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Journal of Asian Earth Sciences 72 (2013) 178–189

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Journal of Asian Earth Sciences

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Delineation of the ca. 2.7 Ga TTG gneisses in the Zanhuang Complex, North China Craton and its geological implications ⇑ Chonghui Yang a, , Lilin Du a, Liudong Ren a, Huixia Song a, Yusheng Wan a,b, Hangqiang Xie a,b, Yuansheng Geng a a Institute of Geology, Chinese Academy of Geological Sciences, Beijing 100037, China b Beijing SHRIMP Center, Beijing 100037, China article info abstract

Article history: Through detailed studies we have delineated a suite of banded TTG gneisses from the Zanhuang Complex. Available online 16 October 2012 The protolith of the gneisses, predominantly tonalite, has undergone intensive metamorphism, deforma- tion and anatexis and in a banded structure is intimately associated with melanocratic dioritic gneiss and Keywords: leucocratic trondhjemitic veins. SHRIMP Zircon U–Pb data show that the tonalite was formed ca. TTG gneisses 2692 ± 12 Ma ago. The tonalitic gneiss has the features of high SiO2 (67.76–73.31%), high Al2O3 (14.38– ca. 2.7 Ga 15.83%), rich in Na2O (4.48–5.07%) and poor in K2O (0.77–1.93%). The gneiss is strongly fractioned in Geochemistry REE ((La/Yb) = 12.02–24.65) and shows a weak positive Eu anomaly (Eu/EuÃ = 1.05–1.64). It has high Zanhuang Complex N contents of Ba (199–588 ppm) and Sr (200–408 ppm), low contents of Yb (0.32–1.00 ppm) and Y North China Craton (3.41–10.3 ppm) with high Sr/Y ratios (21.77–96.77) and depletion in HFSE Nb, Ta and Ti. These charac-

teristics are similar to those of the high-Si adakitic rocks. The melanocratic dioritic gneiss has low SiO2

(59.81%), high MgO (6.34%), high Al2O3 (14.02%) contents, rich in Na2O (3.7%) and poor in K2O (1.79%), with high Mg index (Mg# = 67). REE and trace elements are on the whole similar to that of the tonalitic gneiss, but compatible element abundances V (116 ppm), Cr (249 ppm), Co (37 ppm) and Ni (179 ppm) are higher. The leucocratic felsic bands (approximating trondhjemite in composition) have major oxides similar to that of the TTG gneisses but the REE and compatible elements are extremely low, which are

indicative of the products of anatexis. The tonalitic gneiss has positive eNd(t) (2.37–3.29) and low initial Sr (0.69719–0.70068) values with depleted mantle Nd model age of ca. 2.8 Ga, suggesting its generation from partial melting of mantle-derived juvenile crust. The dioritic gneiss was also derived from subduction environment, but has undergone signiﬁcant metasomatism of mantle wedge. The delineation of the ca. 2.7 Ga TTG gneisses in the Zanhuang Complex further proves that the North China Craton experienced large-scale continental crustal accretion in early Neoarchean, and gives new constraints on the subdivision of the early blocks and greenstone belts of the craton. Ó 2012 Elsevier Ltd. All rights reserved.

1. Introduction et al., 1992; Jahn et al., 1998), the Pilbara and Yilgarn Cratons in Western Australia (Nelson, 1997; Bateman et al., 2001; Rasmussen ca. 2.7 Ga tectonothermal events have been recorded world- et al., 2005; Said et al., 2010), the Kaapvaal and Zimbabwe Cratons wide from the Archean Cratons, e.g. the Superior Craton in southern Africa (Kröner et al., 1999; Matthew et al., 1999; Poujol (Beakhouse et al., 1999; Henry et al., 2000; Polat and Kerrich, et al., 2003; Hofmann et al., 2004; Taylor et al., 2010), and the 2000, 2002; Percival et al., 2001; Polat and Münker, 2004), the Dharwar Craton in India (Nutman et al., 1996; Manikyamba and Wyoming Craton (Carlson and Irving, 1994; Rino et al., 2004), the Kerrich, 2011). The ca. 2.7 Ga events are recognized as a large-scale western Canada Shield (Wyman, 1999; Sandeman et al., 2006) tectonothermal event in the Earth’s history, responsible for the ra- and the southern West Greenland Craton (Friend et al., 1996; pid accretion of the continental crust in a short time span, mani- Thrane, 2002; Steenfelt et al., 2005; Friend and Nutman, 2005; festing the formation of voluminous extrusive and intrusive rocks Polat et al., 2010) in North America, the Baltic Shield in Europe (Condie, 2000; Condie et al., 2009; Condie and Aster, 2010; Barley (Bibikova et al., 2005; Balagansky et al., 2011; Heilimo et al., et al., 2005; Zhai and Santosh, 2011; Wan et al., 2011a). In the 2011; Mikkola et al., 2011) and the Aldan Shield in Siberia (Nutman North China Craton (referred to as NCC hereafter), the most distinguished magmatic event was at ca. 2.5 Ga, as also recorded in the Pilbara Craton, the Dharwar Craton, the West Greenland Craton ⇑ Corresponding author. Tel.: +86 10 68999708; fax: +86 10 68997803. as well as in the East Antarctic Shield (Jayananda et al., 2000; Shen E-mail address: [email protected] (C. Yang).

C. Yang et al. / Journal of Asian Earth Sciences 72 (2013) 178–189 179 et al., 2005; Condie et al., 2009; Nutman et al., 2010; Wan et al., Group in the northwest, are in tectonic contact with the Guandu 2011b). Though well-manifested in the xenocrystic/inherited or Group in the east, while in the southwest the boundary has not detrital zircon U–Pb data and Hf model ages of the North China yet been delineated due to discontinuous outcroups (Fig. 1). The Craton (Shen et al., 2005; Geng et al., 2011), the ca. 2.7 Ga event banded gneisses consist mainly of tonalitic gneiss and melanocrat- is discerned there merely in a few areas within the craton, e.g. ic dioritic gneiss with common occurrence of amphibolite enclaves. the western Shandong terrane (Cao, 1996; Zhuang et al., 1997; This suite of gneisses is distinguished by the development of leuc- Jahn et al., 1988; Du et al., 2003, 2010; Lu et al., 2008; Wang ocratic felsic bands which can be subdivided into two generations. et al., 2009; Wan et al., 2011b), the Jiaodong–Qixia region (Jahn Bands of the earlier generation are parallel to the foliation, 1–2 cm et al., 2008) in Shandong Province and the Huoqiu area in northern in width, dominated by fine-grained plagioclase and quartz Anhui Province (Wan et al., 2010). In the Fuping Complex, Taihang (Fig. 2a); bands of the later generation are wider, 5–20 cm, lying Mts., enclaves of ca. 2.7 Ga hornblende gneiss are found in the TTG generally parallel to, but locally discordant to, the foliation gneisses (Guan et al., 2002), and in Lushan county in western He- (Fig. 2b), composed mainly of medium-to-coarse-grained plagio- nan Province, vestiges of the earlier ca. 2.8 Ga magmatism have clase and quartz. In most cases the bands have straight boundaries been recorded (Kröner et al., 1988; Sun et al., 1994; Liu et al., (Fig. 2a) but sometimes sigmoidal folds occur (Fig. 2c). The bands 2009a; Diwu et al., 2010). Other Archean TTG gneisses of the are heterogeneously distributed and where least developed more NCC are predominantly at 2.5–2.6 Ga. In this paper we delineate protolith features are preserved (Fig. 2d and e). well-exposed ca. 2.7 Ga banded TTG gneisses from the Zanhuang The samples collected are as follows: Z07-6 (Fig. 2e), Z09-1 Complex of the central NCC (Fig. 1). On the basis of petrographical, (Fig. 2d), Z87-1 (Fig. 2f) and Z88-1 (Fig. 2g) for banded tonalitic geochemical, zircon SHRIMP dating and Sr–Nd isotope studies, we gneiss; Z88-4 (Fig. 2g and h) for melanocratic dioritic gneiss, discuss the formation age, magma source, origin and dynamic set- Z88-2 for fine-grained gneissic trondhjemitic veins (Fig. 2g) and ting of the TTG gneisses in an attempt to give new constraints on Z88-3 for medium-coarse-grained trondhjemitic (granitic) veins the basement subdivision and tectonic evolution of the NCC. (Fig. 2g). The banded tonalitic gneiss (samples Z07-6, Z09-1, Z87-1 and Z88-1) is gray, medium-grained and granoblastic in texture. Major 2. Regional geology minerals are biotite, plagioclase and quartz, with minor epidote, muscovite and chlorite, accessory zircon, apatite and magnetite. The Zanhuang Complex occurs in the southern Taihang In some samples, quartz grains are rectangularly shaped and dis- Mountains and belongs to the middle eastern segment of the tributed like ribbons, suggesting static recrystallization after Trans-North China Orogen as delineated by Zhao et al. (2005). mylonitic quartz ribbons. The complex is mainly composed of deformed and metamorphosed Dioritic gneiss (Z88-4) is banded, or lenticular in occurrence and early Precambrian TTG gneisses, monzonitic and potassic granite, in intimate association with tonalitic gneiss (Fig. 2a and h). The with minor supracrustal rocks (Fig. 1), with the TTG gneisses occu- rock has a gneissic structure with few strips developed. Major min- pying some 60% of the area (Trap et al., 2009; Xiao et al., 2011; erals include biotite (10%), hornblende (20%), plagioclase (55%) and Yang et al., 2011a,b). Conventionally the complex as a whole was quartz (15%), with minor epidote and chlorite (<1%). regarded as a single sequence of metamorphic rocks and was Fine-grained gneissic trondhjemitic vein (Z88-2) mostly forms named the Zanhuang Group. Thus according to foliation, a mono- concordant intrusive sheets in the tonalitic gneiss but locally the clinic sequence younging from east to west was discerned and four sheets are discordant. The rock is gneissic in structure and com- formations of Fangjiapu, Shicheng, Honghe and Shijialan were posed of major quartz (some 25%), plagioclase (65%) and micro- named successively from old to young (HBGMR, 1989). The cline (5%), and minor muscovite (2%), biotite and epidote (1–2%). Fangjiapu, Shicheng and Shijialan Formations are consisted of var- Medium-to-coarse-grained trondhjemitic vein (Z88-3) is ious gneisses, while the Honghe Formation is consisted of quartz- weakly foliated and massive in structure, discordantly intruding ite, mica schist and marble (HBGMR, 1989). With further the foliation and bands of the tonalitic gneiss. The rock is domi- research on the complex in recent years, knowledge of the early nated by quartz (35%) and plagioclase (60%), with minor microcline Precambrian sequence pattern has been substantially updated. A (1%), muscovite (1%), biotite (1%) and epidote (1–2%). large volume of TTG gneisses, potassic–monzogranitic gneisses and granites have been removed from the original Zanhuang Group and the remnant minor supracrustal rocks were redefined as 4. Analytical methods Archean Zanhuang Group sensu stricto, apart from the Honghe Formation that was renamed as the Paleoproterozoic Guandu For whole rock analysis, samples were crushed to 200-mesh Group (Yang et al., 2011a,b) (for details see Fig. 1). size for analysis. The major oxides, trace elements and REE con- The meta-plutonic rocks of the Zanhuang Complex can be sub- tents are measured in the Institute of Geological Analysis, Chinese divided into two distinct types. One is banded gneiss with well- Academy of Geological Sciences; the major oxides by XRF with a developed leucocratic felsic bands mostly parallel to the foliation, Rigaku 3080E instrument and the others by ICP-MS. Uncertainties being dominated by tonalitic gneiss and intimately associated with depend upon the concentration in the sample, but generally for melanocratic dioritic gneiss. The other has no leucocratic felsic XRF and ICP-MS are estimated at ±3–5% and ±3–8%, respectively. bands but is rather complicated, composed mainly of tonalitic Zircons were separated by using the conventional heavy liquid gneiss, granodioritic gneiss and monzogranitic–potassic granitic and magnetic techniques and purified by handpicking under a bin- gneiss with an age of 2.51–2.50 Ga (Yang et al., 2011b). ocular microscope at the Hebei Institute of Geological Survey. Zir- con CL images were taken in the scanning electronic microscope 3. TTG gneisses laboratory of the Beijing Center of Ion Microprobe Analyses, with a working voltage at 15 kV, current 4 nA. Zircon SHRIMP U–Pb dat- The banded TTG gneisses are mainly distributed in the area of ing was carried out on the SHRIMP II instrument of the Curtin Uni- Yuantou town, southern Zanhuang County to Haozhuang– versity, western Australia, through remote control system in the Mengjiazhuang villages, Lincheng County. The gneisses are Beijing SHRIMP Center. intruded by the Paleoproterozoic Xuting K-granite to the north, Analytical principles and procedures are referred to Williams and are unconformably overlain by the Paleoproterozoic Gantaohe (1998) and Nelson (1999). Zircon standard SL13 was used for U, Author's personal copy

