Implications for Zircon Geochronology, Elemental and Sr–Nd–Hf Isotopic

Lithos 146–147 (2012) 112–127

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Reactivation of the Archean lower crust: Implications for zircon geochronology, elemental and Sr–Nd–Hf isotopic geochemistry of late Mesozoic granitoids from northwestern Jiaodong Terrane, the North China Craton

Kui-Feng Yang a, Hong-Rui Fan a,⁎, M. Santosh b,c, Fang-Fang Hu a, Simon A. Wilde d, Ting-Guang Lan a, Li-Na Lu a, Yong-Sheng Liu e a Key Laboratory of Mineral Resources, Institute of Geology and Geophysics, Chinese Academy of Sciences, Beijing 100029, China b Division of Interdisciplinary Science, Faculty of Science, Kochi University, Kochi 780-8520, Japan c Geoscience Frontiers, China University of Geosciences, Xueyuan Road, Haidian District, Beijing 100083, China d Department of Applied Geology, Curtin University of Technology, GPO Box U1987, Perth 6845, Australia e State Key Laboratory of Geological Processes and Mineral Resources, China University of Geosciences, Wuhan 430074, China article info abstract

Article history: The late Mesozoic granitoids widely distributed in the northwestern Jiaodong Terrane are important markers Received 12 December 2011 of cratonic destruction and lithospheric thinning of the eastern North China Craton (NCC). Here we investi- Accepted 22 April 2012 gate the Late Jurassic Linglong and Luanjiahe granites and report zircon U–Pb emplacement ages of 157– Available online 12 May 2012 159 Ma. These rocks also contain abundant late Archean, Paleoproterozoic, Neoproterozoic, early Paleozoic and Triassic inherited zircons, suggesting the involvement of continental crustal materials from both the Keywords: NCC and Yangtze Craton in magma tectonics. The rocks investigated in this study show high Na O+K O Geochemistry 2 2 Zircon geochronology and low MgO and are peraluminous, with enrichment in LREEs and LILEs (Rb, Ba, U, and Sr) and depletion ε Late Mesozoic granitoids in HFSEs (Nb, Ta, P, and Ti). They also display low Hf(t) values and high Sr/Y ratios, comparable to adakitic Northwestern Jiaodong Terrane rocks, suggesting that the Linglong and Luanjiahe granitoids formed under relatively high pressure condi- North China Craton tions and were likely derived from the partial melting of the thickened lower crust of the NCC. The Guojialing granodiorites were emplaced in the early Cretaceous (129 Ma), and also contain abundant late Archean and

Paleoproterozoic inherited zircons. The rocks possess high CaO, TFe2O3 and MgO, and are metaluminous, with enrichment in LREEs and LILEs and depletion in HFSEs. They are also characterized by high Sr/Y ratios, and

have higher εNd(t) and εHf(t) values than the Late Jurassic granitoids, suggesting the involvement of mantle components in the magmatic source. We correlate the magma tectonics with the processes accompanying the subduction of the Paciﬁc Plate beneath the NCC and the associated asthenospheric upwelling. © 2012 Elsevier B.V. All rights reserved.

1. Introduction Central Asian Orogeny since the Late Carboniferous at the northern margin of the NCC (Li et al., 2009; Meng, 2003; Zhang et al., 2003, The North China Craton (NCC) preserves some of the oldest re- 2007; Zorin, 1999), and to the collision between the NCC and Yangtze cords of crustal evolution in the Precambrian Earth (Liu et al., 1992; Craton since the Late Triassic at the southern margin of the NCC (Gao Zhai and Santosh, 2011). The eastern part of the NCC had a thick et al., 1998; Li et al., 1993; Yang et al., 2007a, b; Zhang et al., 2002). (>200 km) lithosphere until the early Paleozoic as inferred from The destruction of the NCC was a relatively slow process (continuing the presence of diamondiferous kimberlites such as those at Mengyin for more than 100 Ma), rather than a dramatic event (Xu et al., 2009). and Fuxian (Menzies et al., 1993; Yang et al., 2009; Zhang et al., 2010) Many recent papers favor hydrous weakening over a considerable pe- (Fig. 1a). However, by the Cenozoic, the craton lost at least 75–80 km riod of time as the potential cause for the lithospheric thinning of its keel, as recognized by the presence of spinel–facies xenoliths in (Kusky et al., 2007b; Santosh, 2010; Windley et al., 2010). During alkali basalts, as well as through evidence from geochemical and geo- this period, abundant granitoids developed in the northwestern physical data (Gao et al., 2002; Rudnick et al., 2004; Wu et al., 2005; Jiaodong Terrane in the eastern NCC (Fig. 1b), and these have tradi- Yang et al., 2008; Zhang, 2012; Zhang et al., 2009, 2011; Zhou et al., tionally been divided into two 77 groups. Those of Late Jurassic ages 2002). The onset of lithospheric thinning has been linked to the (155–160 Ma, e.g. Miao et al., 1997; Wang et al., 1998) are known locally as the Linglong and Luanjiahe suites. Those of Early Cretaceous ages (126–130 Ma, e.g. Miao et al., 1997; Wang et al., 1998) are ⁎ Corresponding author. Tel.: +86 10 82998218; fax: +86 10 62010846. referred to as the Guojialing suite. Since these granitic rocks were co- E-mail address: [email protected] (H-R. Fan). eval with lithospheric thinning of the eastern NCC (Wu et al., 2005),

Fig. 1. Geological map of the North China Craton (a) and the Jiaodong Terrane (b), showing the distribution of the basement rocks, UHP metamorphic rocks and Mesozoic igneous rocks. Modiﬁed after Kusky et al. (2007a), Peng et al. (2007) and Goss et al. (2010).

they possess important significance in providing information on the 2. Geological background nature of the continental crust at this time. Of particular importance in this regard are the abundant Neo- The NCC is bounded by the Central Asian Orogenic Belt (CAOB) to proterozoic magmatic inherited zircons with age at 683–773 Ma, the north, the Sulu ultrahigh-pressure (UHP) metamorphic belt to the which are present in the Late Jurassic Linglong and Luanjiahe granit- east and the Qinling–Dabie orogenic belt to the south (Fig. 1a). The oids. Such Neoproterozoic ages are a prominent feature of the Sulu belt was originally part of the Qinling–Dabie belt, but has subse- Yangtze Craton (Ames et al., 1996; Gao et al., 1996; Guo et al., 2005; quently been transported more than 500 km northeast along the Hacker et al., 1998; Rowley et al., 1997; Zheng et al., 2007; Zhou et Tanlu Fault (Ames et al., 1993; Xu and Zhu, 1994; Zhou et al., al., 2006), and the corresponding igneous rocks were considered to 2008a). The Qinling–Dabie–Sulu metamorphic belt is the result of have formed as a response to the breakup of the supercontinent subduction and collision between the NCC and Yangtze Craton Rodinia (Li et al., 2003; Ling et al., 2003; Zheng et al., 2006, 2007). (Mattauer et al., 1985). The absence of Neoproterozoic granitic magmatism in the eastern The Jiaodong Terrane refers to the area east of the Tanlu Fault, NCC during this period is deemed to be an important basis to distin- and forms the eastern margin of the NCC. The Sulu UHP metamor- guish the eastern NCC and the Yangtze Craton (Hacker et al., 1998; phic belt lies to the east and they are separated by the Baichihe–Yan- Tang et al., 2008; Wan and Zeng, 2002). Miao et al. (1997) conducted tai Fault (Zhou et al., 2008b)(Fig. 1b). The Precambrian basement of a detailed statistical analysis of inherited zircon ages in these rocks, the eastern NCC in the Jiaodong Terrane comprises the Archean but they did not carry out in-depth discussion about their signifi- Jiaodong Group composed of metamorphic volcanic sedimentary cance. The occurrence of Neoproterozoic magmatic zircons with an rocks and TTG gneiss, and the Paleoproterozoic Jingshan Group com- age signature of the Yangtze Craton within the eastern NCC more posed of metamorphic clastic rocks together with the Fenzhishan than 100 km north of the Sulu orogenic belt is noteworthy and pro- Group composed of metamorphosed chemical sediments (Guo et vided the impetus for us to conduct further work in the area. al., 2005). Jahn et al. (2008) offered new zircon U–Pb SHRIMP data This region is of critical importance to evaluate the lithosphere that established the existence of Mesoarchean (ca. 2.90 Ga) and interaction during continental collision (Sulu–Dabie orogen), and Neoarchean (2.71 to 2.73 Ga) continental crust in the Jiaodong Ter- for reconstructing the Mesozoic lithospheric structure and crustal rane. However, the basement rocks of the Sulu Belt to the east are composition of the eastern margin of the NCC. mainly composed of Neoproterozoic granitic gneisses. Zheng et al. In this paper, based on detailed petrological, geochronological and (2006, 2008) considered that the protoliths of these granitic geochemical studies on the Late Mesozoic granitic rocks in the north- gneisses were produced by partial melting of continental crust in western Jiaodong Terrane in the eastern NCC, we attempt to define the northern margin of Yangtze Craton, which underwent Triassic their magmatic origin and tectonic setting, and to constrain the litho- UHP metamorphism (Ames et al., 1996; Guo et al., 2005; Hacker et spheric composition and evolution history in the Late Mesozoic. al., 1998). 114 K-F. Yang et al. / Lithos 146–147 (2012) 112–127

