The major minerals are plagioclase (35%), alkali feldspar (30%) and quartz (27–28%), with some biotite (5%) and a small amount of hornblende (2–3%), and the accessory minerals are magnetite, apatite, zircon and allanite. Observed under microscope, plagioclase displays clear

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Fig. 3. (a) Photomicrographs of Late Permian porphyritic biotite-amphibole quartz diorite (Sample 11HNA1-1) under plane-polarized light; (b) porphyritic biotite-amphibole quartz diorite (Sample 11HNA1-1) under cross-polarized light; (c) biotite- and hornblende-bearing monzogranite (Sample 11HNA4-1) under plane-polarized light; (d) biotite- and hornblende-bearing monzogranite (Sample 11HNA4-1) under cross-polarized light; (e) hornblende- and biotite-bearing granodiorite (Sample 11HNA11-1) under plane-polarized light; and (f) hornblende- and biotite-bearing granodiorite (Sample 11HNA11-1) under cross-polarized light.

zoning, alkali feldspar comprises microcline and perthite, and biotite flakes show a preferred orientation that forms a weak gneissose structure. The Lalagou pluton is located near Lalagou Village in Yanminghu Town, Dunhua City, Jilin Province, occurring as a nearly N–S extending irregular stock and consisting mostly of granodiorite (Fig. 2d). The pluton is in intrusive contact with the Tadong monzogranite and the Zhudongdian granodiorite on the eastern and western sides, respectively. It was previously assigned to the second phase of the Late Hercynian batholith, which is part of the Super-large Hercynian Granite Belt in Jilin Province (JBGMR, 1988). Sample 11HNA11-1, collected from the southwest of Lalagou Village (43°49′39.2″N; 128°33′15.9″ E), is hornblende-biotite granodiorite (Fig. 3e, f), with a mediumfine grained subhedral texture and a massive structure. The major minerals are: plagioclase, with zoning (40–45%), alkali feldspar (microcline and perthite, 20–25%), quartz (20–25%), biotite (4%), and a small amount of hornblende (1%); accessory minerals are magnetite, apatite, zircon and allanite.

3. Analytical methods 3.1. U–Pb zircon geochronology and Hf-isotope analysis Each sample for zircon separation weighs about 20 kg. On the basis of field investigations and petrographic examination, zircons were separated from rock samples using magnetic and heavy liquid separation techniques after crushing, screening, washing and drying. Then, they were mounted on adhesive tapes, enclosed in epoxy resin, polished and photographed in reflected and transmitted light. The internal structure of zircons was examined using the cathodoluminescence (CL) image technique at Institute of Geology and Geophysics, China Academy of Sciences. The laser ablation ICP-MS (LA-ICP-MS) U–Pb zircon analyses were carried out at the State Key Laboratory of Geological Process and Mineral Resources (GPMR), China University of Geosciences, Wuhan. Laser sampling was performed using a GeoLas 2005. An Agilent 7500a ICP-MS instrument was used to acquire ion-signal intensities.

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Helium was applied as a carrier gas. Argon was used as the make-up gas and mixed with the carrier gas via a T-connector before entering the ICP. Nitrogen was added into the central gas flow (Ar+He) of the Ar plasma to decrease the detection limit and improve precision (Hu et al., 2008). In the processes of zircon U–Pb dating analysis, synthetic silicate glass standard reference materials NIST SRM610 developed by the U.S. National Institute of Standards and Technology were used to do the instrument optimization. Zircon 91500 was used as external standard for U–Pb dating. All analyses were carried out with a beam diameter of 32 μm, offline selection and integration of background and analytical signals, and time-drift correction and quantitative calibration for trace element analyses and U–Pb dating were performed by ICPMSDataCal (version 7.7; Liu et al., 2008, 2010a,b). Common Pb was corrected after Anderson (2002) and calculated with the Isoplot program (version 3.0) (Ludwig, 2003). Detailed operating conditions for the laser ablation system and the ICP-MS instrument and data reduction are the same as the descriptions of Liu et al. (2008, 2010a,b). Uncertainties given for individual analyses (ratios and ages) are at the level of 1σ. The Neptune Plus MC-ICP-MS was used in the Lu–Hf isotopes analyses. 176Hf/177Hf value of Zircon 91500 used in the tests is 0.282308±12 (2σ). Detailed analytical produces are the same as described by Yuan et al. (2008). 3.2. Major element and trace element analyses Major element data were collected by using X-ray fluorescence (XRF) at the Institute of Geochemistry, Chinese Academy of Sciences, Guiyang. Trace element analyses were conducted by ICP-MS at the State Key Laboratory of Geological Processes and Mineral Resources, China University of Geosciences, Wuhan. The international standard BCR-2 (basalt), BHVO-1 (basalt) and AGV-1 (andesite) analysis results indicate that the precision and accuracy of the major element are better than 5%, and those of the trace element are better than 10% (Rudnick et al., 2004). 4. Results and interpretations 4.1. LA-ICP-MS zircon U–Pb dating results Zircon LA-ICP-MS U–Pb data of three samples are listed in Table 1, and cathodoluminescence (CL) images of some zircons and Concordia plots of LA-ICP-MS U–Pb dating results are described in Fig. 4. Sample 11HNA1-1 collected from the Huangqigou pluton is porphyritic biotite- and amphibole-bearing quartz diorite. Most zircons from this sample are euhedral or subhedral and have obvious oscillatory zoning (Fig. 4), with Th/U ratios ranging from 0.28 to 0.66, indicating their magmatic origin (Pupin, 1980; Koschek, 1993). Eighteen zircons have been successfully extracted for LA-ICP-MS U–Pb dating analysis, and fifteen of them give a range of 206Pb/ 238U ages scattering between 254±3 Ma and 263±3 Ma, defining a weighted average age of 256±1 Ma (NSWD=0.52, n=15; Fig. 4a), which is interpreted as the formation age of the rock. Other two analysis points yielded a weighted average age of 308±4 Ma (NSWD=0.56, n=2), and one analysis point gives a 206Pb/238U age of 290±4 Ma. These two (308 Ma and 290 Ma) are interpreted as the age of the xenocrystic zircons during the magma ascent, which is consistent with ages of Late Carboniferous– Early Permian granites (Wu et al., 2011) and Early Permian volcanic rocks (Meng et al., 2011) in the study area. Sample 11HNA4-1 is amphibole and biotite-bearing monzogranite, collected from the Xiaobeihu pluton. Most zircons from this sample are subhedral and have obvious oscillatory zoning (Fig. 4), with Th/U ratios of 0.29–0.91, which suggest that these zircons should be of magmaticorigin. Twelve zircons have been successfully extracted for LA-ICP-MS U–Pb dating analysis, and eleven of them give a range of 206Pb/238U ages scattering between 252±4 Ma and 257±3 Ma, defining a weighted average age of 255±2 Ma (NSWD=0.14, n =11; Fig. 4b), which is interpreted as the crystallization age of the rock. Another analysis point