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Fig. 1. Geological sketch map of the Zanhuang Complex in the Zanhuang–Xingtai area (modiﬁed after Yang et al. (2011b)), inset after Zhao et al. (2005).

Th, Pb abundance calibration (U = 238 ppm, Williams, 1998), and individual analysis are quoted at 1r level. The ﬁnal results are standard zircon TEMORA1 (238U/206Pb age = 417 Ma) was used for the weighted average of the 207Pb/206Pb ages, errors are quoted age calibration (Black et al., 2003). Mass resolution was over at the 95% conﬁdence level. 5000 (1% peak height), the intensity of the primary ion beam Combined chemical separation of Sm and Nd and isotope ratio

O2 = 1.8–2 nA, spot sizes about 25–30 lm. The ratio of TEMORA1 measurement were performed in the Solid Isotope Geochemistry to unknown analyses was 1:4, with 5 scans through the masses. Laboratory of Institute of Geology and Geophysics, Chinese Acad- Data processing and assessment was carried out using the emy of Sciences. Details of the procedures were described by Zhang SQUID1.02 and ISPLOT programs (Ludwig, 2001). Common lead and Ye (1987). The instrument used was MAT-262 TIMS produced was corrected by using measured 204Pb contents. Age errors on by Finnigan Company, Germany. Nd isotope fractionation was Author's personal copy

C. Yang et al. / Journal of Asian Earth Sciences 72 (2013) 178–189 181

Fig. 2. Field photos of the TTG gneisses (see the text for description). corrected by 146Nd/144Nd = 0.7219. The laboratory background of disconcordant and < 2500 Ma. These sites have been disturbed in Sm and Nd in measuring procedure is less than 50 pg. younger geological events and do not provide direct information on the igneous age. However, regression of this data gives an upper intercept at 2677 ± 13 Ma (MSWD = 2.6). One analysis has indistin- 5. Zircon SHRIMP U–Pb ages guishable 238U/206Pb and 207Pb/206Pb with a 207Pb/206Pb age at 2692 ± 12 Ma (Fig. 4). So the crystallization age of zircons is in The banded tonalitic gneiss sample chosen for zircon U–Pb dat- the range of 2677–2692 Ma and the concordant age of 2692 Ma ing was sample Z09-1. Zircons are light pink and adamantine in is regarded as the real crystallization age of zircons. color, subhedral prismatic and most bipyramidal terminations are rounded. On the surface there are corrosion pits, transparent to semitransparent with fractures developed, suggesting minor 6. Geochemical characteristics zircon dissolution during anatexis. The grains are mostly long columnar and are predominantly 50À100 lm long with some 6.1. Major oxides 100–150 lm long. The length/width ratio is 2–4. In CL images the zircon luminescence is low and shows dense Results of analyses are given in Table 2. Banded tonalitic gneis- oscillatory zones (Fig. 3). Surface morphology and internal texture ses of the Zanhuang Complex have high SiO2 (67.76–73.31%), high of the zircons indicate a typical magmatic origin. Al2O3 (14.38–15.83%), rich in Na2O (4.48–5.07%) and low K2O Thirty-two grains were selected for analysis (Table 1). Most Th/ (0.77–1.93%) (Table 2). The contents of MgO are low, 0.65–1.48%,

U ratios are in the range of 0.30–0.8, with a few higher to 1.0–4.07. and that of TiO2 and P2O5 are even lower, 0.22–0.42% and 0.07– Ã Some are as lower to < 0.10 but in these cases the ages are all 0.13%, respectively. The total Fe2O3 + MgO + MnO + TiO2 is also Author's personal copy

182 C. Yang et al. / Journal of Asian Earth Sciences 72 (2013) 178–189

Fig. 3. CL images of zircon from the banded tonalitic gneiss in the Zanhuang Complex.

Table 1 SHRIMP U–Pb data of zircon from the banded tonalitic gneiss in the Zanhuang Complex.

206 232 238 206 ⁄ 207 ⁄ 206 ⁄ 207 ⁄ 235 206 ⁄ 238 206 238 207 206 Spot % Pbc ppm U ppm Th Th/ U ppm Pb Pb / Pb ±% Pb / U±% Pb / U ±% err corr Pb/ U Age Pb/ Pb Age % Discordant