Mesozoic igneous rocks form another major component of the 3. Sampling and petrography Jiaodong Terrane (Fig. 1b), and include Late Jurassic granites, Early Cretaceous granites and granodiorites and Early Cretaceous volcanic Representative samples were collected from the Linglong granite, rocks (Sang, 1984; Sang and You, 1992). The Late Jurassic granites Luanjiahe granite and Guojialing granodiorite, evenly distributed in are mainly composed of two suites in the Zhaoyuan–Pingdu area in the northwest Jiaodong area (Fig. 2), for detailed petrographic and the northwestern Jiaodong Terrane, the Linglong and Luanjiahe gran- geochemical analysis. Two samples from each of the granitoids were ites. SHRIMP U–Pb zircon geochronological data show that the selected for LA-ICP-MS (laser ablation inductively coupled plasma Linglong and Luanjiahe intrusions were emplaced at 150–160 Ma mass spectrometry) U–Pb zircon dating and Lu–Hf isotopic analysis. (Miao et al., 1997). The Early Cretaceous granodiorites that intrude the former suites are mainly composed of the Guojialing porphyritic 3.1. Linglong granite suite hornblende–biotite granodiorites in the north Zhaoyuan area. SHRIMP U–Pb zircon geochronological data show that the Guojialing The Linglong granite is located in the northwestern Jiaodong Ter- intrusions were emplaced at 126–130 Ma (e.g. Miao et al., 1997). rane covering an area of more than 1000 km2, and consists mainly The Early Cretaceous granites are mainly distributed in the Sulu of biotite granite with an allotriomorphic granular texture. Gneissic UHP metamorphic belt in the southeast Jiaodong Terrane, and a few structures resulting from later deformation are generally developed small stocks in the northwest, which were emplaced at 113–118 Ma in these rocks (Luo and Miao, 2002). The Linglong granite is gray in (e.g. Goss et al., 2010). Early Cretaceous intermediate-acidic volcanic hand specimen (Fig. 3a) and the main minerals are plagioclase (25– rocks are mainly distributed in the Jiaolai Basin, and were formed at 30%), K-feldspar (35–40%), quartz (20–30%) and biotite (5–10%), 108–110 Ma (e.g. Qiu et al., 2001). with accessory titanite, garnet, zircon and apatite. The plagioclase is

Fig. 2. Geological map of the Zhaoyuan–Laizhou area in the northwestern Jiaodong Terrane showing sample locations. Modiﬁed after Wang et al. (1998). K-F. Yang et al. / Lithos 146–147 (2012) 112–127 115

Fig. 3. Hand specimen photos and thin section microphotographs of the granitoids in the northwestern Jiaodong Terrane. Symbols for minerals: Pl, plagioclase; Kfs, K-feldspar; Qz, quartz; Bi, biotite; Hb, hornblende.

albite–andesine with multiple twins. The K-feldspar is microcline– 3.3. Guojialing granodiorite suite perthite with cross-hatched twins and locally forms a granophyric intergrowth with quartz (Fig. 3b). Biotite is typically aligned to form a The Guojialing granodiorite is located to the north of Zhaoyuan gneissic structure, together with elongated quartz. Euhedral titanite and is composed of five small intrusions (Fig. 2), emplaced within is visible in hand specimens with grain size up to 2 mm. Garnet is the Late Jurassic granitoids (Wang et al., 1998). The Guojialing grano- purple and visible in the most hand specimens. diorite is pale red in hand specimen with a porphyritic texture (Fig. 3e). The main minerals are plagioclase (35–55%), K-feldspar 3.2. Luanjiahe granite suite (10–25%), quartz (15–30%), hornblende (5–10%) and minor biotite, with accessory titanite, zircon, apatite and monazite. The K‐feldspar The Luanjiahe granite is located in the northwestern Jiaodong Ter- is microcline–perthite and locally forms granophyric intergrowth rane covering an area of more than 800 km2, and consists mainly of with quartz. The mineral occurs both as phenocrysts (up to 10 cm biotite granite with a coarse-grained allotriomorphic granular tex- in length) and as a fine-granular phase. The plagioclase is mainly ture. The granite was thought to be the slightly later-intruded central albite–andesine and appears both as a phenocryst phase and in the phase of the Late Jurassic granitoids (BGMRS, 1991). The Luanjiahe matrix (Fig. 3f). Hornblende is bottle green in hand specimen and is granite is pale red in hand specimen (Fig. 3c) and the main minerals present only in some samples. Titanite is euhedral and commonly as- are plagioclase (25–45%), K-feldspar (30–50%), quartz (20–40%) and sociated with hornblende and the largest grain is up to 3 mm. biotite (3–5%), with accessory garnet, zircon, apatite and opaque minerals. The plagioclase is mainly oligoclase with multiple twins, pro- 4. Analytical methods gressive zonal texture, and polysynthetic albite twinning at the crystal edge. The K‐feldspar is mainly microcline with cross hatched Fresh rock samples were crushed in a tungsten carbide mill to twins and it is extensively altered to clay minerals (Fig. 3d). 200 mesh powder for major, trace element, and Sr–Nd isotope 116 K-F. Yang et al. / Lithos 146–147 (2012) 112–127 analyses, and 40–60 mesh for selecting zircon grains to use for U–Pb (IGGCAS), Beijing. For major element analyses, mixtures of whole dating and Hf isotope analyses. rock powder (0.5 g) and Li2B4O7 +LiBO2 (5 g) were made into glass disks and analyzed by X-ray fluorescence spectroscopy (XRF) with 4.1. Major and trace elements an AXIOS Minerals spectrometer. The analytical uncertainties were generally within 0.1–1% (RSD). For trace element analyses, whole

Major and trace elements were analyzed in the Laboratories of the rock powders (40 mg) were dissolved in distilled HF+HNO3 in Tef- Institute of Geology and Geophysics, Chinese Academy of Sciences lon screw-cap capsules at 200 °C for 5 days, dried, and then digested

Fig. 4. Representative CL images of zircons analyzed from the Jiaodong Terrane and the scale bar is 100 μm (a). LA-ICP-MS zircon U–Pb concordia diagrams of the Linglong granites (b, c), Luanjiahe granites (d, e) and Guojialing granodiorites (f, g) from the Jiaodong Terrane. K-F. Yang et al. / Lithos 146–147 (2012) 112–127 117

