Detrital Zircon U–Pb, Hf Isotopes, Detrital Rutile and Whole-Rock

Precambrian Research 254 (2014) 290–305

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Precambrian Research

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Detrital zircon U–Pb, Hf isotopes, detrital rutile and whole-rock

geochemistry of the Huade Group on the northern margin of the

North China Craton: Implications on the breakup of the Columbia supercontinent

a,b,∗ b a

Chaohui Liu , Guochun Zhao , Fulai Liu

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

Department of Earth Sciences, The University of Hong Kong, Pokfulam Road, Hong Kong

r t a b

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

Article history: Supracrustal successions in the Zhaertai–Bayan Obo–Huade rift zone on the northern margin of the North

Received 14 August 2013

China Craton include the Zhaertai, Bayan Obo and Huade Groups from west to east. The Huade Group,

Received in revised form 18 August 2014

which has been subdivided into four formations, is composed of basal pebbled quartzites, quartzites,

Accepted 15 September 2014

schists, phyllites, marbles, slates and diopsidites. Geochemistry of the metasedimentary succession indi-

Available online 28 September 2014

cates that source rocks of the lower two formations are felsic, displaying passive margin signatures,

whereas those of the upper two formations have continental island arc or active continental margin

Keywords:

signatures. U–Pb ages of detrital zircons from the group yielded three age populations of 2690–2450,

Zhaertai–Bayan Obo–Huade rift zone

2150–1710 and 1660–1330 Ma, of which the youngest age population only exist in the upper Huade

North China Craton

Geochemistry Group. The dominant 2690–2450 detrital zircons were likely sourced from the granitic rocks in the

Detrital zircon and rutile Yinshan Block. The subordinate 2150–1710 Ma detrital zircons were probably recycled from the metased-

Mesoproterozoic imentary units from the Khondalite Belt and/or derived from the similar aged granitic plutons of the

Hongqiyingzi “Group”, which are also evidenced by the similar geochemical features of rutiles from the

Huade Group and the Khondalite Belt. Minor amounts of 1660–1330 Ma detrital zircons may have derived

from the North American and/or Baltica cratons connected to the northern margin of the North China

Craton in the Columbia supercontinent. The youngest detrital zircon age peak of ∼1337 Ma in the upper

Huade Group suggests that the sedimentation began after ∼1.34 Ga. In combination with the ∼1320 Ma

granitoids cross-cutting it, depositional ages of the upper Huade Group can be constrained between ∼1.34

and ∼1.32 Ga. Taking into account the lithostratigraphic features, provenances and depositional ages, a

continental rift basin deposit represented by the upper Huade Group on the northern margin of the North

China Craton developed between ∼1.34 and ∼1.32 Ga, which indicates that the ﬁnal breakup of the North

China Craton from the Columbia supercontinent happened in the middle Mesoproterozoic.

1. Introduction 2008; Hou et al., 2008; Li et al., 2008; Reddy and Evans, 2009).

Formation of the Columbia supercontinent was thought to have

Assembly, conﬁguration, accretion and breakup history of been completed by global-scale 2.0–1.8 Ga collisional events (Zhao

a Paleo-Mesoproterozoic supercontinent, referred to as Nuna et al., 2002, 2003, 2004, 2006). Fragmentation of Columbia com-

(Hoffman, 1997) or Columbia (Rogers and Santosh, 2002; Zhao menced at ca. 1.5 Ga with the ﬁnal breakup at ca. 1.3–1.2 Ga,

et al., 2002) have been topics of great interest in the last decades marked by widespread Mesoproterozoic continental rifting, anoro-

(Dalziel, 1991; Hoffman, 1991, 1997; Moores, 1991; Condie, 2002; genic magmatic activity and maﬁc dike swarms in most of the

Rogers and Santosh, 2002; Zhao et al., 2002, 2004; Kröner and cratonic blocks forming the supercontinent (Ernst and Buchan,

Cordani, 2003; Zhai and Liu, 2003; Kusky et al., 2007; Ernst et al., 2001; Zhao et al., 2006; Ernst et al., 2008; Hou et al., 2008; Goldberg,

2010).

In the North China Craton (NCC), the history of assembly,

∗ accretion and breakup of the Columbia supercontinent were

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

recorded by three Paleoproterozoic collisional belts (the Khon-

Sciences, Beijing 100037, China. Tel.: +86 10 88332013.