Z09-1-1.1 0.02 222 177 0.82 99.9 0.1843 0.73 13.31 1.1 0.5240 0.83 .748 2716 ± 18 2692 ± 12 À1 Z09-1-2.1 0.07 229 83 0.37 86.9 0.1803 0.71 11.00 1.1 0.4422 0.84 .762 2360 ± 17 2656 ± 12 11 Z09-1-3.1 0.05 935 294 0.33 345 0.17928 0.34 10.614 0.59 0.4294 0.48 .813 2303 ± 9.3 2646.2 ± 5.7 13 Z09-1-4.1 0.46 198 279 1.46 60.9 0.1684 1.0 8.26 1.3 0.3558 0.87 .645 1962 ± 15 2542 ± 17 23 Z09-1-5.1 0.01 235 184 0.81 99.3 0.1818 0.63 12.34 1.0 0.4923 0.81 .789 2581 ± 17 2669 ± 10 3 Z09-1-6.1 0.24 268 1056 4.07 113 0.1823 0.68 12.33 1.1 0.4906 0.85 .783 2573 ± 18 2674 ± 11 4 Z09-1-7.1 0.22 173 125 0.75 64.3 0.1775 0.60 10.54 1.4 0.4306 1.3 .906 2308 ± 25 2629 ± 10 12 Z09-1-8.1 0.07 568 89 0.16 187 0.16907 0.31 8.93 1.2 0.3829 1.1 .964 2090 ± 20 2548.5 ± 5.2 18 Z09-1-9.1 0.11 463 251 0.56 147 0.17099 0.36 8.70 1.2 0.3688 1.1 .953 2024 ± 20 2567.5 ± 6.1 21 Z09-1-10.1 0.07 197 85 0.45 67.4 0.1765 0.93 9.68 1.5 0.3977 1.2 .795 2158 ± 22 2620 ± 15 18 Z09-1-11.1 0.04 519 399 0.80 214 0.17891 0.29 11.82 1.2 0.4793 1.1 .970 2524 ± 24 2642.8 ± 4.7 4 Z09-1-12.1 0.11 2044 3579 1.81 509 0.16319 0.24 6.509 1.1 0.2892 1.1 .978 1638 ± 16 2489.1 ± 4.0 34 Z09-1-13.1 0.29 229 156 0.71 90.1 0.1830 0.68 11.53 1.7 0.4568 1.6 .921 2425 ± 32 2681 ± 11 10 Z09-1-14.1 0.16 245 169 0.71 83.0 0.1772 0.76 9.60 1.5 0.3930 1.3 .863 2137 ± 24 2627 ± 13 19 Z09-1-15.1 0.09 145 75 0.53 53.6 0.1777 0.75 10.53 1.5 0.4299 1.3 .864 2305 ± 25 2631 ± 12 12 Z09-1-16.1 0.53 759 401 0.55 136 0.13338 0.59 3.821 1.3 0.2078 1.1 .889 1217 ± 13 2143 ± 10 43 Z09-1-17.1 0.11 433 145 0.35 149 0.16963 0.35 9.37 1.2 0.4006 1.1 .956 2172 ± 21 2554.1 ± 5.9 15 Z09-1-18.1 0.13 375 41 0.11 114 0.17234 0.42 8.38 1.2 0.3528 1.2 .941 1948 ± 19 2580.6 ± 7.0 25 Z09-1-19.1 0.14 540 54 0.10 141 0.15467 0.41 6.479 1.2 0.3038 1.1 .940 1710 ± 17 2398.3 ± 7.0 29 Z09-1-20.1 0.08 286 178 0.65 125 0.18227 0.39 12.76 1.2 0.5076 1.2 .950 2646 ± 25 2673.6 ± 6.4 1 Z09-1-21.1 0.07 190 69 0.37 64.1 0.1699 0.73 9.17 1.7 0.3915 1.5 .898 2130 ± 27 2557 ± 12 17 Z09-1-22.1 0.09 437 228 0.54 155 0.17713 0.37 10.05 1.2 0.4116 1.1 .952 2222 ± 22 2626.2 ± 6.2 15 Z09-1-23.1 0.22 574 16 0.03 161 0.15936 0.41 7.161 1.2 0.3259 1.1 .941 1818 ± 18 2449.0 ± 6.9 26 Z09-1-24.1 0.05 484 404 0.86 201 0.18171 0.41 12.07 4.4 0.482 4.4 .996 2535 ± 92 2668.5 ± 6.9 5 Z09-1-25.1 0.14 263 125 0.49 109 0.17833 0.43 11.79 1.3 0.4797 1.2 .938 2526 ± 25 2637.4 ± 7.2 4 Z09-1-26.1 0.14 1095 25 0.02 133 0.11531 0.81 2.247 1.4 0.1413 1.1 .809 852.1 ± 8.9 1885 ± 15 55 Z09-1-27.1 0.26 204 86 0.44 77.8 0.16398 0.60 10.00 1.4 0.4421 1.3 .902 2360 ± 25 2497 ± 10 5 Z09-1-28.1 1.26 370 143 0.40 121 0.1671 0.90 8.62 1.6 0.3742 1.3 .835 2049 ± 24 2529 ± 15 19 Z09-1-29.1 0.19 726 700 1.00 176 0.16277 0.36 6.306 1.2 0.2810 1.1 .954 1596 ± 16 2484.8 ± 6.0 36 Z09-1-30.1 0.03 635 426 0.69 210 0.17714 0.30 9.41 1.2 0.3853 1.1 .968 2101 ± 20 2626.3 ± 4.9 20 Z09-1-31.1 0.16 867 402 0.48 209 0.16223 0.42 6.277 1.2 0.2806 1.1 .936 1594 ± 16 2479.2 ± 7.1 36 Z09-1-32.1 0.15 264 189 0.74 94.8 0.17671 0.46 10.17 1.3 0.4173 1.2 .933 2248 ± 22 2622.3 ± 7.6 14

Errors are 1 À r;Pbc and Pb⁄ indicate the common and radiogenic portions, respectively. % discordance = % discordance deﬁned as [(206Pb/238age)/(207Pb/206b)] Â 100. Data were 204Pb corrected, using measured values.

low, <5%. In the normalized An–Ab–Or diagram, three samples are Dioritic gneiss in close association with the banded TTG gneis- plotted in the ﬁeld of tonalite and one in trondhjemite (Fig. 5a). The ses has low SiO2 (59.81%), high MgO (6.34%) and high Al2O3 K2O/Na2O ratio (0.16–0.43) of the rocks is low, suggesting a tron- (14.02%) contents, rich in CaO (5.79%) and Na2O (3.7%), and poor dhjemitic evolution trend of trondhjemite (Fig. 5b). The A/CNK va- in K2O (1.79%). Its MgO, TFeO and CaO contents are substantially lue of the sample is in the range of 0.98–1.07 with an average of higher than that of the TTG gneisses. The gneiss has high Mg index # 1.02, of peraluminous feature, demonstrating the high-Al2O3 char- (Mg = 67), the feature of high-Mg diorite. acteristics of the TTG of gneisses. The Mg# of the samples is 0.32– Trondhjemitic vein in the banded TTG gneisses also has high

0.44, averaging 0.37. All these results suggest that the banded SiO2 (74.78–79.07%), high Al2O3 (12.84À14.47%) and low MgO gneisses of the Zanhuang Complex are typical high-aluminous (0.10À0.25%) contents, and rich in Na2O (4.15–4.32%) and poor in TTG gneisses. K2O (0.72À1.71%) (Table 2), suggesting similarity with the TTG Author's personal copy

C. Yang et al. / Journal of Asian Earth Sciences 72 (2013) 178–189 183

Fig. 4. Concordia diagram of zircon U–Pb ages from the banded tonalitic gneiss in the Zanhuang Complex.

gneisses. The TiO2,P2O5 and TFe2O3 contents are very low, being and Sm. The pattern curve is similar to that of the banded TTG Ã 0.03–0.08%, 0.01% and 0.29–1.0%, respectively, the total Fe2O3 + gneisses, but the contents of HFSE elements Zr and Hf are slightly MgO + MnO + TiO2 contents ranging from 0.43% to 1.45%. lower (Fig. 6b). The trondhjemitic veins have low contents of compatible ele- 6.2. REE and trace elements ments V (3.21–9.53 ppm), Cr (1.08–1.57 ppm), Co (0.66– 2.21 ppm) and Ni (2.3–3.18 ppm), and strong depletion in HFSE The chondrite-normalized REE distribution patterns of the sam- Nb, Zr and Ti (Fig. 6d). The ratio of Rb/Sr is low (0.07–0.19), while ples show strong depletion of the heavy REE (HREE) vs. the light that of the Sr/Y is high (80.42–193.48). REE (LREE) right-inclined curves, indicating the strong fractionation between LREE and HREE (Fig. 6a), (La/Yb) = 12.02–24.65, N 7. Sm–Nd isotope geochemistry which is consistent with that of the Archean TTG (5 < (La/ Yb) < 150) (Martin, 1994). HREE are heavily depleted, with N Two samples of the banded TTG gneisses were chosen for mea- YbN = 1.15À4.78. Except one sample with weak negative Eu anom- Ã suring Sm–Nd isotopes (see Table 3). aly (Eu/Eu = 0.6), all other samples have a weak positive Eu anom- 143 144 Ã The banded TTG gneisses give Nd/ Nd ratio of 0.511281– aly (Eu/Eu = 1.05–1.64). 147 144 0.511407, Sm/ Nd ratio 0.1135–0.1180, and positive eNd(t) va- The dioritic gneiss sample E88-4 has a lower REE content, and R lue in the range of 2.37–3.29 (t = 2692 Ma). The Sm/Nd ratio of the although the HREE are depleted relative to the LREE, the degree of samples is 0.19 and the enrichment coefﬁcient fSm/Nd has negative fractionation is less than for the TTG (La/Yb) = 6.84. The diorite N values (À0.40 to À0.42), suggesting the absence of substantial frac- also displays a weak positive Eu anomaly (Eu/EuÃ = 1.18) (Table 2; tionation of Sm, Nd in the source. The one-stage DM Nd model age Fig. 6a). (TDM) ranges from 2.76 to 2.83 Ga and the two-stage Nd model age The trondhjemitic vein sample E88-3 has low content of REE (TDM) 2.77–2.84 Ga. (RREE = 6.63 ppmÀ30.63 ppm). The chondrite-normalized REE distribution pattern also shows depletion of the HREE vs. the LREE (for some elements under the detective limit, interpolation treat- 8. Discussion ment was used), approximately parallel to that of the banded TTG gneisses. The LREE and HREE are strongly fractionated 8.1. Attributes and genesis of the rocks