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gives a 206Pb/238U age of 485±17 Ma, which can be interpreted as the age of a xenocrystic zircon captured during the magma ascent. It is coincident with the ages of Early Paleozoic granites (Wu et al., 2011; Wang et al., 2012a) in the research area. Sample 11HNA11-1, is amphibole and biotite-bearing granodiorite, collected from the Lalagou pluton. Most zircons from this sample are subhedral and have obvious oscillatory zoning (Fig. 4c), indicating their magmatic origin, which is also consistent with their high Th/U ratios ranging from 0.39 to 1.06. Eighteen analytical points give a range of 206Pb/ 238U ages ranging from 245 ± 5 Ma to 257 ± 5 Ma, defining a weighted mean age of 252 ± 2 Ma (NSWD = 0.44, n = 18; Fig. 4c), which can be interpreted as the emplacement age of the rock. 4.2. Geochemistry 4.2.1. Major elements As shown in Table 2, the Xiaobeihu and Lalagou plutons are enriched in SiO2 and depleted in Al2O3, FeOT (total FeO), MgO and CaO, with Mg # [= Mg 2+ / (Mg 2+ + Fe 2+)] values ranging between 21.8 and 39.6. They have relatively high SiO2 (68.7%–74.3%), Na2O (3.17%–3.76%) and K2O (3.32%–3.95%) contents, with Na2O/K2O ratios of 0.86–1.04. In the TAS diagram, the Xiaobeihu and Lalagou granitic plutons plot in the sub-alkaline granite area (Fig. 5). Compared with the Xiaobeihu and Lalagou plutons, the Huangqigou granite is relatively lower in SiO2 (58.0%–60.0%), Na2O (2.74%–3.36%) and K2O (2.75%–3.81%), but relatively higher and narrow in Mg # values (37.6–39.9). In the TAS diagram, the Huangqigou granite plots in the diorite field or close to the monzonite field (Fig. 5), belonging to the sub-alkaline–alkaline transitional series. Taken together, all samples from the three plutons are metaluminum-peraluminous with a narrow range of A/CNK ratio (A/CNK= 0.88–1.08) (Fig. 6a), and belong to high-K calc-alkaline series in the K2O vs. SiO2 diagram (Fig. 6b). Considering the fact that the three plutons are dominated by quartz diorite, granodiorite and monzogranite with little or no presence of Al-rich minerals, we conclude that the Xiaobeihu, Lalagou and Huangqigou plutons are metaluminous and weakly peraluminous high-K calc-alkaline I-type granites, similar to other late Permian granites at the SW margin of the Jiamusi Massif and the SE margin of the Songnen–Zhangguangcai Range Massif (Li et al., 1999; Wu et al., 2001; Huang et al., 2008; Liu S. et al., 2010). 4.2.2. Trace elements All the granitic rock samples show similar REE patterns that are enriched in LREE and depleted in HREE, with a moderate-minor negative Eu anomaly (Fig. 7a). They have a total REE abundance ranging from 121 to 228 ppm, LREE/HREE ratios between 7.75 and 12.82, (La/Yb)N value of 7.88–14.9, and δEu of 0.56–0.87 (Table 2). Compared with the Huangqigou (∑ REE = 159–191 ppm) and Lalagou (∑REE= 121–1567 ppm) plutons, the Xiaobeihu pluton has a higher total REE abundance (214–228 ppm). In the primitive mantlenormalized trace element spidergram, the granitic rock samples show LILEs (e.g. Rb, Ba, Th, U, K) enrichments, negative HFSEs (e.g. Nb, Ta, Ti, P) and Sr anomalies (Fig. 7b). The Sr and Yb contents of all these samples range from 205 to 350 ppm and from 2.02 to 3.60 ppm, respectively, suggesting that these granitic rocks belong to low Sr (b 400 ppm) and high Yb (>2 ppm) types (Zhang et al., 2006). 4.3. Zircon Hf isotope The Xiaobeihu and Lalagou plutons are different from the Huangqigou pluton in their zircon Hf isotopic composition. The former have 176Hf/177Hf ratios ranging from 0.282728 to 0.282961 (Table 3), εHf(t) values from +3.79 to +11.65, and two-stage Hf model ages ranging from 641 to 942 Ma. These features are similar to those of the Phanerozoic igneous rocks in the eastern segment of the Central Asia Orogenic Belt (Fig. 8), but distinctly different from those of Phanerozoic

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Table 1 LA-ICP-MS dating results of zircons from the Late Permian granitoids. Sample and spot no.