E-mail address: [email protected] (C. Liu). dalite Belt, the Jiao-Liao-Ji Belt and the Trans-North China Orogen),

http://dx.doi.org/10.1016/j.precamres.2014.09.011

C. Liu et al. / Precambrian Research 254 (2014) 290–305 291

the 1.78–1.45 Ga Xiong’er volcanic belt and the Mesoproterozoic 2. Geological background

Zhaertai–Bayan Obo–Huade and Yan-Liao rift zones, respectively

(Zhao et al., 2011 and references therein). However, little consen- As one of the oldest cratonic blocks in the world, the NCC was

sus has been reached regarding the role of the NCC in the Columbia produced by the collision of the Eastern and Western Blocks along

supercontinent because of several unresolved issues. One of these the Trans-North China Orogen at ∼1.85 Ga (Guo et al., 2005; Zhao

issues concerns when the NCC was involved in the breakup of the et al., 2005, 2012; Kröner et al., 2006; Liu et al., 2006; Wang et al.,

Columbia. Some researchers suggested that the continental rifting 2010; Zhang et al., 2012c). After ﬁnal cratonization, the NCC under-

in the northern NCC had ﬁnished before 1.6 Ga and the NCC did went extensive rifting and anorogenic magmatism in the northern

not participate in the ﬁnal breakup of the Columbia at 1.35–1.20 Ga and central parts from 1.78 to 1.68 Ga (Halls et al., 2000; Wang

(Rogers and Santosh, 2002; Zhai, 2004; Hou et al., 2008). However, et al., 2004; Yang et al., 2005; Peng et al., 2005, 2007, 2008; Zhang

other researchers believed that the 1.33–1.31 Ga rift-related maﬁc et al., 2007). In the late Paleoproterozoic to Neoproterozoic, a

sills and granitoids in the northern NCC led to the ﬁnal breakup of thick sequence of sedimentary rocks was unconformably deposited

the Columbia supercontinent (Zhang et al., 2009, 2012a; Shi et al., above the Archean-Paleoproterozoic basement rocks in the Yan-

2012). Also at issue is the position of the NCC in the Columbia Liao and Zhaertai–Bayan Obo–Huade rift zones in the northern NCC

supercontinent. Suggested adjacent craton to the NCC ranges from (Fig. 1). Generally, the rift zone was thought to have developed

the Baltica (Rogers and Santosh, 2009), through the India (Zhao in response to the breakup of the Columbia supercontinent post

et al., 2002, 2004), to the North America (Hou et al., 2008). How- 1.8–1.6 Ga and the sedimentary rocks were deposited in passive

ever, previous conﬁgurations of Columbia were mainly based on continental margins (He et al., 2000; Huang et al., 2001; Zhu et al.,

limited paleomagnetic data or the general geological similarity of 2005; Hou et al., 2006, 2008; Lu et al., 2008; Kusky and Santosh,

the NCC with those of other cratonic blocks, few investigations 2009; Meng et al., 2011). Recently, zircon ages of K-rich volcanic

have been carried out on the supracrustal successions in the con- rocks range from 1.68 to 1.62 Ga have been obtained in the Tuan-

tinental rifts related to the ﬁnal breakup of the Columbia, which shanzi and Dahongyu Formations of the Changcheng Group (Lu and

has hampered further understanding of the role of the NCC in the Li, 1991; Li et al., 1995; Lu et al., 2008; Gao et al., 2008a). In the

Columbia supercontinent. In this contribution, we present inte- Gaoyuzhuang Formation of the Jixian Group, zircon U–Pb dating on

grated detrital zircon U–Pb and Hf isotopic data along with, detrital a tuff bed gave an age of 1559 ± 12 Ma (Li et al., 2010). Most recently,

rutile and whole-rock geochemical studies on the low-grade sedi- the bentonite beds in the Tieling Formation of the Jixian Group and

mentary rocks from the Huade Group in the eastern segment of the the Xiamaling Formation of the Qingbaikou Group yielded zircon

Zhaertai–Bayan Obo–Huade rift zone in the northern NCC. Com- U–Pb ages of 1437 ± 21 Ma and 1368–1366 Ma, respectively (Gao

bined with other sedimentary and lithostratigraphic data, these et al., 2007, 2008b; Su et al., 2008, 2010).

new results place signiﬁcant constraints on the depositional age Besides the late Paleoproterozoic to middle Mesoprotetozoic

and provenance of the Huade Group, helping to provide insight sedimentary rocks in the Yan-Liao rift zone, many diabase sills

into the breakup of the Columbia supercontinent in the northern and granitoids previously regarded as Paleozoic in age have been

NCC. suggested to middle Mesoprotetozoic. For example, a diabase sill

Fig. 1. Tectonic subdivision of the North China Craton (modiﬁed after Zhao et al., 2005). Also shown is location of the Zhaertai–Bayan Obo–Huade rift zone.