(Fig. 6c), (La/Yb)N = 11.34À21.46, with substantial positive Eu anomaly (Eu/EuÃ = 2.21À7.15) and weak negative Ce anomaly, 8.1.1. Banded TTG gneisses which is related to the presence of abundant plagioclase (included Banded gneisses of the Zanhuang Complex have the major oxi- xenocrystic plagioclase) and minor melanocratic and accessory des of high Si and Al, rich in Na and poor in K, enriched in LREE and minerals. depleted in HREE and weak positive Eu anomalies. As to the trace The banded TTG gneisses are characteristic of abundant LILE elements, the rocks are enriched in LILE Ba and Sr and depleted in contents of Ba (199–588 ppm) and Sr (200–408 ppm), slight deple- HFSE Nb, Ta and Ti with low contents of Yb and Y. In the primitive tion in Rb (40.8–72 ppm) and relatively low contents of Yb (0.32 mantle-normalized trace elements partition diagram, negative À1.00 ppm, <1.5 ppm) and Y (3.41–10.3 ppm, <15 ppm), with low anomalies of Nb, Ta, Ti, P and Sm can be discerned. All these fea- Rb/Sr ratio (0.13–0.33), high Sr/Y ratio (21.77–96.77, >20) and tures are similar to that of the high-Al TTG rocks, which suggest depletion in HFSE elements Nb, Ta and Ti. In the primitive man- that the gneisses are of typical Archean TTG rock series. In addition, tle-normalized trace element distribution diagram (Fig. 6b) the the gneisses are consistent with adakite with respect to geochem- TTG samples show negative anomalies of Nb, Ta, Ti, P and Sm, ical characteristics, which are plotted in the high-Si adakite ﬁeld in which are characteristic of the TTG rocks. the trace elements diagram (Fig. 7). The dioritic gneiss Z88-4 has high LILE contents of Rb The high-Al, Na-rich and K-poor features of the banded TTG (92.9 ppm) and Sr (405 ppm) and low contents of Yb (1.37 ppm) gneisses show that the rocks are unlikely derived from remelting and Y (11.4 ppm), whereas the compatible elements V of the continental the crust; and the low abundances of Y, Nb, Ta, (116 ppm), Cr (249 ppm), Co (37 ppm) and Ni (179 ppm) are abun- Zr and Yb and the relevant ratios are characterized virtually by is- dant and substantially higher than that of the banded TTG gneisses. land arc magma. The positive eNd(t) values (2.37–3.29) and the low In the primitive mantle-normalized trace elements distribution initial Sr values (0.69719–0.70068, <0.704) indicate their probable diagram (Fig. 6b) it displays negative anomalies of Nb, Ta, Ti, P derivation from depleted mantle. Moreover, as the Nd model age Author's personal copy

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Table 2 Geochemical date for banded tonalitic gneiss, dioritic gneiss and trondhjemitic veins from Zanhuang Complex and <3.0 Ga TTG.

Sample# Z07-6 Z09-1 Z87-1 Z88-1 Z88-2 Z88-3 Z88-4 <3.0 Ga TTG* Major elements (wt.% oxides)

SiO2 70.04 71.27 67.76 73.31 74.78 79.07 59.81 68.36

TiO2 0.39 0.29 0.42 0.22 0.08 0.03 0.46 0.38

Al2O3 14.38 14.86 15.83 14.47 14.47 12.84 14.02 15.52

Fe2O3 1.49 1.53 1.65 1.19 0.8 0.23 2.05 3.27 FeO 1.99 1.06 1.6 1.42 0.27 0.05 3.68 MnO 0.05 0.03 0.05 0.03 0.02 0.01 0.1 0.05 MgO 1.48 0.74 1.03 0.65 0.25 0.1 6.34 1.36 CaO 2.17 3.11 3.43 3.18 2.56 2.39 5.79 3.23

Na2O 4.53 4.48 5.07 4.8 4.15 4.32 3.7 4.7

K2O 1.93 1.18 1.48 0.77 1.71 0.72 1.79 2

P2O5 0.09 0.07 0.13 0.07 0.01 0.01 0.11 0.15 + H2O 0.84 0.66 0.36 0.06 0.2 0.02 0.3

CO2 0.62 0.12 0.26 0.26 0.34 0.26 0.95 Total 100.00 99.40 99.07 100.43 99.64 100.05 99.10

K2O/Na2O 0.43 0.26 0.29 0.16 0.41 0.17 0.48 0.43 A/CNK 1.07 1.04 0.98 1.00 1.08 1.05 0.76 0.98 Mg# 0.44 0.35 0.37 0.32 0.31 0.41 0.67 0.45 REE (ppm) La 23.3 11.7 12.3 6.93 7.64 1.85 13.9 30.8 Ce 43.7 24 25 24.6 11.6 1.91 28.8 58.5 Pr 4.58 2.2 2.72 1.49 1.52 0.33 3.62 Nd 16.8 7.82 10.4 5.34 5.54 1.1 13.9 23.2 Sm 3.1 1.46 2.23 1.01 1.15 0.22 2.84 3.5 Eu 0.68 0.54 0.73 0.46 0.81 0.55 1.17 0.9 Gd 2.99 1.48 1.94 0.64 1.05 0.25 3.23 2.3 Tb 0.41 0.18 0.29 0.14 0.14 <0.05 0.49 Dy 2.21 0.88 1.58 0.56 0.53 0.18 2.45 1.6 Ho 0.4 0.15 0.27 0.1 0.11 <0.05 0.49 Er 1.07 0.39 0.75 0.33 0.3 0.13 1.55 0.75 Tm 0.15 0.05 0.11 <0.05 <0.05 <0.05 0.23 Yb 1 0.32 0.69 0.33 0.24 0.11 1.37 0.63 Lu 0.14 0.04 0.1 0.05 <0.05 <0.05 0.19 0.12 RREE 100.53 51.21 59.11 41.98 30.63 6.63 74.23 Eu /Eua 0.67 1.11 1.05 1.64 2.21 7.15 1.18

(La/Yb)N 15.71 24.65 12.02 14.16 21.46 11.34 6.84 Trace elements (ppm) Sc 7.6 4.54 4.01 1.59 1.82 0.43 16.3 V 52.7 23.9 39.6 17.3 9.53 3.21 116 52 Cr 51.8 18.7 6.35 5.87 1.57 1.08 249 50 Co 10.9 5.41 6.2 4.01 2.21 0.66 37 Ni 23 11.8 4.38 3.34 3.18 2.3 179 21 Ga 21 18 17.9 13.8 16.9 13.7 19.3 Rb 72 40.8 51.2 46.9 37.6 12.2 92.9 67 Sr 218 200 408 330 193 178 405 541 Zr 169 154 165 156 68.7 9.43 90.2 154 Nb 4.45 4.96 6.57 4.8 3.32 0.54 3.94 7 Cs 1.3 0.48 2.7 3.34 1.41 0.32 5.07 Ba 588 398 295 199 378 185 436 847 Hf 4.57 4.39 4.3 4.77 3.13 0.48 3.05 Ta 0.34 0.31 0.55 0.32 1.01 0.2 0.35 Pb 10.6 4.9 10.8 7.44 11.1 8.17 7.07 Th 5.33 3.06 2.34 3.21 4.21 0.43 2.94 U 0.68 0.64 0.83 0.56 0.6 0.43 0.82 Y 10.3 3.53 8.46 3.41 2.4 0.92 11.4 11 Rb/Sr 0.33 0.20 0.13 0.14 0.19 0.07 0.23 Sr/Y 21.17 56.66 48.23 96.77 80.42 193.48 35.53 49.18

a <3.0 Ga TTG; Martin et al. (2005).

(2.77–2.84 Ga) of the depleted mantle (DM) is slightly older than of the thickened lower (maﬁc) crust (Atherton and Petford, 1993; its formation age, the provenance may come from the ca. 2.8 Ga Arculus et al., 1999; Hou et al., 2004). juvenile crust. Experimental petrology has proved that the mineral compo-

Granitic rocks with positive eNd(t) and low initial Sr values are nents and geochemical characteristics of the TTG rocks require par- usually directly or indirectly related to the mantle (Jahn et al., tial melting of water-bearing basaltic rocks at high pressure 2000). (Barker and Arth, 1976; Kröner and Layer, 1992; Rapp et al., As mentioned above, the Zanhuang banded gneisses are similar 1991; Rapp and Watson, 1995; Xiong, 2006; Xiong et al., 2009). to high-Si adakite in many aspects. For adakite, two hypotheses The similarity of the Sr and Nd isotopes of the TTG to that of the have been proposed for its genesis: one is partial melting of sub- mantle implies that rapid partial melting (60.1 Ga) happened in ducted slab (Kepezhinskas et al., 1995; Martin, 1999; Defant the basic rocks soon after their differentiation from the mantle et al., 2002; Martin et al., 2005) and the other is partial melting (Martin, 1987). Accordingly, many researchers tend to believe that Author's personal copy

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Fig. 5. An–Ab–Or classiﬁcation diagram based on the CIPW norm (a) and K–Na–Ca diagram (b) for banded tonalitic gneiss, dioritic gneiss and trondhjemitic veins from Zanhuang Complex.

