Zircon U–Pb age and Lu–Hf isotope constraints on Precambrian evolution of continental crust in the Songshan area, the south-central North China Craton

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Precambrian Research 226 (2013) 1– 20

Contents lists available at SciVerse ScienceDirect

Precambrian Research

journa l h omepa g e: www.elsev ier .com/ locate /precamres

ircon U–Pb age and Lu–Hf isotope constraints on Precambrian evolution ofontinental crust in the Songshan area, the south-central North China Craton

uan Zhanga,∗, Hong-Fu Zhanga,b,∗∗, Xin-Xiang Luc

State Key Laboratory of Continental Dynamics, Department of Geology, Northwest University, Xi’an 710069, ChinaState Key Laboratory of Lithospheric Evolution, Institute of Geology and Geophysics, Chinese Academy of Sciences, P.O. Box 9825, Beijing 100029, ChinaHenan Academy of Land and Resources Sciences, Zhengzhou 450053, China

r t i c l e i n f o

rticle history:eceived 14 August 2012eceived in revised form4 November 2012ccepted 24 November 2012vailable online 4 December 2012

eywords:ircon U–Pb datingf isotoperecambrian crustal evolutionouth-central North China Craton

a b s t r a c t

A combined whole-rock geochemical and zircon U–Pb and Lu–Hf isotope study on two Precambrianlithotectonic units in the Songshan area, south-central North China Craton (NCC), was performed toconstrain the tectonic evolution of the Trans-North China Orogen (TNCO) during collision between theEastern and Western Blocks of the NCC. The metamorphic unit at Shipaihe consists of dioritic gneisswith minor amphibolitic enclave, whereas the magmatic unit at Shicheng is composed of granite. ZirconU–Pb dating demonstrate that the dioritic gneiss and enclave amphibolite were originally emplacedcontemporaneously at ca. 2.5 Ga. The magmatic zircons exhibit εHf(t) values of 2.2–7.8 and Hf modelages of 2.52–2.73 Ga, suggesting that the dioritic gneiss was produced by reworking of the juvenile crust.The magmatic zircons of amphibolite have εHf(t) values of 0.7–8.1 and Hf model ages of 2.51–2.79 Ga.The granite primarily gave zircon U–Pb ages of ca. 1.78 Ga, with inherited zircons in ca. 1.87 Ga. ZirconLu–Hf isotopic analyses yield negative εHf(t) values of −16.7 to −1.8 and Hf model ages of 2.55–3.47 Ga,indicating that the granite was mainly derived from reworking of ancient Archean crust. The Neoarcheandioritic gneiss and amphibolite show enrichment of LREE and LILE but depletion of HREE and HFSE,suggesting their derivation from anatexis of juvenile arc-type crust and enriched lithospheric mantle,respectively. The dioritic gneiss also has highly fractionated REE patterns and negligible negative Euanomalies, implying anatexis at high pressures, where garnet and possibly amphibole as residual phases.The Paleoproterozoic granite has high K2O + Na2O and Zr, high ratios of total FeO/MgO and Ga/Al, and lowcontents of CaO, Al2O3, Ba, Sr and Eu/Eu* values, consistent with the characteristics of A-type granites. Thenegative Eu, Ba and Sr anomalies suggest that plagioclase acted as a residual phase during partial meltingat relatively low pressures. Taken together, the Songshan metamorphic complex would originally derive
from the reworking of juvenile arc-type crust and coeval partial melting of juvenile, enriched lithosphericmantle. Thus, an active continental margin was present in the late Neoarchean in south-central NCC,generating arc-type magmatism between the Eastern and Western Blocks. During the collisional orogeny,the arc-type crust in southern NCC underwent intensive metamorphism that followed by post-collisionalextension at ca. 1.78 Ga, and the reworking of the old continent in the southern TNCO yield ShichengA-type granite.
. Introduction

The North China Craton (NCC) is one of the oldest cratons in the
orld, with widespread occurrence of Archean to Paleoproterozoic
rustal basement. A new progress in understanding the evolutionf the NCC has resulted in a broad consensus that the NCC can be

∗ Corresponding author.∗∗ Corresponding author at: State Key Laboratory of Continental Dynamics, Depart-

ent of Geology, Northwest University, Xi’an 710069, China.E-mail addresses: [email protected] (J. Zhang), [email protected]

H.-F. Zhang).

301-9268/$ – see front matter © 2012 Elsevier B.V. All rights reserved.ttp://dx.doi.org/10.1016/j.precamres.2012.11.015

© 2012 Elsevier B.V. All rights reserved.

divided into two independently developed Eastern and WesternBlocks that are separated by the Trans-North China Orogen (TNCO)(Zhao et al., 1998, 2001a,b, 2002, 2005; Zhai et al., 2000, 2003, 2005;Guan et al., 2002; Wilde et al., 2002; Kusky and Li, 2003; Wang et al.,2004a; Polat et al., 2005, 2006a; Wilde and Zhao, 2005; Wu et al.,2005a; Kröner et al., 2006; Li and Kusky, 2007; Trap et al., 2007,2008, 2009a,b, 2011; Kusky, 2011). The Western Block is consideredto have formed by the amalgamation of the Yinshan in the north andthe Ordos Block in the south along the east-west-trending Khon-
dalite Belt (Zhao et al., 2005; Santosh et al., 2007; Xia et al., 2008; Yinet al., 2009, 2011; Zhao, 2009; Guo et al., 2012), whereas the East-ern Block is considered to have formed a Paleoproterozoic riftingbasin in the period 2.2–1.95 Ga, which was closed at 1.93–1.90 Ga,
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orming the Jiao–Liao–Ji Belt (Li et al., 2004, 2012; Li and Zhao, 2007;hou et al., 2008; Tam et al., 2011, 2012a,b).

Controversy has long surrounded the timing and tectonic pro-esses of collision between the Eastern and Western Blocks. Athe centre of the controversy is whether the collision between theastern and Western Blocks along the TNCO occurred at the end-rchean or in the Paleoproterozoic. Some researchers proposedastward subduction with the collision at ca. 1.85 Ga (Zhao et al.,001a,b; Guan et al., 2002; Guo et al., 2002, 2005; Wilde et al.,002, 2005; Kröner et al., 2005a,b, 2006; Liu et al., 2005, 2006;ilde and Zhao, 2005; Zhang et al., 2006a, 2007, 2009; Li et al.,

010), whereas others suggested westward subduction with col-ision at ca. 2.5 Ga (Kusky and Li, 2003; Polat et al., 2005, 2006a;usky et al., 2007; Li and Kusky, 2007; Kusky, 2011). The majorrgument for the ca. 2.5 Ga collision assumes the existence of annd-Neoarchean (ca. 2.5 Ga) foreland basin (the Qinglong forelandasin), which extends N to NE up to 1600 km long along the east-rn side of the TNCO. Recently, Faure et al. (2007) and Trap et al.2007, 2008, 2009a,b, 2012) suggested west-dipping subductionith two collisional events, in which the earlier amalgamation of

he Eastern Block and a micro-continental block (Fuping Block) ata. 2.1 Ga before the final collision between the Eastern and West-rn Blocks at 1.9–1.8 Ga. However, Zhao et al. (2012) argued thathere are no reliable metamorphic ages supporting the existence of

∼2.1 Ga collisional event. The amalgamation between the Easternnd Western Blocks at ca. 1.85 Ga is primarily based on the follow-ng observations: (1) zircon U–Pb dating exhibits both the Archeannd Paleoproterozoic rocks of the TNCO yield consistent metamor-hic ages of ca. 1.85 Ga (Guan et al., 2002; Wilde et al., 2002; Zhaot al., 2002, 2008a,b; Guo et al., 2005; Kröner et al., 2005a, 2006; Liut al., 2006; Xia et al., 2006a, 2009; Trap et al., 2007, 2008; Zhangt al., 2009; Wang et al., 2010a,b; Li et al., 2011); (2) the presencef granulites and retrograded ecologites in the TNCO, which expe-ienced high-pressure metamorphism at ca. 1.85 Ga (Zhai et al.,993, 2003; Zhao et al., 2001a,b; O’Brien and Rotzler, 2003; Krönert al., 2006; Zhang et al., 2006b; Zhao and Guo, 2012; Zhao andawood, 2012); (3) the collision-related deformation occurred ata. 1.85 Ga (Kröner et al., 2005a,b; Zhang et al., 2006b, 2007, 2009,012d; Faure et al., 2007; Trap et al., 2007; Li et al., 2010; Wang,010; Wang et al., 2010b; Zhao et al., 2010b). While the collision-elated deformation and metamorphism are evident at ca. 1.85 Gan the TNCO, they are not so in geological records of ca. 2.5 Ga. Inhis regard, the Qinglong foreland basin could be developed duringastward subduction of the oceanic crust beneath the continentalargin of the eastern NCC.In order to constrain the timing and tectonic evolution involved

n the collision between the two blocks, many studies have devotedo rocks from the TNCO in recent years (e.g., Wang, 2009; Zhao et al.,009, 2010a,b; Huang et al., 2010, 2012; Li et al., 2010; Wang et al.,010a,b; Liu et al., 2011a,b, 2012a,b,c). Most investigations focusedn the various complexes within the TNCO. The TNCO is a nearlyouth-north-trending Belt, with 100–300 km width and 1200 kmength (Zhao et al., 2001a). The basement of the TNCO is composed

ainly of Paleoproterozoic to Neoarchean TTG gneisses with minorupracrustal rocks and syn- and post-collisional granitoid rocksZhao et al., 2008b and reference therein).