292 C. Liu et al. / Precambrian Research 254 (2014) 290–305

Fig. 2. A simpliﬁed geological map of the Shangdu–Huade–Kangbao area.

Modiﬁed after Hu et al. (2009).

intruding into the Jixian and Qingbaikou Groups gave zircon and U–Th–Pb monazite age of 1917 ± 48 Ma (Santosh et al., 2007). On

baddeleyite U–Pb ages of 1.35–1.32 Ga (Zhang et al., 2009, 2012a; Li the other way, the Guyang and Wuchuan complexes have tradi-

et al., 2009). In the Zhaertai–Bayan Obo–Huade rift zone, the exist- tionally been regarded as a Neoarchean granite-greenstone belt

ence of middle Mesoproterozoic granitoids has been proved by the and a Neoarchean granulite-facies complex, respectively (Li et al.,

1.33–1.31 Ga A-type granites in the Shangdu–Huade region (Zhang 1987). Recent SIMS and LA-ICP-MS U–Pb zircon dating results indi-

et al., 2012a; Shi et al., 2012). cate that granitic and volcanic rocks in both of the two complexes

Compared with the detailed investigations in the Yan-Liao rift were formed during late Archean and metamorphosed at ∼2.5 Ga

zone, the Zharertai–Bayan Obo–Huade rift zone has been less stud- (Jian et al., 2005, 2012; Chen, 2007; Dong et al., 2012).

ied, possibly due to its strong deformation and poor exposure of the Because of the extensive Phanerozoic cover and emplacement

Paleo- to Mesoproterozoic rocks (Wang et al., 1992a). Supracrustal of Paleozoic granitoids, the relatively continuous stratigraphic

successions in the rift zone were distributed in an E–W trending sequences of the Huade Group are only exposed in the northwest

basin and have been subdivided and given different stratigraphic of the Kangbao County, the south of the Huade County and the

names in different areas (Qiao, 1991; Wang et al., 1992a). Never- northwest of the Shangdu County (Fig. 2). Generally, the Huade

theless, the Zhaertai, Bayan Obo and Huade Groups are thought to Group was subdivided into the Maohuqing, Gejiaying, Sanxiatian

have been deposited roughly simultaneously in the late Paleopro- and Hujiertu Formations, all of which have been metamorphosed

terozoic to early Mesoproterozoic (Wang et al., 1992a). Based on to subgreenschist facies (Li et al., 2005; Hu et al., 2009). The low-

the detrital zircon U–Pb and Hf isotopic data and whole-rock Nd est Maohuqing Formation is >3200 m thick and its main lithologic

isotopic data from the Zhaertai Group, Li et al. (2007) suggested sequences change from the lower feldspar quartzites and quartz

that the group was derived from the late Archean basement rocks schists, through the middle sericite schists and quartzites, to the

∼

underlying the group and was deposited from 1.75 Ga during the upper phyllites (Fig. 3). Conformably overlying the Maohuqing

breakup of the Columbia supercontinent. Formation is the Gejiaying Formation that is composed of ∼2000 m-

The Huade Group is located at the eastern segment of the rift thick bed of basal pebbled quartzites, quartz schists, quartzites

zone and bounded by the Yan-Liao rift zone to the east, the west- and slates in the lower and ∼2300 m-thick phyllites, slates, quartz

ern part of the Hongqiyingzi “Group” and the Khondalite Belt to schists and marbles in the middle and upper sequences, inter-

the south, the Guyang and Wuchuan complexes to the southwest, preted as upward-deeping sequences changing from a coastal

and the Bayan Obo Group to the west (Fig. 1). The Hongqiyingzi to a shallow-marine depositional environment (Fig. 3; Li et al.,

“Group” is a complex of granitic gneisses, migmatites, paragneisses, 2005). The conformably overlying Sanxiatian Formation consists of

amphibolites, marbles, quartzites and schists (Liu et al., 2007). SIMS quartzites, quartz schists and phyllites interlayered with slates in

and LA-ICP-MS zircon dating results revealed that the “group” has the middle sequence. Widespread cross-bedding and ripple marks

experienced at least four episodes of tectonothermal events at preserved in the quartzites suggest a coastal depositional environ-

∼

∼ ∼

2.50, 2.18, 1.85 and 0.4–0.3 Ga (Liu et al., 2007). The major ment (Li et al., 2005). The Sanxiatian Formation is overlain by the

lithologies of the Khondalite Belt are khondalite series, TTG gneisses Hujiertu Formation, which consists mainly of quartzites, marbles,

with minor maﬁc granulites, syntectonic charnockites and S-type diopsidites and schists (Fig. 3). The overall sedimentary facies of

granites (Zhao et al., 2005). Recent LA-ICP-MS and SIMS U–Pb zir- the Huade Group suggest major changes in the basin conﬁguration

con data suggest that the protoliths of the khondalite rock series related to a rifting event in the northern NCC (Li et al., 2005; Hu

were deposited and metamorphosed in the Paleoproterozoic, with et al., 2009).