Fig. 6. Chondrite-normalized REE patterns (a) banded tonalitic gneiss, dioritic gneiss and <3.0 Ga TTG, (c) Trondhjemitic veins and primitive mantle-normalized spidergrams trace elements spider-diagrams (b) banded tonalitic gneiss, dioritic gneiss and <3.0 Ga TTG, (d) Trondhjemitic veins. most Archean TTG rocks were formed by partial melting of sub- 8.1.2. Dioritic gneiss ducted oceanic crust under high temperature (Martin, 1999; Dioritic gneiss in close association with the Zanhuang banded Defant et al., 2002; Martin et al., 2005). Viewed in combination gneisses has the characteristics of low-Si, high-Mg and high-Al, with the petrology, geochemistry and isotope geochemistry of rich in Na, poor in K, and high Mg#, which are consistent with that the banded gneisses, we postulate that the rocks were formed from of the high-Mg diorite. It has high-Sr content, high Sr/Y ratio partial melting of the mantle-depleted juvenile basic crust and the (35.53), fractionation between LREE and HREE and negative anom- possible mechanism is the subduction of the slab. In addition, the alies of Nb, Ta, Ti, P and Sm. These geochemical features are iden- rocks have low Mg# (averaging 0.37), low contents of compatible tical with those of the banded gneisses, indicating that dioritic elements Cr (mean 20.72 ppm) and Ni (mean 10.63 ppm) that sug- gneiss was also derived from subduction environment. One view gest the absence of substantial metasomatism between the melt is that the high-Mg diorites were derived from the subducted slab and the mantle peridotite. contaminated by mantle peridotite during ascent (Rapp et al., Author's personal copy

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Fig. 7. MgO vs. SiO2, Nb vs. SiO2, Sr vs. (CaO + Na2O), (Sr/Y) vs. Y, (Cr/Ni) vs. TiO2, and (Sr/Y) vs. Y diagrams comparing high-SiO2 and low-SiO2 adakites with banded tonalitic gneiss, dioritic gneiss and trondhjemitic veins from Zanhuang Complex. LSA À low-SiO2 adakites; HSA À high-SiO2 adakites (Martin et al., 2005).

1999; Kelemen et al., 2003; Kamei et al., 2004). The other model is that ﬂuxing of the mantle wedge by dewatering of a subducted slab triggers melting directly in the mantle wedge (Stern and Hanson, 1991; Smithies and Champion, 2000). Although the two models are different, they suggest a tectonic setting of hot slab subduction. Moreover, the gneiss has low Si, high Mg contents and substantial enrichment of compatible elements V, Cr and Ni. The primitive high-Mg andesitic melt produced via interaction between subducted slab melt and mantle peridotite, if not differentiated, may have high Mg# index (generally over 60) (Kelemen et al., 2003). The dioritic gneiss of the study area has Mg# = 67, showing no sign of substantial crystallization differentiation.

8.1.3. Leucocratic trondhjemitic vein Field occurrence shows that the leucocratic trondhjemitic vein was formed in a late stage and is younger than the tonalitic gneiss. Fig. 8. Sketch map of the NCC showing distribution of ancient nuclei, Archean Major oxides are of high-Al, rich in Na and poor in K, very similar to micro-blocks and greenstone belts. (revised from Zhai and Santosh (2011)). ALS À that of the dioritic gneiss. The REE is low in content, but the distri- Alashan Block; JN À Jining Block; OR À Ordos Block; XCH À Xuchang Block; QH À bution patterns are parallel to that of the tonalitic gneiss. HFSE Nb, Qianhuai Block; XH À Xuhuai Block; JL À Jiaoliao Block; GB À greenstone belt. P and Ti are strongly depleted (Fig. 6d), Sr/Y ratio is high, also similar to that of the dioritic gneiss. In addition, the vein has high Si 8.2. Crustal accretion and evolution of NCC in early Neoarchean and low maﬁc contents. Thus we consider that the leucocratic trondhjemitic vein was produced by partial melting of the tonalitic The Zanhuang banded gneisses were formed at ca. 2.7 Ga gneiss. through partial melting of mantle-derived juvenile crust, Author's personal copy

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Table 3 Sm–Nd isotopic compositions of the banded tonalitic gneiss in the Zanhuang Complex.

147 144 143 144 Sample Sm (ppm) Nd (ppm) Sm/ Nd Nd/ Nd Error (2r) eNd(t) fSm/Nd TDM(Ma) T2DM(Ma) Z07-6 3.01 15.5 0.1180 0.511407 0.000014 3.29 À0.40 2759 2765 Z09-1 1.47 7.85 0.1135 0.511281 0.000012 2.37 À0.42 2826 2848

suggesting an extensive continental accretion happened in the crystallization fractionation. The dioritic gneiss was formed study area in early Neoarchean. Actually, the magmatism of ca. in a similar way but perhaps metasomatism of mantle peri- 2.5 Ga was much larger in scale than that of ca. 2.7 Ga in Zanhuang dotite occurred or it formed directly from ﬂuxing of the Complex (Fig. 1). However, both the dioritic gneiss enclaves of mantle wedge. Their formation mechanism may relate to

