Zircon U–Pb and Lu–Hf Isotopic and Whole-Rock Geochemical Constraints on The

Precambrian Research 233 (2013) 297–315

Contents lists available at SciVerse ScienceDirect

Precambrian Research

jou rnal homepage: www.elsevier.com/locate/precamres

Zircon U–Pb and Lu–Hf isotopic and whole-rock geochemical constraints on the

protolith and tectonic history of the Changhai metamorphic supracrustal

sequence in the Jiao–Liao–Ji Belt, southeast Liaoning Province, northeast China

a,∗ a b a

En Meng , Fu-Lai Liu , Ying Cui , Jia Cai

Institute of Geology, Chinese Academy of Geological Sciences, Beijing 100037, China

School of Earth and Space Sciences, Peking University, Beijing 100871, China

a r a

t i c l e i n f o b s t r a c t

Article history: The Changhai metamorphic supracrustal rocks, located in the eastern–central part of the Jiao–Li–Ji Belt

Received 3 February 2013

in the North China Craton (NCC), are composed mainly of various garnet–mica schists, along with minor

Received in revised form 4 May 2013

quartzites and marbles. This study presents whole-rock major and trace element data, zircon U–Pb dates

Accepted 16 May 2013

and Hf isotope data for these rocks in order to constrain their protolith age and provenance, and discuss

Available online 23 May 2013

the tectonic implications. Geochemical results indicate that the source rocks were mainly granitoids with

a possible minor contribution from clastic sediments with an active continental margin signature. Detrital

Keywords:

zircons have U–Pb age peaks at approximately 1887, 2174, 2552, 2765, and 3212 Ma, εHf values of −11.1

Metamorphic supracrustal rocks C

to +13.0, and three major time windows of average continent crustal model ages (T ) of 2.04–2.33,

Detrital zircon U–Pb–Hf isotopes DM

Geochemistry 2.48–2.56, and 2.72–2.93 Ga. Besides, these units also contain signiﬁcant numbers of concordant meta-

Protolith morphic zircons that yielded a peak age of ca. 248 Ma, indicating that the region was modiﬁed by an

Tectonic implications early Triassic tectono-thermal event. These results suggest that sediments of the Changhai metamorphic

Northeast China supracrustal rocks were mainly sourced from nearby basement granitoid rocks and, to a lesser extent,

from Paleoproterozoic metamorphosed strata such as the North and South Liaohe groups. Furthermore,

the source rocks of the magmatic zircons analyzed in this study appear to have originated from inter-

action between old continental crust and juvenile material. The youngest concordant zircon age peak at

1879 Ma coincides with the timing of formation of regionally widespread granitoids, maﬁc igneous rocks,

and metamorphism of the South Liaohe and Ji’an groups in the Jiao–Liao–Ji Belt, and suggest that the sed-

imentary protoliths of the Changhai metamorphic supracrustal rocks were deposited after this time. The

results indicate that the Archean Liaobei–Jinan Complex in the north and the Liaonan–Nangrim Complex

in the south were already a single continental block by 1887 Ma, and that the Changhai metamorphic

supracrustal rocks were deposited at an active continental margin.

1. Introduction Khondalite Belt resulted from collision between the Yinshan and

Ordos blocks to form the Western Block at ca. 1.95 Ga (Zhao et al.,

In the past two decades, major achievements from structural, 2005, 2010a; Santosh et al., 2006, 2007a, 2007b, 2009a,b, 2012; Xia

metamorphic, geochemical, and geochronological studies on the et al., 2006a, 2006b, 2008; Yin et al., 2009, 2011; Santosh and Kusky,

basement rocks of the North China Craton (NCC), which is the 2010; Li et al., 2011a; Peng et al., 2011, 2012a,b; Wang et al., 2011a;

largest and oldest craton in China, have identiﬁed three major Dan et al., 2012; Guo et al., 2012), whereas the Trans-North China

Paleoproterozoic mobile belts (Khondalite Belt, Trans-North China Orogen resulted from the amalgamation of the Western and East-

Orogen, and Jiao–Liao–Ji Belt) in the western, central, and eastern blocks to form the coherent basement of the NCC at ca. 1.85 Ga

ern parts of the craton, respectively (Fig. 1a; Zhao et al., 2000, (Zhao et al., 2001, 2005, 2006a, 2006b, 2007, 2008a,b; Guo et al.,

2001, 2005; Zhao, 2009). Now there is a broad agreement that the 2002, 2005; Wilde et al., 2002; Kröner et al., 2005, 2006; Zhang

et al., 2006, 2007, 2009, 2012; Li et al., 2010; Liu et al., 2011a,b,

2012a,b,c,d). This research has provided a coherent understanding

∗ of the timing and tectonic processes involved in these Paleopro-

Corresponding author at: Institute of Geology, Chinese Academy of Geological

Sciences, 26 Baiwanzhuang Street, Beijing 100037, China. Tel.: +86 10 68999960; terozoic orogenic events and of the pre-collisional history of the

fax: +86 10 68992873.

Khondalite Belt and Trans-North China Orogen (Zhao et al., 2001,

E-mail addresses: [email protected], [email protected]

2002, 2005, 2007, 2010b, 2012; Liu et al., 2002, 2006, 2007; Wilde

(E. Meng), lﬂ[email protected] (F.-L. Liu), [email protected]

et al., 2002; Zhai and Liu, 2003; Zhai et al., 2005; Zhai and Santosh,

(Y. Cui), [email protected] (J. Cai).

298 E. Meng et al. / Precambrian Research 233 (2013) 297–315 –

Block;

Western

– N N

WB 35 40

elt ( b ) B rectangle.

Belt the

Assemblage eongnam Macheonryeong Y by

200k

Laoling elt

elt B eoul Gyeonggi

Assemblage B N S indicated

Ji n

0 2

Imjingang Ji`a Fig.

Nangrim of

outhern Jilin outhern Assemblage Pyeonrand

S a 2 . iaoning location

n L a i

The

. Se Fig. F

outh Liaohe outh CiaSe China Norther Assemblage S

(2005)

Liao

ellow East

al. Y

enzishan F

Assemblage

ingshan

Zhao iao J iaoning J n iaohe Assemblage n L L after

Wester Liaoning EE a outher handong

S Assemblage North Se

n S

120 125 130

elt modiﬁed

ohai B

Easter

NCC,

k Ultrahigh-pressure Su-Lu the

Eastern Hebei Eastern in

Block

ogen

r O Western Shandong Western

Eastern

hina eijing

uhe C B Duolun the W E

5 n Block. Assemblage

11 hijiazhuang ans-North Bloc Eastern S inyang

loc Tr X Ordos

geology B

–

Wester OB

h 35 00' d k Block;

b Precambrian

ig.2) the ssociated n F

of Yinshan

d a –

iaohe,Ji’an map iao-Liao-Ji YB

h L e J regional Orogen;

105 00' in th s and r iao-Liao-Ji Belt iao-Liao-Ji

China

(a) Legends

e J elt alaeoproterozoic granites in alaeoproterozoic granites in ault enzishan,North Liaoheenzishan,North an

m ingshan,Sout

egion of Eastern the Bloc

the Jiao-Liao-Jithe Belt th Liaonan-Nangrim complex Liaobei-Jinan complex Exposed basement in other r Post-Palaeoproterozoic cove B F Laoling Groups an P J P Changhai Supercrustal Rcoks, regaredtraditionally as Sout the Liaohe Group-Ji Belt (i Macheonayeong Group (North Korea) in Jiao-Liao-Ji the Belt in Jiao-Liao-Ji the Belt F and Wuheand Groups associated and NCC

1000k the N

Trans-North

0 ( a ) –

setting

TNCO

Block;

Tectonic

Fig. Eastern

E. Meng et al. / Precambrian Research 233 (2013) 297–315 299

122 30' 122 45' 123 00' 40 ( a ) 00' Shicheng iver Zhuanghe island ( b ) N R

39 iliu 39 30' B 39 30' Pulandian Pikou 30' N Sea ohai B b 39 Dalian 00' Yellow Sea 0 30km Legends

39 Exposed basement 39 20' Dachangshan island in the Eastern Block 20' Post-Palaeoprotero Changhai Xiaochangshan -zoic cover in the island Jiao-Liao-Ji Belt Changhai Supercrustal

DD10-1 Rocks, traditionally r egared as the South Liaohe Group Towns

39 Sampling location 39 10' Sea 10' Yellow

Guanglu island Haiyang island Z hangzi island

HY06-1 HY03-1 0 10km HY05-1 DD23-3 HY05-2 DD20-1 HY01-1

122 30' 122 45' 123 00'

Fig. 2. Tectonic setting (a) and map of the Precambrian geology (b) of Changhai in southeast Liaoning province, including representative sample locations (modiﬁed after

LBGMR, 1989). (For interpretation of the references to color in this ﬁgure, the reader is referred to the web version of the article.)