detrital zircon ages ranging between 2.3 and 1.8 Ga and metamor-

phic zircon ages at 2.0–1.9 Ga (Wan et al., 2006; Xia et al., 2006a, 3. Samples and analytical methods

2006b; Santosh et al., 2007; Yin et al., 2009, 2011). Other dating

techniques have also given similar or younger metamorphic ages, Twenty metasedimentary samples (18 meta-sandstones and

including U–Pb rutile age of 1793 Ma (Wu et al., 1998) and EPMA two meta-siltstones) were collected from different stratigraphic

C. Liu et al. / Precambrian Research 254 (2014) 290–305 293

Fig. 3. Stratigraphic subdivision of the Huade Group.

Modiﬁed after Li et al. (2005).

positions of the Huade Group for major and trace element anal- Ti concentration of 599 343 ppm based on the atomic masses of

ysis. Whole-rock geochemical analyses were performed at the Ti and O. NIST 610 glass was used as the external standard and

National Research Center for Geoanalysis, Beijing. Major elements analyzed after every 10 sample analyses, with recommended

were determined by X-ray ﬂuorescence techniques on fused glass values taken from Pearce et al. (1997). Two formulae of Zr-in-rutile

beads using a Rigaku-2100. The samples for trace element anal- thermometers from Zack et al. (2004) and Watson et al. (2006)

ysis were prepared in closed beakers in high-pressure bombs to (abbreviated as TZ and TW, respectively) were applied in this study

ensure complete digestion and trace element data were acquired to calculate the formation temperature of each rutile grain.

by a TJA-PQ-Excel ICP-MS. Four meta-sandstones and two meta-siltstones were chosen for

Three meta-sandstone samples were also chosen for rutile detrital zircon U–Pb and Hf isotopic analyses. Zircons were sepa-

geochemical analysis by LA-ICP-MS using an Agilent 7500a mass rated by standard heavy liquid and magnetic separation methods.

spectrometer equipped with a New-Wave UP-193 at the Geolog- Then they were mounted in epoxy resin discs, polished and imaged

ical Lab Center, China University of Geosciences, Beijing. Rutile in both reﬂected and transmitted light. In order to reveal internal

grains were picked from heavy-mineral residues, after crushing, structures of the zircons, CL imaging was carried out by a JSM6510

sieving and standard magnetic and heavy liquid separation, and SEM with attached Gatan CL detector. U–Pb isotopic analyses were

ﬁnally mounted on double sided adhesive tape, enclosed in epoxy performed using a New-Wave UP-213 laser-ablation system cou-

resin and polished to about half their size. For LA-ICP-MS analysis, pled with a Thermo-Finnigan Neptune MC-ICP-MS at MRL Key

samples were ablated with a spot size of 36 ␮m at a pulse rate of Laboratory of Metallogeny and Mineral Assessment, Institute of

10 Hz for 45 s duration. Element concentrations were calculated Mineral Resources, Chinese Academy of Geological Sciences, Bei-

by the software “GLITTER” using measurements of the following jing. The 213 nm ArF excimer laser, homogenized by a set of beam

29 49 53 90 93 178 181 208 232 238

isotopes: Si, Ti, Cr, Zr, Nb, Hf, Ta, Pb, Th, U, delivery groups, was focused on the zircon surface with the energy

49 2

dwell-times were 6–30 ms. Ti was used as the internal standard density of 2.5 J/cm . The ablation protocol employed a spot diam-

and the rutile was assumed to be stoichiometric with a calculated eter of 25 ␮m at 10 Hz repetition rate for 30 s. Helium was used as

294 C. Liu et al. / Precambrian Research 254 (2014) 290–305

Fig. 4. Classiﬁcation for samples of the Huade Group after Herron (1988) using log(Fe2O3/K2O) vs. log(SiO2/Al2O3).

carrier gas to efﬁciently transport aerosol to the MC-ICP-MS. Zircon geochemistry (McLennan et al., 1993). However, a large number

GJ-1 was used as the external standard while U–Pb raw data were of geochemical studies have revealed that high ﬁeld strength ele-

corrected ofﬂine using ICPMSDataCal 8.3 (Liu et al., 2010). More ments (HFSEs) and rare earth elements (REEs) are reliable to be used

detailed instrumental setting and analytical procedures have been as provenance indicators for low-grade metasedimentary rocks

described by Hou et al. (2009). Concordia diagrams and binned fre- (Winchester and Floyd, 1977; Taylor et al., 1986; Tran et al., 2003;

quency histograms were generated using the Isoplot 3.23 program Wang and Zhou, 2012). Therefore, in this study, HFSEs and REEs