with HNO3 at 150 °C for one day. They were taken to dryness again Goolaerts et al. (2004). Detailed analytical procedures were described and digested with HNO3 at 150 °C for another day. Dissolved samples by Xie et al. (2008). were diluted to 49 ml with 1% HNO3 and 1 ml 500 ppb indium was added to the solution as an internal standard. Trace element abun- 5. Results dances were determined by inductively coupled plasma mass spectrometry (ICP-MS) using a Finnigan MAT Element spectrometer, 5.1. Geochronology which has analytical uncertainties within 5% for most elements. 5.1.1. Linglong granite 4.2. Sr and Nd isotopes The zircon crystals in samples 08G33 and 08G59 of the Linglong granite are mostly prismatic and range from 60 to 200 μm in size. Whole rock powders for Sr and Nd isotopic analyses were dissolved Most grains are transparent and pale yellow in color, and display os- in Teflon bombs after being spiked with 87Rb, 84Sr, 149Sm and 150Nd cillatory zoning. Some of the grains have circular or irregular cores tracers prior to HF+HNO +HClO dissolution. Rb, Sr, Sm and Nd were 3 4 mantled by euhedral overgrowths that also show oscillatory zoning separated using conventional ion exchange procedures and measured (Fig. 4a). 19 spots from 13 grains were analyzed from 08G33 and using a Finnigan MAT262 multi-collector mass spectrometer at IGGCAS. the data yield a weighted mean 206Pb/238U age of 159±2 Ma (2σ) Detailed descriptions of the analytical techniques have been document- (Fig. 4b; Supplemental electronic data Table 1), which is taken to de- ed in Chu et al. (2009). Procedural blanks are b100 pg for Sm and Nd, fine the crystallization age of the granite. Of the six remaining grains, and b300 pg for Rb and Sr. The isotopic ratios were corrected for mass one grain shows a significantly older 207Pb/206Pb age of 2083 Ma and fractionation by normalizing to 86Sr/88Sr=0.1194 and 146Nd/144Nd= is likely an inherited zircon from the basement of the eastern NCC. 0.7219, respectively. The measured values for the JNdi-1 Nd standard Another grain yields a 206Pb/238U age of 774 Ma, which could be an and NBS987 Sr standard were 143Nd/144Nd=0.512118±12 (2σ, inherited zircon from the northern margin of the Yangtze Craton. n=10) and 87Sr/86Sr=0.710257±12 (2σ,n=10),respectively.USGS The remaining four grains have concordant ages that range from reference material BCR-2 was measured to monitor the accuracy of the 220 Ma to 240 Ma, which is consistent with the age of UHP metamor- analytical procedures, with 143Nd/144Nd=0.512633±13 (2σ, n=12) phism in the Dabie–Sulu orogen. and 87Sr/86Sr=0.705035±12 (2σ, n=12). 23 spots from 16 zircons were analyzed from sample 08G59 Linglong granite and the results show a weighted mean 206Pb/238U 4.3. Zircon U–Pb dating and in situ Hf isotopic analyses age of 159±1 Ma (2σ)(Fig. 4c; Supplemental electronic data Table 1), which is taken to define the crystallization age of the gran- U–Pb dating and trace element analyses of zircon were conducted ite. Of the seven remaining grains, one grain yields a discordant age synchronously by LA-ICP-MS at the State Key Laboratory of Geological (Supplemental electronic data Table 1), which is not further consid- Processes and Mineral Resources, China University of Geosciences, ered. Another grain yields a 206Pb/238U age of 208 Ma, which corre- Wuhan. Detailed operating conditions for the laser ablation system, lates with the timing of magmatism following the mantle upwelling the ICP-MS instrument, and the data reduction process are described induced by slab breakoff after continental subduction of the Yangtze by Liu et al. (2010). Laser sampling was performed using a GeoLas Craton (e.g., Guo et al., 2005). The remaining five grains show con- 2005. An Agilent 7500a ICPMS was used to acquire ion-signal intensi- cordant to weakly discordant ages that range from 435 Ma to ties. Each analysis incorporated a background acquisition of approxi- 514 Ma and from 751 Ma to 776 Ma, which correspond to represen- mately 20–30 s (gas blank) followed by 50 s data acquisition from the tative ages recorded from the Yangtze Craton. sample. An Agilent Chemstation was utilized for the acquisition of each individual analysis. Off-line selection and integration of background and analytical signals, time-drift correction, and quantitative 5.1.2. Luanjiahe granite calibration for trace element analyses and U–Pb dating were per- The zircons in samples 08G40 and 08G42 of Luanjiahe granites formed by ICPMSDataCal (Liu et al., 2010). are mostly prismatic and range from 100 to 200 μm in size with sim- Zircon 91500 was used as the external standard for U–Pb dating, ilar characteristics to samples from the Linglong granite (Fig. 4a). 19 and was analyzed twice every five analyses. Time-dependent drifts spots were analyzed from 12 grains in sample 08G40 yielding a of U–Th–Pb isotopic ratios were corrected using a linear interpolation weighted mean 206Pb/238Uageof158±2Ma(2σ)(Fig. 4d; Supple- (with time) for every five analyses according to the variations of mental electronic data Table 1), which is taken to define the crystal- 91500 (Liu et al., 2010). Preferred U–Th–Pb isotopic ratios used for lization age of the granite. Among the seven remaining grains, one 91500 were from Wiedenbeck et al. (1995). Uncertainties of pre- yields a discordant younger age, which is discarded. Two other ferred values for the external standard 91500 were propagated grains yield significantly older 207Pb/206Pb ages of 1792 Ma and through to the ultimate results of the samples. Concordia diagrams 1952 Ma and are likely to be inherited zircons from the basement and weighted mean calculations were made using Isoplot/Ex ver3 of the eastern NCC. Another two grains yield 206Pb/238Uagesof (Ludwig, 2003). Trace element compositions of zircons were calibrat- 688 Ma and 691 Ma, which are considered as inherited zircons ed against reference material GSE-1G combined with internal stan- from the northern margin of the Yangtze Craton. The remaining dardization (Liu et al., 2010). two grains yield 206Pb/238U ages of 200 Ma and 203 Ma. In situ zircon Hf isotopic analyses were conducted in the same 21 spots were analyzed from 12 grains in sample 08G42and the spots which were analyzed for U–Pb dating. Hf isotopic compositions data define a weighted mean 206Pb/238U age of 157±2 Ma (2σ) were determined by a Neptune MC–ICP-MS equipped with a (Fig. 4e; Supplemental electronic data Table 1), which is taken to rep- GeolasPlus 193 nm ArF excimer laser at the IGGCAS. A laser spot resent the crystallization age of the granite. Of the nine remaining size of 40 μm and laser repetition of 8 Hz with energy density of grains, three yield discordant ages and are not discussed further. 15 J/cm2 was used during the analyses. The signal collection model Two grains yield significantly older 207Pb/206Pb ages of 2213 Ma and is one block with two hundred cycles. Each cycle has 0.131 s integra- 2857 Ma, and are likely inherited zircons from the basement of the tion time and the total time is about 26 s for each analysis. Zircon eastern NCC. Two other grains yield 206Pb/238U ages of 683 Ma and 91500 was used as an external standard for Hf isotopic analyses and 742 Ma, and may be inherited zircons from the northern margin of was analyzed twice every five analyses. Repeated analyses of 91500 Yangtze Craton. The remaining two grains yield 206Pb/238U ages of yielded a mean 176Hf/177Hf ratio of 0.282303±37 (2σ, n=35), 226 Ma and 235 Ma, and these ages are consistent with the timing which is consistent with the 176Hf/177Hf ratios measured by of UHP metamorphism in the Dabie–Sulu orogen. 118

Table 1 Major oxides (wt.%) and trace elements (ppm) for the Jiaodong granitoids.

Sample no. 08G01 08G02 08G03 08G04 08G05 08G19 08G20 08G40 08G42 08G50 08G52 08G53 08G15 08G16 08G17 08G18 08G21 08G22

Rock-type Luanjiahe granite Linglong granite

SiO2 71.6 73.1 71.3 74.1 74.4 73.3 74.5 72.3 73.9 71.6 72.9 74.4 73.2 73.6 70.9 71.6 74.8 75.9 TiO2 0.13 0.15 0.12 0.12 0.12 0.16 0.12 0.15 0.05 0.15 0.11 0.06 0.25 0.15 0.19 0.16 0.06 0.16 Al2O3 14.4 13.9 14.5 14.2 14.2 14.3 13.9 15.2 14.5 15.2 15.0 13.9 14.2 14.1 14.3 14.3 13.9 12.9 TFe2O3 1.42 0.94 1.32 1.09 1.16 1.44 1.20 1.14 0.40 1.51 1.07 0.77 1.64 1.50 1.67 1.49 0.90 1.50 MnO 0.07 0.04 0.05 0.02 0.02 0.02 0.03 0.02 0.02 0.03 0.03 0.05 0.03 0.02 0.02 0.02 0.02 0.02 MgO 0.11 0.10 0.19 0.10 0.10 0.16 0.15 0.20 0.05 0.18 0.14 0.09 0.25 0.21 0.27 0.21 0.06 0.22 CaO 1.66 1.64 1.83 0.82 0.87 1.16 1.22 1.64 0.50 2.12 1.82 0.92 1.54 1.45 1.62 1.43 1.15 1.45 Na2O 4.71 4.02 4.46 4.26 4.40 4.12 4.23 4.78 4.91 4.79 5.01 5.12 3.99 4.28 4.18 4.06 4.46 3.59 K2O 3.49 4.23 3.71 4.17 4.04 4.27 3.85 3.86 4.37 3.34 3.53 4.20 4.08 3.92 3.91 4.52 4.02 3.53 P2O5 0.04 0.03 0.04 0.03 0.02 0.04 0.03 0.03 0.02 0.04 0.03 0.02 0.04 0.03 0.04 0.04 0.02 0.03 LOI 1.82 1.24 2.16 0.54 0.40 0.48 0.38 0.32 0.58 0.34 0.28 0.26 0.20 0.26 0.34 0.40 0.10 0.18 -.Yn ta./Lto 146 Lithos / al. et Yang K-F. Total 99.46 99.36 99.63 99.37 99.70 99.44 99.54 99.67 99.32 99.33 99.92 99.82 99.37 99.55 97.35 98.21 99.50 99.42 Mg# 15.3 19.9 25.1 17.6 16.7 20.6 22.6 29.0 22.6 21.7 23.3 21.5 26.2 24.6 27.4 24.7 13.4 25.5 Cr 158 141 146 124 156 152 153 170 144 166 140 203 143 145 161 156 151 158 Ni 2.39 2.92 2.80 1.69 9.01 2.17 2.73 4.47 4.01 4.49 2.51 4.33 1.51 3.00 2.73 4.94 3.77 4.05 Rb 123 166 134 119 132 128 116 73.1 136 96.5 113 150 106 97.1 87.9 107 120 71.6 Ba 907 988 1166 1248 880 1634 1299 2470 1082 2798 2160 999 2020 1599 2114 2376 684 2194 Th 3.52 3.29 3.75 7.29 4.98 5.44 8.75 3.65 3.76 4.05 3.80 6.65 8.35 7.20 7.89 7.03 5.47 5.34 U 2.33 1.85 1.90 0.98 1.12 1.48 0.87 0.40 0.45 1.20 1.37 5.16 1.46 0.96 0.76 0.87 2.23 0.53 Pb 24.0 35.6 30.2 28.6 26.4 28.3 27.9 34.7 29.3 27.6 32.8 48.1 37.5 26.7 26.7 28.2 39.0 23.9 –