11HNA1-1-01 11HNA1-1-02 11HNA1-1-03 11HNA1-1-04 11HNA1-1-05 11HNA1-1-06 11HNA1-1-07 11HNA1-1-08 11HNA1-1-09 11HNA1-1-10 11HNA1-1-11 11HNA1-1-12 11HNA1-1-13 11HNA1-1-14 11HNA1-1-15 11HNA1-1-16 11HNA1-1-17 11HNA1-1-18 11HNA4-1-01 11HNA4-1-02 11HNA4-1-03 11HNA4-1-04 11HNA4-1-05 11HNA4-1-06 11HNA4-1-07 11HNA4-1-08 11HNA4-1-09 11HNA4-1-10 11HNA4-1-11 11HNA4-1-12 11HNA11-1-01 11HNA11-1-02 11HNA11-1-03 11HNA11-1-04 11HNA11-1-05 11HNA11-1-06 11HNA11-1-07 11HNA11-1-08 11HNA11-1-09 11HNA11-1-10 11HNA11-1-11 11HNA11-1-12 11HNA11-1-13 11HNA11-1-14 11HNA11-1-15 11HNA11-1-16 11HNA11-1-17 11HNA11-1-18

Th (ppm)

U (ppm)

Th/U

207 277 324 285 191 157 373 302 273 203 476 471 162 358 410 168 200 195 700 136 296 110 163 154 328 323 664 647 182 284 60.0 121 52.3 165 85.9 56.5 67.1 58.5 243 60.8 41.8 40.2 61.4 68.4 59.3 65.3 51.7 50.6

632 787 759 692 534 446 1008 884 738 723 1100 716 551 977 1069 555 632 588 1147 310 450 362 299 530 627 480 728 1304 464 492 107 161 85.8 196 221 89.9 117 98.0 229 104 69.2 75.2 107 124 104 109 93.9 79.3

0.33 0.35 0.43 0.41 0.36 0.35 0.37 0.34 0.37 0.28 0.43 0.66 0.29 0.37 0.38 0.30 0.32 0.33 0.61 0.44 0.66 0.30 0.54 0.29 0.52 0.67 0.91 0.50 0.39 0.58 0.56 0.75 0.61 0.84 0.39 0.63 0.57 0.60 1.06 0.58 0.60 0.54 0.57 0.55 0.57 0.60 0.55 0.64

Isotopic ratios 207

Pb/206Pb

U–Pb age (Ma) 207

Pb/235U

206

Pb/238U

207

Pb/206Pb

207

Pb/235U

206

Pb/238U

Ratio

1σ

Ratio

1σ

Ratio

1σ

Age

1σ

Age

1σ

Age

1σ

0.05213 0.05211 0.05426 0.05289 0.05153 0.05164 0.05242 0.05428 0.05147 0.05232 0.05451 0.05131 0.05138 0.05306 0.05222 0.05161 0.05459 0.05480 0.05364 0.05710 0.05518 0.05443 0.04877 0.05182 0.05844 0.05671 0.05249 0.04998 0.05274 0.04605 0.06051 0.05314 0.05072 0.05209 0.05564 0.06085 0.05607 0.05264 0.05093 0.05298 0.05736 0.06579 0.05479 0.05415 0.05131 0.05348 0.05330 0.05939

0.00225 0.00159 0.00180 0.00175 0.00178 0.00195 0.00197 0.00286 0.00173 0.00228 0.00181 0.00170 0.00210 0.00158 0.00145 0.00176 0.00210 0.00286 0.00158 0.00266 0.00183 0.00168 0.00259 0.00206 0.00229 0.00225 0.00310 0.00155 0.00248 0.00333 0.00441 0.00309 0.00781 0.00319 0.00738 0.00361 0.00252 0.00382 0.00209 0.00312 0.00559 0.00399 0.00296 0.00308 0.00313 0.00290 0.00315 0.00492

0.28944 0.29234 0.30316 0.35820 0.34863 0.32912 0.30184 0.30563 0.28598 0.29085 0.30441 0.28595 0.28618 0.29635 0.29252 0.28787 0.30495 0.30663 0.29774 0.32158 0.30888 0.61229 0.27053 0.28495 0.32807 0.31773 0.29611 0.28069 0.29635 0.25300 0.33259 0.28963 0.27089 0.28210 0.29995 0.32357 0.30789 0.28479 0.27839 0.28841 0.31616 0.35038 0.29544 0.29340 0.28193 0.29482 0.28526 0.32282

0.01208 0.00869 0.00960 0.01129 0.01128 0.01173 0.01086 0.01565 0.00936 0.01219 0.00936 0.00945 0.01167 0.00932 0.00836 0.00954 0.01182 0.01528 0.00804 0.01630 0.01044 0.03183 0.01424 0.01085 0.01287 0.01225 0.01738 0.00776 0.01418 0.01779 0.02405 0.01691 0.04130 0.01729 0.03939 0.01851 0.01372 0.01961 0.01111 0.01753 0.03014 0.02007 0.01471 0.01667 0.01715 0.01655 0.01642 0.02611

0.04027 0.04050 0.04037 0.04884 0.04892 0.04605 0.04158 0.04084 0.04020 0.04032 0.04048 0.04050 0.04044 0.04036 0.04050 0.04044 0.04043 0.04061 0.04033 0.04039 0.04038 0.07808 0.04044 0.04060 0.04038 0.04048 0.04060 0.04063 0.04034 0.03985 0.04015 0.03984 0.03874 0.03930 0.03910 0.03938 0.03983 0.04016 0.04003 0.04016 0.03998 0.03992 0.03978 0.03965 0.04003 0.04015 0.03963 0.04066