2011; Kröner et al., 2005, 2006; Santosh et al., 2006, 2007a, 2007b, and in adjacent regions, particularly with regards to the nature of

2009a; Wan et al., 2006; Xia et al., 2006a, 2006b, 2008, 2009; Zhang their protoliths and their tectonic nature.

et al., 2006, 2007, 2009; Yin et al., 2009, 2011; Peng et al., 2011; Zhao The Changhai Islands in the southern Liaoning Province of

and Guo, 2012; Zhao and Cawood, 2012). northeast China are located in the southeastern Liaoning–Nangrim

However, the formation and evolution of the Jiao–Liao–Ji Complex (Nangrim Block), locating in the eastern part of the central

Belt remain controversial, despite extensive geochronological and Jiao–Liao–Ji Belt (Fig. 2a). Our recent investigations and previous

geochemical research focused on the metamorphic supracrustal, studies have revealed voluminous granitoids and metamorphic

granitoid, and volcanic rocks within the belt (e.g., Li et al., 2001a, supracrustal rocks in this region (Meng et al., 2012). Due to the

2003, 2005, 2006, 2011b,c,d, 2012; Faure et al., 2004; Luo et al., lack of exposure in the region between the islands and the Chi-

2004, 2008; Zhao et al., 2005, 2012; Lu et al., 2006; Li and Zhao, nese mainland, the igneous and metamorphic ages, petrogenesis,

2007; Tam et al., 2011; Zhao and Guo, 2012). Some researchers con- and tectonic setting of these rocks are not well constrained. In

sider that this belt represents a continent–arc–continent collisional this study, we carried out a detailed petrological, geochemical,

belt, along which the Archean Liaobei–Jinan Complex (Longgang geochronological (zircon U–Pb), and isotopic (zircon Hf) data for

Block) in the north and the Liaonan–Nangrim Complex (Nan- the Changhai metamorphic supracrustal rocks. These new data,

grim Block) in the south collided to form a coherent block in in combination with available regional geological data, are used

the Paleoproterozoic (Hu, 1992; Bai, 1993; Bai and Dai, 1998; He to constrain the depositional age and the nature of the protolith,

and Ye, 1998a,b; Faure et al., 2004; Lu et al., 2006). In contrast, and place important constraints on the tectonic history of the

another school of thought interpret it as a Paleoproterozoic intra- Jiao–Liao–Ji Belt.

continental rift zone along the eastern continental margin of the

NCC, based on analyses of volcanism, granitoid rocks, and meta- 2. Regional geology

morphic P–T paths (Zhang and Yang, 1988; Peng and Xu, 1994; Peng

and Palmer, 1995; Yang et al., 1995; Liu et al., 1997; Li et al., 2001a, The Paleoproterozoic Jiao–Liao–Ji Belt is situated in the east-

2003, 2005; Luo et al., 2004, 2008; Li and Zhao, 2007). Such con- ern region of the Eastern Block of the NCC, and is dominated by

troversy has arisen because of the lack of a systematic comparative Neoarchean rocks with minor Meso- and Paleoarchean compo-

study of the Early Precambrian rocks within the Jiao–Liao–Ji Belt nents (Zhao et al., 1998, 2006a; Lu et al., 2008; Wu et al., 2012).

300 E. Meng et al. / Precambrian Research 233 (2013) 297–315

The northern part of the Jiao–Liao–Ji Belt is located between the maﬁc intrusions consist of gabbros and dolerites that have been

Liaobei–Jinan Complex (Longgang Block) and the Liaonan–Nangrim mostly metamorphosed under greenschist and amphibolite facies

Complex (Nangrim Block), and its southern part extends across the conditions (Zhao et al., 2005; Li and Zhao, 2007), although original

northern Yellow Sea into the Eastern Shandong Complex (Fig. 1b; igneous textures are still preserved.

Li and Yang, 1997; Li et al., 2001a, b, 2005, 2011c; Zhao et al., 2001, The present study area is located in the Changhai Islands

2005, 2007; Li and Zhao, 2007; Zhao et al., 2011). The belt mainly to the northeast of Dalian City, southeastern Liaoning Province.

comprises sedimentary and volcanic rock successions metamor- The rocks in this area were previously considered as part of the

phosed from greenschist to lower amphibolite facies, in association South Liaohe Group within the eastern–central Jiao–Liao–Ji Belt

with some granitic and maﬁc igneous intrusions (Lu, 1996; Li et al., (Figs. 1b and 2a). Archean–Paleoproterozoic crystalline basement

2001b, 2003; Lu et al., 2004a,b, 2005, 2006; Luo et al., 2004, 2008; and metamorphic supracrustal rocks of the South Liaohe Group are

Li and Zhao, 2007; Wang et al., 2011b; Dong et al., 2012; Tam widely exposed in this region, along with local occurrences of post-

et al., 2012a,b,c). The metamorphosed sedimentary and volcanic Paleoproterozoic cover rocks (Fig. 2b). The South Liaohe Group is

successions include the Fenzishan and Jingshan groups in eastern dominated of staurolite-bearing garnet–mica schist, garnet–mica

Shandong, the North and South Liaohe groups in eastern Liao- schist (containing kyanite or andalusite), chlorite–sericite–quartz

ning, the Ji’an and Laoling groups in southern Jilin, and possibly schist, quartzite, chlorite–mica schist, minor graphite-bearing

the Macheonryeong Group in North Korea (Fig. 1b). These suc- biotite gneiss, and boron-bearing marbles, which are analogous to

cessions grade upwards from a basal clastic-rich sequence and a a khondalite series (Jiang, 1987; Lu, 1996).

lower bimodal volcanic sequence, through a middle carbonate-rich Available geochronological data show that the regional sed-

sequence, to an upper pelitic sequence (Li et al., 1995). The Fen- imentary and volcanic successions of the Jiao–Liao–Ji Belt were

zishan and Jingshan groups in eastern Shandong are stratigraphic formed at ca. 2.10–1.93 Ga and were then metamorphosed and

equivalents of the North and South Liaohe groups in Liaoning, and deformed at ca. 1.93–1.85 Ga (Luo et al., 2004, 2008; Li et al.,

the Laoling and Ji’an groups in southern Jilin, respectively (Wang 2005; Lu et al., 2006; Wan et al., 2006; Li and Zhao, 2007; Zhou

et al., 1997). Therefore, the Jiao–Liao–Ji Belt can be further subdi- et al., 2008a,b,c,d). Recent SHRIMP U–Pb zircon dating results have

vided into northern (Fenzishan, North Liaohe, and Laoling groups) shown that deformed A-type granites and monzogranitic gneisses

and southern belts (Wuhe, Jingshan, South Liaohe, and Ji’an groups) from the Jiao–Liao–Ji Belt were emplaced at ca. 2.17–2.14 Ga (Li

(He and Ye, 1998a,b; Li et al., 2005), separated by ductile shear zones et al., 2005; Lu et al., 2006; Wan et al., 2006; Li and Zhao, 2007), and

and faults (Li et al., 1996; Liu and Li, 1996; Liu et al., 1997). later metamorphosed at ca. 1.91 Ga (Luo et al., 2004, 2008; Li and

The main lithostratigraphic unit of the Jiao–Liao–Ji Belt is Zhao, 2007). These studies also dated post-tectonic granitic rocks

divided into the North and South Liaohe groups on the basis of vari- that yielded ages of 1.88–1.84 Ga.

ations in lithology, metamorphism, deformation, and evolutionary

history (He and Ye, 1998a,b; Li et al., 2005). One of the impor-

tant differences between these groups is that the North Liaohe 3. Samples and analytical methods

Group has a clockwise P–T–t path, whereas the South Liaohe Group

has an anticlockwise P–T–t path (He and Ye, 1998a,b; Li et al., Rock samples selected for this study were collected from the

2003). The two groups crop out as a long, linear, NE–SW-trending major rock types of the Changhai metamorphic supracrustal rocks,

belt that extends from Haicheng, Dashiqiao, and Gaixian in the mainly staurolite-bearing garnet–mica schists, garnet–mica schists

southwest, through Fengcheng in the central part, to Hunjiang in (containing minor kyanite or sillimanite), chlorite–mica schists,

the northeast (Fig. 1b). The North and South Liaohe groups have and quartzites. Details of sampling locations, lithologies, and min-

been divided into ﬁve formations: the Langzishan, Li’eryu, Gaoji- eral compositions are shown in Fig. 2b and described in Section 4.

ayu, Dashiqiao, and Gaixian formations (Yang et al., 1988; Zhang Major and trace element data for 14 schist samples were obtained

and Yang, 1988; Liu et al., 1997; Wang et al., 1997; Li et al., 1998, by X-ray ﬂuorescence (XRF) and inductively coupled plasma-mass

2001b, 2004, 2005). The lowermost Langzishan Formation uncon- spectrometry (ICP-MS) at the National Research Center for Geo-

formably overlies the late Archean Anshan Complex and comprises analysis, Chinese Academy of Geological Sciences (CAGS), Beijing,

basal conglomerate-bearing quartzites, which transition upwards China. Major elements were analyzed by XRF and have analytical

into chlorite–sericite–quartz schists, phyllites, garnet-bearing mica uncertainties <±5%. Trace elements were analyzed by LA-ICP-

schists, minor graphite-bearing garnet–staurolite–mica schists, MS, as were rare earth elements (REE) after separation using

and kyanite-bearing mica schists. The Langzishan Formation is cation-exchange techniques. Analytical uncertainties for LA-ICP-

conformably overlain by the Li’eryu and Gaojiayu formations MS analyses are ±10% and ca. ±5% for elements with abundances

that consist of boron-bearing volcano-sedimentary successions lower and higher than 10 ppm, respectively (Zeng et al., 2011).

metamorphosed to ﬁne-grained felsic gneiss, amphibolite, and Zircon grains were obtained by a combination of standard heavy

mica–quartz schist. The Dashiqiao Formation overlies the Gaojiayu liquid and magnetic separation techniques from six garnet–mica

Formation and is predominantly dolomitic marbles intercalated schists and two quartzites, for zircon U–Pb dating and in situ trace

with minor carbonaceous slates and mica schists; this forma- element analysis. The zircons were mounted on an epoxy resin

tion hosts the largest magnesite deposit in the world (Zhang disc, polished, and imaged in both reﬂected and transmitted light.

and Yang, 1988; Liu et al., 1997). The uppermost Gaixian For- Prior to U–Pb isotopic analysis, the internal structures of zircon

mation comprises phyllites, andalusite–cordierite–mica schists, grains were photographed using cathodoluminescence (CL) imag-

staurolite–mica schists, and sillimanite–mica schists, along with ing by a HITACHI S-3000N electron microprobe (GATAN) at the

minor quartzites and marbles (LBGMR, 1989). Beijing SHRIMP Centre, CAGS, Beijing, China. Zircon U–Pb dating