Nb 12.0 9.75 9.79 9.20 10.6 8.46 9.86 4.14 5.88 9.80 11.6 13.3 6.36 7.87 6.07 7.10 11.59 5.25 112 (2012) 147 Ta 0.72 0.59 0.58 0.73 1.37 0.86 0.82 0.15 0.51 0.36 1.25 1.42 0.21 0.37 0.20 0.34 0.86 0.22 La 11.1 9.38 12.4 25.3 18.7 28.9 30.4 20.9 8.5 29.1 16.1 11.3 36.6 35.9 43.5 39.7 11.1 28.2 Ce 19.0 18.2 21.6 47.1 34.0 50.7 51.1 33.7 14.8 46.3 27.1 20.8 60.6 62.3 75.8 66.0 19.8 48.5 Pr 2.20 1.99 2.57 5.02 3.59 5.19 5.68 3.56 1.79 4.96 3.02 2.50 6.84 6.97 8.46 7.06 2.47 5.18

Sr 349 351 424 390 348 566 491 1002 373 964 762 431 693 569 713 682 288 653 – 127 Nd 7.56 6.84 8.54 16.7 11.8 16.9 18.9 11.4 6.61 16.4 10.6 9.56 21.7 21.7 25.9 22.3 8.85 16.7 Zr 90.9 76.0 96.5 99.8 58.2 113 108 110 52.3 137 97.2 60.7 146 118 151 151 73.6 139 Hf 3.04 2.45 3.11 3.24 1.86 3.58 3.37 3.23 1.97 3.66 3.18 2.80 4.46 3.46 4.29 4.71 2.80 3.97 Sm 1.41 1.27 1.48 2.71 2.20 2.33 2.83 1.69 1.44 2.21 2.06 2.60 2.88 3.06 3.43 2.87 2.08 2.09 Eu 0.52 0.41 0.37 0.55 0.50 0.68 0.56 0.52 0.30 0.60 0.46 0.39 0.76 0.67 0.83 0.73 0.57 0.69 Gd 1.45 1.23 1.47 2.30 2.37 2.04 2.48 1.22 1.16 1.78 2.16 3.29 2.59 2.58 2.82 2.49 1.75 1.77 Tb 0.24 0.19 0.21 0.30 0.48 0.27 0.33 0.12 0.17 0.19 0.37 0.69 0.26 0.27 0.25 0.24 0.24 0.17 Dy 1.52 1.20 1.32 1.47 3.57 1.42 1.70 0.55 0.90 0.80 2.38 4.82 1.13 1.13 0.99 0.91 1.16 0.66 Y 12.1 8.15 9.55 8.23 25.2 8.78 9.37 3.25 5.48 4.57 14.82 30.8 5.86 5.61 4.64 5.16 5.23 3.75 Ho 0.34 0.27 0.28 0.27 0.82 0.27 0.30 0.11 0.17 0.13 0.48 1.07 0.21 0.20 0.17 0.16 0.19 0.12 Er 1.03 0.84 0.87 0.70 2.22 0.69 0.76 0.30 0.46 0.37 1.24 2.98 0.53 0.48 0.44 0.40 0.43 0.31 Tm 0.18 0.15 0.15 0.10 0.32 0.10 0.10 0.04 0.07 0.05 0.18 0.47 0.08 0.06 0.06 0.06 0.06 0.04 Yb 1.40 1.07 1.20 0.61 1.87 0.64 0.62 0.30 0.44 0.39 1.06 3.03 0.47 0.40 0.40 0.37 0.37 0.30 Lu 0.26 0.18 0.22 0.09 0.24 0.10 0.09 0.05 0.07 0.07 0.15 0.46 0.07 0.06 0.06 0.06 0.05 0.05 (La/Yb)N 5.68 6.30 7.40 29.8 7.20 32.3 35.1 49.4 14.0 54.1 10.9 2.68 55.7 64.8 78.3 77.6 21.7 66.9 Eu/Eu* 1.12 1.00 0.76 0.67 0.67 0.95 0.65 1.10 0.72 0.93 0.67 0.41 0.85 0.73 0.81 0.83 0.90 1.11 Table 1

08G24 08G33 08G38 08G39 08G49 08G59 08G07 08G08 08G13 08G25 08G26 08G28 08G29 08G30 08G31 08G32 08G37 08G61

Linglong granite Guojialing granodiorite

73.5 72.2 69.2 75.9 74.1 74.8 69.8 70.4 70.0 68.5 68.8 68.2 68.9 70.8 72.6 70.7 71.2 71.4 0.18 0.18 0.29 0.06 0.06 0.04 0.31 0.29 0.31 0.35 0.31 0.34 0.32 0.20 0.13 0.27 0.19 0.26 14.1 15.1 16.1 13.2 14.1 14.0 15.1 15.3 14.9 15.9 15.3 15.6 15.5 15.7 15.2 14.9 15.4 15.1 1.67 1.34 2.21 0.83 0.90 0.65 2.26 2.04 2.26 2.22 2.21 2.49 2.37 1.57 1.30 1.56 1.14 1.58 0.02 0.02 0.03 0.01 0.01 0.01 0.03 0.03 0.04 0.03 0.04 0.04 0.03 0.02 0.02 0.01 0.01 0.02 0.23 0.25 0.46 0.07 0.07 0.08 1.10 1.03 1.11 1.03 1.24 1.10 1.17 0.62 0.39 0.46 0.38 0.55 1.54 1.71 2.50 0.55 1.04 0.98 2.62 2.62 2.83 2.56 2.42 2.71 2.74 2.58 2.49 1.99 2.12 2.42 3.98 4.81 4.46 3.21 4.58 4.01 4.50 4.62 4.79 4.81 4.46 4.85 4.86 5.58 5.92 4.58 4.73 5.19 4.01 3.65 3.59 5.39 4.40 4.68 3.42 3.37 2.80 3.70 4.37 3.45 3.25 2.49 1.46 3.49 3.66 2.50 0.04 0.04 0.08 0.02 0.01 0.01 0.10 0.10 0.10 0.14 0.15 0.16 0.14 0.06 0.04 0.07 0.05 0.07 0.20 0.54 0.48 0.44 0.38 0.48 0.16 0.00 0.32 0.16 0.24 0.50 0.18 0.26 0.56 1.38 0.44 0.56

99.43 99.81 99.32 99.67 99.68 99.73 99.43 99.85 99.43 99.34 99.57 99.45 99.46 99.94 100.18 99.45 99.37 99.63 146 Lithos / al. et Yang K-F. 24.3 30.3 32.7 16.4 15.3 22.2 53.1 54.1 53.4 52.0 56.7 50.8 53.5 48.0 41.1 40.7 43.8 44.8 185 168 143 134 161 220 150 149 142 77.1 104 158 118 89.8 198 90.4 74.8 103 3.12 10.45 7.25 3.68 5.76 26.0 10.9 11.9 11.1 8.25 21.2 10.9 14.7 4.87 5.44 3.01 2.38 4.48 74.5 72.2 75.6 113 90.9 101 85.1 83.6 77.0 72.6 86.4 67.5 69.6 55.1 38.3 83.2 74.3 55.8 2262 2104 2340 1457 2560 1325 1416 1470 837 3461 3482 3104 2931 1644 581 1609 1785 1284 9.50 3.34 10.49 4.65 2.10 3.24 7.72 8.76 9.43 16.8 23.6 22.9 16.8 3.07 3.45 8.58 4.06 6.39 0.85 0.45 0.53 0.49 0.71 0.90 1.01 2.38 3.18 1.73 1.91 2.03 1.57 0.84 0.45 0.90 0.71 0.83 24.7 35.9 21.4 36.4 28.5 30.6 31.6 33.2 31.8 30.4 40.6 31.7 28.8 28.4 28.9 22.9 27.4 23.0