0.00044 0.00039 0.00039 0.00051 0.00056 0.00064 0.00053 0.00050 0.00041 0.00047 0.00049 0.00052 0.00061 0.00048 0.00051 0.00043 0.00035 0.00056 0.00051 0.00065 0.00045 0.00290 0.00065 0.00075 0.00045 0.00042 0.00047 0.00062 0.00054 0.00066 0.00077 0.00069 0.00084 0.00056 0.00075 0.00061 0.00052 0.00069 0.00048 0.00063 0.00080 0.00082 0.00063 0.00056 0.00064 0.00060 0.00071 0.00082

291 290 382 324 264 270 304 383 262 299 392 255 258 331 295 268 396 404 356 495 420 389 137 277 546 480 307 194 318

101 50 54 53 53 56 58 122 56 102 47 52 66 50 42 57 71 87 38 83 55 57 90 54 66 67 114 37 84 160 123 101 311 114 299 97 76 126 70 110 222 85 83 103 110 100 98 141

258 260 269 311 304 289 268 271 255 259 270 255 256 264 261 257 270 272 265 283 273 485 243 255 288 280 263 251 264 229 292 258 243 252 266 285 273 254 249 257 279 305 263 261 252 262 255 284

10 7 7 8 8 9 8 12 7 10 7 7 9 7 7 8 9 12 6 13 8 20 11 9 10 9 14 6 11 14 18 13 33 14 31 14 11 15 9 14 23 15 12 13 14 13 13 20

254 256 255 307 308 290 263 258 254 255 256 256 256 255 256 256 256 257 255 255 255 485 256 257 255 256 257 257 255 252 254 252 245 248 247 249 252 254 253 254 253 252 251 251 253 254 251 257

3 2 2 3 3 4 3 3 3 3 3 3 4 3 3 3 2 3 3 4 3 17 4 5 3 3 3 4 3 4 5 4 5 3 5 4 3 4 3 4 5 5 4 3 4 4 4 5

igneous rocks in the North China Craton (Yang et al., 2006). In contrast, the Huangqigou pluton has relatively lower 76Hf/ 177Hf ratios (0.282728–0.282961) and εHf(t) values (from −2.22 to −0.25), and higher two-stage Hf model ages ranging from 1165 to 1274 Ma. These features are similar to the zircon Hf isotope compositions and two-stage Hf model ages of igneous rocks in both the Xingmeng Orogenic Belt (i.e., eastern segment of the Central Asia Orogenic Belt) and the North China Craton as shown in the εHf(t)–t diagram (Fig. 8). 5. Discussion 5.1. Recognition of Late Permian granites on the southeastern margin of the Songnen–Zhangguangcai Range Massif The granitic rocks in the Songnen–Zhangguangcai Range Massif were traditionally considered to have formed during Caledonian and Hercynian times (Huang, 1945; Huang et al., 1977; JBGMR, 1988; HBGMR, 1993), but this was not confirmed by any reliable isotopic age data. In the last two decades, geochronological investigations

622 335 228 289 438 634 455 313 238 328 505 800 404 377 255 349 342 581

have been carried out on most granitic rocks in this massif, and the results show that most granitic rocks in the massif were emplaced in the Early Mesozoic (Li and Zhao, 1991, 1992; Xu et al., 1994; Wu et al., 1998, 2000a, 2002, 2003, 2011; Li et al., 1999; Sun et al., 2001, 2004a, 2005). However, it still remains unknown whether or not there are Caledonian- and/or Hercynian granites in this massif. The most possible candidates of granitic plutons with such age are the Huangqigou and Xiaobeihu plutons, which were previously considered to have formed in the Neoproterozoic, and together with the Chushan, Huling and other plutons in the north, they form a Proterozoic granite belt, called the Proterozoic Jiayin–Mudanjiang granite belt (HBGMR, 1993). Such a conclusion was mainly established on a few Rb–Sr whole-rock isochron ages and the observation that these granitic plutons intrude the Zhangguangcailing group that was considered to be of Neoproterozoic age. However, as the massif experienced reworking of a multiple phase of tectonothermal events, the available Rb–Sr whole-rock isochron ages are not reliable. More importantly, recent data indicate that the Zhangguangcailing group was not made up of Neoproterozoic strata, but formed in the Paleozoic and Lower Mesozoic

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ages of 300–200 Ma (JBGMR, 1988). However, these K–Ar ages may not represent the crystallization age of the pluton as it underwent tectonothermal events after it was emplaced. Also, it still remains controversial whether or not the granitic pebbles in the basal conglomerates of the Lower Triassic Lujiatun Group were really derived from the Lalagou granite. For these reasons, the age of the Lalagou granitic pluton has not been well determined. In this study, we used the LA-ICP-MS zircon dating technique to precisely determine the ages of the Huangqigou, Xiaobeihu and Lalagou plutons. Zircon crystals from these plutons are euhedral to subhedral in shape, display distinctly oscillatory zoning, and possess high Th/U ratios, all of which are consistent with their magmatic origin. Therefore, the zircon U–Pb ages of 256 Ma, 255 Ma and 252 Ma yielded from the Huangqigou, Xiaobeihu and Lalagou plutons, respectively, should be interpreted as their magmatic crystallization ages. These ages demonstrate that the Huangqigou, Xiaobeihu and Lalagou plutons were emplaced during the Late Permian time, which confirms the existence of the Hercynian-aged magmatism at the SE margin of the Songnen– Zhangguangcai Range Massif. Most recently, other types of Middle Permian magmatic rocks have also been found in the study area, including the 263–262 Ma Shimengzi dolerite and gabbros (Liu S. et al., 2010), 264–262 Ma Yumuchuan diabase (Feng et al., 2010), and ~263 Ma Wangbaozhen gabbros (Wang et al., in press). These Middle Permian mafic intrusive rocks have similar ages to the Late Permian granitoids within age uncertainty. Moreover, Late Permian granites were also recognized at the southwestern margin of Jiamusi Massif, including the ~ 256 Ma Chushan pluton (Li et al., 1999; Wu et al., 2001), the 254–250 Ma Chaihe pluton (Li et al., 1999; Wu et al., 2001), the 258–254 Ma Gangzigou pluton (Li et al., 1999), and the ~ 259 Ma Meizuo pluton (Huang et al., 2008). Taken together, the new data presented in this study combined with previous data clearly indicate the existence of large-scale Late Permian magmatism in the eastern part of Northeast China, especially at southern margin of the Songnen– Zhangguangcai Rang Massif. 5.2. Nature of the magma source