2.51 Ga and the K-granite of 2.50 Ga have positive eNd(t) values plate subduction. and Nd model ages of ca. 2.7 Ga (Yang et al., 2011b), proving that (3) Similar to the Wangfushan gneiss of western Shandong the major crust accretion event occurred at ca. 2.7 Ga. The mag- Province, the Zanhuang area experienced a continental matic activities of ca. 2.5 Ga, though rather intensive, were pre- accretion at ca. 2.7 Ga and was strongly reworked later by dominantly manifested by the reworking of the earlier crust and the ca. 2.5 Ga tectonothermal event. probably no substantial mantle materials added to the crust during this period. Similarly, the most intensive magmatic activity in the whole NCC occurred at 2.50–2.55 Ga, i.e. the end of Neoarchean Acknowledgments (Guan et al., 2002; Wilde et al., 2005; Kröner et al., 2005; Shen et al., 2005; Zhao et al., 2008; Yang et al., 2008; Condie et al., The research was supported by China Geological Survey 2009; Grant et al., 2009; Liu et al., 2009b; Geng et al., 2010), but (1212010611802, 1212011120152, 1212011120129, studies show that many rocks of this period have the Nd and Hf 1212010711815) and the National Natural Science Foundation of model ages of 2.7–2.8 Ga and the eNd(t) and eHf(t) values adjacent China (41172171). We are grateful to Prof. Dunyi Liu, Yuhai Zhang, to the evolution curve of the DM (Lu et al., 1996; Zhai, 2004; Wu Chun Yang, Zhiqing Yang, Hui Zhou, Qing Ye and Huiyi Sun for their et al., 2005; Geng et al., 2011; Wan et al., 2011b,c; Zhai and San- help of mount making, cathodoluminescence images and SHRIMP tosh, 2011), suggesting the large-scale crust accretion of NCC at dating. The authors are also indebted to Ms. Huaisu Zhang for ca. 2.7 Ga. While the ca. 2.5 Ga thermal event was severely rework- the improvement of English. Finally, we thank Allen Nutman and ing the earlier crust, some information on crust accretion was re- two anonymous reviewers for helpful comments and polishing corded in Huai’an, northwestern Hebei Province (Liu et al., English. 2009b), eastern Hebei Province (Yang et al., 2008), western Liaon- ing Province (Grant et al., 2009) and the Wutai Mts (Wilde et al., References 2004; Kröner et al., 2005). Zhai and Santosh (2011) have subdivided the basement of NCC Arculus, R.J., Lapierrre, H., Jaillard, E., 1999. Geochemical window into subduction and accretion processes: raspas metamorphic complex, Ecuador. Geology 27, into six microblocks surrounded by greenstone belts and amal- 547–550. gamated through arc-continent collisions to form the united NCC. Atherton, M.P., Petford, N., 1993. Generation of sodium-rich magmas from newly They ascribed both the Fuping–Zanhuang Complexes and the Wu- underplated basaltic crust. Nature 362, 144–146. Balagansky, V.V., Alexejev, N.L., Huhma, H., Azimov, P.Ya., Levsky, L.K., Pin’kova, L.O., tai terrene to the ca. 2.5 Ga Wutai greenstone belt (Fig. 8). The 2011. Provenance of the Sumian basal schists and age of the Lopian present study shows that a large area of the ca. 2.7 Ga TTG gneisses metavolcanic rocks at the archean–proterozoic boundary in the Kukasozero exists in the Zanhuang region. Besides, taking into consideration structure, North-Karelian zone of the Karelides, Baltic shield. Stratigraphy and the presence of the ca. 2.7 Ga hornblende gneiss enclaves hosted Geological Correlation 19, 369–384. Barker, F., Arth, J.G., 1976. Gencration of trondhjemitic–tonalitic liquids and in the ca. 2.5 Ga granitic gneisses (Guan et al., 2002) with the detri- archaean bimodal trondhjemitcs-bassett suites. Geology 4, 596–600. tal zircons in the Fuping Complex (Cheng et al., 2004), we suggest Barley, M.E., Andrey, B., Bryan, K., 2005. Late archean to early paleoproterozoic that a ca. 2.7 Ga Zanhuang Greenstone Belt (Zanhuang GB) of cer- global tectonics, environmental change and the rise of atmospheric oxygen. Earth and Planetary Science Letters 238, 156–171. tain scale occur in the area but was strongly reactivated and bro- Bateman, R., Costa, S., Swe, T., Lambert, D., 2001. Archaean mafic magmatism in the ken apart in the later ca. 2.5 Ga tectonothermal event so that Kalgoolie area of the Yilgarn craton, western Australia: a geochemical and Nd little of it survived. Characteristics of the ca. 2.7 Ga TTG gneisses isotopic study of the petrogenetic and tectonic evolution of a greenstone belt. Precambrian Research 108, 75–112. of this area are rather consistent with that of the Wangfushan Beakhouse, G.P., Heaman, L.M., Creaser, R.A., 1999. Geochemical and U–Pb zircon gneiss in western Shandong Province (Jahn et al., 1988). But sepa- geochronological constraints on the development of a late archean greenstone rated by Cenozoic basins, the two terrenes have no direct contacts belt at Birch lake, Superior province, Canada. Precambrian Research 105, 315– 330. observed. Continued research is necessary to provide new clues or Bibikova, E.V., Petrova, A., Claesson, S., 2005. The temporal evolution of sanukitoids constraints on the basement subdivision and structural evolution in the Karelian craton, Baltic shield: an ion microprobe U–Th–Pb isotopic study of the NCC. of zircons. Lithos 79, 129–145. Black, L.P., Kamo, S.L., Allen, C.M., Aleinikoff, J.K., Davis, D.W., Korsch, R.J., Foudoulis, C., 2003. TEMORA1: a new zircon standard for phanerozoic U–Pb 9. Conclusions geochronology. Chemical Geology 200, 155–170. Cao, G.Q., 1996. Early Precambrian Geology of Western Shandong. Geological Publishing House, Beijing, pp. 1–210 (in Chinese). (1) The protolith of the Zanhuang banded gneisses is predomi- Carlson, R.W., Irving, A.J., 1994. Depletion and enrichment history of subcontinental nantly tonalite with TTG and high-Si adakite features. The lithospheric mantle: An Os, Sr, Nd and Pb isotopic study of ultramafic xenoliths associated dioritic gneiss is of high-Mg diorite affinity. from the northwestern Wyoming craton. Earth and Planetary Science Letters 126, 457–472. (2) Zircon SHRIMP U–Pb and whole rock Nd isotopic data show Cheng, Y.Q., Yang, C.H., Wan, Y.S., Liu, Z.X., Zhang, X.P., Du, L.L., Zhang, S.G., Wu, J.S., that the Zanhuang banded TTG gneisses was formed ca. Gao, J.F., 2004. Early Precambrian Geological Characters and Anatectic 2.7 Ga ago through partial melting of the juvenile crust Reconstruction of Crust in North Part of Middle Taihang Mountain. Geological Publishing House, Beijing, pp. 1–191 (in Chinese). derived from depleted mantle, and the melt has not under- Condie, K.C., 2000. Episodic continental growth models: afterthoughts and gone substantial metasomatism of mantle peridotite or extensions. Tectonophysics 322, 153–162. Author's personal copy