5.22 4.69 5.75 3.47 3.72 4.02 5.53 5.29 6.53 7.95 7.34 8.87 6.50 6.90 3.31 5.19 2.60 4.91 – 4 21)112 (2012) 147 0.25 0.21 0.17 0.17 0.25 0.24 0.35 0.33 0.39 0.53 0.45 0.55 0.37 0.51 0.17 0.28 0.14 0.29 49.8 21.4 50.4 10.9 9.26 4.92 26.6 31.9 26.3 82.6 109 109 84.2 14.6 15.0 49.4 21.2 34.4 85.2 35.2 88.7 17.0 14.9 7.82 47.0 56.9 47.2 145 183 183 147 26.6 24.6 79.0 34.9 58.7 9.18 3.96 9.48 2.18 1.74 1.03 5.74 6.76 5.58 17.4 20.9 19.9 16.1 3.11 2.64 8.36 3.83 6.57 689 965 906 338 731 401 1035 1136 895 1788 1809 1650 1708 1267 1082 913 1058 1109 –

28.1 12.4 32.0 7.98 5.94 3.83 20.0 23.9 20.1 55.3 67.7 63.5 54.3 11.7 8.80 26.7 13.1 23.8 127 155 140 193 78.2 52.3 76.0 127 154 128 229 192 210 194 100 87 158 125 140 4.49 3.99 5.55 2.82 1.48 3.21 3.69 4.45 3.95 5.82 5.34 5.41 4.86 2.86 2.70 4.48 3.53 4.10 3.56 1.95 4.39 1.55 1.01 0.96 3.27 3.72 3.21 8.29 8.77 9.38 7.35 2.25 1.42 3.92 2.03 3.77 0.84 0.55 1.08 0.49 0.33 0.25 0.88 0.95 0.95 2.02 2.15 2.05 1.78 0.64 0.45 0.91 0.63 0.95 2.84 1.54 3.32 1.14 0.84 0.81 2.85 3.06 2.71 6.36 7.05 7.08 5.85 1.92 1.05 2.91 1.53 2.60 0.26 0.17 0.31 0.14 0.11 0.11 0.31 0.32 0.32 0.61 0.64 0.67 0.54 0.23 0.11 0.27 0.14 0.28 1.08 0.72 1.13 0.69 0.56 0.66 1.42 1.43 1.49 2.52 2.48 2.73 2.11 1.12 0.51 1.04 0.54 1.14 5.82 4.50 5.23 3.84 4.14 4.56 7.09 6.86 7.60 11.1 11.0 12.4 9.79 5.67 2.86 5.20 2.98 5.30 0.19 0.13 0.18 0.13 0.12 0.14 0.26 0.24 0.26 0.39 0.41 0.46 0.34 0.20 0.09 0.16 0.09 0.18 0.53 0.35 0.44 0.34 0.35 0.39 0.62 0.61 0.68 0.90 1.00 1.12 0.85 0.50 0.22 0.38 0.21 0.42 0.08 0.05 0.06 0.05 0.06 0.06 0.09 0.08 0.10 0.12 0.14 0.16 0.12 0.07 0.03 0.05 0.03 0.06 0.49 0.34 0.36 0.35 0.51 0.41 0.54 0.52 0.64 0.73 0.86 0.95 0.75 0.44 0.19 0.29 0.17 0.34 0.07 0.05 0.06 0.05 0.09 0.07 0.08 0.08 0.10 0.11 0.13 0.14 0.11 0.07 0.03 0.04 0.03 0.05 73.3 44.9 99.8 22.4 13.1 8.68 35.1 43.9 29.4 80.9 90.4 82.3 80.4 23.6 57.3 122 89.6 71.7 0.81 0.96 0.87 1.12 1.11 0.87 0.88 0.86 0.99 0.85 0.83 0.77 0.83 0.94 1.12 0.83 1.09 0.93 119 120 K-F. Yang et al. / Lithos 146–147 (2012) 112–127

5.1.3. Guojialing granodiorite The zircons in samples 08G32 and 08G37 from the Guojialing granodiorite are mostly prismatic and range from 50 to 150 μmin size. Most grains are transparent and pale yellow in color, and have oscillatory zoning. Some grains have circular or irregular cores mantled by euhedral overgrowths (Fig. 4a), similar to samples from the Linglong and Luanjiahe granites. 21 spots were analyzed from 19 grains in sample 08G32 yielding a weighted mean 206Pb/238U age of 129±1 Ma (2σ)(Fig. 4f; Supplemental electronic data Table 1), which is taken to define the crystallization age of the granodiorite. The other two grains show significantly older 207Pb/206Pb ages of 2435 Ma and 2438 Ma, which are likely to be inherited zircons from the basement of the eastern NCC. 20 spots on 15 grains from sample 08G37 yield a weighted mean 206Pb/238U age of 129±1 Ma (2σ) (Fig. 4g; Supplemental electronic data Table 1). Of the five remaining grains, one yields a 206Pb/238U age of 157 Ma, which is likely an inherited zircon from the Late Jurassic granitoid. The remaining four Fig. 5. R2 (R2=6Ca+2Mg +Al) versus R1 [R1=4Si−11(Na +K)−2(Fe+Ti)] plot fi 207 206 grains yield signi cantly older Pb/ Pb ages that range from for the granitoids in the northwestern Jiaodong Terrane. 1789 Ma to 2356 Ma, which are likely to be inherited zircons from (After De la Roche et al., 1980). the basement of the eastern NCC.

5.2. Major and trace elements suggesting their relatively more basic nature. All of the samples are metaluminous with low A/CNK ratios of 0.92–1.00 (Fig. 6). The Mg# Most of the Late Jurassic granitoids in the northwestern Jiaodong values of Guojialing granodiorites are higher than Linglong and Terrane, including the Linglong granite and Luanjiahe granite, have Luanjiahe granitoids, and range from 40.0 to 58.9 (Table 1). similar lithological features and emplacement ages. Their salient geo- Most of the Guojialing granodiorites have higher total REE content chemical features as obtained from this study are briefly described (ΣREE=55.1–404.1 ppm) than the Late Jurassic granitoids and are below. enriched in LREE [(La/Yb)N =23.6–122.6] (Fig. 8e). In the primitive The major and trace element data on all the granitoids examined mantle-normalized spider diagrams (Fig. 8f), all the samples are in this study are presented in Table 1. The SiO2 contents of the Late Ju- enriched in LILE such as Rb, Th, U, Ba and Sr, and depleted in HFSE rassic granitoids range from 69.2 wt.% to 75.9 wt.%. In the R1–R2 clas- such as Nb, Ta, Zr, Hf, P and Ti. Most of samples do not show signifi- sification diagram (De la Roche et al., 1980), most of the samples plot cant Eu anomalies (Eu/Eu*=0.77–1.12). The rocks are also enriched in the monzogranite and syenogranite fields (Fig. 5). All the in Sr (895–1809 ppm) and depleted in Y (2.86–12.4 ppm), and have samples are high in Na2O+K2O (7.12–9.32 wt.%) and low in CaO higher Sr/Y ratios and more obvious Nb and Ta negative anomaly (0.50–2.50 wt.%, average 1.38 wt.%), TFe2O3 (0.40–2.21 wt.%, aver- than the Linglong and Luanjiahe granitoids. age 1.24 wt.%) and MgO (0.06–0.46 wt.%). Most samples are peraluminous with high A/CNK ratio of 0.95–1.09 (Fig. 6). The Mg# values of these rocks are relatively low and range from 13.4 to 32.7 5.3. Sr–Nd isotopes (Table 1). Overall, many of the major oxides in the Late Jurassic granitoids show a strong negative correlation with SiO2 (correlation coef- Strontium and Nd isotopic compositions of the granitoids in the ficient from −0.6 to −0.9) (Fig. 7a, b and c), except for K2O which northwestern Jiaodong Terrane are presented in Table 2 and plotted 87 86 increases with SiO2 (r=+0.7) (Fig. 7d). These correlations imply in Fig. 9. The Linglong granites have uniform initial Sr/ Sr ratios the rocks are co-magmatic. Most of the Linglong granites have low total REE content (ΣREE=21.5–191.9 ppm) and are enriched in light rare earth elements (LREE) [(La/Yb)N =8.7–99.8] (Fig. 8a). The Luanjiahe granites also have low total REE contents (ΣREE=36.9–115.9 ppm) and are slightly more enriched in LREE [(La/Yb)N =7.2–54.1] (Fig. 8c), except for a few samples (08G01, 08G05, 08G52, and 08G53) that have high heavy rare earth element (HREE) contents and show flat HREE patterns in the chondrite-normalized REE diagram (Fig. 8c). In the primitive mantle-normalized spider diagrams (Fig. 8b, d), all samples from the Linglong and Luanjiahe granitoids are enriched in large ion lithophile elements (LILE) such as Rb, Ba, U and Sr, and depleted in high-field strength elements (HFSE) such as Nb, Ta, P and Ti, except for Zr and Hf. Samples are also enriched in Sr (288–1002 ppm) and depleted in Y (3.25–30.8 ppm), and have high Sr/Y ratios, which are features comparable with adakitic rocks (e.g., Defant and Drummond, 1990; Eyuboglu et al., 2011; Guo et al., 2006; Liu et al., 2009; Yu et al., 2011; Zhang et al., 2001). The silica contents of the Early Cretaceous Guojialing granodiorites range from 68.2 wt.% to 72.6 wt.%. In the R1–R2 classification diagram (De la Roche et al., 1980), nearly all of the samples plot in the granodiorite field (Fig. 5). Compared with the Linglong and Luanjiahe Fig. 6. A/NK [molar ratio Al2O3/(Na2O+K2O)] vs. A/CNK [molar ratio Al2O3/(CaO+ granitoids, the Guojialing granodiorites have higher CaO (1.99– Na2O+K2O)] plot for the granitoids in the northwestern Jiaodong Terrane. 2.83 wt.%), TFe2O3 (1.14–2.49 wt.%) and MgO (0.39–1.24 wt.%), (After Maniar and Piccoli, 1989). K-F. Yang et al. / Lithos 146–147 (2012) 112–127 121