Fig. 4. Concordia plots of LA-ICP-MS U–Pb zircon analytical results for the (a) Huangqigou, (b) Xiaobeihu and (c) Lalagou granitic plutons. The insets are representative cathodoluminescene (CL) zircon images where all scale bars are 100 μm.

(Wang et al., 2012a,b). Thus, these old data and geological observations cannot provide any constraints on the ages of the Huangqigou and Xiaobeihu plutons. The Lalagou pluton was previously interpreted as a Late Hercynian-aged granitic pluton, being part of the Super-large Hercynian Granite Belt in Jilin Province (JBGMR, 1988). This conclusion was based on the facts that (1) some granitic pebbles in the basal conglomerates of the Lower Triassic Lujiatun Group display the same composition as that of the Lalagou granite and (2) it yielded the K–Ar

Geochemical data and zircon Hf isotopes of the Late Permian granitic rocks at the southeastern margin of the Songnen–Zhangguangcai Range Massif can be used to trace the nature of the source. Geochemically, the Huangqigou, Xiaobeihu and Lalagou granitic plutons are characterized by enrichment in SiO2 and K2O and depletion in MgO, FeO, CaO and transition elements (Sc, Ti, V, Cr, etc.), suggesting that the primitive magma to have formed these granitic rocks was originated from the partial melting of the crust. In addition, the Late Permian granitic rocks in the study area and adjacent areas belong to metaluminous and weakly peraluminous, high potassium calc-alkaline I type granites, implying the magma source were most likely mafic rocks (Li et al., 1999; Wu et al., 2001; Huang et al., 2008; Liu S. et al., 2010). On the other hand, the composition of the trace elements suggests that these granitic rocks can be classified as low-Sr and high-Yb type granites, implying that the primitive magma to form these granitic rocks was most likely derived from a garnet-free source which is dominated by amphibole and plagioclase (Zhang et al., 2005, 2006). This is consistent with characteristics of rare earth elements, such as moderate enriched right slope REE patterns, weak heavy REE fractionation and high abundance of heavy REE and moderate-weak negative Eu anomalies (Fig. 7a). Further constraints on the nature of the magma source come from the zircon Hf isotope data of these granitic rocks. For example, zircon εHf(t) values of the Xiaobeihu and Lalagou pluton are positive (ranging from +3.79 to +9.10), implying that the primitive magma was derived from a juvenile crust, similar to the magma sources of many other Phanerozoic granites in the Central Asian Orogenic Belt (Wu et al., 1999, 2000b, 2003, 2007b; Jahn et al., 2000; Jahn, 2002, 2004; Yang et al., 2006; Sui et al., 2007; Zhang et al., 2010). Available zircon two-stage model ages indicate that such a juvenile crust was accreted mainly in the Neoproterozoic. However,

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Table 2 Analytical results of major (wt.%) and trace elements (ppm) for the Late Permian granitoids. Sample

11HNA1-1

11HNA1-2

11HNA1-3

11HNA1-4

11HNA4-1

11HNA4-2

11HNA4-3

11HNA11-1

11HNA11-2

11HNA11-3

11HNA11-4

11HNA11-5

SiO2 TiO2 Al2O3 TFe2O3 MnO MgO CaO Na2O K2O P2O5 LOI Total Mg# Na2O/K2O A/CNK Sc V Cr Co Ni Ga Rb Sr Y Zr Nb Ba Hf Ta Th U La Ce Pr Nd Sm Eu Gd Tb Dy Ho Er Tm Yb Lu δEu LREE HREE LREE/HREE ∑REE (La/Yb)N

59.2 0.68 16.6 7.40 0.12 2.46 5.92 3.10 2.75 0.18 1.15 99.5 39.9 1.13 0.88 13.9 75.4 12.2 14.8 3.29 20.4 140 345 35.6 300 12.8 733 7.22 0.76 14.5 2.50 41.3 78.3 9.06 33.1 6.23 1.22 5.87 0.94 5.78 1.23 3.41 0.52 3.60 0.49 0.61 169 21.8 7.75 191 8.23

60.0 0.60 17.0 6.43 0.11 1.97 4.74 3.00 3.81 0.17 0.74 98.5 38.0 0.79 0.96 12.0 66.1 9.74 13.1 2.99 19.3 134 350 30.0 264 11.3 1338 6.4 0.67 9.44 2.10 33.5 65.0 7.74 28.1 5.25 1.28 4.78 0.78 4.69 0.95 2.89 0.41 3.05 0.44 0.77 141 18.0 7.83 159 7.88

59.9 0.56 17.5 5.93 0.10 1.79 4.89 3.36 3.32 0.15 1.22 98.7 37.6 1.01 0.97 11.4 61.9 10.0 12.6 2.88 20.2 132 411 28.0 249 10.4 979 5.83 0.61 11.4 2.16 35.7 65.1 7.52 26.9 5.05 1.26 4.68 0.76 4.53 0.90 2.79 0.42 2.85 0.39 0.78 142 17.3 8.17 159 8.99