The two groups are tectonically separated by ductile shear zones and in situ trace element analyses were carried out using an Agi-

and faults, and are associated with voluminous Paleoproterozoic lent 7500a quadruple LA-ICP-MS and a Neptune multiple collector

granitoids (Liaoji Granitoids) and maﬁc intrusions (Zhang and Yang, LA-ICP-MS, respectively, at the Geological Laboratory Center, China

1988; Li et al., 1996, 2003, 2005; Liu and Li, 1996; Liu et al., 1997; Li University of Geosciences, Beijing, China. A 193 nm excimer laser

and Zhao, 2007). The Liaoji Granitoids are predominantly deformed was focused on the surface of zircon grains with an energy density

A-type granites and monzogranitic gneisses, and undeformed of 10 J/cm . The laser beam diameter was 30 ␮m and operated at

porphyritic monzogranites, rapakivi granites, and alkaline syenites a repetition rate of 5 Hz. Helium was used as a carrier gas to efﬁ-

(Lu et al., 2004a,b, 2005; Zhao et al., 2005; Li and Zhao, 2007). The ciently transport the ablation aerosol to the LA-ICP-MS. Details of

E. Meng et al. / Precambrian Research 233 (2013) 297–315 301

the LA-ICP-MS analytical procedures are described in Song et al. Supplementary material related to this article found, in

(2010). Each set of eight sample analyses was bracketed by anal- the online version, at http://dx.doi.org/10.1016/j.precamres.

ysis of the zircon standards 91500, TEM, and NIST612. Each spot 2013.05.004.

analysis comprised ca. 5 s of background data acquisition and 45 s Chondrite-normalized REE patterns of all the Changhai meta-

207 206 206 238 207 235

of sample data acquisition. Pb/ Pb, Pb/ U, U/ U, and morphic supracrustal rocks are shown in Fig. 4a, and the rare

208 232

Pb/ Th ratios were corrected for analytical isotopic and ele- earth element (REE) data are given in Supplementary Table 2 These

mental fractionation effects by using the analyses of the zircon rocks are characterized by enrichment in light REEs (LREEs), rela-

standard 91500. Trace element concentrations and U–Pb isotopic tive depletion in heavy REEs (HREEs), and have marked negative

compositions were calculated using the GLITTER 4.4.1 program and Eu anomalies (␦Eu = 0.48–0.65). [La/Yb]N ratios vary in the range

calibrated using Si as an internal standard and NIST612 as an 5.9–17.7 and LREEs show distinct fractionation with [La/Sm]N ratios

external standard. Common Pb was corrected using the method of 3.83–5.19 (Fig. 4a).

proposed by Anderson (2002). Weighted mean U–Pb ages and con- Supplementary material related to this article found, in

cordia plots were processed using ISOPLOT 3.0 with uncertainties the online version, at http://dx.doi.org/10.1016/j.precamres.

quoted at the 1 error and 95% conﬁdence levels (Ludwig, 2003). 2013.05.004.

In situ zircon Hf isotope analysis was performed using a New The analyzed samples are characterized by: (1) variable contents

Wave UP213 laser ablation microprobe coupled to a Neptune of Cr (50.7–98.6 ppm) and Ni (4.2–34.2 ppm); (2) relatively high

multiple collector ICP-MS at the Institute of Mineral Resources, La/Sc (2.0–4.8), La/Y (1.2–3.1), and Ti/Zr (12.7–32.9); and (3) low

CAGS, Beijing, China. For details on instrumental conditions and Cr/Zr (0.16–0.49) and Sc/Cr (0.19–0.31) (Supplementary Table 1).

data acquisition, see Wu et al. (2006) and Hou et al. (2007). All the samples are relatively depleted in high ﬁeld strength ele-

A stationary spot with a beam diameter of either 40 or 55 ␮m ments (HFSEs; e.g., Nb, Ta, P, and Ti) and strongly enriched in large

was used for the analyses. The ablated material was transported ion lithophile elements (LILEs; e.g., Rb, Cs, Ba, and Th) as com-

from the laser ablation cell using helium as a carrier gas, and pared with upper continental crust, which most likely reﬂects the

then combined with argon in a mixing chamber before being abundance of clay minerals in these rocks (McLennan et al., 1993)

176 176

introduced to the ICP-MS plasma. Correction for Lu and Yb (Fig. 4b). Data for all the samples exhibit relatively strong linear

176 176 175

isobaric interferences on Hf utilized Lu/ Lu = 0.02658 and correlations between each of Th, Y, and Zr with SiO2, suggest-

176 173

Yb/ Yb = 0.796218, respectively (Chu et al., 2002). Instrumen- ing that HFSE concentrations are likely related to and controlled

tal mass bias was accounted for by normalizing Yb isotope ratios by felsic source components and were relatively immobile during

172 173

to Yb/ Yb = 1.35274 (Chu et al., 2002) and Hf isotope ratios to weathering, diagenesis, and low-grade metamorphism (Lahtinen

179 177

Hf/ Hf = 0.7325, using an exponential mass fractionation law. et al., 2010). As such, these relatively immobile elements (HFSEs

The mass bias behavior of Lu was assumed to follow that of Yb. and REEs) can be used to determine provenance (Winchester and

For details on the mass bias correction protocols, see Iizuka and Floyd, 1977; Taylor et al., 1986). On a diagram used for distinguish-

Hirata (2005), Wu et al. (2006), and Hou et al. (2007). The zircon ing the origins of sediments (La/Yb vs. REEs; Fig. 3c), protoliths

GJ1 was used as the reference standard and yielded a weighted of these rocks appear to have been mainly shale and clay rocks

176 177

mean Hf/ Hf ratio of 0.282008 ± 27 (2) during the present with some contribution from sandstone. This is consistent with the

analyses. This ratio is indistinguishable from a weighted mean protolith origin identiﬁed from Fig. 3d, which is principally used

176 177

Hf/ Hf ratio of 0.282013 ± 19 (2) obtained by Elhlou et al. to distinguish Archean or post-Archean sediments using Cr and Ni

(2006). The individual Hf isotopic analyses were located directly concentrations, and suggests that the protolith was post-Archean

on top of the U–Pb ablation pits. All Hf isotope data are reported argillaceous sediment.

ε with an error of 2 of the mean, and values of Hf were calcu-

176 −11 −1

lated using a Lu decay constant of 1.865 × 10 yr (Scherer 4.2. Zircon U–Pb dating and Hf isotopes

et al., 2001). Depleted mantle model ages (TDM) were calculated

176 177 176 177

based on the measured Lu/ Hf and Hf/ Hf ratios with ref- U–Pb detrital zircon ages for six schists and two quartzites

176 177

erence to depleted mantle with present-day Hf/ Hf = 0.28325 collected from the Changhai metamorphic supracrustal rocks are

176 177

and Lu/ Hf = 0.0384 (Grifﬁn et al., 2000). Average continent presented in Supplementary Table 2. From these analyses, 210 rep-

T crustal model ages ( DM) were calculated for the magma source resentative concordant and nearly concordant zircons with age

176 177

using the initial Hf/ Hf ratio of the zircon and assuming a mean discordance <15, which we consider to be reliable and were used in

176 177

crustal Lu/ Hf value of 0.015 (Grifﬁn et al., 2004). binned frequency histograms, were selected for Hf isotope analy-

sis. Supplementary Table 3 lists Hf isotopic data for the concordant

4. Analytical results zircons, and CL images of representative zircons are shown in

Fig. 5.

4.1. Whole-rock major and trace element geochemistry Supplementary material related to this article found, in

the online version, at http://dx.doi.org/10.1016/j.precamres.

Chemical compositions of the analyzed Changhai metamorphic 2013.05.004.

supracrustal rocks are listed in Supplementary Table 1. In general,

these rocks are rich in Al2O3 (16.9–30.2 wt.%; average = 23.0 wt.%), 4.2.1. Sample DD10-1

similar to typical khondalite series rocks in the NCC (Lu, 1996). The Sample DD10-1 is a ﬁne-grained, garnet–muscovite schist col-

samples have variable SiO2 (45.5–69.8 wt.%), FeOtotal (2.7–9.1 wt.%), lected from the east of Jinpen Harbor on the southern part

◦ ◦

MgO (0.8–1.9 wt.%), CaO (0.04–1.80 wt.%), Na2O (0.6–1.6 wt.%), and of Dachangshan Island (122 39 35.5 E, 39 15 19.0 N; Fig. 2b).

relatively high TiO2 (0.6–1.2 wt.%) and K2O (2.6–7.4 wt.%) contents The sample has a schistose–granular crystalloblastic texture and

(Supplementary Table 1). Average SiO2, FeOtotal, MgO, CaO, Na2O, contains a mineral assemblage of muscovite (55–65%), quartz

TiO2, and K2O contents are 58.5, 6.3, 1.2, 0.54, 1.1, 0.93, and 4.7 wt.%, (20–30%), plagioclase (0–10%), and garnet + biotite + hornblende

respectively. On the protolith discrimination diagram of Simonen (0–8%). Zircons separated from this sample are mainly rounded or

(1953), all of the samples plot in the ﬁeld of argillaceous sediments subhedral columnar in shape with variable grain size (30–80 ␮m).