that range from 0.711281 to 0.712418, and εNd(t) values that range The zircons from the Guojialing granodiorites (08G32 and 08G37) from −21.6 to −19.4. The isotope data from Luanjiahe granites clear- yield εHf(t) values that range from −24.2 to −18.6 with an average of ly deﬁne two groups (Fig. 9). One group has composition similar to −20.1 (except for the inherited zircons), which is slightly higher than that of the Linglong granites, but the other (samples 08G01, 08G02, the values of the Linglong and Luanjiahe granitoids. The inherited zir- 87 86 and 08G50) shows lower initial Sr/ Sr ratios that range from cons with ages of 1789–2438 Ma yield εHf(t) values that range from 0.708333 to 0.709672, suggesting that the Luanjiahe granites were −18.8 to 4.4 and plot mainly in the region between the 2.5 and derived from more complex magmatic source. The Guojialing grano- 3.0 Ga crustal evolution lines. diorites have relatively uniform initial 87Sr/86Sr ratios that range from 0.710175 to 0.711588, and εNd(t) values that range from −16.8 to −11.8, which is similar to the maﬁc dykes from the north- 6. Discussion western Jiaodong area (e.g., Yang et al., 2004)(Fig. 9). 6.1. Petrogenesis

5.4. Zircon Hf isotope data The Late Jurassic granitoids in northwestern Jiaodong Terrane have high Sr/Y ratios, and most of the samples plot in the adakite re- In situ Hf isotopic analyses of zircons from the granitoids in the gion in the Sr/Y vs. Y diagram (Fig. 11), suggesting that the Linglong northwestern Jiaodong Terrane are listed in Supplemental electronic and Luanjiahe granitoids may have formed in a high pressure envi- data Table 2 and plotted in Fig. 10. ronment. These characteristics are comparable with the C-type The zircons from the Linglong granites (08G33 and 08G59) yield adakitic rocks formed in thickened continental crust (e.g., Guo et al.,

εHf(t) values that range from −28.7 to −17.6 with an average of 2006; Liu et al., 2009; Zhang et al., 2001). Furthermore, most of the −25.1, except for the inherited zircons. One of the inherited zircons εHf(t) values of zircons from these granitoids plot in between the with an age of 2083 Ma yields an εHf(t)=0. The other grains with 2.5 and 3.0 Ga crustal evolution lines (Fig. 10), which indicates that ages of 751–776 Ma, 435–514 Ma and 208–240 Ma yield εHf(t) values the Late Jurassic granitic magma might have originated from partial ranging from −17.1 to −11.4, which mainly plot in between the 1.9 melting of the continental crust of the eastern NCC. Hou et al. and 2.5 Ga crustal evolution lines in the Hf isotopic evolution diagram (2007) proposed that the Linglong granitoids were derived by partial (Fig. 10). The age correlates with timing of the major crust formation melting of Neoarchean metamorphic lower crustal rocks, based on event in the Yangtze Craton (Chen and Jahn, 1998). detailed petrological and geochemical data. However, these granit- Zircons from the Luanjiahe granites (08G40 and 08G42) yield oids also contain abundant Neoproterozoic (683–774 Ma), Early Pa-

εHf(t) values that range from −28.2 to −17.4 with an average of leozoic (435–514 Ma) and Triassic (200–240 Ma) inherited zircons, −24.1, except for the inherited zircons. The inherited zircons with as well as some Late Archean (2857 Ma) and Paleoproterozoic 87 86 ages of 1792–2857 Ma yield εHf(t) values that range from −16.4 to (1792–2213 Ma) grains. The initial Sr/ Sr and εNd(t) values of 1.9 and mainly plot in between the 2.5 and 3.0 Ga crustal evolution most of the granitoids also plot between the region of upper crust lines or below these in Fig. 10, suggesting that these rocks formed of the NCC and lower crust of the Yangtze Craton (Fig. 9), which indi- from partial melting of the ancient continental crust in the eastern cates that the Late Jurassic granitoids possess a complex source NCC. The grains with ages of 683–742 Ma and 200–235 Ma yield composition.

εHf(t) values ranging from −19.3 to −5.6, which are similar to The eastern margin of the NCC has no major magmatic records dur- those of the Linglong granites. ing Neoproterozoic, although this period marks the main crustal

Fig. 7. Harker diagrams for the granitoids in the northwestern Jiaodong Terrane. Plots of MgO (a), Al2O3 (b), K2O (c), CaO (d), vs. SiO2 (wt.%). 122 K-F. Yang et al. / Lithos 146–147 (2012) 112–127 generation time of the Yangtze Craton (Chen and Jahn, 1998). There are result from the mixing of continental crustal materials derived from numerous Neoproterozoic granites or granitic gneisses distributed in the the Yangtze Craton, which were carried down by the subducted slab of Sulu orogenic belt, which are typical of the northern margin of the Yang- the Dabie–Sulu collisional orogeny. This appears more obvious in the tze Craton (Ames et al., 1996; Gao et al., 1996; Guo et al., 2005; Hacker et Luanjiahe granites. For example, four Luanjiahe granites samples al., 1998; Rowley et al., 1997; Zheng et al., 2007; Zhou et al., 2006). (08G01, 08G05, 08G52, and 08G53) are high in HREE and show ﬂat Therefore the Neoproterozoic inherited zircons in the Linglong and HREE patterns in the chondrite-normalized REE diagrams (Fig. 8c), Luanjiahe granitoids are likely to be derived from the Yangtze Craton. which is similar to the characteristic pattern of Neoproterozoic meta- As the Triassic marks the important period of Dabie–Sulu continental granites from the northern margin of Yangtze Craton (e.g., Hu et al., collision and exhumation of UHP metamorphic rocks, the presence of 2010). Among these, three samples (08G01, 08G05, and 08G53) plot Triassic inherited zircons in the Linglong and Luanjiahe granitoids sug- in the region of typical arc-derived rocks within the Sr/Y vs. Y diagram gests that the UHP metamorphic rocks or collision-related magmatic (Fig. 11), which is also similar to the Neoproterozoic granites from the rocks might have also contributed to the magma source of the Late Juras- Yangtze Craton (e.g., Zheng et al., 2006, 2008). Three more samples sic granitoids in the northwestern Jiaodong Terrane. Furthermore, there (08G01, 08G02, and 08G50) have relatively lower initial 87Sr/86Sr com- 87 86 is no obvious correlation between SiO2, εNd(t) and initial Sr/ Sr in the positions than the others, and plot close to the region deﬁning the lower 87 86 Late Jurassic granitoids, suggesting that source heterogeneity might crust of the Yangtze Craton in the εNd(t) versus initial Sr/ Sr diagram have played an important role in the magma evolution rather than (Fig. 9), which is similar to the isotope composition of Late Triassic sye- crustal contamination during emplacement. This heterogeneity may nite in Sulu orogenic belt (Yang et al., 2005). These characteristics show

Fig. 8. Chondrite-normalized REE patterns and Primitive Mantle (PM) normalized trace element diagrams for Linglong granites (a, b), Luanjiahe granites (c, d) and Guojialing granodiorites (e, f). Chondrite and PM values are from Sun and McDonough (1989). K-F. Yang et al. / Lithos 146–147 (2012) 112–127 123

Table 2 Sr–Nd isotopic compositions for the Jiaodong granitoids.