58.0 0.79 16.3 8.21 0.13 2.54 5.04 2.74 3.57 0.20 0.98 98.6 38.2 0.77 0.93 14.2 84.3 12.9 16.8 3.8 20.2 144 314 34.0 310 13.8 1213 7.35 0.79 10.7 2.57 40.8 75.4 8.88 32.5 6.07 1.26 5.48 0.89 5.28 1.10 3.29 0.52 3.52 0.48 0.66 165 20.6 8.02 185 8.31

74.3 0.30 12.5 2.71 0.06 0.39 1.58 3.17 3.32 0.08 0.55 99.0 22.3 0.95 1.07 8.82 17.7 2.67 2.53 1.36 17.2 101 205 33.2 280 11.0 888 6.85 0.68 14.5 1.97 43.8 96.6 9.94 35.9 6.63 1.16 5.80 0.93 5.20 1.04 2.99 0.47 3.09 0.44 0.56 194 20.0 9.72 214 10.2

73.3 0.29 13.2 2.65 0.06 0.37 1.61 3.38 3.53 0.08 0.54 99.0 21.8 0.96 1.07 8.47 16.3 2.71 2.41 1.38 17.4 101 214 30.9 259 11.0 971 6.49 0.68 14.0 1.81 47.4 105 10.7 38.1 6.64 1.20 5.65 0.89 4.93 1.01 2.87 0.41 2.87 0.42 0.58 209 19.1 10.97 228 11.9

72.6 0.30 13.6 2.70 0.06 0.39 1.72 3.41 3.58 0.08 0.57 99.0 22.4 0.95 1.08 8.64 18.3 2.57 2.48 1.08 18.7 108 237 32.8 281 11.4 1106 6.93 0.75 12.3 1.2 46.5 94.8 10.3 37.7 6.67 1.22 6.03 0.94 5.33 1.03 3.15 0.45 3.09 0.49 0.58 197 20.5 9.61 218 10.8

69.8 0.36 14.7 2.64 0.05 0.69 2.29 3.56 3.79 0.10 0.61 98.5 34.3 0.94 1.04 5.00 33.7 1.75 3.13 0.85 15.6 123 297 18.9 150 11.8 673 3.99 1.15 13.6 3.42 30.2 51.5 5.46 18.8 3.22 0.86 2.89 0.48 2.87 0.57 1.79 0.28 2.14 0.35 0.85 110 11.4 9.68 121 10.1

68.7 0.41 15.2 2.98 0.07 0.80 2.54 3.76 3.61 0.12 0.64 98.8 34.9 1.04 1.03 5.82 39.6 2.45 4.54 1.06 16.2 116 325 20.3 186 12.5 797 4.82 1.25 13.1 2.72 28.5 51.0 5.63 19.7 3.39 0.94 3.08 0.50 2.86 0.61 1.95 0.31 2.13 0.34 0.87 109 11.8 9.27 121 9.60

69.4 0.38 14.7 2.92 0.06 0.92 2.61 3.54 3.54 0.11 0.54 98.7 38.7 1.00 1.02 5.34 37.3 2.33 3.03 0.87 16.1 128 309 22.3 199 11.8 737 5.18 1.10 16.4 2.93 38.4 69.4 7.31 24.7 3.94 0.92 3.34 0.50 2.95 0.60 1.80 0.29 2.10 0.34 0.76 145 11.9 12.14 157 13.1

71.0 0.31 14.6 2.25 0.05 0.57 2.08 3.39 3.95 0.09 0.54 98.7 33.6 0.86 1.07 4.38 27.3 1.52 3.36 0.77 14.9 111 266 17.6 145 9.30 694 3.84 0.80 14.8 2.12 34.8 58.7 5.99 19.5 2.91 0.75 2.60 0.39 2.42 0.47 1.52 0.23 1.68 0.26 0.82 123 9.57 12.82 191 14.9

70.1 0.35 14.2 2.68 0.05 0.88 2.58 3.36 3.91 0.10 0.77 99.0 39.6 0.86 0.98 4.88 32.6 1.84 3.29 0.87 15.0 125 277 19.7 169 11.4 667 4.5 1.05 18.2 3.46 35.9 63.3 6.58 21.8 3.61 0.82 3.02 0.45 2.83 0.56 1.76 0.29 2.02 0.32 0.74 132 11.3 11.73 159 12.8

Note: LOI = Loss on ignition; Mg# = Mg2+ /(Mg2+ + TFe2+); A/CNK = mole[Al2O3 /(CaO + Na2O + K2O)]; δEu = (Eu)N / [(Gd)N + (Sm)N] /2; LREE = La + Ce + Pr + Nd + Sm + Eu; HREE = Gd + Tb + Dy + Ho + Er + Tm + Yb + Lu; ∑REE = LREE + HREE; and (La/Yb)N = (La / 0.237) /(Yb / 0.170).

compared with the Xiaobeihu and Lalagou plutons, the Huangqigou pluton possesses lower zircon εHf(t) values ranging from − 2.22 to −0.25 and older zircon two-stage model ages ranging from 1165 Ma to 1274 Ma, suggesting that the magma source of the Huangqigou pluton was mixed with some older crustal material, which was most likely derived from the Precambrian Dongfengshan Group in the study area (e.g. Gao et al., in press). Additionally, the Huangqigou pluton have lower SiO2 contents than the Xiaobeihu and Lalagou plutons, which is consistent with the mixing of mafic and granitic magmas from field observation. This mixing phenomenon implies that the mantle material had been involved in magma source and/or petrogenesis for the Huangqigou pluton. Based on these data, we can conclude that the source of the studied Late Permian granitic rocks is characterized by a juvenile crust mixed with some older crustal material, and that the composition of deep continental crust beneath the southeastern margin of the Songnen– Zhangguangcai Range Massif was heterogeneous.