(Fig. 3a). Moreover, the sediment classiﬁcation diagram of Herron Most grains are yellow in color and have obvious oscillatory zon-

(1988) suggests that the protoliths of these rocks were shale with ing. These features, together with their high Th and U contents, and

some contribution by wacke (Fig. 3b). Th/U ratios (0.10–1.57) (Fig. 5a; Supplementary Table 2), indicate

302 E. Meng et al. / Precambrian Research 233 (2013) 297–315

80 2 ( a ) ( b ) 70 Algillaceous

60 ) field

k) Fe-Shale Fe-Sand 2 1 50

Quartz S andy field Lith- Sublith-

V TeOT/K e 30 olcanic arenite arenite arenite ck field 0 Shale

al+fm)-(c+al

20 Log( Wa ( Arkose Subarkose 10 Calcium field -1 0 100 200 300 400 500 600 0 0.5 1 1.52 2.5 Si (Simonen, 1953) Log(SiO22 /Al O3)

100 200

100 Shale Claystone ) ield Sandy f Wacke Post-Archean

ppm La/Yb 10 0 Carbonate a ( 10 d L fiel La/Th=1 n

Amphibolite Archea La/Th=1 ( c ) ( d )

1 1

10 100 1000 0.1 1 10 100

ΣREE ( ppm) Th (ppm)

Fig. 3. Simonen (a), log(Fe2O3/K2O) vs. log(SiO2/Al2O3) (b), La/Yb vs. REE (c), and La–Th (d) classiﬁcation diagrams for samples from the Changhai metamorphic supracrustal

rocks, modiﬁed after Simonen (1953), Herron (1988), Gromet et al. (1984), and McLennan et al. (1990), respectively.

a magmatic origin (Hoskin, 2001; Belousova et al., 2002; Liu et al., 2156 ± 34 Ma (n = 2) (Fig. 6a). All the other analyses deﬁne two

2009a,b). upper intercept ages of 2542 ± 25 Ma (n = 10) and 1875 ± 22 Ma

207 206

Fifty analyses of zircon were obtained from sample DD10-1. (n = 37), which are consistent with Pb/ Pb weighted average

On a concordia diagram, three concordant analyses have older ages of 2549 ± 14 Ma (n = 6) and 1883 ± 13 Ma (n = 14) obtained

207 206

ages of 2668 ± 20 Ma and a Pb/ Pb weighted average age of from the concordant or almost concordant zircons (Supplementary

1000 3000

( a ) 1000 ( b )

antle 100 100

10 10

Sample/Chondrit

Sample/Primitive m Sample/Primitive

1 1 Cs Ba U Nb La Sr P Zr Sm Ti Y Lu La Ce Pr Nd Sm Eu Gd Tb Dy Ho Er Tm Yb Lu

Rb Th K Ta Ce Nd Pb Hf Eu Tb Yb

Fig. 4. Chondrite-normalized REE (a) and primitive mantle-normalized trace element (b) patterns for samples from the Changhai metamorphic supracrustal rocks. Normal-

izing values are after Boynton (1984) and Sun and McDonough (1989), respectively.

E. Meng et al. / Precambrian Research 233 (2013) 297–315 303

Fig. 5. Cathodoluminescence (CL) images of selected zircons from the Changhai metamorphic supracrustal rocks.

Table 2). Hf values for concordant zircons with ages of ca. 1883 Ma texture and contains a mineral assemblage of muscovite (45–55%),

range from −11.1 to −0.8 (Fig. 7a; Supplementary Table 3), suggest- garnet (25–35%), quartz and plagioclase (10–15%), and minor

ing that these zircons largely crystallized from magma derived from amounts of biotite and opaque minerals (0–8%). Zircon grains sepa-

old continental crust. A minor population of zircons with ages of rated from this sample are mainly subhedral to euhedral prismatic

ε ␮

ca. 2668, 2549, and 2156 Ma has Hf values from +1.7 to +8.2 (apart in shape, and have a variable grain size (50–100 m). Most of the

from one analysis with −0.6), indicating derivation from juvenile zircons are yellow in color, exhibit obvious oscillatory zoning, and

magma with a depleted mantle source. The DM model age spec- have high Th/U ratios (0.11–1.23) (Fig. 5b; Supplementary Table 2),

trum of this sample has two major age peaks at 2.73 and 2.78 Ga, which are indicative of a magmatic origin.

with other less prominent peaks close to these ages at 2.54, 2.65, Zircons were not abundant in the heavy mineral fraction of this

2.85, and 2.95 Ga, and two further minor peaks at 2.31 and 3.25 Ga sample and are also relatively small; consequently, only 40 analyses

(Fig. 7b). were obtained from this sample. Nearly all the concordant or nearly

207 206

concordant analyses yielded three Pb/ Pb weighted average

± ± ±

4.2.2. Sample DD20-1 ages of 2548 17 Ma (n = 3), 2174 26 Ma (n = 2), and 1894 8 Ma

Sample DD20-1 is also a quartz-bearing, garnet–muscovite (n = 12). The latter age is consistent with the upper intercept age

schist that was collected from Dongbang Village on the south- of 1887 24 Ma (n = 32) within error (Fig. 6b; Supplementary Table

◦ ◦

eastern part of Zhangzidao Island (122 45 14.7 E, 39 01 23.4 N; 2). Hf values of zircons with concordant ages of ca. 1894 Ma range

− ε

Fig. 2b). The sample has a schistose–granular crystalloblastic from 1.4 to +6.5, and 78% of the zircons have positive Hf values

304 E. Meng et al. / Precambrian Research 233 (2013) 297–315

0.6

0.6 0.5

0.4 8

8 0.4

23 /U

/U 0.3

Pb Pb

6 206 23 20 0.2 0.2

0.1

0.0 0.0 0 4 8 12 16 024681120 14 207 235 207Pb/ 235 U 0.5 0.6

0.4 0.5

0.3 0.4

/U /U

0.2 0.3

Pb Pb

06 23

2 206 238

0.1 0.2

0.0 0.1 0 2 4 6810 024681012 207Pb/ 235 U 207Pb/ 235 U

0.6 0.5

0.5 0.4

0.4

23 /U

/U 0.3 0.3

Pb Pb 206 238 0.2 206 0.2 0.1

0.0 0.1 0 2 4 681012 14 0 246810 207Pb/ 235 U 207Pb/ 235 U

0.6 0.7

8 8

23 0.5

/U 0.4

Pb Pb

623

20 206

0.2 0.3

0.0 0.1 0 4 8 12 16 0 4 8 12 16 20 24 28

207Pb/ 235 U 207Pb/ 235 U

Fig. 6. Zircon U–Pb isotopic compositions of detrital zircons from the Changhai metamorphic supracrustal rocks.

E. Meng et al. / Precambrian Research 233 (2013) 297–315 305

4 5 DD10-1( a ) DD10-1 ( b ) 4 3

3 2 2

Number 1 Number 1

0 0

-14 -10 -6 -2 2 610 14 2.1 2.3 2.5 2.7 2.9 3.1 3.3 3.5

2 2 DD20-1 ( c ) DD20-1 ( d )

1 1

Number

0 0 -4 -2 0 2 4 681012 14 2.0 2.2 2.4 2.6 2.8 3.0 3.2 3.4

6 4

5 DD23-3 ( e ) DD23-3 ( f ) 3 4

3 2

Number Number 2 1 1

0 0

-30 -20 -10 0 10 20 1.7 1.9 2.1 2.3 2.5 2.7 2.9 3.1

3 3

HY01-1 ( g ) HY01-1 ( h )

2 2

Number 1 Number 1

0 0 -6 -4 -2 0 2 4 6810 2.1 2.2 2.3 2.4 2.5 2.6 2.7 2.8 2.9 3.0 ε (t) C

Hf T DM (Ga)

Fig. 7. Hf isotopic compositions of samples from the Changhai metamorphic supracrustal rocks. Left: Relative probability plots of εHf values. Right: Relative probability plots

C T

of DM data.

(Fig. 7c; Supplementary Table 3), indicating that most of them crys- 4.2.3. Sample DD23-3

tallized from a juvenile magma derived from a depleted mantle Sample DD23-3 is a medium-grained garnet–muscovite schist

source, while some were derived from the remelting of old con- collected from southwest of Xigou Village on Zhangzi Island

◦ ◦

tinental crust. However, the zircons with lower Hf values were (122 43 09.1 E, 39 01 04.8 N; Fig. 2b). The sample has a

derived from the remelting of old continental crust. Notably, all schistose–granular crystalloblastic texture and contains a min-

zircons with ages of ca. 2174 or 2548 Ma have positive Hf values eral assemblage of muscovite (30–35%), quartz (15–20%), garnet

that vary from +0.6 to +9.1, suggesting derivation from juvenile (20–25%), and minor amounts of biotite and feldspar (5–10%). The

material with a depleted mantle source. The DM model age spec- quartz grain size is relatively large and locally quartz is concen-

trum of this sample has major peaks at 2.16, 2.35, 2.53, and 3.04 Ga trated in veins. Garnet crystals are cracked with some inﬁlling by

(Fig. 7d). ﬁne-grained quartz inclusions. Zircons separated from this sample

306 E. Meng et al. / Precambrian Research 233 (2013) 297–315

are mainly subhedral prismatic in shape and have a variable grain crystalloblastic texture and contains a mineral assemblage of

size (30–80 ␮m). Most zircon crystals are pale-brown to brown in quartz (35–40%), muscovite (20–25%), garnet (15–20%), and minor

color. Cathodoluminescence images show that most of these zir- amounts of opaque minerals (0–5%). Zircons separated from this

cons have oscillatory zoning, and this feature, coupled with their sample are mainly subhedral to euhedral prismatic, and have a

high Th and U contents, and Th/U ratios (0.11–1.49) (Fig. 5c; Sup- variable grain size (30–150 ␮m). Most of the zircon grains are

plementary Table 2), indicates a magmatic origin. A small number pale yellow in color. Cathodoluminescence images show that most

of grains are structure-less and cloudy in appearance (e.g., anal- of these zircons have a core surrounded by a structure-less and

ysis 24; Fig. 5c), and have very high U contents (>1500 ppm) and relatively high-luminescence rim (Fig. 5e) that has a low Th/U

low Th/U ratios (0.01–0.07) (Supplementary Table 2), indicating a ratio (0.01–0.02; Supplementary Table 2), which implies that these

metamorphic origin (Belousova et al., 2002; Hoskin, 2001). zircons have a metamorphic origin. The zircon cores and grains

Ninety-eight U–Pb analyses were obtained from this sample. without rims have clear oscillatory zoning with high Th and U

206 238

Seventeen concordant zircons yielded a Pb/ U weighted aver- contents, and Th/U ratios (0.13–1.30; Supplementary Table 2),

age age of 249 ± 3 Ma (n = 17), and all the other analyses deﬁne which are indicative of a magmatic origin.

two upper intercept ages of 1878 ± 13 Ma (n = 77) and 2225 ± 63 Ma Sixty U–Pb analyses show that grains with concordant ages

207 206 207 206

(n = 4), which are consistent with the Pb/ Pb weighted aver- yield Pb/ Pb weighted average ages of 2506 ± 15 Ma (n = 3),

age ages of 1881 ± 12 Ma (n = 27) and 2223 ± 23 Ma (n = 1) obtained 2242 ± 14 Ma (n = 4), and 1879 ± 7 Ma (n = 18). The latter two ages

from the concordant or nearly concordant zircons (Fig. 6c; Supple- are consistent with two upper intercept ages of 2258 ± 56 Ma

mentary Table 2). Two metamorphic zircons also have concordant (n = 8) and 1884 ± 16 Ma (n = 43) (Fig. 6e). Four analyses of the

206 238

ages of ca. 1878 and 1882 Ma, which coincide with the major age high-luminescence metamorphic rims yield a Pb/ U weighted

ε ±

peak of 1881 Ma. Hf values of zircons with concordant ages of ca. average age of 247 4 Ma (Fig. 6e), which coincides with the ages

249 Ma range from −23.0 to −11.1, whereas the grains with ages of of ca. 249 Ma for the metamorphic zircons from sample DD23-3.