The Precambrian crustal evolution of the NCC has been investi-ated intensively in the past two decades (e.g., Kusky and Li, 2003;ang et al., 2003, 2004a; Li et al., 2005, 2010; Zhao et al., 2005;

u et al., 2006, 2008a; Xia et al., 2006b; Kusky et al., 2007; Wangt al., 2010a; Wu et al., 2012; Zhang et al., 2012a,b,e,f; Zhao andhai, 2013). Most of these studies were focused mainly on the East-
rn and Western Blocks and the central and northern segmentsf the TNCO, little attention has been paid to the southern TNCO.he Songshan area is located in the southern TNCO. Precambrianetamorphic and magmatic rocks of felsic composition are well
esearch 226 (2013) 1– 20

preserved in this region, making it an ideal terrane to investigate thecrustal evolution of the south-central NCC. These magmatic rocksof granitic composition also provide us an excellent opportunity todecipher the reworking of the continental crust.

In this paper, we present a combined study of whole-rock geo-chemistry with zircon U–Pb age and Lu–Hf isotopes for the dioriticgneiss and granite from the Songshan area. The results are used toplace constraints on the source nature and petrogenesis of gran-itoid rocks and their bearing on continental collision between theWestern and Eastern Blocks of the NCC. This study finally aims toprovide important insights into the Precambrian crustal evolutionof the south-central NCC.

2. Geological setting and samples

The NCC preserves some of the oldest continental rocks as oldas 3.8 Ga (e.g., Liu et al., 1992; Song et al., 1996); and is composedof the Eastern Block, the Western Block and the TNCO (Fig. 1a). TheEastern Block consists of the Archean basement and the Paleopro-terozoic Jiao–Liao–Ji tectonic belt, whereas the Western Block iscomposed of the Yinshan Block in the north and the Ordos Block inthe south (Zhao et al., 2005). Their lithological, geochemical, struc-tural, metamorphic and geochronological differences have beenbriefly summarized by Zhao et al. (2001a, 2005). The TNCO can befurther divided into high-grade complexes and low-grade granite-greenstone complexes (Zhao et al., 2001a). The former includesTaihua (TH), Fuping (FP), Hengshan (HS), Huai’an (HA) and Xuanhua(XH) complexes, and the latter consistents of Dengfeng (DF), Zhong-tiao (ZT), Zanhuang (ZH), Lüliang (LL) and Wutai (WT) complexes(Fig. 1a, Zhao et al., 2001a).

The Precambrian basement in the Songshan area (Fig. 1b) isthe Dengfeng Complex which distributed in the southern TNCO.The Dengfeng Complex consists of Neoarchean and Paleopro-terozoic plutonic rocks and supracrustal rocks (Fig. 1b) (Kröneret al., 1988; Zhao et al., 2000; Xue et al., 2004; Wan et al.,2009; Zhou et al., 2009a,b, 2011). The supracrustal rocks can bedivided into Neoarchean Dengfeng Group and PaleoproterozoicSongshan Group (HBGMR, 1989; Fig. 1b). The Dengfeng Group isa greenschist-facies metamorphosed complex, and mainly com-prises metadiorite, plagioclase metadioritic schist, leptynite inthe lower part and marble, mica schists, mica quartz schists andquartzite in the upper part (Guan, 1996). The Songshan Group is agreenschist-facies metasedimentary complex, and comprises con-glomerates at the bottom, quartzite and schist in the middle andcoast quartzite in the upper part (Liu et al., 2012b).

In the Songshan area, metaigneous rocks are primarily com-posed of gneiss in regional distribution and dioritic gneiss atShipaihe, and igneous rocks are primarily composed of potas-sic granite (Fig. 1b). Both the gneiss and granite enclose minoramphibolitic enclaves. The TTG and dioritic gneiss have similarzircon U–Pb ages of ca. 2.5 Ga (Wang et al., 2004b; Wan et al.,2009; Zhou et al., 2009a, 2011; Diwu et al., 2011). Paleoproterozoicgranitic rocks intruded into the TTG and dioritic gneiss, includingthe Shicheng, Baijiazhai and Lujiagou plutons (Zhou et al., 2011).The Shicheng pluton occurs in the southern part of the DengfengComplex with an area of ∼60 km2 (Fig. 1b). SHRIMP zircon U–Pbdating yielded ages between 1739 and 1784 Ma for the Shichengpluton (Wan et al., 2009; Zhao and Zhou, 2009).

Five samples were collected from the Shipaihe dioritic gneiss,including three samples of the dioritic gneiss and two enclavesof the plagioclase amphibolite. The dioritic gneiss samples are
medium-coarse grained and show gneissic structure. The dioriticgneisses are mainly composed of hornblende (∼30%), plagioclase(∼30%), K-feldspar (∼20%), quartz (∼15%) and biotite (∼5%). Theplagioclase amphibolites are coarse grained, and mainly consist of

J. Zhang et al. / Precambrian Research 226 (2013) 1– 20 3

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ornblende (∼55%), plagioclase (∼35%) and biotite (∼10%). Acces-ory phases include magnetite, apatite and zircon.

Three samples were collected from the Shicheng pluton, includ-ng two samples of the granite and one enclave of the plagioclasemphibolite. The granites are medium-coarse grained, and mainlyonsist of quartz (∼35%), plagioclase (∼30%), K-feldspar (∼30%) and
iotite (∼5%). The plagioclase amphibolite is medium grained, andainly consists of hornblende (45%), plagioclase (40%) and biotite
10%) and quartz (5%). Accessory phases include magnetite, apatitend zircon.

the southern NCC (modified after Zhao et al., 2005). (b) Simplified geological map of of the references to color in the artwork, the reader is referred to the web version

Due to hydrothermal alteration, hornblende is partially replacedby chlorite, and plagioclase is often replaced by sericite for mostsamples.

3. Analytical methods

3.1. Zircon U–Pb ages and trace elements

Zircons were separated using standard magnetic-gravimetrictechnology, and representative zircons were selected by

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and-picking under a binocular microscope. Then the zirconsere mounted in an epoxy mount and polished to section crystals

or analysis. Transmitted and reflected light micrographs wereaken before cathodoluminescence (CL) imaging, U–Pb dating andf isotope analysis. CL images were obtained using a CAMECAX-50 microprobe at the Institute of Geology and GeophysicsIGG), the Chinese Academy of Sciences, Beijing.

Zircon LA-ICPMS U–Pb dating and trace element analyses werearried out at the State Key Laboratory of Continental Dynamics,orthwest University, Xi’an, by using an Agilent 7500a ICP-MSquipped with a 193 nm LASER. Instrumental conditions and datacquisition methods follow those described by Yuan et al. (2004).elium gas was used as carrier gas to enhance transport effi-iency of the ablated materials. Spot diameter was 30 �m. Zircon1500 was used as the external standard with a recommended06Pb/238U age of 1065.4 ± 0.6 Ma (Wiedenbeck et al., 1995). Thetandard silicate glass NIST SRM610 was used to calibrate U, Thnd Pb concentrations. Raw data were processed using GLITTER.0 (Macquarie University), age calculations and concordia dia-rams were made using the ISOPLOT program of Ludwig (2003). Theommon Pb correction was made using the EXCEL program ComP-Corr# 151 (Andersen, 2002). Trace element concentrations werealibrated by using 29Si as internal calibration and NIST SRM610s reference material. The precision and accuracy of the NIST-610nalyses are 2–5 wt.% for most elements at the ppm concentrationevel.

.2. Zircon Lu–Hf isotopic analysis

In-situ zircon Lu–Hf isotope analysis was also carried out athe State Key Laboratory of Continental Dynamics, Northwestniversity, Xi’an, using a Nu Plasma HR MC-ICPMS (Nu Instru-ents Ltd., UK) equipped with a GeoLas 2005 193 nm ArF-excimer

aser-ablation system. The analytical procedures followed thoseescribed by Yuan et al. (2008). Typical ablation time for eachnalysis is about 30 s for 200 cycles, with a 10 Hz repetition rate,nd a laser power of 100 mJ/pulse. The analysis spots are usu-lly 44 �m and helium was used as carrier gas. εHf(t) valuesere calculated with the reference to the chondritic reservoir

CHUR) at the time of zircon crystallization. The decay con-tant for 176Lu of 1.865 × 10−11 year−1 (Scherer et al., 2001), theresent-day chondritic ratios of 176Hf/177Hf and 176Lu/177Hf ratiosf 0.282772 and 0.0332 (Blichert-Toft and Albarede, 1997) weredopted to calculate εHf(t) values. Single-stage model ages (TDM1)ere calculated referred to the depleted mantle with a present-day

76Hf/177Hf ratio of 0.28325 and 176Lu/177Hf ratio of 0.0384 (Nowellt al., 1998; Griffin et al., 2000). Two-stage Hf model ages (TDM2)ere calculated relative to the average continental crust with a

76Lu/177Hf ratio of 0.015 (Griffin et al., 2002). Zircon Hf modelges are interpreted following the convention that adopts TDM1 rel-tive to the depleted mantle when εHf(t) values are positive, butDM2 relative to average continental crust when εHf(t) values areegative.