(Ludwig, 2003) and the results were reported with 1 errors. In the rather than major and other trace elements will be used for inter-

data interpretation, zircon ages with 70–105% concordance were pretation to minimize possible chemical alteration.

thought to be reliable. Geochemical compositions of the analyzed metasedimentary

Zircon Hf analyses were also ﬁnished at MRL Key Labora- samples from the Huade Group are listed in Supplementary Table

tory of Metallogeny and Mineral Assessment, Institute of Mineral 1. The meta-siltstone samples as a whole are relatively immature,

Resources, Chinese Academy of Geological Sciences, Beijing, using which is reﬂected by relatively low SiO2 contents (61.3% and 55.6%),

the method of Hou et al. (2007). Analyses were measured in situ and high Al2O3 contents (10.3% and 16.0%), suggesting pelitic com-

with the laser-ablation system New-Wave UP-213 coupled with a positions (Supplementary Table 1). On the sediment classiﬁcation

Thermo-Finnigan Neptune MC-ICP-MS. All analyses used a beam diagram of Herron (1988), the meta-siltstone samples were plot-

diameter of 55 ␮m and energy density of 15–20 J/cm . Pleso- ted within the shale and arkose ﬁelds, respectively (Fig. 4). On the

176 177

vice standard zircon, with a recommended Hf/ Hf ratio of other hand, the meta-sandstone samples have higher and vari-

0.282482 ± 0.000013, was used as the reference standard (Slama able SiO2 contents (61.2–89.8%) and relatively low Al2O3 contents

et al., 2008). All the Hf isotope analysis results were reported with (2.6–20.2%), protoliths of which range from shale, wacke, arkose,

ε an error of 2 of the mean and values of Hf were calculated using Fe-sand, sublithrenite, to subarkose, possibly reﬂecting potassium

176 −11 −1

the decay constant for Lu of 1.865 × 10 year (Scherer et al., metasomatism (Fig. 4; Condie et al., 1992; Fedo et al., 1995).

2001). Depleted mantle model ages (TDM) were calculated based on Supplementary table related to this article can be found,

176 177

the measured Lu/ Hf ratios, referred to the depleted mantle in the online version, at http://dx.doi.org/10.1016/j.precamres.

176 177 176 177

with present-day Hf/ Hf = 0.28325 and Lu/ Hf = 0.0384 2014.09.011.

(Grifﬁn et al., 2000). Crustal model ages (Tc), assuming a mean Chondrite-normalized REE patterns are shown in Fig. 5 and

176 177

crustal value of Lu/ Hf = 0.015, were calculated for the source most of them are characterized by light REEs enrichment rela-

176 177

rock of the magma using the initial Hf/ Hf ratio of the zircon tive to heavy REEs (La/YbN = 5.5–19.8) and negative Eu anomalies

(Grifﬁn et al., 2004). (Eu/Eu* values = 0.48–0.74), similar to that of the upper continen-

tal crust (Taylor and McLennan, 1985). Furthermore, the lack of

chondrite-normalized negative Ce anomalies rules out signiﬁcant

4. Analytical results

hydrothermal alteration (Plank and Langmuir, 1998). It is also wor-

thy to note that the La/Yb ratios of samples 11HD16-1, 11HD16-2

4.1. Whole-rock geochemistry N

and 11HD35-1 are 2.9, 3.3 and 1.7, respectively, suggesting higher

inputs of maﬁc sources than in other samples (Bhatia, 1985).

As mentioned above, most of the metasedimentary rocks in

For trace elements, the Huade samples are characterized by

the Huade Group have experienced subgreenschist-facies meta-

variable contents of Th (1.5–20.8 ppm), Sc (1.9–25.2 ppm), Zr

morphism (Li et al., 2005; Hu et al., 2009), and it is very possible

(31–414 ppm) and Co (0.1–38.6 ppm). Compared with the post-

that whole-rock geochemical compositions, especially major ele-

Archean Australian shale (PAAS; Taylor and McLennan, 1985), the

ments, have been affected by solid state diffusion or mobilizing

metasedimentary samples show little negative anomalies in CaO,

elements in a ﬂuid phase (Taylor et al., 1986; Tran et al., 2003). Fur-

Na O and Sr, likely reﬂecting minimal dissolution of plagioclase

thermore, the complex processes involved in chemical weathering, 2

(Fig. 6; Mader and Neubauer, 2004). In addition, most of the Huade

mechanical breakdown, and continued chemical alteration during

samples have high La/Sc, Th/Sc and La/Co ratios with the exception

transport, burial, and diagenesis may also change the whole-rock

C. Liu et al. / Precambrian Research 254 (2014) 290–305 295

Fig. 5. Chondrite-normalized REE pattern for samples of the Huade Group. Normalizing values after Boynton (1984). The dotted line corresponds to the PAAS (Post Archean