ε −

1881 and 2225 Ma have Hf values from +0.5 to +10.9 (apart from Hf values of zircons with ages of ca. 247 Ma vary from 23.5 to

one analysis with −0.1), indicating that these zircons were derived −8.3 (Fig. 8a; Supplementary Table 3) and are similar to those of

from old continental crust and juvenile material with a depleted sample DD23-3, indicating a source from recycled ancient conti-

ε mantle source, respectively (Fig. 7e; Supplementary Table 3). How- nental crust. The grains with ages of ca. 1879 Ma have Hf values

T −

ever, the two groups of zircons have similar DM model age spectra, ranging from 5.0 to +6.8 (Fig. 8a; Supplementary Table 3), possibly

with a major peak at 2.36 Ga, less prominent peaks at 1.98 and indicating interaction between old continental crust and juvenile

2.15 Ga, and a minor peak at 2.78 Ga (Fig. 7f). material with a depleted mantle source. However, Hf values of zir-

cons with ages of 2242 and 2506 Ma vary from −1.2 to +7.8, and 85%

4.2.4. Sample HY01-1 of the grains have positive Hf values (Fig. 8a; Supplementary Table

Sample HY01-1 is also a ﬁne-grained garnet–muscovite schist 3), implying that these zircons crystallized from a juvenile magma

that was collected from Qinglong Hill in the central region of with a depleted mantle source. The DM model age spectrum shows

◦ ◦

Haiyang Island (123 11 29.9 E, 39 03 28.1 N; Fig. 2b). This sam- two major peaks at 2.56 and 2.79 Ga, a less prominent peak at

ple has a schistose–granular crystalloblastic texture and contains 2.73 Ga, and some minor peaks between 1.88 and 2.33 Ga (Fig. 8b).

a mineral assemblage of muscovite (40–50%), garnet (35–45%),

quartz (5–10%), tourmaline + epidote + quartz (0–5%), and minor

amounts of opaque minerals (0–3%). Zircon grains separated from 4.2.6. Sample HY05-1

this sample are mainly subhedral to euhedral prismatic in shape, Sample HY05-1 is a coarse-grained staurolite–kyanite–garnet-

and have a variable grain size (30–120 ␮m). Most of these zircons bearing muscovite schist collected from northeast of Laojiang

◦ ◦

are pale yellow to light green in color. Apart from one grain (anal- Village on Haiyang Island (123 09 51.2 E, 39 01 57.5 N; Fig. 2b).

ysis 52) that has a Th/U ratio of 0.08, indicative of a metamorphic This sample has a schistose–granular crystalloblastic texture and

origin, all the other grains exhibit clear oscillatory zoning or are contains a mineral assemblage of quartz (25–30%), muscovite

homogeneous, and have high Th and U contents, and Th/U ratios (15–20%), garnet (30–35%), and minor amounts of staurolite, kya-

(0.11–2.22) (Fig. 5d; Supplementary Table 2), which are indicative nite, and opaque minerals (5–10%). Zircons separated from this

of a magmatic origin. sample are mainly rounded or subhedral short prisms and have

Sixty-four analyses were carried out on this sample (Sup- a variable grain size (30–150 ␮m). Most of the zircon grains are

plementary Table 2), and two age populations were identiﬁed pale yellow in color. Cathodoluminescence images show that most

207 206

(Fig. 6d). The oldest grain has a concordant Pb/ Pb age of of the zircons have low luminescence and clear oscillatory zon-

2550 ± 50 Ma, which is consistent with the upper intercept age of ing (Fig. 5e), and these features, along with their high Th and U

2541 ± 50 Ma of a discordia line deﬁned by 10 zircons. Many of contents, and Th/U ratios (0.11–1.92; Supplementary Table 2), indi-

the remaining 54 zircons are discordant and deﬁne an upper inter- cate a magmatic origin.

207 206

cept age of 1881 ± 26 Ma, which is consistent with the Pb/ Pb Sixty-one analyses of zircons in this sample deﬁne a complex

weighted average age of 1890 ± 6 Ma from 22 concordant analy- age pattern (Fig. 6f; Supplementary Table 2). Eight analyses fall on a

207 206

ses. The metamorphic zircon (analysis 52) yielded a Pb/ Pb discordia line with an upper intercept age of 2230 Ma, which is con-

207 206

± ε − ±

age of 1890 14 Ma. Hf values of these zircons range from 1.3 sistent with a Pb/ Pb weighted average age of 2241 21 Ma

to +5.5 (Fig. 7g; Supplementary Table 3), and indicate interaction of four concordant zircons. A further six grains have ages of 2174

between older continental crust and juvenile material derived from (n = 3), 2093 (n = 1), and 2032 Ma (n = 2). The remaining zircons have

T a depleted mantle source. The DM model ages of this sample have ages that cluster at ca. 1881 Ma, with an upper intercept age of

207 206

a bimodal distribution with major peaks at 2.45 and 2.72 Ga and 1887 ± 15 Ma (n = 47) and a Pb/ Pb weighted average age of

± ε

two minor peaks at 2.30 and 2.65 Ga (Fig. 7h). 1891 4 Ma (n = 30). Hf values of zircons with concordant ages of

1891 and 2032–2174 Ma vary from −2.9 to +6.9, and suggest inter-

4.2.5. Sample HY03-1 action between old continental crust and juvenile magma with a

Sample HY03-1 is a ﬁne-grained garnet-bearing muscovite depleted mantle source. Hf values of the minor population of zir-

− − schist collected from northeast of Laojiang Village on the north- cons with ages of ca. 2241 Ma vary from 1.7 to 5.3, which implies

◦ ◦

western part of Haiyang Island (123 10 10.2 E, 39 04 39.6 N; that they mostly crystallized from old continental crust (Fig. 8c;

Fig. 2b). This sample has a porphyritic granular–schistose Supplementary Table 3). The DM model ages of all the zircons

E. Meng et al. / Precambrian Research 233 (2013) 297–315 307

5 5 HY03-1 ( a ) HY03-1 ( b ) 4 4

3 3

2 2

Number

Number 1 1

0 0 -30 -20 -10 0 10 20 1.6 1.8 2.0 2.2 2.4 2.6 2.8 3.0 3.2

5 4 HY05-1 ( c ) HY05-1 ( d ) 4 3

3 2 2

Number

Number 1 1

0 0 -8 -4 0 4 8 12 2.0 2.2 2.4 2.6 2.8 3.0 3.2 3.4

5 3

HY05-2 ( e ) HY05-2 ( f ) 4 2 3

Number Number 1 1

0 0 -25 -15 -5 5 15 25 1.4 1.8 2.2 2.6 3.0 3.4 3.8

5 6

HY06-1 ( g ) HY06-1 ( h ) 4 5

4 3 3 2

Number Number 2 1 1

0 0 -16 -12 -8 -4 0 4 8 12 2.2 2.6 3.0 3.4 3.8 4.2 4.6

ε (t) C

Hf T DM (Ga)

Fig. 8. Hf isotopic compositions of samples from the Changhai metamorphic supracrustal rocks. Left: Relative probability plots of εHf values. Right: Relative probability plots

C T

of DM data.

exhibit two major peaks at 2.58 and 2.75 Ga and two minor peaks and two groups of grains are recognizes based on the internal struc-

at 2.13 and 3.17 Ga (Fig. 8d). ture. One group has cores with oscillatory zoning and narrow rims

with high luminescence, which coupled with their high Th and U

contents, and Th/U ratios (0.15–2.61; Supplementary Table 2) in

4.2.7. Sample HY05-2

the cores indicates a magmatic origin. The other group has rela-

Sample HY05-2 is a quartzite collected from quartz veins associ-

tively small, inherited cores and wide rims with low luminescence

ated with the schistose fabric of sample HY05-1. This sample has a

and Th/U ratios (0.02–0.07; Supplementary Table 2), indicating a

granular crystalloblastic texture and is mainly comprised of quartz

metamorphic origin.