188 C. Yang et al. / Journal of Asian Earth Sciences 72 (2013) 178–189

Condie, K.C., Aster, R.C., 2010. Episodic zircon age spectra of orogenic granitoids: the Kröner, A., Compston, W., Zhang, G.W., Guo, A.L., Todt, W., 1988. Age and tectonic supercontinent connection and continental growth. Precambrian Research 180, setting of late archean greenstone-gneiss terrain in Henan province, China, as 227–236. revealed by single-grain zircon dating. Geology 16, 211–215. Condie, K.C., Belousova, E., Griffin, W.L., Sircombe, K.N., 2009. Granitoid events in Kröner, A., Jaeckel, P., Brandl, G., Nemchin, A.A., Pidgeon, R.T., 1999. Single zircon space and time: constraints from igneous and detrital zircon age spectra. ages for granitoid gneisses in the central zone of the Limpopo belt, southern Gondwana Research 15, 228–242. Africa and geodynamic significance. Precambrian Research 93, 299–337. Defant, M.J., Xu, J., Kepezhinskas, P., Wang, Q., Zhang, Q., Xiao, L., 2002. Adakites: Kröner, A., Wilde, S.A., Li, J.H., Wang, K.Y., 2005. Age and evolution of a late archean some variations on a theme. Acta Petrologica Sinica 18, 129–142. to paleoproterozoic upper to lower crustal section in the Wutaishan/Hengshan/ Diwu, C.R., Sun, Y., Lin, C.L., Wang, H.L., 2010. LA-(MC)–ICPMS U–Pb zircon Fuping terrain of northern China. Journal of Asian Earth Sciences 24, 577–595. geochronology and Lu–Hf isotope compositions of the Taihua complex on the Liu, D.Y., Wilde, S.A., Wan, Y.S., Wang, S.Y., Valley, J.W., Kita, N., Dong, C.Y., Xie, H.Q., southern margin of the north China craton. Chinese Science Bulletin 55, 2557– Yang, C.X., Zhang, Y.X., Gao, L.Z., 2009a. Combined U–Pb, hafnium and oxygen 2571. isotope analysis of zircons from meta-igneous rocks in the southern north China Du, L.L., Yang, C.H., Zhuang, Y.X., Wei, R.Z., Wan, Y.S., Ren, L.D., Hou, K.J., 2010. Hf craton reveal multiple events in the late mesoarchean–early neoarchean. isotopic compositions of zircons from 2.7 Ga metasedimentary rocks and Chemical Geology 261, 140–154. biotite–plagioclase gneiss in the Mengjiatun formation complex, western Liu, F., Guo, J.H., Lu, X.P., Diwu, C.R., 2009b. Crustal growth at 2.5 Ga in the China Shandong province. Acta Geologica Sinica 84, 991–1001 (in Chinese with craton: evidence from whole-rock Nd and zircon Hf isotopes in the Huai’an English abstract). gneiss terrane. Chinese Science Bulletin 54, 4704–4713. Du, L.L., Zhuang, Y.X., Yang, C.H., Wan, Y.S., Wang, X.S., Wang, S.J., Zhang, L.F., 2003. Lu, S.N., Chen, Z.H., Xiang, Z.Q., 2008. Geochronological Framework of Ancient Characters of zircons in the Mengjiatun formation in Xintai of Shandong and Intrusions in Taishan Geopark, China. Geological Publishing House, Beijing, pp. their chronological significance. Acta Geologica Sinica 77, 359–366 (in Chinese 1–90 (in Chinese). with English abstract). Lu, S.N., Yang, C.L., Jiang, M.M., Li, H.K., Li, H.M., 1996. Tracing Precambrian Crustal Friend, C.R.L., Nutman, A.P., 2005. Complex 3670–3500 Ma episodes superimposed Evolution. Geological Publishing House, Beijing, pp. 1–156 (in Chinese). on juvenile crust between 3850 and 3690 Ma, Itsaq Gneiss complex, southern Ludwig, K.R., 2001. Squid 1.02: A User’s Manual. Berkeley Geochronology Centre, west Greenland. Journal Geology 113, 375–397. Special Publication 2, 1–19. Friend, C.R.L., Nutman, A.P., Baadsgaard, H., Kinny, P.D., McGregor, V.R., 1996. Manikyamba, C., Kerrich, R., 2011. Geochemistry of alkaline basalts and associated Timing of late archaean terrane assembly, crustal thickening and granite high-Mg basalts from the 2.7 Ga Penakacherla terrane, Dharwar craton, India: emplacement in the Nuuk region, southern West Greenland. Earth and an archean depleted mantle-OIB array. Precambrian Research 188, 104–122. Planetary Science Letters 142, 353–365. Martin, H., 1987. Petrogenesis of archaean trondhjemites, tonalities and Geng, Y.S., Du, L.L., Ren, L.L., 2011. Growth and reworking of the early precambrian granodiorites from eastern Finland: major and trace element geochemistry. continental crust in the north China craton: constraints from zircon Hf isotopes. Journal Petrology 28, 921–953. Gondwana Research. http://dx.doi.org/10.1016/j.gr.2011.07.006. Martin, H., 1994. Archean gray gneisses and continental crust origin. In: Condie Geng, Y.S., Shen, Q.H., Ren, L.D., 2010. Late neoarchean to early paleoproterozoic (Ed.), Archean Crustal Evolution. Elsevier, Amsterdam, pp. 205–259. magmatic events and tectonothermal system in the north China craton. Acta Martin, H., 1999. Adakitic magmas: modern analogues of archaean granitoids. Petrologica Sinica 26, 1945–1966 (in Chinese with English abstract). Lithos 46, 411–429. Grant, M.L., Wilde, S.A., Wu, F.Y., Yang, J.H., 2009. The application of zircon Martin, H., Smithies, R.H., Rapp, R., Moyen, J.F., Champion, D., 2005. An overview of Cathodoluminescence imaging, Th–U–Pb chemistry and U–Pb ages in adakite, tonalite–trondhjemite–granodiorite (TTG), and sanukitoid: interpreting discrete magmatic and high-grade metamorphic events in the relationships and some implications for crustal evolution. Lithos 79, 1–24. north China craton at the archean/proterozoic boundary. Chemical Geology 261, Matthew, S.A., Robert, W.N., Stephen, R., James, F., 1999. U–Pb zircon evidence for 155–171. an extensive early archean craton in Zimbabwe: a reassessment of the timing of Guan, H., Sun, M., Wilde, S.A., Zhou, X., Zhai, M.G., 2002. SHRIMP U–Pb zircon craton formation, stabilization, and growth. Geology 27, 707–710. geochronology of the Fuping complex: implications for formation and assembly Mikkola, P., Huhma, H., Heilimo, E., Whitehouse, M.J., 2011. Archean crustal of the north China craton. Precambrian Research 113, 1–18. evolution of the Suomussalmi district as part of the Kianta complex, Karelia: HBGMR, 1989. Regional geology of Beijing, Tianjin and Heibei Province. Geology constraints from geochemistry and isotopes of granitoids. Lithos 125, 287–307. Publishing House, Beijing, pp. 16–30 (in Chinese with English abstract). Nelson, D.R., 1997. Evolution of the archaean granite–greenstone terranes of the Heilimo, E., Halla, J., Huhma, H., 2011. Single-grain zircon U–Pb age constraints of eastern Goldfields, western Australia: SHRIMP U–Pb zircon constraints. the western and eastern sanukitoid zones in the Finnish part of the Karelian Precambrian Research 83, 57–81. province. Lithos 121, 87–99. Nelson, D.R., 1999. Compilation of SHRIMP U–Pb Geochronology Data. Geological Henry, P., Stevenson, R.K., Larbi, Y., Gariepy, C., 2000. Nd isotopic evidence for early Survey of Western Australia Record, Perth, p. 189. to late archean (3.4À2.7 Ga) crustal growth in the western Superior province Nutman, A.P., Chernyshev, I.V., Baadsgaard, H., Smelov, A.P., Smelov, A.P., 1992. The (Ontario, Canada). Tectonophysics 322, 135–151. Aldan shield of Siberia, USSR: the age of its archaean components and evidence Hofmann, A., Dirks, P.H.G.M., Jelsma, 2004. Clastic sedimentation in a late archaean for widespread reworking in the mid-proterozoic. Precambrian Research 54, accretionary terrain, Midlands greenstone belt, Zimbabwe. Precambrian 195–210. Research 129, 47–69. Nutman, A.P., Chadwick, B., Krishna Rao, B., Vasudev, V.N., 1996. SHRIMP U/Pb Hou, Z.Q., Gao, Y.F., Qu, X.M., Rui, Z.Y., Mo, X.X., 2004. Origin of adakitic intrusives zircon ages of acid volcanic rocks in the Chitradurga and Sandur groups and generated during mid-miocene eastÀwest extension in southern Tibet. Earth granites adjacent to the Sandur schist belt, Karnataka. Journal of the Geological and Planetary Science Letters 220, 139–155. Society India 47, 153–164. Jahn, B.M., Auvray, B., Shen, Q.H., Liu, D.Y., Zhang, Z.Q., Dong, Y.J., Ye, X.J., Cornichet, Nutman, A.P., Friend, C.R.L., Hiess, J., 2010. Setting of the 2560 Ma Qôrqut Granite J., Mace, J., 1988. Archaean crustal evolution in China: the Taishan complex and complex in the archean crustal evolution of southern west Greenland. American evidence for juvenile crustal addition from long term depleted mantle. Journal of Science 310, 1081–1114. Precambrian Research 38, 381–403. Percival, J.A., Stern, R.A., Skulski, T., 2001. Crustal growth through successive arc Jahn, B.M., Liu, D.Y., Wan, Y.S., Song, B., Wu, J.S., 2008. Archean crustal evolution of magmatism: reconnaissance U–Pb SHRIMP data from the northeastern Superior the Jiaodong Peninsula, China, as revealed by zircon SHRIMP geochronology, province, Canada. Precambrian Research 109, 203–238. elemental and Nd-isotope geochemistry. American Journal of Science 308, 232– Polat, A., Frei, R., Scherstén, A., Appel, P.W.U., 2010. New age (ca. 2970 Ma), mantle 269. source composition and geodynamic constraints on the archean Fiskenæsset Jahn, B.M., Wu, F.Y., Chen, B., 2000. Granitoids of the central Asian orogenic belt and Anorthosite complex, SW Greenland. Chemical Geology 277, 1–20. continental growth in the phanerozoic. Transactions of the Royal Society of Polat, A., Kerrich, R., 2000. Archean greenstone belt volcanism and the continental Edinburgh. Earth Sciences 91, 181–193. growth-mantle evolution connection: constraints from Th–U–Nb–LREE Jahn, B.M., Gruau, G., Capdevila, R., Cornichet, J., Nemchin, A., Pidgeon, R., 1998. systematics of the 2.7 Ga Wawa subprovince, Superior province, Canada. Archean crustal evolution of the Aldan shield, Siberia: geochemical and isotopic Earth and Planetary Science Letters 175, 41–54. constraints. Precambrian Research 91, 333–363. Polat, A., Kerrich, R., 2002. Nd-isotope systematics of 2.7 Ga adakites, magnesian Jayananda, M., Moyen, J.F., Martin, H., Peucat, J.J., Auvray, B., Mahabaleswar, B., andesites and arc basalts, Superior province, Canada: evidence for shallow 2000. Late archaean (2550–2520 Ma) juvenile magmatism in the eastern crustal recycling at archean subduction zones. Earth and Planetary Science Dharwar craton, southern India: constraints from geochronology, Nd–Sr Letters 202, 345–360. isotopes and whole rock geochemistry. Precambrian Research 99, 225–254. Polat, A., Münker, C., 2004. Hf–Nd isotope evidence for contemporaneous Kamei, A., Owada, M., Nagao, T., Shiraki, K., 2004. High-Mg diorites derived from subduction processes in the source of late archean arc lavas from the sanukitic HMA magmas, Kyushu island, southwest Japan arc: evidence from Superior province, Canada. Chemical Geology 213, 403–429. clinopyroxene and whole rock compositions. Lithos 75, 359–371. Poujol, M., Robb, L.J., Anhaeusser, C.R., Gericke, B., 2003. A review of the Kelemen, P.B., Hanghøj, K., Greene, A.R., 2003. One view of the geochemistry of geochronological constraints on the evolution of the Kaapvaal craton, South subduction-related magmatic arcs, with an emphasis on primitive andesite and Africa. Precambrian Research 127, 181–213. lower crust. In: Holland, H.D., Turekian, K.K. (Eds.), Treatise on Geochemistry. Rapp, R.P., Watson, E.B., 1995. Dehydration melting of metabasalt at 8–32 kbar: In: Rudnick, R.L. (Executive editor), vol. 3, The Crust, Elsevier. pp. 593–659. implications for continental growth and crust–mantle recycling. Journal of Kepezhinskas, P.K., Defant, M.J., Drummond, M.S., 1995. Na-metasomatism in the Petrology 36, 891–931. island arc mantle by slab melt–peridotite interaction: evidence from mantle Rapp, R.P., Watson, E.B., Miller, C.F., 1991. Partial melting of amphibolite/eclogite xenoliths in the north Kamchatka arc. Journal of Petrology 36, 1505–1527. and the origin of archean trondhjemites and tonalites. Precambrian Research Kröner, A., Layer, P.W., 1992. Crust formation and plate motion on the early archean. 51, 1–25. Science 256, 1405–1411. Author's personal copy