Australian Shale; Taylor and McLennan, 1985).

of Samples 11HD06-1, 11HD16-1 and 11HD16-2, suggesting more Rutiles in the samples 11HD16-1 and 11HD16-2 from the Sanx-

maﬁc sources than other samples (Supplementary Table 1; Cullers, iatian Formations have relatively narrow range of geochemical

2000). compositions of Cr (103–595 ppm), Nb (1419–5656 ppm) and Zr

(291–3293 ppm), whereas rutiles from Sample 11HD31-1 of the

Hujiertu Formation display relatively wide range of geochemical

4.2. Rutile geochemistry compositions of Cr (629–5353 ppm), Nb (607–4143 ppm) and Zr

(482–17995 ppm). In the Nb vs. Cr diagram (Meinhold et al., 2008),

The analyzed rutiles from the Huade Group vary in size from 40 rutile geochemical data indicated a mixed source for the Hujierte

␮

to 300 m and are yellowish to reddish-brown in color. The results Formation and single metapelitic sources for the Sanxiatian Forma-

of 178 single LA-ICP-MS spot measurements are summarized in tion (Fig. 7a–c).

Supplementary Table 2. Results of Zr-in-rutile thermometry are showed as binned

Supplementary table related to this article can be found, histograms in Fig. 7d–f. It is worthy to note that application of Zr-in-

in the online version, at http://dx.doi.org/10.1016/j.precamres. rutile thermometry to detrital zircons is based on the assumption

2014.09.011. of excess ZrO2 and SiO2 in meta-pelites (Zack et al., 2004). In this

Fig. 6. Upper continental crust-normalized selected major and trace element abundance for samples of the Huade Group. Normalizing values after Taylor and McLennan

(1985). The dotted line corresponds to the PAAS (Post Archean Australian Shale; Taylor and McLennan, 1985).

296 C. Liu et al. / Precambrian Research 254 (2014) 290–305

Fig. 7. Relative abundance of metamaﬁc and metapelitic rutiles (a–c) and rutile formation temperatures (d–f) for samples of the Huade Group. Discrimination of metamaﬁc

and metapelitic rutile is based on Meinhold et al. (2008). Temperatures were calculated using the Watson et al. (2006) formula.

◦

study, calculated temperatures are between ca. 715 and 1040 C of 2865 Ma, nearly all the grains lie within the age range between

◦

(TZ) and ca. 640–890 C (Tw), respectively (Fig. 7d–f). In general, 2639 and 1855 Ma. Within the major age range, there is a major age

TZ gives a wider range and higher formation temperatures than peak at ∼1895 Ma and a subordinate age peak at ∼2520 Ma, which

TW, except for grains with <74 ppm Zr contents (Watson et al., are deﬁned by 29 and 23 zircon ages, respectively (Fig. 9a).

2006). However, both of TZ and Tw show a change toward “hotter” Supplementary table related to this article can be found,

rutiles from the Sanxiatian to the Hujiertu Formation (Fig. 7d–f). in the online version, at http://dx.doi.org/10.1016/j.precamres.

Furthermore, very ﬁne zircon inclusions in rutile may cause ele- 2014.09.011.

vated Zr contents and calculated temperatures (Zack et al., 2004).

High Zr concentrations in our rutiles are not accompanied by high

4.3.2. Gejiaying Formation

Si contents, we therefore interpret the high temperatures calcu-

Sample 11HD01-2 is quartzite collected from the lower succes-

lated for these grains as real formation temperatures and not due

sion of the Gejiaying Formation (Fig. 3). Zircons are variable in size

to zircon inclusions.

and shape ranging from small (80 ␮m) round to large (200 ␮m)

prismatic grains (Fig. 8e–h). From a total of 80 analyses, two

4.3. U–Pb zircon ages

discordant analyses are excluded for the further discussion (Sup-

plementary Table 3). Of the remaining 78 zircon ages, except one

U–Pb zircon ages of ﬁve meta-sandstones and one meta-

grain with an older age of 2651 Ma, all others yielded concordant

siltstone collected from the four formations of the Huade Group

ages ranging from 2587 to 1857 Ma with a major peak at ∼1960 Ma

were studied. All analytical data are presented in Supplementary

and a minor peak at ∼2550 Ma, which are deﬁned by 45 and 14

Table 3 and detrital zircon ages with concordance of 70–105%

zircon ages, respectively (Fig. 9b).

are thought to be reliable and accepted for binned frequency his-

Sample 11HD07-1 is ﬁned-grained quartzite from the middle

207 206

tograms and ε vs. Pb/ Pb age diagrams.