(>99%). Zircons separated from this sample are mainly rounded to

Fifty zircons from this sample were subjected to U–Pb dating.

subhedral stubby prisms, with a variable grain size (50–200 ␮m),

Apart from one analysis with a concordant age of 2603 Ma, all

and a pale yellow or brown color. Cathodoluminescence images

207 206

the magmatic zircons have Pb/ Pb weighted average ages of

show that the internal structure of these grains is complex (Fig. 5g),

308 E. Meng et al. / Precambrian Research 233 (2013) 297–315

2765 ± 14 Ma (n = 4), 2142 ± 14 Ma (n = 4), and 1884 ± 8 Ma (n = 11). 5.2. Provenance

The latter age is consistent with the upper intercept age of

1897 ± 36 Ma deﬁned by 36 analyses (Fig. 6g). One metamorphic The provenance of low-grade metasedimentary rocks can be

zircon (analysis 25) has a concordant age of 1885 ± 14 Ma, which is investigated using elements that are immobile (e.g., Th, Sc, Hf,

within analytical uncertainty of the major age peak at ca. 1884 Ma. and Co) during weathering, transport, diagenesis, and low-grade

206 238

Four metamorphic zircons yielded a Pb/ U weighted average metamorphism (Taylor and McLennan, 1985; Bhatia and Crook,

age of 250 ± 4 Ma (Fig. 6g), which overlaps with the younger meta- 1986; McLennan et al., 1990). Chondrite-normalized REE patterns

morphic ages from samples DD23-3 and HY03-1. Hf values for of the Changhai metamorphic supracrustal rocks are characterized

zircons with ages between 1884 and 2765 Ma mainly vary from +1.4 by LREE enrichment ([La/Yb]N = 5.9–17.7), negative Eu anoma-

to +13.0 (apart from one analysis with −1.4), implying that these lies (␦Eu = 0.48–0.65), and fractionated LREEs ([La/Sm]N = 3.8–5.2),

zircons largely crystallized from juvenile magma with a depleted which are features consistent with the source rocks having felsic

mantle source. Hf values of the minor population of zircons with to intermediate compositions (Slack and Stevens, 1994). More-

ages of 250 Ma vary from −11.1 to −17.1, which are similar to over, the Cr/Zr ratio indicates the relative proportion of zircon and

those of zircons from samples DD23-3 and HY03-1 (Supplementary chromite in the source that can be linked to the relative proportion

Table 3), indicating that they mostly crystallized from old conti- of contributions from granite and komatiite, respectively. Low Cr/Zr

nental crust. The DM model ages of all the zircon grains exhibit (0.16–0.49) and Cr/Th (1.4–2.9) ratios, and high Zr/Y (4.5–13.2)

two major peaks at 2.28 and 2.93 Ga, two less prominent peaks at and Th/U (7.2–13.1) ratios are distinct from the Witwatersrand

2.38 and 2.85 Ga, and three minor peaks at 2.04, 2.66, and 3.32 Ga and Pongolar Supergroups in South Africa and Archean basalts,

(Fig. 8f). but are similar to Archean granite (Wronkiewicz and Condie, 1987,

1989; Condie and Wronkiewicz, 1990; Condie, 1993). These ele-

mental ratios suggest that the sediments were derived mainly

4.2.8. Sample HY06-1 from an intermediate to silicic source, which is consistent with

Sample HY06-1 is a ﬁne-grained quartzite collected from high La/Sc (2.0–5.4), Th/Sc (1.4–2.6), and La/Co (5.1–9.2, apart from

◦

Qinglongshan Hill in central Haiyang Island (123 10 24.6 E, two samples with 33.7 and 2.7) ratios in these samples (Cullers,

◦

39 02 38.1 N; Fig. 2b). This sample has a granular crystalloblastic 2000). Moreover, the low to moderate contents of Cr (<100 ppm)

texture and is largely comprised of quartz (95%) and minor amounts and Ni (<35 ppm) in the Changhai metamorphic rocks are consis-

of muscovite and feldspar (5%). Zircons separated from this sam- tent with the paucity of maﬁc rocks in the source region (Garver

ple are mainly rounded or subhedral short prisms, with a variable et al., 1996). On source rock discrimination diagrams based on

␮

grain size (30–200 m), and are pale yellow or gray-brown in color. major elements, the present samples mainly plot in the ﬁelds of

Cathodoluminescence images show that most of these zircons have intermediate–acidic igneous provenance (Roser and Korsch, 1988).

oscillatory zoning (Fig. 5h), and this feature, along with their high Th On a plot of La/Th vs. Hf, using elements that are insensitive to

and U contents, and Th/U ratios (0.14–1.28; Supplementary Table metamorphism, the data largely fall in the ﬁeld for an acidic arc

2), is indicative of a magmatic origin. volcanic source with limited input from ancient crustal material

Ninety-nine U–Pb dates of this sample have a relatively simple (Floyd and Leveridge, 1987). In addition, most of the detrital zir-

age pattern (Fig. 6h). Apart from four grains with older concord- cons have subhedral to euhedral prismatic shapes and magmatic

± ±

ant ages of 3212 38 Ma (n = 2) and 2547 35 Ma (n = 2), all the oscillatory zoning (Fig. 5), which are also features consistent with

remaining zircons fall on a discordia line with an upper inter- an intermediate–acidic source. Therefore, it is considered that the

207 206

cept age of 1889 12 Ma, which is consistent with the Pb/ Pb source rocks of the Changhai metamorphic supracrustal rocks were

± ε

weighted average age of 1882 9 Ma of 33 concordant analyses. Hf mainly granitoids that may have contained minor amounts of clas-

− −

values of zircons in this sample range from 12.4 to 1.8 (apart tic sediments.

from one analysis with +6.1) (Fig. 8g; Supplementary Table 3), U–Pb ages and Hf isotopes of detrital zircons from the Chang-

implying that the zircons crystallized from old continental crust. hai metamorphic supracrustal rocks provide further information

± T

The major age population (1882 9 Ma) yields a DM model age about their source rocks. From a K–S test for detrital zircons in six

peak at 2.87 Ga and two smaller peaks at 2.94 and 3.05 Ga. The DM schists and two quartzites samples (For details on the deﬁnition

ε −

model ages of the ca. 3200 Ma zircons are ca. 3.95 Ga ( Hf = 6.1) and and usage of the K and S values see Liu et al. (2012a)), P values

ε −

4.36 Ga ( Hf = 12.4), which may identify the existence of ancient are >0.05 for 72% of the 28 sample pairs. In contrast, P values are

continental crust in the basement of this region (Fig. 8h; Supple- >0.05 for only one of eight K–S comparisons of sample DD23-3.

mentary Table 3). Sample DD23-3 contains a greater number of younger metamor-

phic zircons (peak at 249 Ma) as compared with the other seven

samples, which leads to the low P values. Apart from this sample,

5. Discussion the detrital zircon ages of the Changhai metamorphic supracrustal

rocks are remarkably similar. Therefore, U–Pb ages and Hf isotope

5.1. Nature of the protolith data for all the detrital zircons obtained in this study are combined

in a binned frequency histogram (Fig. 9a) and a Hf vs. time (Ma)

The Changhai metamorphic supracrustal rocks consists mainly plot (Fig. 9b).

of multiple types of schists, such as garnet–mica schists with dif- The age histogram of 521 detrital zircon analyses (Fig. 9a)

ferent aluminum-rich minerals, chlorite–sericite–quartz schists, enables identiﬁcation of some major age peaks. The major pop-

and minor quartzites and marbles. These rocks are character- ulation, comprising 89% of zircons from two quartzite samples

ized by enrichment in Al2O3, depletion in CaO, K2O/Na2O > 1, and and 74% of zircons from the six schist samples, exhibits an age

the presence of aluminum-rich metamorphic minerals (e.g., gar- range between 1856 and 1916 Ma (discordance ≤ 10; Supplemen-

net and kyanite) and small amounts of accessory minerals. These tary Table 2) with an age peak of ca. 1887 Ma (Fig. 9a). This age

features are consistent with a metasedimentary origin (Fig. 3a range is consistent with those of other rocks in the Jiao–Li–Ji

and d). On elemental discrimination diagrams (Fig. 3b and c), the Belt, such as rapakivi granite, porphyritic monzogranite, and K-

protolith is identiﬁed as being ﬁne-grained clastic sedimentary feldspar granite (1860–1889 Ma; Li et al., 2003; Lu et al., 2005,

material dominated by shale and clay rocks with some sandstone 2006; Wan et al., 2006; Li and Zhao, 2007); the Kuangdonggou alka-

contribution. line syenite (1866–1879 Ma; Cai et al., 2002; Yang et al., 2007);

E. Meng et al. / Precambrian Research 233 (2013) 297–315 309

the zircons crystallized in magmas formed from the mixing of

1887 Ma

( a ) Paleoproterozoic–Mesoarchean crustal components with magmas

100

derived from depleted mantle.

A subordinate population of detrital zircons has ages between

80 2142 and 2258 Ma with a main age peak of ca. 2172 Ma (Fig. 9a),

which constitutes 17% and 5% of the detrital zircons in the schist and

quartzite samples, respectively. A number of felsic rocks with ages

249 Ma within this range have been reported from the study area, including

2174 Ma the extensive Liao’Ji granites with ages of 2143–2176 Ma, includ-

40 ing magnetite-bearing monzogranites in the Liaoning Province (Lu

Number

et al., 2004a, 2005, 2006; Li et al., 2005; Wan et al., 2006; Li and

3212 Ma

Zhao, 2007) and similar rocks in the Tonghua region (Lu et al.,

20 2552 Ma

2004a,b, 2006). Many detrital zircons from the Laoling, Ji’an, and

2765 Ma

North and South Liaohe groups also have ages of 2032–2282 Ma

(Luo et al., 2004, 2008; Lu et al., 2006; Wan et al., 2006), suggesting

0 1000 2000 3000 4000

that zircons of this age (2036–2093 Ma) were derived from these

t(Ma) granitic rocks and/or the aforementioned groups. However, Hf iso-

tope data for this population of zircons have a wide range of ε 20 Hf

Depleted

values from −5.3 to +7.8 (Fig. 9b; Supplementary Table 3), indi- m

15 antle ( b )

cating that inputs of juvenile magma also occurred, which is also

10 a C

G T 8 consistent with their scattered DM model ages from 2.31 to 3.19 Ga 1. Ga

t 5

5 2. Ga (Supplementary Table 3).