87 86 87 86 87 86 147 144 143 144 Sample Rb (ppm) Sr (ppm) Rb/ Sr Sr/ Sr ±2σ Sr/ Sr (i) Sm (ppm) Nd (ppm) Sm/ Nd Nd/ Nd ±2σεNd(t) Luanjiahe granite 08G01 124.7 344.9 1.0473 0.712054 0.000014 0.709672 1.4 7.3 0.1137 0.511652 0.000011 −17.6 08G02 172.5 359.5 1.3895 0.712197 0.000013 0.709037 1.2 6.3 0.1104 0.511643 0.000013 −17.7 08G20 123.3 479.4 0.7451 0.713781 0.000012 0.712086 3.3 22.1 0.0897 0.511456 0.000012 −20.9 08G40 72.0 993.4 0.2098 0.712334 0.000014 0.711856 1.6 11.7 0.0835 0.511446 0.000021 −20.9 08G42 141.7 372.3 1.1027 0.714291 0.000014 0.711783 1.4 6.4 0.1348 0.511471 0.000012 −21.5 08G50 98.5 957.1 0.2980 0.709010 0.000012 0.708333 1.8 13.3 0.0833 0.511446 0.000014 −20.9 08G53 153.6 417.7 1.0652 0.714551 0.000013 0.712128 2.5 9.4 0.1586 0.511519 0.000016 −21.1

Linglong granite 08G15 108.3 668.8 0.4689 0.713194 0.000014 0.712128 3.2 24.3 0.0798 0.511437 0.000011 −21.1 08G17 90.1 702.8 0.3714 0.713263 0.000013 0.712418 2.6 18.9 0.0839 0.511421 0.000011 −21.4 08G21 128.2 291.2 1.2757 0.714697 0.000013 0.711795 2.1 8.4 0.1484 0.511509 0.000011 −21.1 08G33 70.0 976.8 0.2074 0.711753 0.000014 0.711281 2.0 13.2 0.0913 0.511447 0.000013 −21.1 08G38 74.7 916.6 0.2358 0.712239 0.000015 0.711703 3.7 25.0 0.0886 0.511420 0.000013 −21.6 08G59 149.7 376.9 1.1504 0.714674 0.000014 0.712058 0.8 3.3 0.1481 0.511593 0.000016 −19.4

Guojialing granodiorite 08G08 84.1 1109.2 0.2195 0.711106 0.000013 0.710700 4.0 25.7 0.0948 0.511948 0.000013 −11.8 08G25 71.2 1744.9 0.1181 0.711417 0.000012 0.711199 8.5 58.2 0.0884 0.511715 0.000014 −16.2 08G29 66.7 1708.3 0.1130 0.711237 0.000012 0.711028 8.4 89.6 0.0569 0.511777 0.000013 −14.5 08G30 49.8 1214.3 0.1187 0.711620 0.000013 0.711401 1.9 10.5 0.1078 0.511801 0.000012 −14.9 08G32 84.2 895.3 0.2724 0.712066 0.000013 0.711563 3.4 21.0 0.0989 0.511692 0.000014 −16.8 08G37 76.1 1025.5 0.2148 0.711985 0.000015 0.711588 1.9 11.7 0.0969 0.511727 0.000019 −16.1 08G61 318.9 1076.1 0.8583 0.711761 0.000015 0.710175 3.3 23.0 0.0862 0.511693 0.000013 −16.6 that the magma source of the Luanjiahe granites may have more in com- subduction of south Mongolia from the north since Late Carbonifer- mon with crustal materials of the Yangtze Craton than the eastern NCC. ous (Li et al., 2009; Zhang et al., 2007), Yangtze Craton from the The Early Cretaceous granodiorites in the northwestern Jiaodong south since Late Triassic (Yang et al., 2007a, b) and especially the Pa- Terrane show large variations when compared with the Late Jurassic cific Plate from the east since Late Triassic–Early Jurassic beneath the granitoids in terms of emplacement age and geochemistry. The NCC (Santosh, 2010; Wu et al., 2007; Zhou et al., 2009, 2010), and the granodiorites are metaluminous with high CaO and MgO contents. water derived from the subducted plate remarkably weakened the Most samples are enriched in LREE and show strong fractionation be- sub-continental lithosphere and accordingly facilitated or triggered tween LREE and HREE [(La/Yb)N values range from 23.6 to 122] the cratonic destruction (Windley et al., 2010). (Table 1). The rocks are also enriched in Sr and depleted in Y, and The late Jurassic, the mountain root of Jiaodong Terrene gradually have higher Sr/Y ratios than the Linglong and Luanjiahe granitoids. underwent collapse due to post-collisional lithospheric extension and All of the samples plot in the adakite region in the Sr/Y vs. Y diagrams regional thermal anomaly (Zhang, 2009). As mentioned above, the (Fig. 11). However, unlike typical adakitic rocks, the Guojialing grano- Late Jurassic granitoids (157–159 Ma) in the Jiaodong Terrane at the 87 86 diorites have high initial Sr/ Sr and negative εNd(t) values, which is eastern margin of the NCC are crustal-derived granites emplaced similar to the TTG rocks and mafic dykes from the Jiaodong Terrane after the Dabie–Sulu continental collision and exhumation of UHP (Yang et al., 2003a). The common presence of Paleoproterozoic (1789–2438 Ma) inherited zircons shows that basement rocks of the eastern NCC were involved in the formation of the Guojialing granodiorites. Nevertheless, the zircon εHf(t) values of the granodiorites are less negative than the Linglong and Luanjiahe granitoids and plot above the 2.5 Ga crustal evolution line (Fig. 10). The εNd(t) values of granodiorites are also higher than the Late Jurassic granitoids, and plot close to mafic dykes from the Jiaodong Terrane in Fig. 9, which suggest that some mantle source components were involved in the formation of these rock. Yang et al. (2003a) proposed that the Guojialing granodiorites were derived from dehydrational partial melting of mafic lower crust altered by ancient underplated mantle- derived magma. Hou et al. (2007) argued that the Guojialing suite was formed by the reaction of delaminated eclogitic crust derived melt with the upwelling asthenospheric mantle. There are various in- dications that the Guojialing granodiorite was likely the result of crust–mantle mixing.

ε 87 86 6.2. Tectonic implications Fig. 9. Nd(t) versus initial Sr/ Sr diagram for the granitoids from the northwestern Jiaodong Terrane. The isotopic composition of maﬁc dykes from Jiaodong (Yang et al., 2004) and syenites from Sulu UHP metamorphic belt (Yang et al., 2005)areshownfor Guo et al. (2005) and Zhang et al. (2001) argued that the eastern comparison. The ﬁelds for lower crust of the Yangtze Craton, upper and lower crusts of part of the NCC underwent crustal thickening in the Mesozoic, the NCC are from Jahn et al. (1999). DM, EM1 and EM2 are from Zindler and Hart 87 86 ε which might have resulted from the collision between the NCC and (1986). The ( Sr/ Sr)i and Nd(t) values of Linglong and Luanjiahe granitoids are rec- alculated at 160 Ma and the Guojialing granodiorites at 130 Ma. Chondrite Uniform the Yangtze Craton. Windley et al. (2010) also proposed that post- 87 86 87 86 Reservoir (CHUR) values of Rb/ Sr=0.0847 and Sr/ Sr=0.7045 (λRb= collisional thrusting thickened considerably the lower crust and the −11 −1 147 144 143 144 1.42×10 year ), and Sm/ Nd=0.1967 and Nd/ Nd=0.512638 (λSm= upper mantle root of the eastern NCC in the Jurassic. Multiple 6.54×10−12 year−1)(Lugmair and Marti, 1978) are used for the calculation. 124 K-F. Yang et al. / Lithos 146–147 (2012) 112–127