Hf succession of the Gejiaying Formation (Fig. 3). Zircons range in

length from 100 to 200 ␮m and most of them show banded or

4.3.1. Maohuqing Formation oscillatory zoning structures (Fig. 8i–l). A total of 80 analyses were

Sample 11HD10-1 is quartz schist from the upper succes- performed and all of them gave reliable ages (Supplementary Table

sion of the Maohuqing Formation (Fig. 3). Zircons have relatively 3). The binned frequency histogram of these analyses shows that

␮

small sizes (50–100 m) and subrounded to well-rounded shapes most grains lie within the age range of 2698 and 1847 Ma with the

(Fig. 8a–d). A total of 80 analyses yielded 75 usable ages (Supple- exception of two older grain with ages of 2740 and 2855 Ma. Within

mentary Table 3). With the exception of one older grain with the age the age range, there is one major age peak at ∼1880 Ma and a minor

C. Liu et al. / Precambrian Research 254 (2014) 290–305 297

207 206

Fig. 8. Representative selection of cathodoluminescence (CL) zircon images. Circles (55 and 25 ␮m) show positions of Hf and U–Pb analytical sites. Pb/ Pb and εHf(t)

values are also plotted. The scale bar is 100 ␮m long.

age peak at ∼2540 Ma, which include 42 and 11 analytical results, range between 2618 and 1510 Ma. Inspection of the histogram

respectively (Fig. 9c). shows there is a major peak at ∼1890 Ma (18 grains), with one

shoulder at ∼2530 Ma (16 grains) and one minor peak at ∼1780 Ma

4.3.3. Sanxiatian Formation (13 grains; Fig. 9d). The youngest age peak formed by two grains

Sample 11HD06-1, a ﬁne-grained sericite quartzite, was col- yielded the weighted average age of 1333 17 Ma (MSWD = 0.74).

lected from the lower succession of the Sanxiatian Formation. Sample 11HD16-1 is a ﬁne-grained quartz schist collected from

Generally, smaller zircons (∼30 ␮m) are round and larger zircons the middle succession of the Sanxiatian Formation (Fig. 3). Zircons

∼

( 100 ␮m) are elongate or prismatic in this sample (Fig. 8m–p). are not plentiful in the heavy mineral fraction and have relatively

␮

From a total of 80 analyses, one discordant analysis was excluded small size and round shape (<80 m; Fig. 8q–t), implying long-

(Supplementary Table 3). Of the remaining 79 zircon grains, except distance transport. A total of 80 analyses yielded 70 usable ages

four older grains with ages of 3102–2714 Ma and ﬁve younger (Supplementary Table 3). The age histogram of this sample is dif-

grains with age of 1444–1328 Ma, most grains lie within the age ferent from other samples from the Huade Group, with most zircon

298 C. Liu et al. / Precambrian Research 254 (2014) 290–305

Fig. 9. Binned frequency histograms of detrital zircons for metasedimentary samples from the Huade Group. Plots are arranged with the oldest unit at the left bottom and

the youngest unit at the right top.

grains showing ages between 1643 and 1451 Ma and a major age 4.4. Zircon Hf isotopes

peak of ∼1500 Ma deﬁned by 58 analytical results (Fig. 9e). The

youngest age peak formed by three grains yielded the weighted From ﬁve meta-sandstone samples (11HD01-2, 11HD06-1,

average age of 1368 ± 31 Ma (MSWD = 0.069). 11HD07-1, 11HD16-1, 11HD31-1) and one meta-siltstone sam-

ple (11HD10-1), zircons with 70–105% concordance U–Pb ages

were chosen for Hf isotopic analyses. The analyzed zircons with

176 177

4.3.4. Hujiertu Formation Yb/ Hf ratios more than 0.15 and display positive linear rela-

176 177 176 177

Sample 11HD31-1 is a sericite quartz schist from the lower suc- tionship between Yb/ Hf and Hf/ Hf ratios are excluded

cession of the Hujiertu Formation (Fig. 3). A total of 80 spot analyses for further calculation and discussion and other results are listed

were measured in this sample and nearly all of them are concordant in Supplementary Table 4 and presented in Fig. 10 on the Hf vs.