.3. Whole-rock major and trace element analyses

Samples were crushed and powered to less than 200 meshes inn agate mill. Whole-rock major and trace elements were analyzedt the State Key Laboratory of Continental Dynamics, Northwestniversity, Xi’an. Major elements were analyzed by X-ray fluo-

escence (Rikagu RIX 2100). Trace and rare earth elements were
easured by an Agilent 7500a ICP-MS. Accuracies of the XRF anal-
ses are estimated to be better than 5% for major elements. Theccuracies of the ICP-MS analyses were estimated to be better than0% for trace elements.

esearch 226 (2013) 1– 20

4. Results

4.1. Zircon U–Pb ages, Hf isotopes and trace elements

The U–Pb, Lu–Hf isotopes and trace elements results are givenin supplemental electronic data Tables 1, 2 and 3 and illustratedin Figs. 2–4. The representative CL images of the studied zirconstogether with spot ages and εHf(t) values are also shown on Fig. 2.

The zircons in these samples are generally euhedral to subhe-dral, equant, trigonal to long prismatic and range from 50 to 300 �min lengths with length/width ratios of about 1:1 to 5:1. They com-monly show magmatic oscillatory or planar zoning features, andhave Th/U ratios >0.3, consistent with a magmatic origin (Hoskinand Black, 2000; Corfu et al., 2003; Grant et al., 2009) (Fig. 2). A fewzircons in the Shicheng pluton show core-rim textures (Fig. 2g).

4.1.1. Shipaihe gneissThree samples of the dioritic gneiss (SPH1101, SPH1102 and

SPH1103) from the Shipaihe area were selected for LA-ICPMS zir-con U–Pb dating, trace elements and in situ Lu–Hf isotopic analysis(Tables S1–S3).

Twenty-five spots were made on 25 zircon grains for sam-ple SPH1101. Twenty-two spots plot on a discordia trend, with aweighted mean 207Pb/206Pb age of 2506 ± 5 Ma, consistent with theupper intercept age of 2505 ± 19 Ma (Fig. 2a). Three analyses (spots5, 10 and 25) have younger 207Pb/206Pb ages of 2123–2445 Ma.Thirty spots for sample SPH1102 are displaced along a discordiatrend to upper intercepts at 2511 ± 11 Ma (Fig. 2b), with a weightedmean 207Pb/206Pb age of 2516 ± 18 Ma. Thirty spots were ana-lyzed for sample SPH1103 and 27 spots yielded a weighted mean207Pb/206Pb age of 2504 ± 4 Ma, similar to the upper intercept ageof 2504 ± 14 Ma (Fig. 2c). Three analyses (spots 9, 10 and 12) haveyounger 207Pb/206Pb ages between 2096 and 2364 Ma.

These zircons show a narrow range in initial 176Hf/177Hf ratiosfrom 0.2812 to 0.2814 (Table S2), yielding εHf(t) values of 2.2–7.8with a weighted mean of 4.9 ± 0.3 (Fig. 3a). They also produce anarrow range in TDM1 ages of 2516–2730 Ma, with a weighted meanof 2630 ± 10 Ma (Table 2, S2 and Fig. 3d), slightly older than their207Pb/206Pb ages.

Most of these zircons have similar REE patterns (Fig. 4a–c),which are characterized by an enrichment of HREE with(Yb/La)N = 33–11675 and (Yb/Sm)N = 4–57, negative Eu anomalies(Eu/Eu* = 0.3–0.9) and positive Ce anomalies (Ce/Ce* = 5–232), sim-ilar to magmatic zircons (e.g., Hoskin and Irland, 2000; Belousovaet al., 2002; Rubatto, 2002; Hoskin and Schaltegger, 2003; Hancharand van Westrenen, 2007). Some zircons show significantlyelevated LREE, poorly developed positive Ce and negative Euanomalies (Table S3 and Fig. 4), implying the presence of min-eral inclusions (Hoskin and Schaltegger, 2003; Schulz et al., 2006).Except for one spot with high Ti contents (>50 ppm), zirconsfrom these dioritic gneiss have relatively low Ti concentrationsof 1–34 ppm (Table S3). According to the Ti-in-zircon thermome-ter of Watson et al. (2006), this corresponds to temperatures of534–861 ◦C. The broad and elevated Ti-in-zircon temperature (TTi)range is diagnostic of a magma cooling from high temperatureaccording to Harrison et al. (2007).

4.1.2. Plagioclase amphibolite enclaveTwo samples of the amphibolite (SPH1104 and SPH1105) from

the Shipaihe area and one sample of the plagioclase amphibolite(SC1103) in the Shicheng pluton were selected for LA-ICPMS zir-con U–Pb dating, trace elements and in situ Lu–Hf isotopic analysis
(Tables S1–S3).
Thirty-one spots were analyzed for sample SPH1104 and 30spots yield a discordia line intersecting the concordia curveat 2501 ± 10 Ma, with a weighted mean 207Pb/206Pb age of


Fig. 2. (a–h) Zircon U–Pb concordia diagrams of samples collected from the Songshan area and representative CL images of zircons.

6 J. Zhang et al. / Precambrian Research 226 (2013) 1– 20

0

3

6

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18

21

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27

2400 2450 2500 2550 2600 2650 2700 2750 2800 2850

TDM1 (Ma)

Num

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(d) Dioritic gneiss

Mean = 2630±10 Ma

0

5

10

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30

-1 1 3 5 7 9 11

Num

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εHf(t)

Mean=4.9±0.3

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Mean = 4.7±0.4(b) Amphibolite

0

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Mean = 2634±13 Ma

0

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Rim

Core

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Core

F d fromz

22

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ig. 3. Initial Hf isotope ratio and Hf model ages for zircons from samples collecteircon Hf model ages.

502 ± 4 Ma (Fig. 2d). One analysis (spot 31) has a younger07Pb/206Pb age of 2446 Ma. Thirty spots were made on 30 zir-on grains for sample SPH1105, of which 26 plot on a discordia
rend to upper intercepts at 2506 ± 12 Ma (Fig. 2e), with a weighted
ean 207Pb/206Pb age of 2504 ± 5 Ma. Four analyses (spots 21, 26,8, 30) have younger 207Pb/206Pb ages of 2373–2429 Ma. Of 25nalyses for sample SC1103, 23 analyses yield a weighted mean

the Songshan area. (a–c) Histograms of initial zircon εHf(t). (d–f) Histograms of

207Pb/206Pb age of 2506 ± 21 Ma, consistent with the upper inter-cept age of 2506 ± 13 Ma (Fig. 2h). These ages are much older thanthose of granites from the Shicheng pluton, indicating the amphi-
bolite sample is a xenolithic origin. The other two analyses (spots5 and 20) yield relatively concordant ages with 207Pb/206Pb agesof 2639 ± 50 Ma, interpreted as the ages of xenocrystic/inheritedzircons (Fig. 2h).


Fig. 4. (a–h) Chondrite normalized REE diagrams of zircons from samples collected from the Songshan area. Normalization values for chondrite are taken from Sun andMcDonough (1989).

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These zircons also have a narrow range in initial 176Hf/177Hfatios (0.2812–0.2814; Table S2). The calculated εHf(t) values varyrom 0.7 to 8.1 with a weighted mean of 4.7 ± 0.4 (Fig. 3b), corre-ponding to TDM1 values of 2509–2788 Ma with a weighted meanf 2634 ± 13 Ma (Table 2, S2 and Fig. 3e), very similar to those ofhe dioritic gneiss.