Fig. 10. Diagram of Hf isotopic evolution in zircons for each sample analyzed. CHUR, chondritic uniform reservoir; CC, continental crust. Depleted mantle evolution is calculated by using εHf(t)=16.9 at t=0 Ga and εHf(t)=6.4 at t=3.0 Ga. The corresponding lines of crustal extraction are calculated by using the 176Lu/177Hf ratio of 0.015 for the average 176 177 continental crust (Griffinetal.,2002). The parameters of ( Lu/ Hf)CHUR =0.0332 176 177 176 177 176 177 and ( Hf/ Hf)CHUR=0.282772, and ( Lu/ Hf)DM=0.0384 and ( Hf/ Hf)DM= −11 −1 Fig. 12. Tectonic discrimination diagram for the granitoids in the northwestern 0.28325 (λLu=1.867×10 year )(Blichert-Toft and Albaréde, 1997; Griffinetal., 2000; Söderlund et al., 2004) were applied to the calculation. Jiaodong Terrane. Fields indicate island arc granitoids (IAG), continental arc granitoids (CAG), continental collision granitoids (CCG), post-collisional granitoids (POG), rift- related granitoids (RRG) and continental epeirogenic uplift granitoids (CEUG). metamorphic rocks. They plot mostly in the post-collisional granitoid (After Maniar and Piccoli, 1989). (POG) field in tectonic discrimination diagram (Fig. 12). Contempo- rary granitoids are also found in the Sulu orogenic belt such as the Accompanied with asthenosphere upwelling, the eastern margin of Kunyushan pluton (Guo et al., 2005). The Jurassic granitoids have the NCC entered a phase of cratonic destruction and lithospheric thin- trace element compositions similar to those of adakitic rocks, which ning (Gao et al., 2002, 2009). The Guojialing granodiorites formed at formed under high pressure conditions and likely originated from this stage with emplacement ages of 128–130 Ma. There are also abun- the partial melting of residual thickened Archean lower crust dant felsic and mafic igneous rocks of Early Cretaceous (110–130 Ma) (Fig. 13a). The presence of a large number of inherited zircons, espe- age distributed not only along the margin of the NCC (e.g., Dabie–Sulu cially the Neoproterozoic and Early Paleozoic populations that are orogenic belt, Jiaodong and Liaodong peninsulas) but also within the representative for the Yangtze Craton, shows that the Late Jurassic craton (e.g., Luxi Terrane, Yangshan and Taihang mountains, Fan et al., granitoids have a relatively complex magmatic source composition. 2001; Goss et al., 2010; Guo et al., 2005; Kusky et al., 2007c; Wilde et These crustal materials of the Yangtze Craton, including the al., 2003; Wu et al., 2005; Ying et al., 2006; Zhao and Zheng, 2009). Neoproterozoic granites, were likely carried beneath the eastern These intrusives are considered as a principle marker for cratonic de- NCC by the subducted slab during the process of Dabie–Sulu conti- struction and lithospheric thinning of the NCC (Xu et al., 2004, 2009). nental collision in the Triassic. The melts derived from the subducted Such a major magmatic event must be related to strong lithospheric ex- Yangtze Craton accordingly promoted reactivating and partial melt- tension and large-scale asthenospheric upwelling. Previous research ing of the residual Archean lower crust, thus forming the adakitic has attempted to explain the tectonic milieu including: a) collision be- Linglong and Luanjiahe granitoids in the northwestern Jiaodong tween the NCC and the Yangtze Craton (Gao et al., 1998; Li et al., Terrane, which preserve the age signature of the Yangtze Craton. 1993; Yang et al., 2007a, b), b) collision between India and the Eurasian Plates (Menzies et al., 1993), c) collision between the Siberian and North China–Mongolia Plates (Meng, 2003; Zorin, 1999), d) subduction of the Pacific Plate beneath China (Fan et al., 2000; Goss et al., 2010; Tatsunoto et al., 1992; Wu et al., 2005; Xu, 2007; Yang et al., 2003b), and e) a mantle plume (Deng et al., 2004). Subduction of the Pacific Plate is considered as the most likely explanation for lithospheric thinning in the eastern NCC (Goss et al., 2010; Santosh, 2010; Xu et al., 2009). During the Early Cretaceous, subduction of the PacificPlatebe- neath the NCC, possibly with slab break-off and roll back, led to back- arc spreading and asthenospheric upwelling, which would aid lithospheric thinning and partial delamination. This in turn led to partial melting of the lithospheric mantle, and the resulting mafic magmas were underplated below eastern China (Goss et al., 2010). These magmas provided the heat source for crustal melting which produced

the Early Cretaceous granodiorites (127–129 Ma). The high εHf(t) values of these rocks also indicate that mantle components were involved in the formation of the Guojialing granodiorites. Although the Guojialing granodiorites have adakitic compositions similar to that of the Linglong and Luanjiahe granitoids, their petrogenesis and tectonic setting are markedly different. The majority of samples of Linglong and Luanjiahe granitoids plot in the POG region Fig. 11. Plot of Sr/Y versus Y for the granitoids in the northwestern Jiaodong Terrane. in the tectonic discrimination diagram (Fig. 12), albeit the Guojialing (After Defant and Drummond, 1990). granodiorites plot in the island arc granitoids (IAG), continental arc K-F. Yang et al. / Lithos 146–147 (2012) 112–127 125

Fig. 13. Schematic map of Mesozoic lithospheric evolution of the Jiaodong Terrane. (Modiﬁed after Groves and Bierlein, 2007).

granitoids (CAG) and continental collision granitoids (CCG) fields and also have higher εNd(t) values than the Late Jurassic granitoids, (Fig. 12). The former may result from reactivation of Archean lower indicating that some mantle components were involved in the mag- crust and post-collisional lithospheric extension (Fig. 13a), but the matic source, and this was possibly triggered by subduction of the Pa- latter is likely triggered by subduction of the Pacific Plate beneath cific Plate beneath the NCC and accompanied by asthenospheric the NCC and associated asthenospheric upwelling (Fig. 13b). It is upwelling. worth mentioning that no Neoproterozoic or Early Paleozoic Supplementary materials related to this article can be found on- inherited zircons are found in the Guojialing granodiorites, which in- line at http://dx.doi.org/10.1016/j.lithos.2012.04.035. dicates that previous continental lithosphere of the eastern NCC in northwestern Jiaodong Terrane that was mixed with crustal materials Acknowledgments from the Yangtze Craton, was either lost or exhausted. We owe our special thanks to Professor Hong-Fu Zhang, Dr. C.V. Dharma Rao and Editor-in-Chief Professor Nelson Eby for their 7. Conclusions many pertinent comments and patient revisions that greatly im- proved the manuscript. We are grateful to Chao-Feng Li and Xiang- The Linglong and Luanjiahe granitoids were emplaced in the Hui Li for help during Sr and Nd isotope analyses and Zhao-Chu Hu Late Jurassic (157–159 Ma), and contain abundant Late Archean, for help during zircon LA ICP-MS U–Pb dating. This study was finan- Paleoproterozoic, Neoproterozoic, Early Paleozoic and Triassic cially supported by the Natural Science Foundation of China inherited zircons, implying the involvement of continental crustal (41173056) and the Crisis Mines Continued Resources Exploration materials from both the eastern NCC and the Yangtze Craton. The Project of the China Geological Survey (20089930). Guojialing granodiorites were emplaced in the Early Cretaceous (129 Ma), and contain abundant Late Archean and Paleoproterozoic inherited zircons, but no Neoproterozoic and Early Paleozoic zir- References cons are present. – The Late Jurassic granitoids in the northwestern Jiaodong Terrane Ames, L., Tilton, G.R., Zhou, G., 1993. Timing of collision of the Sino Korean and Yangtze Cratons: U–Pb zircon dating of coesite-bearing eclogites. Geology 21, 339–342. are peraluminous with enrichment in LREE and depletion in HFSE. Ames, L., Zhou, G.Z., Xiong, B.C., 1996. Geochronology and isotopic character of – The rocks are also high in Sr/Y and low in εHf(t) and plot in between ultrahigh-pressure metamorphism with implications for collision of the Sino – the 2.5 and 3.0 Ga crustal evolution lines, suggesting that the Linglong Korean and Yangtze Cratons, central China. Tectonics 15, 472 489. BGMRS, 1991. Regional Geology of the Shandong Province. Geological Memories, Series and Luanjiahe granitoids were formed under relatively high pressure 1, 26. Geological Publishing House, Beijing. in Chinese. conditions, and were likely derived from the partial melting of a re- Blichert-Toft, J., Albaréde, F., 1997. The Lu–Hf isotope geochemistry of chondrites and sidual thickened Archean lower crust. the evolution of the mantle–crust system. Earth and Planetary Science Letters 148, 243–258. The Early Cretaceous granodiorites are metaluminous with enrich- Chen, J., Jahn, B.M., 1998. Crustal evolution of southeastern China: Nd and Sr isotopic ment in LREE and depletion in HFSE. They show high in MgO and Sr/Y, evidence. Tectonophysics 284, 101–133. 126 K-F. Yang et al. / Lithos 146–147 (2012) 112–127

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