C. Yang et al. / Journal of Asian Earth Sciences 72 (2013) 178–189 189

Rapp, R.P., Shimizu, N., Norman, M.D., Applegate, G.S., 1999. Reaction between slab trondhjemite. Geological Review 55, 737–744 (in Chinese with English derived melts and peridotite in the mantle wedge: experimental constraints at abstract). 3.8 GPa. Chemical Geology 160, 335–356. Wilde, S.A., Cawood, P.A., Wang, K.Y., Nemchin, A.A., 2005. Granitoid evolution in Rasmussen, B., Blake, T.S., Fletcher, L.R., 2005. U–Pb zircon age constraints on the the late archean Wutai complex, north China craton. Journal of Asian Earth Hamersley spherule beds: evidence for a single 2.63 Ga Jeerinal – Carawine Sciences 24, 597–613. impact ejecta layer. Geology 33, 725–728. Wilde, S.A., Cawood, P.A., Wang, K.Y., Nemchin, A.A., Zhao, G.C., 2004. Determining Rino, S., Komiya, T., Windley, B.F., Katayama, I., Motoki, A., Hirata, T., 2004. Major Precambrian crustal evolution in China: a case study from Wutaishan, Shanxi episodic increases of continental crustal growth determined from zircon ages of Province, demonstrating the application of precise SHRIMP U–Pb river sands: implications for mantle overturns in the early precambrian. Physics geochronology. In: Malpas, J., Fletcher, C.J.N., Ali, J.R., Aitchison, J.C. (Eds.), of the Earth and Planetary Interiors 146, 369–394. Aspects of the Tectonic Evolution of China, vol. 226. The Geological Society of Said, N., Kerrich, R., Groves, D., 2010. Geochemical systematics of basalts of the London Special Publication, pp. 5–26. lower basalt unit, 2.7 Ga Kambalda sequence, Yilgarn craton, Australia: plume Williams, I.S., 1998. U–Th–Pb geochronology by ion microprobe. In: McKibben, impingement at a rifted craton margin. Lithos 115, 82–100. M.A., Shanks, W.C., Ridley, W.I. (Eds.), Applications of Microanalytical Sandeman, H.A., Hanmer, S., Tella, S., Armitage, A.A., Davis, W.J., Ryan, J.J., 2006. Techniques to Understanding Mineralizing Processes, vol. 7. Reviews in Petrogenesis of neoarchean volcanic rocks of the MacQuoid supracrustal belt: a Economic Geology, pp. 1–35. back-arc setting for the northwestern Hearne subdomain, western Churchill Wu, F.Y., Zhao, G.C., Wilde, S.A., Sun, D.Y., 2005. Nd isotopic constraints on crustal province, Canada. Precambrian Research 144, 140–165. formation in the north China craton. Journal of Asian Earth Sciences 24, 523– Shen, Q.H., Geng, Y.S., Song, B., Wan, Y.S., 2005. New information from the surface 545. outcrops and deep crust of archean rocks of the north China and Yangtze blocks, Wyman, D.A., 1999. A 2.7 Ga depleted tholeiite suite: evidence of plume–arc and Qinling–Dabie Orogenic belt. Acta Geologica Sinica 79, 616–627 (in Chinese interaction in the Abitibi greenstone belt, Canada. Precambrian Research 97, with English Abstract). 27–42. Smithies, R.H., Champion, D.C., 2000. The archaean high-Mg diorite suite: links to Xiao, L.L., Wu, C.M., Zhao, G.C., Guo, J.H., Ren, L.D., 2011. Metamorphic P–T paths of tonalite–trondhjemite–granodiorite magmatism and implications for early the Zanhuang amphibolites and metapelites: constraints on the tectonic archaean crustal growth. Journal of Petrology 41, 1653–1671. evolution of the paleoproterozoic trans-north China orogen. International Steenfelt, A., Garde, A.A., Moyen, J.F., 2005. Mantle wedge involvement in the Journal of Earth Sciences 100, 717–739. petrogenesis of archean grey gneisses in west Greenland. Lithos 79, 207–228. Xiong, X.L., 2006. Trace element evidence for the growth of early continental crust Stern, R.A., Hanson, G.H., 1991. Archaean high-Mg granodiorite: a derivative of light by melting of rutile-bearing hydrous eclogite. Geology 34, 945–948. rareearth elements-enriched monzodiorite of mantle origin. Journal of Xiong, X.L., Keppler, H., Audétat, A., Gudﬁnnsson, G., Sun, W.D., Song, M.S., Xiao, Petrology 32, 201–238. W.S., Yuan, L., 2009. Experimental constraints on rutile saturation during partial Sun, Y., Yu, Z.P., Kröner, A., 1994. Geochemistry and single zircon geochronology of melting of metabasalt at the amphibolite to eclogite transition, with archaean TTG gneisses in the Taihua high-grade terrain, Lushan area, central applications to TTG genesis. American Mineralogist 94, 117–1186. China. Journal of Southeast Asian Earth Sciences 10, 22–233. Yang, C.H., Du, L.L., Ren, L.D., Song, H.X., Wan, Y.S., Xie, H.Q., Liu, Z.X., 2011b. Taylor, J., Stevens, G., Armstrong, R., Kisters, A.F.M., 2010. Granulite facies anatexis Petrogenesis and geodynamic setting of the Jiandeng potassic granite at the end in the Ancient Gneiss complex, Swaziland, at 2.73 Ga: mid-crustal metamorphic of the neoarchean in the Zanhuang complex, north China craton. Earth Science evidence for mantle heating of the Kaapvaal craton during Ventersdorp Frontiers 18, 62–78 (in Chinese with English abstract). magmatism. Precambrian Research 177, 88–102. Yang, C.H., Du, L.L., Ren, L.D., Song, H.X., Wan, Y.S., Xie, H.Q., Liu, Z.X., 2011a. The age Thrane, K., 2002. Relationships between archaean and palaeoproterozoic crystalline and petrogenesis of the Xuting granite in the Zanhuang complex, Hebei basement complexes in the southern part of the east Greenland caledonides: an province – constraints on the structural evolution of the trans-north China ion microprobe study. Precambrian Research 113, 19–42. orogen, north China craton. Acta Petrologica Sinica 27, 1003–1016 (in Chinese Trap, P., Faure, M., Lin, W., Monié, P., Meffre, S., Melletton, J., 2009. The Zanhuang with English abstract). Massif, the second and eastern suture zone of the paleoproterozoic trans-north Yang, J.H., Wu, F.Y., Wilde, S.A., Zhao, G.C., 2008. Petrogenesis and geodynamics of China orogen. Precambrian Research 172, 80–98. late archean magmatism in eastern Hebei, eastern north China craton: Wan, Y.S., Liu, D.Y., Wang, S.J., Dong, C.Y., Yang, E.X., Wang, W., Zhou, H.Y., Du, L.L., geochronological, geochemical and Nd–Hf isotopic evidence. Precambrian Yin, X.Y., Xie, H.Q., Ma, M.Z., 2011c. Juvenile magmatism and crustal recycling at Research 167, 125–149. the end of neoarchean in western Shandong province, north China craton: Zhai, M.G., 2004. Precambrian geological events in the north China craton. In: evidence from SHRIMP zircon dating. American Journal of Science. http:// Malpas, J., Fletcher, C.J.N., Ali, J.R., Aitchison, J.C. (Eds.), Tectonic Evolution of dx.doi.org/10.2475/10.2010.11. China, vol. 226. Geological Society of London Special Publication, pp. 57–72. Wan, Y.S., Liu, D.Y., Wang, S.J., Yang, E.X., Wang, W., Dong, C.Y., Zhou, H.Y., Du, L.L., Zhai, M.G., Santosh, M., 2011. The early precambrian odyssey of north China craton: Yang, Y.H., Diwu, C.R., 2011a. 2.7 Ga juvenile crust formation in the north a synoptic overview. Gondwana Research 20, 6–25. China craton (Taishan–Xintai area, western Shandong province): further Zhang, Z.Q., Ye, X.J., 1987. Mass-spectrometric isotope dilution analysis of REE and evidence of an understated event from zircon U–Pb dating and Hf isotope precise measurement of 143Nd/144Nd ratios. Bulletin of the Institute of Geology. composition. Precambrian Research 186, 169–180. Chinese Academy of Geological Sciences 1, 108–128 (in Chinese with English Wan, Y.S., Dong, C.Y., Liu, D.Y., Kröner, A., Yang, C.H., Wang, W., Du, L.L., Xie, H.Q., abstract). Ma, M.Z., 2011b. Zircon ages and geochemistry of late neoarchean Zhao, G.C., Wilde, S.A., Sun, M., Guo, J.H., Kröner, A., Li, S.Z., Li, X.P., Zhang, J., 2008. syenogranites in the north China craton: a review. Precambrian Research, SHRIMP U–Pb zircon geochronology of the Huai’an complex: constraints on late 10.1016/j.precamres.2011.05.001. archean to paleoproterozoic magmatic and metamorphic events in the trans- Wan, Y.S., Dong, C.Y., Wang, W., Xie, H.Q., Liu, D.Y., 2010. Archean basement and a north China orogen. American journal of Science 270, 270–303. paleoproterozoic collision orogen in the Huoqiu area at the southeastern Zhao, G.C., Sun, M., Wilde, S.A., Li, S.Z., 2005. Late archean to paleoproterozoic margin of north China craton: evidence from Sensitive high resolution ion evolution of the north China craton: key issues revisited. Precambrian Research micro-probe U–Pb zircon geochronology. Acta Geologica Sinica 84, 91–104. 136, 177–202. Wang, W., Yang, E.X., Wang, S.J., Du, L.L., Xie, H.Q., Dong, C.Y., Wan, Y.S., 2009. Zhuang, Y.X., Wang, X.S., Xu, H.L., Ren, Z.K., Zhang, F.Z., Zhang, X.M., 1997. Main Petrography of archean metamorphic pillow basalt in Taishan rock group, geological events and crustal evolution in early precambrian of Taishan region. western Shandong, and SHRIMP U–Pb dating of zircons from intruding Acta Petrologica Sinica 13, 313–330 (in Chinese with English abstract).