Most of these zircons have trace element compositions andEE patterns very similar to those of the dioritic gneiss (Fig. 4d,, h), including an enrichment of HREE with (Yb/La)N = 44–4244,oderate negative Eu anomalies (Eu/Eu* = 0.4–0.9) and positive

able 1ajor and trace element compositions of the samples collected from the Songshan area i

Lithology Dioritic gneiss Plagi

Sample SPH11-01 SPH11-02 SPH11-03 SPH1

Major oxides (%)SiO2 63.20 62.35 62.22 56TiO2 0.48 0.53 0.50 0Al2O3 16.10 15.02 16.18 14Fe2O3t 4.11 4.32 4.23 6MnO 0.05 0.05 0.06 0MgO 2.51 3.19 2.63 6CaO 2.96 3.62 3.08 7Na2O 5.25 4.39 5.15 2K2O 4.11 4.81 4.30 2P2O5 0.31 0.42 0.32 0LOI 0.88 0.82 0.84 1Mg# 59 63 59 69TZr (◦C) 810 806 810 –TOTAL 99.96 99.52 99.51 99FeOt/MgO 1.47 1.22 1.45 0A/CNK 0.87 0.79 0.86 0K2O/Na2O 0.78 1.10 0.83 1

Trace elements (ppm)Ba 1375 1626 1448 843Rb 110 140 112 331Sr 1004 1172 1072 1837Nb 10.6 14.6 11.0 8Ta 0.58 1.00 0.56 0Hf 7.40 8.65 7.52 5Zr 340 389 352 281Th 27.1 38.8 22.2 4U 3.17 4.65 2.99 1Cr 148 182 155 323Ni 47.8 79.9 51.9 146Sc 6.18 7.35 6.80 14V 65.9 64.1 69.3 112Cu 26.6 5.03 17.9 26Pb 19.9 23.7 22.1 18Zn 63.9 69.1 68.4 93Co 12.7 15.9 13.3 29Ga 21.8 22.6 22.6 23

REE (ppm)La 53.4 117 69.0 110Ce 117 240 149 239Pr 14.0 25.7 16.9 28Nd 53.5 96.8 62.6 116Sm 8.84 15.3 10.2 19Eu 2.48 3.61 2.64 4Gd 5.13 8.78 5.91 11Tb 0.60 1.02 0.69 1Dy 2.58 4.23 2.91 5Ho 0.37 0.58 0.41 0Er 0.95 1.46 1.05 1Tm 0.12 0.17 0.13 0Yb 0.73 0.98 0.77 1Lu 0.11 0.14 0.11 0Y 11.6 18.0 12.9 23�REE 271 534 335 563Eu/Eu* 1.13 0.95 1.04 0Sr/Y 86 65 83 78(La/Yb)N 53 86 64 62Yb/Ta 1.26 0.97 1.38 5Ce/Nb 11.0 16.5 13.6 28Y/Nb 1.10 1.24 1.17 2

/CNK = Al2O3/(CaO + Na2O + K2O) molar ratio; Eu/Eu* = EuN/(SmN × GdN)1/2.

esearch 226 (2013) 1– 20

Ce anomalies (Ce/Ce* = 7–101). Except for one spot with highTi contents (>100 ppm), zircons from amphibolite have Ti con-centrations of 9–77 ppm (Table S3), corresponding Ti-in-zircontemperatures of 735–959 ◦C.

4.1.3. Shicheng graniteTwo samples of the granite (SC1101 and SC1102) from the

Shicheng pluton were selected for LA-ICPMS zircon U–Pb dating,trace elements and in situ Lu–Hf isotopic analysis (Tables S1–S3).

n southern NCC.

oclase amphibolite Granite

1-04 SPH11-05 SC11-03 SC11-01 SC11-02

.89 57.17 55.54 73.58 72.77

.67 0.65 1.53 0.32 0.36

.29 14.50 13.93 12.33 12.51

.64 6.52 12.08 3.75 3.93

.10 0.11 0.16 0.06 0.06

.47 6.02 3.76 0.18 0.18

.70 7.14 6.29 1.00 1.32

.14 2.50 2.44 3.19 3.30

.58 2.56 2.72 4.92 4.81

.74 0.71 0.50 0.06 0.07

.32 1.63 1.12 0.60 0.75 68 42 10 10

– – 872 887.54 99.51 100.07 99.99 100.06.92 0.97 2.89 18.75 19.65.70 0.73 0.76 0.99 0.96.21 1.02 1.11 1.54 1.46

978 1478 961 1109 306 64.6 233 212

1748 478 97.9 113.30 19.4 10.9 29.8 31.2.24 3.58 0.55 2.47 2.12.84 4.83 5.98 11.8 13.5

215 244 412 506.21 6.80 2.69 25.0 24.2.35 1.99 0.44 3.42 2.51

329 169 214 207 131 31.8 6.29 6.66.9 14.8 25.1 6.68 7.32

111 164 5.72 6.46.5 30.9 25.2 4.46 6.37.3 19.3 12.6 31.4 31.3.1 97.9 122 77.2 87.7.8 26.8 30.7 3.59 3.71.1 24.7 21.2 25.5 25.7

110 46.8 158 150 239 98.9 301 311.4 28.0 11.8 35.0 33.6

111 47.6 126 123.6 19.0 9.25 22.4 21.5.60 4.50 2.43 1.65 1.79.5 11.4 8.47 19.2 18.3.34 1.35 1.24 2.71 2.59.64 5.78 7.46 15.8 15.0.78 0.81 1.50 3.02 2.90.91 2.02 4.32 8.71 8.47.22 0.24 0.63 1.27 1.25.27 1.51 4.04 8.19 8.01.18 0.22 0.62 1.21 1.20.5 25.4 43.0 88.2 86.0

559 288 793 784.94 0.93 0.84 0.24 0.28

69 11 1 1 52 8 14 13.22 0.42 7.36 3.32 3.77.8 12.3 9.1 10.1 10.0.83 1.31 3.94 2.96 2.76

rian Research 226 (2013) 1– 20 9

t2

a(i2

amti

0−2fac

awnl(Ni

4

y

4

6TAr(a

ra

Fig. 6. (a) A/NK vs. A/CNK plots showing that the rocks from the Songshan area are


Thirty spots of sample SC1101 plot on a discordia trend tohe upper intercept age of 1772 ± 33 Ma, with a weighted mean07Pb/206Pb age of 1775 ± 6 Ma (Fig. 2f). Twenty-nine spots werenalyzed for sample SC1102. A few zircons show core-rim texturesFig. 2g). Of 29 analyses, 23 yields a discordiant age intersect-ng the concordia curve at 1777 ± 13 Ma, with a weighted mean07Pb/206Pb age of 1776 ± 6 Ma, interpreted as the crystallizationge of the rock (Fig. 2g). The cores (spots 9, 11, 15, 20, 21, 25) com-only show micro-scale oscillatory (Fig. 2g) and plot on a discordia

rend, with a weighted mean 207Pb/206Pb age of 1873 ± 13 Ma, sim-lar to the upper intercept age of 1872 ± 35 Ma.

Zircons from the granites have initial 176Hf/177Hf ratios from.2812 to 0.2816 (Table S2) and produce εHf(t) values from −16.7 to1.8 with a weighted mean of −10.2 ± 0.6, corresponding to TDM2 of551–3466 Ma with a weighted mean of 3048 ± 31 Ma (Fig. 3c and). Six spots of inherited zircons from sample SC1102 (207Pb/206Pbges of 1870–1877 Ma) yield negative εHf(t) values of −11.9 to −7.2,orresponding to the TDM2 of 2959–3114 Ma.

These zircons have similar REE patterns (Fig. 4f and g), whichre characterized by steep slopes from the LREE to the HREEith (Yb/La)N = 30–160602 and (Yb/Sm)N = 9–79, very pronouncedegative Eu anomalies (Eu/Eu* = 0.1–0.2) and positive Ce anoma-

ies (Ce/Ce* = 1.1–61). Their Ti contents vary from 6 to 20 ppmTable S3), and the calculated temperatures vary from 694 to 804 ◦C.o apparent differences in REE contents and patterns are observed

n the cores and the rims of zircon grains.

.2. Whole-rock major and trace element geochemistry

Eight samples were selected for major and trace elements anal-ses, the results are listed in Table 1.

.2.1. Dioritic gneissDioritic gneiss samples have SiO2 concentrations of

2.2–63.2 wt.%, and plot in the quartz monzonite field on theAS diagram (Fig. 5). They have metaluminous (A/CNK = moll2O3/(CaO + Na2O + K2O), 0.79–0.87) characteristics and exhibitelatively low MgO (2.5–3.2 wt.%), Cr (148–182 ppm), Ni48–80 ppm), and high Na2O (4.4–5.3 wt.%), K2O (4.1–4.8 wt.%),
nd fall in shoshonitic series (Fig. 6).
These dioritic gneisses show significant enrichment of LREEelative to HREE with high (La/Yb)N ratios of 53–86, without Eunomalies (Eu/Eu* = 1.0–1.1) (Fig. 7a). In the spidergrams, they are

Fig. 5. TAS diagram for samples collected from the Songshan area.

metaluminous. (b) K2O vs. SiO2 diagrams showing the high-K compositions of thesesamples (after Rickwood, 1989). Symbols are the same as those in Fig. 5.

characterized by enrichment of LILE (e.g., Ba, Rb, K) and LREE, rel-atively depleted in HFSE (e.g., Nb, Ta, Ti) (Fig. 7b). They have lowY and Yb contents, and high Sr/Y and (La/Yb)N ratios, similar toadakite and TTG (e.g., Martin et al., 2005).