5.3. Tectonic setting of Late Permian granitic magmatism and regional tectonic evolution Controversy has long surrounded the tectonic setting of the Late Permian granitic magmatism in the study area and adjacent areas. One school of thought argues that the Late Permian granitic magmatism along the southeastern margin of the Songnen–Zhangguangcai Range Massif occurred in a subduction zone (Li et al., 1999; Wu et al., 2001), some others propose that these granites were emplaced under a collisional environment (Sun et al., 2004b). Most recently, Liu S. et al. (2010) suggested that these granites formed in a post-collision extensional setting. Such controversy resulted from a diversity of tectonic settings for metaluminous or weakly peraluminous high-K calc-alkaline I-type granites. Thus, it is unreliable to determine the tectonic setting of metaluminous or weakly peraluminous high-K calc-alkaline I-type granites only based on their geochemical signatures (e.g. Wu et al., 2007b). Instead, an integrated analysis, including petrological, geochemical,

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Fig. 5. The TAS diagram (Irvine and Baragar, 1971) for the Late Permian granitic rocks and mafic rocks in the study area and adjacent areas. Data for granites are from Wu et al. (2001), Liu S. et al. (2010) and Huang et al. (2008); data for mafic rocks are from Liu S. et al. (2010) and Feng et al. (2010).

sedimentary and geochronological considerations is essential to constrain the tectonic setting and evolution of the Late Permian granites on the southeastern margin of the Songnen–Zhangguangcai Range Massif. Combining geochemical and geochronological data and zircon Hf isotopes presented in this study with previous geological data, we favor an extensional setting for the Late Permian granites at the southeastern

Fig. 7. (a) Chondrite-normalized rare earth element and (b) primitive mantle-normalized spidergram for the Late Permian granitic rocks. Legends are the same as those in Fig. 5. Data for chondrite are from Boynton (1984); data for primitive mantle are from Sun and McDonough (1989).

Fig. 6. (a) A/NK–A/CNK diagrams (Peccerillo and Taylor, 1976) and (b) K2O–SiO2 diagram (Maniar and Piccoli, 1989) for the Late Permian granitic rocks.

margin of the Songnen–Zhangguangcai Range Massif, because such a tectonic setting can well explain the coexistence of Late Permian granites and mafic intrusions in the studied area and adjacent areas (Fig. 5). As mentioned earlier, large volumes of Middle Permian mafic intrusions have been recognized along the southeastern margin of the Songnen– Zhangguangcai Range Massif, including the ~262 Ma Shimengzi dolerite and gabbros (Liu S. et al., 2010), the 264–262 Ma Yumuchuan diabase (Feng et al., 2010) and the ~263 Ma Wangbaozhen gabbros (Wang et al., in press). These mafic intrusions were emplaced slightly earlier or nearly simultaneously within age errors with the emplacement of the Huangqigou, Xiaobeihu and Lalagou granitic plutons in the studied area and other granitic plutons in the adjacent areas, including the ~ 256 Ma Chushan granitic pluton (Li et al., 1999; Wu et al., 2001), the 254–250 Ma Chaihe granitic pluton (Li et al., 1999; Wu et al., 2001), the 258–254 Ma Gangzigou granitic pluton (Li et al., 1999), and the ~ 259 Ma Meizuo granitic pluton (Huang et al., 2008). We interpret these mafic intrusions and granitic plutons in the study area and adjacent areas as a bimodal intrusive rock assemblage that was emplaced under an extensional setting. Such an interpretation is consistent with the widespread development of extensional basins in Northeast China during end-Permian time (Li, 2006). Generally, an extensional setting can be further subdivided into anorogenic within-plate extension and post-orogenic extension, of which the former often results from intracontinental rifting or mantle plume uprising, whereas the latter is related to slab break-off or lithospheric delamination following continent–continent collision. In this study, we favor a post-collision extensional setting for the Late Permian granitic plutons and associated mafic rocks at the southeastern margin of the Songnen–Zhangguangcai Range Massif because the spatial

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Table 3 Analytical results of zircon Hf isotopes for the Late Permian granitoids. Sample no

t (Ma)

176

Yb/177Hf

11HNA1-1-1 11HNA1-1-2 11HNA1-1-3 11HNA1-1-4 11HNA1-1-5 11HNA1-1-6 11HNA1-1-7 11HNA1-1-8 11HNA1-1-9 11HNA1-1-10 11HNA1-1-11 11HNA1-1-12 11HNA4-1-1 11HNA4-1-2 11HNA4-1-3 11HNA4-1-4 11HNA4-1-5 11HNA4-1-6 11HNA11-1-1 11HNA11-1-2 11HNA11-1-3 11HNA11-1-4 11HNA11-1-5 11HNA11-1-6 11HNA11-1-7 11HNA11-1-8 11HNA11-1-9 11HNA11-1-10

256 256 256 256 256 256 256 256 256 256 256 256 258 258 258 258 258 258 252 252 252 252 252 252 252 252 252 252

0.034486 0.043691 0.031955 0.030564 0.040102 0.023829 0.044776 0.051321 0.033358 0.035695 0.024532 0.044337 0.143562 0.067759 0.059161 0.078311 0.081758 0.108955 0.056211 0.043344 0.036138 0.031311 0.103696 0.047941 0.046267 0.027462 0.030343 0.045156