) Chondrite Crus 3.0

(t 0 A few detrital zircons have age peaks of ca. 3212, 2765,

and 2552 Ma (Fig. 9a), and constitute 7% of all concordant zir- −5 t

Crus cons from the Changhai metamorphic supracrustal rocks. These

−10

ages are comparable with those of Archean basement rocks, t 5

−15 01

Crus =.0 such as tonalite, granodiorite, and syenogranite that have expe-

−20 rienced upper amphibolite to granulite facies metamorphism in

Lu/ DD10-1 DD20-1 DD23-3 HY01-1

−25 HY03-1 HY05-1 HY05-2 HY06-1 the basement of the Liaobei–Jinan Complex in the north, and

the Liaonan–Nangrim Complex in the south (3.85–2.50 Ga; Liu

−30

0 500 1000 15002000 2500 3000 3500 et al., 1992, 2008; Song et al., 1996; Wu et al., 2005, 2008; Zhang

t(Ma) et al., 2011). Zircon U–Pb dates for granitic rocks in the basement

of the Changhai area indicate that they formed at 2.50–2.55 Ga,

Fig. 9. Zircon U–Pb age spectra (t(Ma), a) and εHf (t) vs. t(Ma) (b) for analyzed zircons but include some inherited zircons with ages of 2.60–3.30 Ga

207 206

from the Changhai metamorphic supracrustal rocks. Pb/ Pb ages are presented

(En Meng, unpubl. data). Therefore, it is speculated that these

206 238

for Precambrian zircons and Pb/ U ages for Phanerozoic zircons.

ancient inherited zircons may be derived from basement gran-

itoids. Moreover, Neoarchean detrital zircons from the studied

ε samples have Hf values from +0.6 to +9.1 (apart from one anal-

− T

alkaline syenite, granitic pegmatite, and metamorphosed pillow ysis with 1.4) and DM model ages from 2.48 to 3.32 Ga (peak at

lavas (1870–1880 Ma; Wang et al., 2011b; Dong et al., 2012); 2.72–2.93 Ga), whilst two Paleoarchean grains have ages of 3208

ε − − T

and the metamorphic ages of 1872–1896 Ma obtained from the and 3215 Ma with Hf values of 6.1 and 12.4 and DM model

present samples and from the biotite–plagioclase gneiss and meta- ages of 3.95 and 4.36 Ga (Fig. 9b; Supplementary Table 3). These

sandstone of the Liaohe and Ji’an groups (Li et al., 2003; Luo results suggest that a minor component of the Changhai metamor-

et al., 2004, 2008; Lu et al., 2006; Wan et al., 2006; Li and Zhao, phic supracrustal rocks was derived from the magmatic erosion

2007). Therefore, the present U–Pb age data for the Changhai of Paleoarchean, Mesoarchean, and even Hadean crust of the East-

metamorphic supracrustal rocks when compared with previously ern Block. There are also some metamorphic zircons with an age

ε − − T

published data (Li et al., 2003; Luo et al., 2004, 2008; Lu et al., peak of 248 Ma, Hf values of 11.1 to 23.7, and DM model

2006; Wan et al., 2006; Li and Zhao, 2007), and the occurrence ages of 1.98–2.77 Ga (Fig. 9; Supplementary Table 3), suggesting

of the Seongnam migmatite and Nonggeori and Naedeokri gran- derivation from recycling of older crust during an Early Triassic

ites with ages of 1862–1868 Ma in South Korea (Kim et al., 1999; tectono-thermal event that may have been associated with tec-

Kim and Cho, 2003; Lee et al., 2005) and porphyritic monzo- tonism related to the Mesozoic Sulu-Dabie Orogen (Li et al., 2009,

granites with ages of 1865–1843 Ma in North Korea (Zhao et al., 2011d). Although the nature and geodynamic setting of this event

2005), all suggest that the age peak of ca. 1887 Ma represents require further investigation, the identiﬁcation of an Early Triassic

an important late Paleoproterozoic magmatic–thermal event in metamorphic event in the Changhai area has provided clues to the

the Jiao–Liao–Ji Belt and adjacent regions. Given the geochemical northward extension of the Sulu Ultrahigh-Pressure belt (Li et al.,

characteristics of these rocks, it might be concluded that coeval 2009, 2011d).

granitic rocks are the most important source (Lu et al., 2006; In summary, the new geochronological and Hf isotopic data

Wan et al., 2006; Li and Zhao, 2007). In addition, Hf values of reveal that detrital zircons from these metamorphic supracrustal

zircons largely range from −11.1 to +13.0 (Fig. 9b; Supplemen- rocks yield age peaks at 1887, 2174, 2552, 2765, and 3212 Ma

T ε − tary Table 3). The DM model ages vary between 1.97 and 3.25 Ga (Fig. 9a), have Hf values from 11.1 to +13.0 (Fig. 9b), and yield

with three peaks (i.e., 2.04–2.33, 2.56, and 2.72–2.93 Ga; Supple- three major groupings of DM model ages at 2.04–2.33, 2.48–2.56,

mentary Table 3), which is consistent with the ages of granitic and 2.72–2.93 Ga (Fig. 10). These age constraints show that most

rocks in the Paleoproterozoic Jiao–Liao–Ji Belt (Lu et al., 2005, of the sediments of the Changhai metamorphic supracrustal rocks

2006; Wan et al., 2006; Li and Zhao, 2007), and with Neoarchean were sourced from ancient granitoid rocks and that some were

and Mesoarchean basement (Wan et al., 2001; Wu et al., 2005; sourced directly from Paleoproterozoic metamorphic strata (e.g.,

Zhao et al., 2005; Liu et al., 2007). As such, it is proposed that North and South Liaohe groups).

310 E. Meng et al. / Precambrian Research 233 (2013) 297–315

20 which is clearly younger than the depositional ages of the North

2.04~

2.72~2.93 Ga and South Liaohe groups in mainland China. However, this age is

2.33 Ga

16 consistent with the age of regionally widespread granitoids, maﬁc

rocks, and metamorphic ages of the South Liaohe and Ji’an groups

in the Jiao–Liao–Ji Belt (Cai et al., 2002; Li et al., 2003, 2011c; Luo

et al., 2004, 2008; Lu et al., 2005, 2006; Wan et al., 2006; Li and Zhao,

2.48~2.56 Ga

2007; Yang et al., 2007; Wang et al., 2011b). These results, combined

Number with coeval concordant metamorphic ages from our samples, indi-

cate that this age (1879 Ma) represents the metamorphic peak age

4 of the South Group; i.e., the minimum depositional age of the South

Group is earlier than 1879 Ma.

1.4 1.9 2.4 2.9 3.4 3.9 4.4 4.9 5.4 5.4. Tectonic implications C

T DM (Ga)

Two models have been proposed to explain the tectonic nature

C of the Jiao–Liao–Ji Belt. The ﬁrst considers that formation of this belt

Fig. 10. Histogram showing zircon DM model ages of the analyzed detrital zircon

ages from the Changhai metamorphic supracrustal rocks. involved the opening and closing of an intra-continental rift along

the eastern continental margin of the NCC (Zhang, 1988; Peng and

Palmer, 1995; Li et al., 2003), which has also been supported by a

5.3. Maximum depositional age number of recent studies (Chen et al., 2003; Li et al., 2003, 2005; Luo

et al., 2004, 2008; Zhao et al., 2005; Li and Zhao, 2007). The second

The depositional age of the Changhai metamorphic supracrustal model proposes that this belt represents a continent–arc–continent

rocks has not been well constrained due to the lack of exposure collisional belt (Bai, 1993; He and Ye, 1998a,b; Faure et al., 2004;

and absence of volcanogenic interbeds suitable for dating. Thus, the Lu et al., 2006; Wang et al., 2011b).

Changhai metamorphic supracrustal rocks were previously classi- According to the rift model, the Archean Liaobei–Jinan Com-

ﬁed as part of the Paleoproterozoic South Liaohe Group based on plex in the north, and the Liaonan–Nangrim Complex in the south

lithostratigraphic relationships (LBGMR, 1989). However, the age were originally situated on a single continental block that under-

of the protolith of the regional South Liaohe Group had not been went early Paleoproterozoic rifting. Rifting was associated with the

previously determined precisely and remains controversial (Luo formation of volcano-sedimentary rocks, and granitoid and maﬁc

et al., 2004, 2008; Lu et al., 2006). Previously published data, includ- intrusions. The rift then closed in the late Paleoproterozoic to form

ing K–Ar and Rb–Sr whole-rock isochron dates and conventional the Jiao–Liao–Ji Belt (Yang et al., 1988; Zhang and Yang, 1988; Li

multi-grain zircon U–Pb ages, have been used to infer that Pale- et al., 2001b, 2004, 2005; Luo et al., 2004, 2008; Li and Zhao, 2007).

oproterozoic volcano-sedimentary rocks in the Liao’ji area were The following major lines of evidence support the rift model (Zhao

deposited between 2400 and 2000 Ma (Zhang, 1988). However, the et al., 2005; Li and Zhao, 2007; Luo et al., 2008): (1) the presence

K–Ar dating method does not yield reliable constraints on the depo- of bimodal volcanic rocks in the form of metabasalts (greenschists

sitional age of metamorphic supracrustal rocks. The present results, and amphibolites) and metarhyolites (Zhang and Yang, 1988; Sun

along with previously published data for the Liaohe Group (Luo et al., 1993; Peng and Palmer, 1995); (2) the existence of volumi-

et al., 2004, 2008; Lu et al., 2006), show that zircons from these nous pre-tectonic A-type granites and minor post-tectonic alkaline

rocks have complex age patterns, indicating that multi-grain zircon syenites and rapakivi granites (Zhang and Yang, 1988; Sun et al.,

U–Pb ages are geologically meaningless (e.g., Mezger and Krogstad, 1993; Peng and Palmer, 1995); (3) the occurrence of geochemi-

1997). The narrow range of Rb/Sr ratios, combined with uncer- cally and geochronologically similar late Archean TTG basement

tainties surrounding whether analyzed samples have a cogenetic gneisses and maﬁc dyke swarms at both margins of the Jiao–Liao–Ji

origin, means that Rb–Sr whole-rock isochron ages are similarly Belt (Zhang and Yang, 1988; Lu et al., 2005); (4) the fact that the

unreliable. low-P and anticlockwise P–T paths of the Ji’an, South Liaohe, and

Recently, Luo et al. (2004, 2008) used the LA-ICP-MS U–Pb zir- Jingshan groups (Lu, 1996; He and Ye, 1998a,b; Li et al., 2001b) are

con dating technique to determine that both the North and South not consistent with a continent–continent collision model; (5) the

Liaohe groups were deposited after 2.03 Ga and metamorphosed at fact that the ﬁrst phase of deformation was extensional in nature (Li

1.93–1.90 Ga. However, Lu et al. (2006) used the same technique to et al., 2005); (6) the similar Nd isotopic compositions of the Liaoji

date detrital zircons from two samples of the South Liaohe Group granitoids associated with the North and South Liaohe groups (Li

and concluded that it was deposited at 2.12–1.85 Ga, and expe- et al., 2006); and (7) the presence of non-marine borate-bearing

rienced a 1.85 Ga metamorphic event along with the Ji’an Group. sedimentary successions (Jiang, 1987; Peng and Palmer, 1995).