4.2.2. Plagioclase amphiboliteThe plagioclase amphibolites contain SiO2 concentrations of

55.5–57.2 wt.%, and plot in the diorite and gabbroic diorite fieldson the TAS diagram (Fig. 5). They exhibit relatively high MgO(3.8–6.5 wt.%), Cr (169–329 ppm), Ni (32–146 ppm), low Na2O(2.1–2.5 wt.%), K2O (2.6–2.7 wt.%). All the samples are metalum-inous in composition (A/CNK = 0.70–0.76), and plot to high-Kcalc-alkaline series (Fig. 6).

These amphibolites show LREE-enriched patterns, withoutobvious Eu anomalies (Eu/Eu* = 0.8–0.9) (Fig. 7c). In the spider-grams, they also show an enrichment in LILE (e.g., Ba, Rb, K) andLREE, and relative depletion in HFSE (e.g., Nb, Ta, Ti), Th and U(Fig. 7d).

4.2.3. GraniteThe granite samples are highly siliceous with SiO2 concentra-

tions of 72.8–73.6 wt.% (Fig. 5). They exhibit relatively low CaO(1.0–1.3 wt.%), Al O (12.3–12.5 wt.%) and MgO (0.2 wt.%), high
2 3Na2O (3.2–3.3 wt.%), K2O (4.8–4.9 wt.%) and K2O/Na2O (1.46–1.54).They also have high Fe* [FeOt/(FeOt + MgO)] of 0.95, similar tothe ferroan granitoids of Frost et al. (2001). The granites are

10 J. Zhang et al. / Precambrian Research 226 (2013) 1– 20

F elemef r SunM

ml

1(mShlcev(

ig. 7. Chondrite-normalized REE patterns and Primitive mantle-normalized trace) from the Songshan area in the southern NCC. Chondritic REE abundances are afte

cDonough and Sun (1995).

etaluminous in composition (A/CNK = 0.96–0.99) and rich in alka-is plotting to high-K calc-alkaline series (Fig. 6).

They exhibit an enrichment in LREE with (La/Yb)N ratios of3 to 14, and significant negative Eu anomalies (Eu/Eu* = 0.2–0.3)Fig. 7e). In the spidergrams, they are characterized by an enrich-

ent in LILE (e.g., Ba, Rb, K, Pb) and LREE, and relative depletion inr, P and HFSE (e.g., Nb, Ta, Ti) (Fig. 7f). Meanwhile, these granitesave high K2O/Na2O, Fe* and total alkalis contents, and relatively

ow CaO, Al2O3, MgO and Sr contents (98–113 ppm) (Table 1),
onsistent with the characteristics of A-type granite (e.g., Collinst al., 1982; Whalen et al., 1987). In the plots of 10,000 Ga/Als. FeOt/MgO and Nb, they indeed fall in the A-type granite fieldFig. 8).
nt diagrams for dioritic gneiss (a and b), amphibolite (c and d) and granite (e and and McDonough (1989) and the primitive mantle trace element contents are after

4.2.4. Zr saturation temperatureZr saturation temperatures (TZr) were calculated after Watson

and Harrison (1983) and range from 806 to 810 ◦C for dioritic gneissand 872–887 ◦C for granite from the Shicheng pluton. Because thesamples of dioritic gneiss usually contain few inherited zircons,these temperatures provide good estimate of magma temperaturesaccording to Miller et al. (2003). If samples contain some inheritedzircons, the temperatures would constrain upper limit on magmatemperature according to Miller et al. (2003). Because of their low
concentrations of SiO2 (55.5–57.2 wt.%) and Zr (215–281 ppm) aswell as its M value (2.46–2.63) outside the experimental calibra-tion range of Watson and Harrison (1983), the amphibolites arenot suitable for this thermometry.


F et ala

5

5

piha(

5

2

wa2

aadεd

TS

ig. 8. 10,000 Ga/Al vs. FeOt/MgO (a) and Nb (b) discrimination diagrams of Whalens those in Fig. 5.

. Discussion

.1. Source nature

Zircon U–Pb ages, εHf(t) values and Hf model ages of sam-les are summarized in Table 2. Most zircons including the

nherited zircons exhibit oscillatory or planar zoning, high Th/U,igh formation temperature, clear negative Eu anomalies, as wells HREE-enriched patterns, suggesting their magmatic originsTable S3 and Figs. 2 and 4).

.1.1. Dioritic gneissThe zircons from these gneisses yielded a weighted mean

07Pb/206Pb age of 2505 ± 3 Ma for Shipaihe dioritic gneiss (Table 2),hich is interpreted as its protolith intrusion age. Our results

re consistent with previous zircon U–Pb ages from 2493 ± 7 to520 ± 17 Ma (Wang et al., 1987, 2004b; Diwu et al., 2011).

However, these zircons have less positive εHf(t) values of 2.2–7.8nd slightly older TDM1 of 2516–2730 Ma than 2.5 Ga (Table S2
nd Fig. 3a and d), suggesting that the protoliths were not directlyerived from the differentiation of a depleted mantle. The positiveHf(t) values and zircon Hf model ages of 2.5–2.7 Ga indicate that theioritic gneiss was produced by the partial melting of newly formed
able 2ummary of zircon U–Pb age and Lu–Hf isotopic compositions of the samples collected fr

Sample Rock type U–Pb age (Ma) Lu–H

εHf(t)

SPH1101 Dioritic gneiss 2506 ± 5 (n = 22)2505 ± 3

2.2–6SPH1102 Dioritic gneiss 2516 ± 18 (n = 30) 2.5–7SPH1103 Dioritic gneiss 2504 ± 4 (n = 27) 3.3–7SPH1104 Plagioclase

amphibolite2502 ± 4 (n = 30)

2503 ± 3

2.5–6

SPH1105 Plagioclaseamphibolite

2504 ± 5 (n = 26) 3.4–7

2506 ± 21 (n = 23) 0.7–8SC1103 Plagioclase

amphibolite2639 ± 50 (n = 2) 5.7–6

(xenocrystic/inheritedzircon)

(xenozirco

SC1101 Granite 1775 ± 6 (n = 30)

1776 ± 4

−12.0

SC1102 Granite1776 ± 6 (n = 23)

−16.7−3.7

1873 ± 13 (n = 6)(inherited zircon)

−11.9(inhe

. (1987), showing the A-type nature of the Shicheng granites. Symbols are the same

juvenile crust. Thus, the U–Pb and Hf isotope feature of these zir-cons indicates that the source materials of the dioritic gneisses oflate Neoarchean in the southern NCC were juvenile crust which wasreworked during the ca. 2.5 Ga anatexis, resulting in the widespreadrocks of late Neoarchean in the NCC.

5.1.2. AmphiboliteThe amphibolites have yielded a weighted mean 207Pb/206Pb

age of 2505 ± 3 Ma (Table 2). This suggests that the protoliths of theamphibolites were produced simultaneously with dioritic gneisses.These ages are identical to the Neoarchean TTG gneisses, amphibo-lites and granites widely distributed in the Songshan area (Wanget al., 2004b; Wan et al., 2009; Zhou et al., 2009a, 2011; Diwu et al.,2011).

The positive εHf(t) values of 0.7–8.1 and older zircon Hf modelages of 2509–2788 Ma (Table S2) indicate that the protoliths of theamphibolites were juvenile basic crust.

5.1.3. Granite
Two granites from Shicheng pluton yielded a weighted mean
207Pb/206Pb age of 1776 ± 4 Ma (Table 2) for magmatic zircon, con-sistent with previous zircon U–Pb ages of 1775 ± 9 Ma (Wan et al.,2009). The Xiong’er volcanic rocks of same ages constitute a large

om the Songshan area in southern NCC.

f isotopes

Hf model age (Ma)

.2 (n = 25)4.9 ± 0.3

2580–27302630 ± 10.2 (n = 30) 2551–2726

.8 (n = 30) 2516–2686

.1 (n = 31)

4.7 ± 0.4

2579–2715

2634 ± 13.5 (n = 30) 2530–2682

.1 (n = 23) 2509–2788

.3 (n = 2) 2690–2712

crystic/inheritedn)

(xenocrystic/inheritedzircon)

to −7.5 (n = 30)

−10.2 ± 0.6

2901–3177

3048 ± 31 to −6.1 (n = 20) 2819–3466

to −1.8 (n = 3) 2551–2670 to −7.2 (n = 6)

rited zircon)2959–3114 (inheritedzircon)

1 rian R

v2CoP

tnco−a

5

5

facetf

ard(cLTMao

caderoa2mtga2AaMpc1ita1

dfTiLfo

2 J. Zhang et al. / Precamb

olcanic belt along the southern margin of the NCC (Zhao et al.,004, 2009; Peng et al., 2008; He et al., 2009; Wang et al., 2010c;ui et al., 2011). Paleoproterozoic mafic dikes also occur through-ut the NCC (e.g., Halls et al., 2000; Wang et al., 2003, 2004a, 2008;eng et al., 2005, 2007, 2008; Hou et al., 2006; Han et al., 2007).