176

Lu/177Hf

0.000978 0.001318 0.000922 0.000857 0.001112 0.000687 0.001254 0.001372 0.001049 0.000968 0.000682 0.001281 0.004167 0.001996 0.001784 0.002368 0.002504 0.003453 0.001871 0.001289 0.001048 0.000913 0.003245 0.001538 0.001293 0.000782 0.000911 0.001451

176

Hf/177Hf

0.282563 0.282600 0.282560 0.282554 0.282595 0.282609 0.282578 0.282564 0.282584 0.282572 0.282593 0.282565 0.282961 0.282773 0.282728 0.282761 0.282824 0.282851 0.282854 0.282828 0.282823 0.282801 0.282888 0.282839 0.282833 0.282833 0.282820 0.282868

distribution of these rocks is largely restricted to a belt along which the united Songnen–Zhangguangcai Range–Jiamusi Massif collided with the Khanka (Xingkai) Massif (Fig. 1), and, more importantly, the emplacement of these Late Permian granitic plutons and associated mafic rocks occurred shortly after this collision, which is considered to have happened at some time after 270 Ma, based on the presence of the ~ 270 Ma subduction-related rhyolites at the southern margin of the Jiamusi Massif (Meng et al., 2008). If the Late Permian granitic plutons and associated mafic rocks at the SE margin of the Songnen– Zhangguangcai Range Massif were the products of post-collisional extension, the collision between the Khanka Massif and the united Songnen– Zhangguangcai Range–Jiamusi Massif must have occurred in the period 270–264 Ma, since the earliest post-collisional magmatism occurred at 264–262 Ma, represented by the ~262 Ma Shimengzi dolerite and gabbros (Liu S. et al., 2010), the 264–262 Ma Yumuchuan diabase

1σm

εHf(0)

εHf(t)

1σ

TDM1 (Ma)

TDM2 (Ma)

fLu/Hf

0.000006 0.000009 0.000005 0.000005 0.000007 0.000005 0.000006 0.000008 0.000008 0.000005 0.000005 0.000006 0.000013 0.000010 0.000011 0.000015 0.000016 0.000018 0.000012 0.000007 0.000006 0.000006 0.000008 0.000010 0.000007 0.000005 0.000006 0.000009

−7.39 −6.07 −7.51 −7.69 −6.25 −5.76 −6.85 −7.36 −6.65 −7.06 −6.33 −7.32 6.68 0.05 −1.57 −0.38 1.83 2.78 2.92 1.98 1.82 1.04 4.10 2.38 2.17 2.15 1.71 3.38

−1.93 −0.67 −2.04 −2.22 −0.82 −0.25 −1.44 −1.97 −1.21 −1.60 −0.82 −1.92 11.65 5.38 3.79 4.89 7.07 7.86 8.14 7.31 7.18 6.43 9.10 7.67 7.50 7.56 7.10 8.68

0.58 0.61 0.56 0.56 0.58 0.56 0.57 0.60 0.60 0.56 0.56 0.57 0.73 0.64 0.67 0.77 0.79 0.85 0.70 0.58 0.58 0.57 0.62 0.63 0.59 0.56 0.58 0.62

974 930 978 983 932 903 960 983 947 961 925 980 450 697 759 722 632 609 577 606 608 637 549 593 598 591 610 551

1259 1189 1265 1274 1197 1165 1231 1261 1218 1240 1197 1258 504 854 942 881 759 715 695 742 748 790 641 721 731 727 753 665

−0.97 −0.96 −0.97 −0.97 −0.97 −0.98 −0.96 −0.96 −0.97 −0.97 −0.98 −0.96 −0.87 −0.94 −0.95 −0.93 −0.92 −0.90 −0.94 −0.96 −0.97 −0.97 −0.90 −0.95 −0.96 −0.98 −0.97 −0.96

(Feng et al., 2010) and the ~263 Ma Wangbaozhen gabbros (Wang et al., in press). Based on the distribution of high-SiO2 rhyolites with the age of ~270 Ma (restricted to the southern margin of the Jiamusi Massif, Meng et al., 2008), we consider that the final collision between the Khanka Massif and the united Songnen–Zhangguangcai Range–Jiamusi Massif could happen along the Duhua–Mishan Fault (Fig. 1). 6. Conclusions (1) New LA-ICPMS zircon U–Pb data indicate that the Huangqigou, Xiaobeihu and Lalagou granitic plutons at the southeastern margin of the Songnen–Zhangguangcai Massif were formed in the Late Permian (256–252 Ma). (2) Geochemical data and zircon Hf isotopes suggest that the granitic magmas of the Xiaobeihu and Lalagou plutons were derived from the partial melting of a juvenile crust, whereas granitic magmas to form the Huangqigou pluton were derived from the partial melting of a juvenile crust mixed with some older crustal material, which implies that the composition of deep continental crust beneath the southeastern margin of the Songnen–Zhangguangcai Range Massif was heterogeneous. (3) The Late Permian granitic plutons and mafic intrusions in the study area and adjacent areas constitute a typical bimodal rock assemblage, which is considered to have formed under an extensional setting following collision between the Khanka (Xingkai) Massif and the united Songnen–Zhangguangcai Range–Jiamusi Massif. Acknowledgments

Fig. 8. εHf(t)–t diagram of the Late Permian granitic rocks in the study area. CAOB = the Central Asian Orogenic Belt and YFTB = the Yanshan Fold and Thrust Belt (Yang et al., 2006). Legends are the same as those in Fig. 5.

This research was funded by a Chinese NSFC Grant (41072038 and 41272075) and two projects (1212010070301 and 1212321013019) from the Geological Survey of China. We thank Dr. Wenchun Ge, Deyou Sun and Xiaoguo Chi for their thoughtful discussions and constructive comments on the early version of this paper. Miss Yanlin Zhu and Dr. Guochun Zhao are thanked for improving the English exposition of the paper.

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