The metamorphic age previously assigned to the North and South In contrast, the continent–arc–continent collision model sug-

Liaohe groups was based on a small number of largely discordant gests that the two aforementioned complexes represent different

metamorphic zircons. In addition, this metamorphic age is consis- Archean continental blocks (Longgang and Nangrim blocks; Bai,

tent with the timing of a major magmatic event in this region (Li 1993; He and Ye, 1998a,b), whereas the Jiao–Liao–Ji Belt is an

et al., 2001b, 2003, 2011c; Cai et al., 2002; Lu et al., 2005, 2006; intervening island arc and back-arc basin (Bai, 1993). In the Pale-

Wan et al., 2006; Li and Zhao, 2007; Yang et al., 2007; Wang et al., oproterozoic, the Longgang Block was an active-type continental

2011b) and, in particular, the southern Liaoning Province. As such, margin on its present-day southern side, where a continental mag-

it is proposed that the ages of these metamorphic zircons cannot matic arc and a back-arc basin developed, and were subsequently

represent the peak age of metamorphism; instead, they constrain incorporated into the Jiao–Liao–Ji Belt. The Nangrim Block had a

the minimum depositional age of the South Liaohe Group. passive-type continental margin on its present-day northern side

The new geochronological data of the present study show that along which stable continental margin sediments were deposited.

the major population of detrital zircons from six schists and two An ocean was situated between the two blocks, which was under-

quartzites in the Changhai area displays an age peak at ca. 1887 Ma going subduction beneath the present-day southern margin of the

with the youngest concordant age being 1879 Ma (Fig. 9a). This con- Longgang Block. Final closure of this ocean in the late Paleopro-

strains the maximum depositional age of the protolith to 1879 Ma, terozoic led to the continent–arc–continent collision that formed

E. Meng et al. / Precambrian Research 233 (2013) 297–315 311

Th Sc ( b ) ( c ) 60 ACM: active continental margin ( a ) OIA CIA-continental island arc OIA 50 PM-passive continental margin OIA-oceanic island arc ACM CIA 40

PM Ti/Zr 30 ACM ACM PM 20 CIA CIA 10

OIA PM 2 4 618 0 12 Co Zr/10

La/Sc

Fig. 11. Co–Th–Zr/10 (a), Sc–Th–Zr/10 (b) and Ti/Zr vs. La/Sc tectonic discrimination diagrams (Bhatia and Crook, 1986) for analyzed samples from the Changhai metamorphic

supracrustal rocks. OIA – oceanic island arc; CIA – continental island arc; ACM – active continental margin; and PM – passive continental margin.

the Jiao–Liao–Ji Belt (Bai, 1993). In contrast, Faure et al. (2004) sug- derived from the basement gneisses, as would be expected in the

gested that subduction was toward the south and that the 1.9 Ga case of a rifting model. Therefore, it is proposed that (1) the Long-

maﬁc–ultramaﬁc rocks mark a Paleoproterozoic active continental gang and Nangrim blocks were already a single continental block

margin that was part of the southern block. at 1887 Ma (i.e., the rift had closed before 1887 Ma), (2) the pro-

The whole-rock geochemical and zircon U–Pb dating and Hf iso- toliths of the Changhai metamorphic supracrustal rocks formed in

topic data of the present study are not able to unequivocally resolve an active continental margin setting, and (3) coeval igneous rocks

this controversy, but do provide some constraints on these models. with subduction-related properties could have formed in an exten-

The Changhai metamorphic supracrustal rocks are characterized sional environment such as a back-arc basin (Cai et al., 2002; Li et al.,

by LREE enrichment, HREE depletion, and negative Eu anomalies, 2003; Li and Zhao, 2007; Yang et al., 2007; Wang et al., 2011b; Dong

and also have relatively high La/Sc (2.0–4.8), La/Y (1.2–3.1), and et al., 2012).

Ti/Zr (12.7–32.9) ratios, and low Sc/Cr ratios (0.19–0.31), which

are consistent with protolith formation in a continental margin

6. Conclusions

tectonic setting (Bhatia and Crook, 1986; Long et al., 2008). Further-

more, ␦Ce values range from 0.81 to 0.94 (apart from two analyses

A geochemical, isotopic, and geochronological study of the

of 0.71 and 0.75), which are markedly higher than those of mid-

Changhai metamorphic supracrustal rocks in southeast Liaoning

ocean ridge (0.29) and ocean basin (0.55) basalts, but similar to

Province, northeast China has led to the following major conclu-

continental margin rocks (0.90–1.30) (Murray et al., 1990). Con-

sions:

versely, almost all of the samples plot in the active continental

margin ﬁeld, apart from a few samples that plot within or near

the continental island arc ﬁeld (Fig. 11). Thus, it is considered that (1) The Changhai metamorphic supracrustal rocks mainly com-

the protolith of the Changhai metamorphic supracrustal rocks may prise various types of garnet–mica schists, along with minor

have formed in an active continental margin setting. The timing amounts of quartzites and marbles. The protoliths of these rocks

of regional magmatism at ca. 1887 Ma (Lu et al., 2006; Wan et al., were mainly shale and clay rocks with some contribution from

2006; Li and Zhao, 2007) also provides an important constraint on sandstone.

the provenance of the Changhai metamorphic supracrustal rocks, (2) The whole-rock geochemistry of the metamorphic supracrustal

ε −

as do the Hf values of these zircons ( 11.1 to +13.0) (Fig. 9b; rocks indicates that their source rocks were mainly granitoids,

Supplementary Table 3). These results, combined with the similar possibly with minor amounts of clastic sediments. U–Pb ages

ages of ancient zircons (2.5–3.2 Ga) in the Changhai metamorphic of detrital zircons yield age peaks at 1887, 2174, 2552, 2765,

supracrustal rocks, the North Liaohe Group (Luo et al., 2004, 2008), and 3212 Ma, which coincide with the emplacement ages of

and the basement (Liu et al., 1992, 2008; Song et al., 1996), it can granitoids in the Paleoproterozoic Jiao–Liao–Ji Belt and Archean

be concluded that the Archean Liaobei–Jinan Complex in the north basement. These ages are also consistent with those of detri-

and the Liaonan–Nangrim Complex in the south were already a tal zircons from the metamorphosed sedimentary and volcanic

single continental block at 1887 Ma, and their source rocks were successions (e.g., North and South Liaohe groups). Thus, the

derived from reworking of old continental crust and juvenile crustal age data suggest that the sediments of the Changhai metamor-

additions, with the latter perhaps related to arc magmatism. P–T–t phic supracrustal rocks were largely sourced from the regional

paths for the garnet–mica schist obtained by phase equilibrium granitoids, along with some direct contributions from the afore-

simulations are clockwise (En Meng, unpubl. data), which is incon- mentioned metamorphic successions.

sistent with P–T–t paths reported in previous studies (He and Ye, (3) The major population of detrital zircons from the Changhai

1998a,b). This discrepancy indicates the need for further study of metamorphic supracrustal rocks has an age peak at ca. 1887 Ma

the metamorphic history of this region. Finally, we note that the with a youngest concordant age peak of 1879 Ma, which are

Changhai metamorphic supracrustal rocks and the North and South the same as the age data for regionally widespread granitoids,

Liaohe, and Ji’an groups in the Jiao–Liao–Ji Belt all contain abundant maﬁc rocks, and metamorphic ages of the South Liaohe and

2258–2765 Ma detrital zircons, along with some grains with ages Ji’an groups in the Jiao–Liao–Ji Belt. This result indicates that

of ca. 2174 Ma, and this is similar to zircon ages in nearby Archean the Changhai metamorphic supracrustal rocks do not belong to

to Paleoproterozoic basement gneisses (Lu et al., 2004a,b, 2006; Li the regional South Liaohe Group as previously thought, and it

et al., 2005; Wan et al., 2006; Li and Zhao, 2007). These results indi- constrains the maximum depositional age of their protoliths to

cate that part of the protoliths of these groups was most probably 1879 Ma.

312 E. Meng et al. / Precambrian Research 233 (2013) 297–315

(4) Metamorphic zircons with ages of ca. 248 Ma suggest that the Grifﬁn, W.L., Pearson, N.J., Belousova, E.A., Jackson, S.E., van Achterbergh, E., O’Reilly,

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gram on Key Basic Research Project (973 Program, Grant No. Guo, J.H., Peng, P., Chen, Y., Jiao, S.J., Windley, B.F., 2012. UHT sapphirine granulite

metamorphism at 1.93–1.92 Ga caused by gabbronorite intrusions: implications

2012CB416603), the National Natural Science Foundation of China

for tectonic evolution of the northern margin of the North China Craton. Precam-

(Grant Nos. 40725007 and 41202136), the China Geological Survey

brian Research 222/223, 124–142.

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