Most zircons of the granites have negative εHf(t) values of −16.7o −6.1, corresponding to TDM2 of 2819–3466 Ma (Table 2). Theegative εHf(t) values and much older zircon Hf model ages indi-ate that the Archean crustal rocks were involved in the formationf these granites. A few zircons have relative high εHf(t) values of3.7 to −1.8 and similar zircon Hf model ages to dioritic gneiss andmphibolite (Fig. 10), suggesting its inherited origin.

.2. Petrogenesis

.2.1. Dioritic gneissGenerally, the dioritic gneisses in the Shipaihe area have highly

ractionated REE patterns with weak to negligible negative Eunomalies, and negative HFSE anomalies (Fig. 7), similar to theharacteristics of the average TTGs (e.g., Martin et al., 2005). How-ver, they are different from typical TTG (Martin et al., 2005) dueo their low SiO2 (62.2–63.2 wt.%), high K2O, K2O/Na2O ratios anderromagnesian characteristics.

The high Sr/Y and La/Yb ratios are typical characteristics of TTGsnd adakites (Martin et al., 2005). Such a signature could eitheresult from melting of a high Sr/Y source (Moyen, 2009), or withifferent roles of plagioclase, amphibole or garnet during meltinge.g., Drummond and Defant, 1990; Martin et al., 2005) or fractionalrystallization (Macpherson et al., 2006). Melting of a high Sr/Y anda/Yb source is a possible explanation, however, high Mg# (59–63;able 1) is inconsistent with such a suggestion (usually low Mg#;oyen, 2009). High Sr/Y and La/Yb ratios in the dioritic gneisses

re likely due to different contributions of plagioclase, amphiboler garnet in their sources.

The absence of Eu anomalies accompanied by high Sr and Euontents and Sr/Y ratios reflects little contributions of plagioclases a residual phase during partial melting or via its fractionationuring magma differentiation. These dioritic gneisses display steep,nriched LREE relative to HREE patterns with High Sr/Y and La/Ybatios (Table 1 and Fig. 7), which are consistent with fractionationf garnet and/or amphibole or residual garnet and/or amphibolet relatively high pressures (e.g., Castillo et al., 1999; Martin et al.,005). Amphibole has a high KD for HREEs, but medium REEs areore compatible than HREEs (e.g., Dy); the low HREE concen-

rations and normalized Dy/Yb > 2 point to a predominant role ofarnet as a fractionated or residual phase. Furthermore, fraction-tion of garnet could also elevate SiO2 content (Macpherson et al.,006) and reduce Al2O3 content. The low SiO2 (<63 wt.%) and highl2O3 (∼16 wt.%) indicate that the high Sr/Y and La/Yb in these rocksre due to the garnet as a residual phase at relatively high pressures.oreover, the large variation of HREE and the relatively flat HREE

attern for zircons from the dioritic gneisses (Fig. 4a–c) also supportoeval precipitation of zircons with garnets (e.g., Schaltegger et al.,999; Rubatto, 2002; Rubatto and Hermann, 2003). Partial melt-

ng experiments show that magmas generated at pressures higherhan 1.5 GPa would be able to leave garnet and possibly amphiboles residual phases (e.g., Sen and Dunn, 1994; Rapp and Watson,995; Litvinovsky et al., 2000; Patino Douce, 2005).

In addition, zircon U–Pb and Hf isotopic data show that theioritic gneisses derived from the juvenile crust which extractedrom the mantle shortly before the occurrence of partial melting.heir trace element features are similar to those of arc tholei-
te (Pearce and Cann, 1973; Pieter, 2006), e.g. an enrichment inREE and LILE and a depletion in HREE and HSFE. These chemicaleatures suggest that the dioritic gneisses originated from anatexisf juvenile arc-type crust.
esearch 226 (2013) 1– 20

5.2.2. AmphiboliteAmphibolties in the Shipaihe area have high MgO, Cr and Ni

contents (Table 1) compared with crust-derived magma, indicat-ing a dominant derivation from the mantle. The Mg# numbersof amphibolite in the Shipaihe area range from 68 to 69, simi-lar to high-magnesian tholeiitic basalt. High Ba (up to 978 ppm)and Sr (up to 1837 ppm) contents, much higher than its coun-terpart of continental crust (Ba = 390 ppm; Sr = 325 ppm; Rudnickand Fountain, 1995), exclude the possibility of massive crustalassimilation. These rocks have Th/U ratios of 3.1–3.4 lower thanthose of crustal rocks (∼5.0) (Rudnick and Fountain, 1995) butsimilar with MORBs (∼3.0) and OIBs (∼3.4), also supporting thatcrustal assimilation played little contribution in their petrogenesis.These amphibolites are enriched in LREE and LILEs and depleted inHFSEs (Fig. 7), indicating their origin from an enriched lithosphericmantle. Compared to those of the dioritic gneisses, zircons fromamphibolites have higher Ti contents and thus higher Ti-in-zircontemperatures (Table S3), consistent with the general consensus thatmafic melts are produced at higher temperatures than felsic ones.Based on the above observations, a juvenile lithospheric mantlemodified by LILE and LREE-enriched melt/fluid is suggested as thesource of amphibolites.

However, the amphibolite from the Shicheng pluton displays theless fractionated REE patterns with higher HREE and Y, and lowerSr and Eu contents, Sr/Y and (La/Yb)N ratios (Table 1 and Fig. 7).These features imply that this amphibolite was produced at lowerpressure. Therefore, we suggest that partial melting of a juvenilelower crust and lithospheric mantle at different depths perhapsinduced by underplating of mantle-derived magmas resulted in theformation of all dioritic gneisses and amphibolites at ca. 2.5 Ga.

5.2.3. GraniteThe Shicheng samples have geochemical characteristics (Table 1

and Figs. 6 and 8) of A-type granite (e.g., Whalen et al., 1987; Eby,1992; King et al., 1997; Bonin, 2007). In the total FeO/MgO and Nbvs. 10,000 Ga/Al discrimination diagrams of Whalen et al. (1987)(Fig. 8), these granite also plot in the A-type granite field. Their highZn contents of 77–88 ppm are similar with A-type granites (Whalenet al., 1987). Furthermore, they have low Nb and Ta contents,and high Yb/Ta (3.32–3.77), Ce/Nb (ca. 10) and Y/Nb (2.76–2.96)ratios, similar with A2-type granites which were mainly formed ina post-collision extensional setting according to the geochemicalsubdivision of A-type granites by Eby (1992).

Petrogenesis of A-type granites has still been controversial sincethe term was introduced by Loiselle and Wones (1979). Severalgenetic models have been proposed, including fractional crys-tallization of mantle-derived melts, partial melting of either themantle or the crust, AFC processes (crustal assimilation plus frac-tional crystallization) and magma mixing between basaltic andcrustal melts (e.g., Collins et al., 1982; Clemens et al., 1986; Whalenet al., 1987; Creaser et al., 1991; Eby, 1992; Turner et al., 1992;Frost and Frost, 1997; King et al., 1997; Sylvester, 1998; Frost et al.,1999; Wu et al., 2002; Kemp et al., 2005; Kim et al., 2006; Yang et al.,2006; Dall’Agnol and de Oliveira, 2007; Wei et al., 2008; Wang et al.,2010c).

Since the granite cannot be drived directly from mantle(Hofmann, 1988) the high SiO2 (>70 wt.%), and low MgO (<0.2 wt.%)and Mg# (<11), suggest that the Shicheng A-type granite was notdirectly derived from the mantle. All the zircons have negativeεHf(t) values and old Hf model ages, suggesting their origin of thegranites from the old continental crust. Mafic and intermediaterocks associated with the Shicheng granite have not been found.
Although some contemporaneous mafic dykes occur in TNCO(e.g., Wang et al., 2004a, 2008; Peng et al., 2005; Han et al., 2007),they do not display a continuous compositional trend with the A-type granite. The zircons of Shicheng A-type granite have εHf(t)

rian R

vtnTnnnSSog

gpcm(htEaaDi

Ftee


alues lower than contemporaneous mafic dikes in the NCC (−6.4o 0.4, Han et al., 2007), suggesting that the granitic rocks canot be generated by fractional crystallization of mafic magma.he Shicheng granites have extremely high SiO2 contents and aarrow range (68–74 wt.%, Zhao and Zhou, 2009), also suggestingone of fractional crystallization origin. Absence of contempora-eous mafic to intermediate rocks from adjacent regions of theongshan area excludes the magma mixing as an origin of thehicheng granite. Therefore, we suggest that the partial meltingf continental crust is a viable mechanism for the Shicheng A-typeranite.

The negative Eu, Ba and Sr anomalies of the Shicheng A-typeranite (Fig. 7) suggest that plagioclase is an important residualhase. The flat HREE distribution can be explained by plagio-lase rather than garnet as a residual phase, consistent with theelting at low pressure. The high Zr saturation temperatures

TZr) and Ti-in-zircon temperatures (755–887 ◦C) demonstrate aigh temperature origin (∼900 ◦C). Such a low pressure and highemperature required an extensional setting during the melting.xperimental studies indicate that dehydration melting of tonalitend granodiorite may produce melts similar to A-type granites
t low pressures (4 kbar) and high temperatures (950 ◦C) (Patinoouce, 1997). The obtained melts are usually high in K2O and high
n K2O/Na2O > 1, consistent with our results.

ig. 9. (a–d) Histograms showing 207Pb/206Pb ages and Hf model ages of Precambrian zircext. The data sources of Hf model age for magmatic zircon are from these studies: Chen et al. (2009), Liu et al. (2009, 2011c), Du et al. (2010), Huang et al. (2010, 2012), Jiang et al.t al. (2012). The data sources of U–Pb and Hf model ages for detrital zircon are from Xia

esearch 226 (2013) 1– 20 13

5.3. Precambrian crustal evolution of the southern NCC

5.3.1. ca. 2.5 Ga crustal reworkingThe gneisses and amphibolites in the Songshan area all con-

tain igneous zircons that yielded identical 207Pb/206Pb ages of ca.2.5 Ga. This demonstrates that the protoliths for these gnesises andamphibolites in the southern TNCO formed at Neoarchean. Thetectonothermal event at ca. 2.5 Ga is also widespread throughoutthe NCC (e.g., Guan et al., 2002; Zhao et al., 2002, 2008a,b; Kröneret al., 2005a,b; Wilde et al., 2005; Grant et al., 2009; Liu et al., 2009,2011c,d; Wang et al., 2011). Massive zircon geochronology for base-ment rocks of the TNCO (e.g., Guan et al., 2002; Zhao et al., 2002,2008a,b; Kröner et al., 2005a,b; Wilde et al., 2005; Chen et al., 2006;Diwu et al., 2007, 2010a, 2011; Han et al., 2007; Guo et al., 2008; Heet al., 2009; Liu et al., 2009, 2011c; Du et al., 2010; Huang et al., 2010,2012; Jiang et al., 2010; Wang et al., 2010b,c; Cui et al., 2011; Zhanget al., 2011, 2012c; Zhou et al., 2011; Geng et al., 2012), as well asthe lower crust (e.g. Zhang et al., 2012a,b and references therein),have devoted to the Archean crustal evolution of the NCC in recentyears. As shown in the histogram of zircon U–Pb ages (Fig. 9a), asignificant magmatic event in the TNCO happened at ca. 2.5 Ga. The
U–Pb ages of detrital zircons from the TNCO further confirm thatthe ca. 2.5 Ga magmatic event was a predominant thermal eventduring the Neoarchean (Fig. 9c).
ons in the TNCO. The data sources of U–Pb age for magmatic zircon are given in thet al. (2006), Diwu et al. (2007, 2010a, 2011), Han et al. (2007), Guo et al. (2008), He

(2010), Wang et al. (2010c), Zhou et al. (2011), Zhang et al. (2011, 2012c) and Genget al. (2006c), Liu et al. (2011a,b, 2012a,b,c) and Geng et al. (2012).

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Zircon Hf isotope studies are important in deciphering theource nature from which the zircon host rocks were produced.lthough there indeed exist a few zircons of ca. 2.5 Ga with neg-tive εHf(t) values (Fig. 10), which suggests some involvements ofncient crustal rocks in their origins, the predominant magmaticircons as well as detrital zircons of ca. 2.5 Ga U–Pb ages have lessositive εHf(t) values which yielded Hf model ages of ca. 2.7 GaFigs. 9 and 10) much older than their U–Pb ages, implying that therotoliths for these zircons were produced by the partial melting of

juvenile crust rather than direct differentiation from the mantle.his suggests that ca. 2.5 Ga magmatic event represent an impor-ant period of crustal reworking of the ca. 2.7 Ga juvenile crust.

Furthermore, as shown in Fig. 10, some magmatic and detri-al zircons of ca. 2.5 Ga have high positive εHf(t) values yieldingf modle ages of 2.5–2.6 Ga, very close to their U–Pb ages. This

ndicates that the ca. 2.5 Ga thermal event was accompanied by arustal growth, even though its insignificance. The occurrence of ca..5 Ga mafic to ultramafic rocks in the TNCO supports the presencef a juvenile crustal growth at ca. 2.5 Ga (Polat et al., 2006a; Wang,009).

In summary, the ca. 2.5 Ga was an important crustal reworking
vent in the TNCO with only a subordinate crustal growth. Thisvent produced the widespread protoliths containing the 2.5 Gaagmatic zircons.
ig. 10. (a and b) εHf(t) versus age for the dioritic gneiss, amphibolite and granite from

olor in the artwork, the reader is referred to the web version of the article.)

esearch 226 (2013) 1– 20

5.3.2. ca. 2.7 Ga crustal growthThe Neoarchean is a crucial stage when continental crust was

rapidly produced in our planet. Previous works have demonstratedthat the principal continental growth occurred in the Neoarchean atca. 2.7 Ga (e.g., McCulloch and Bennett, 1994; Condie, 1998, 2000).This is true in many ancient cratons around the world, such as theSuperior Craton (Beakhouse et al., 1999; Polat and Kerrich, 2000;Percival et al., 2001), southern West Greenland Craton (Thrane,2002; Steenfelt et al., 2005; Polat et al., 2008, 2011), the Pilbara andYilgarn Cratons of western Australia (Bateman et al., 2001; Blake,2001; Rasmussen et al., 2005). Thus the ca. 2.7 Ga tectonother-mal events were an extremely important period for the continentgrowth on Earth.

However, on the NCC, upper crustal rocks containing zirconswith ca. 2.7 U–Pb Ga ages were only developed in a few localitesof the Eastern Block and TNCO (e.g., Jahn et al., 1988, 2008; Zhuanget al., 1997; Du et al., 2003, 2010; Polat et al., 2006b; Wan et al.,2011; Zhai and Santosh, 2011). These zircons have positive εHf(t)values and TDM1 ages very close to their U–Pb ages (Du et al.,2010; Jiang et al., 2010; Wan et al., 2011), indicating that theca. 2.7 Ga tectonothermal event represent juvenile crustal growth
from depleted mantle (Zhai and Santosh, 2011). A few zirconsfrom lower crust granulite xenoliths collected from the TNCO alsoyielded 2.6–2.7 Ga U–Pb ages, producing positive εHf(t) values and
the TNCO. Data sources are given in Fig. 9. (For interpretation of the references to

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f model ages of 2.7–2.8 Ga (Zhang et al., 2012a,b and referencesherein), consistent with principal global continental growth.

The conclusion that the ca. 2.7 Ga tectonothermal event waslso an exceedingly important crustal growth event on the TNCOas been extracted from Hf isotope compositions of huge amountsf magmatic and detrital zircons (Figs. 9 and 10). The peak of Hfodel ages at ca. 2.7 Ga (Figs. 9 and 10) for large amounts of ca.

.5 Ga magmatic zircons further confirms that the ca. 2.7 Ga was anmportant period for crustal growth and the ca. 2.5 Ga was a mainrustal reworking event in the TNCO.

In addition, for the TTG gneisses and amphibolites in the Taihuaomplex in the southern margin of TNCO, a few magmatic zirconsf 2.7–2.8 Ga ages and inherited zircons of 2.9–3.1 Ga ages werebtained (Liu et al., 2009; Diwu et al., 2010a; Huang et al., 2010,012). These samples also exhibit a range εHf(t) values of −11.8o 9.48 (Fig. 10), indicating that the reworking of ancient crustal

aterials to some extents was also involved in the 2.7–2.8 Gaectonothermal event.

.3.3. Earliest crust formation in the TNCOca. 3.8 Ga zircons of U–Pb ages have been reported from Anshan

etamorphic terrain (Liu et al., 1992, 2008; Song et al., 1996; Want al., 2005) and Caozhuang complex in Eastern Hebei (Wu et al.,005b), indicating the presence of old continental crust in the East-rn Block at least as old as 3.8 Ga. The 3.8 Ga zircons from the Easternlock yielded Hf model ages up to 4.0 Ga (Wu et al., 2005b, 2008).hese zircons have positive εHf(t) values (Wu et al., 2005b, 2008;iu et al., 2008), suggesting the formation of the oldest crust per-aps as old as 4.0 Ga in the NCC. Zircons of detrital xenocrysts with–Pb ages of 3.9–4.1 Ga ages have been recovered from Paleozoicyroclastic rocks in Qinling (Wang et al., 2007; Diwu et al., 2010b)lthough its derivation is still not well-constrained.

Based on the studies on the granulite xenoliths from Mesozoicolcanic rocks in Xinyang, Henan Province, the southern margin ofhe NCC, Zheng et al. (2004) found the oldest zircon of ca. 3.6 Ga inhe lower crust. These zircons have negative εHf(t) values, produc-ng Hf modal age up to 4.0 Ga. Thus, the available data indicate thendeed presence of ca. 4.0 Ga lower crust in the southern margin ofhe NCC, just as the upper crust of the NCC, which was reworked ata. 3.6 Ga.

As also shown in Figs. 9d and 10b, some detrital zircons ofa. 3.5 Ga from the Zhongtiao Complex, the southern TNCO, gaveegative εHf(t) values and Hf model ages of 3.8–4.0 Ga. All thesebservations demonstrated the earliest continental crust of theouthern TNCO was indeed formed in the Late Hadean–Earlyrchean.

.3.4. ca. 1.8 Ga post-collisional magmatismThe ca. 1.85 Ga is another crucial tectonothermal event in NCC,

s defined by metamorphic zircons from various high-grade rockshroughout the TNCO (e.g., Guan et al., 2002; Wilde et al., 2002;hao et al., 2002; Guo et al., 2005; Kröner et al., 2005a, 2006;an et al., 2006; Xia et al., 2006a; Zhang et al., 2009; Wang

t al., 2010a,b). Zircon U–Pb dating on anatectic granites from theCC, such as Huai’an charnockite, Dapinggou garnet-bearing K-ranite, and Huijiazhuang gneissic granite, has yielded similar agesf 1832 ± 11 to 1850 ± 17 Ma (Zhao et al., 2008a,b). The U–Pb andf isotopic data of the inherited zircons of Shicheng granite pre-

ented in this study reveal that the 1.87 Ga was a reworking event ofhe basement rocks. Recent studies also revealed that syn-collision

agmatism occurred at 1.90–1.85 Ga (e.g., Geng et al., 2000; Zhaot al., 2008b) in the TNCO.

After the amalgamation of two blocks, the ca. 1.8 Ga mag-atism was vigorous including voluminous Xiong’er volcanics,

otassic granites and coeval mafic dyke swarms in the TNCOe.g., Wang et al., 2003, 2004a, 2008; Zhao et al., 2004; Peng

esearch 226 (2013) 1– 20 15

et al., 2005, 2007, 2008; Han et al., 2007; Hou et al., 2008a,b;He et al., 2009; Zhao et al., 2009; Wang et al., 2010c; Cui et al.,2011). Most zircons from the ca. 1.8 Ga magmatic rocks havenegative εHf(t) values (Fig. 10a), suggesting their derivation fromthe reworking of the old crust. Furthermore, most of these rocksexhibit insignificant deformation or metamorphism, implying thattheir formation post-dates the collisional event. Around 1.8 Ga,the amalgamated NCC was suffered extensively orogenic collapseand extension, resulting in the generation of voluminous post-collisional magmatic rocks and sedimentary rocks in the craton (Luet al., 2008b).

5.3.5. 2.5–2.0 Ga crustal reworking of the TNCO2.5–2.0 Ga magmatic rocks are also preserved through the TNCO.

SHRIMP zircon U–Pb dating on gray gneisses of Taihua complexin the Yiyang area revealed their formation age of 2316 ± 16 to2336 ± 13 Ma (Diwu et al., 2007), The negative εHf(t) values ofthese zircons indicate that they were derived from the rework-ing of ancient crust (Fig. 10a). Zircon U–Pb results also revealthat granitic rocks in the Hengshan–Wutai–Fuping Complexes pro-duced in a range of 2358–2024 Ma (Guan et al., 2002; Zhao et al.,2002; Kröner et al., 2005a; Wilde et al., 2005). Garnet-syenogranitesof the Huai’an Complex dated by zircon LA-ICPMS method formedbetween 1977 and 2003 Ma. The positive εNd(t) values and Hf modelages of ca. 2.5 Ga indicate that these rocks of ca. 2.0 Ga were gener-ated by partial melting of ca. 2.5 Ga juvenile crust (Zhang et al.,2011). Furthermore, recent zircon U–Pb analyses have revealedthe widespread presence of Paleoproterozoic (2.5–2.0 Ga) detri-tal zircons in the Yejishan Group of the Lüliang Complex (Liuet al., 2011a), the Hutuo Group (Liu et al., 2011b), the GantaoheGroup in the Zanhuang Complex (Liu et al., 2012a), the SongshanGroup (Liu et al., 2012b) and Zhongtiao Group (Liu et al., 2012c).Those zircons show εHf(t) values range from positive to nega-tive and Hf model ages mostly between 2.5 and 3.0 Ga (Fig. 10b),indicating that the Archean crust was intensely reworked during2.5–2.0 Ga.

5.4. Tectonic implications

The integration of zircon U–Pb, Hf isotopic and geochemical dataprovides important insights into the Neoarchean to Paleoprotero-zoic crust evolution, especially for the southern of the NCC. Fourmajor evolution stages can be summarized as follows:

(1) Hf isotopic compositions demonstrate that ca. 2.7 Ga was a sig-nificant stage for the continental crustal growth in the NCC,consistent with the other cratons in the world.

(2) The present zircon Hf isotopic and U–Pb data suggest that thejuvenile crust was reworked at ca. 2.5 Ga, shortly after the con-tinental growth at ca. 2.7 Ga. The enrichment in LILE and LREEas well as negative anomalies in P and HFSE are characteris-tics of the continental crust that is usually assumed to originatefrom arc-derived magmas (Taylor and McLennan, 1995). There-fore, the arc-like trace element distribution pattern of ca. 2.5 Garocks was possible derived from arc-type juvenile continentalcrust. This suggests an active continental margin was present inthe late Neoarchean in south-central NCC, generating arc-typemagmatism between the Eastern and Western Blocks.

(3) The zircon Hf isotopic and U–Pb data of 2.5–2.0 Ga magmaticrocks indicate that the crust was intensely reworked during thisperiod, including both juvenile and ancient crust.

(4) At around 1.8 Ga, the emplacement of post-collision granitoids
(e.g., Shicheng A-type pluton) and mafic dike swarms through-out the TNCO (e.g., Halls et al., 2000; Wang et al., 2003, 2004a,2008; Peng et al., 2005, 2007, 2008) indicate that the TNCOunderwent extensively orogenic collapse and extension at ca.

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1.8 Ga. The ca. 1.8 Ga magmatic events were probably relatedto the initiation of breakup of the Columbia supercontinent.

. Conclusions

On the basis of geochemical and in situ zircon U–Pb, Hf and tracelement data, major conclusions from this study can be summa-ized as follows:

1) Zircon U–Pb dating demonstrates that the Precambrianbasement in the Songshan area formed mainly in theNeoarchean to Early Paleoproterozoic, including Shipaihedioritic gneiss (2504 ± 4 to 2516 ± 18 Ma), amphibolite(2502 ± 4 to 2506 ± 21 Ma) and Shicheng A-type granite(1775 ± 6 to 1776 ± 6 Ma).

2) The highly fractionated REE patterns of the dioritic gneiss withnegligible negative Eu anomalies could be derived from par-tial melting of lower crust at relatively high pressures (ca.1.5 GPa), where garnet ± amphibole minerals left as residualphases without plagioclase. The coeval amphibolite maybe pro-duced by partial melting of enriched lithospheric mantle. Theflat HREE patterns of A-type granite with negative Eu anomaliesindicate that they were most likely partial melting at relativelylow pressures (<1.0 GPa), where the plagioclase left as residualphases.

3) The zircon Hf isotopic and U–Pb data suggest that ca. 2.7 Gais an important stage for the continental crustal growth in theTNCO, and the juvenile crust was reworked shortly at ca. 2.5 Ga.At ca. 1.78 Ga, the reworking of the old continental crust in thesouthern TNCO yield Shicheng A-type granite.

4) This work further demonstrates that the Archean to Paleopro-terozoic crust in the southern portion of the TNCO underwentthe similar tectonothermal events as those in the northernportion after their formation in the Archean. This similarity inthe crust evolution suggests the TNCO is entire Paleoprotero-zoic collisional orogen from the North to the South.

cknowledgments

We are grateful to Prof. Yong-Fei Zheng and Zi-Fu Zhao forheir insightful suggestions and revisions of the manuscript. Weppreciate the assistance of X.M. Liu, C.R. Diwu, H.D. Gong and.H. Yang with LA-ICPMS zircon U–Pb dating, H.L. Yuan, M.N.ai and H. Zhang for their assistance with LA-MC-ICPMS zirconu–Hf isotope analysis, J.Q. Wang, Y. Liu, Y.Q. Zhang and Y. Huith major and trace elements analysis and J.F. Ying, Y.J. Tang,. Yang, X.M. Zhao, B.X. Sun and Y. Xiao with field work. Two

nonymous reviewers are thanked for their constructive reviewshat improve the paper greatly. This study was supported by fundsrom the NSFC (Grant 90714008), China Postdoctoral Science Foun-ation (Grant 2011M501465 and 2012T50813) and the Northwestniversity.

ppendix A. Supplementary data

Supplementary data associated with this article can be found,n the online version, at http://dx.doi.org/10.1016/j.precamres.012.11.015.

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Zircon U–Pb age and Lu–Hf isotope constraints on Precambrian evolution of continental crust in the Songshan area, the south-central North China Craton