207 206

or nearly concordant (Supplementary Table 3). Fig. 9f shows the Pb/ Pb age plots.

binned frequency histogram for 78 of all the analyses, all between Supplementary table related to this article can be found,

70% and 105% concordant. With the exception of eight older grains in the online version, at http://dx.doi.org/10.1016/j.precamres.

with ages between 2573 and 2051 Ma, most grains scatter within 2014.09.011.

the age range of 1917 and 1222 Ma. Within the age range, the major An older age population (2690–2458 Ma) deﬁned by zircons in

age peak of ∼1490 Ma is deﬁned by 16 zircon ages (Fig. 9f). The Samples 11HD01-2, 11HD07-1 and 11HD10-1 from the lower part

youngest zircon identiﬁed in this sample is grain 15 that yields of the Huade Group, predominantly exhibit a range of Hf values

−

an age of 1222 ± 13 Ma with concordance of 92% (Supplementary from 3.9 to +8.7 (Fig. 10a–c) and Tc model ages of 2.45–3.37 Ga,

Table 3), whereas the youngest age peak formed by nine zircons suggesting reworking of an older crust and juvenile crustal addi-

gives the weighted average age of 1337 ± 7 Ma (MSWD = 0.22). tions. A younger population (2171–1770 Ma) of these three samples

C. Liu et al. / Precambrian Research 254 (2014) 290–305 299

207 206

Fig. 10. Plots of εHf (t) vs. Pb/ Pb ages of detrital zircons for metasedimentary samples from the Huade Group. CHUR, chondrite uniform reservoir; DM, depleted mantle.

ε −

plots within a relatively wide range of Hf values from 7.8 to the upper continental crust and low La/Sc, Th/Sc and La/Co ratios,

+8.3, with Tc model ages of 2.14–3.22 Ga, indicative of a mixing suggesting signiﬁcant inputs of maﬁc components (Cullers, 2000).

of the older crust with juvenile materials (Fig. 10a–c). Zircons U–Pb ages of detrital zircons from the metasedimentary rocks

from Sample 11HD06-1 display two age populations (2650–2458 of the Huade Group place more constraints on their source rocks.

and 2158–1750 Ma) similar to samples from the lower part of the From a K–S test (Press et al., 1988) for detrital zircon ages of sam-

Huade Group, with nearly the same range of Hf values and Tc ples in this study and data from Hu et al. (2009), P values are higher

model ages (Fig. 10d). Furthermore, for the younger population than 0.08 for sample pairs of 11HD06-1/06KB18, 06SD12/06SD01,

(1700–1305 Ma) in Sample 11HD06-1, most zircons possess pos- 11HD01-2/11HD07-1 and 11HD10-1/11HD01-2 because of the

ε ∼ ∼

itive Hf values, suggesting dominant inputs of juvenile crust with similar age peaks at 1.9 and 2.5 Ga, most likely suggesting statis-

limited reworking of an older crust (Fig. 10d). In Sample 11HD31- tically indistinguishable provenance. By contrast, when comparing

1, zircons with ages between 1932 and 1707 Ma exhibit similar Hf the detrital zircon ages of Samples 11HD16-1 and 11HD31-1 with

values to those of similarly ages zircons from the Maohuqing and the other samples, the calculated P values are near to 0. In Fig. 9e

Geijiaying Formations, whereas younger zircons of 1627–1297 Ma and f, one can see that the dominance of the ∼1.5 Ga detrital zir-

display similar Hf values to the youngest age population of Samples cons of the two samples from the upper two formations is the main

11HD06-1 (Fig. 10f). reason leading to the low values of P. Therefore, U–Pb ages of all

detrital zircons in this study are combined with data from Hu et al.

5. Interpretations and discussion (2009) based on the formation and displayed in binned frequency

histograms (Fig. 11), which provide more information about the

5.1. Provenance of the Huade Group source rocks.

Detrital zircons from the metasedimentary rocks of the Huade

Geochemically, most of the Huade sedimentary rocks have REE Group exhibit a major age range between 2690 and 2450 Ma,

∼

patterns similar to that of the upper continental crust, showing with a peak at 2520 Ma (Fig. 11). This age range is well consis-

light REEs enrichment relative to heavy REEs and negative Eu tent with the ages of the diorites and granitoids (2556–2520 Ma;

anomalies (Fig. 5; Taylor and McLennan, 1985). In addition, high Jian et al., 2005, 2012) and the metadacites in the Guyang com-

La/Sc, Th/Sc and La/Co ratios in these samples indicate that the plex (2516–2500 Ma; Chen, 2007), the orthopyroxene-bearing

major provenance of the Huade Group was composed of felsic TTG gneisses in the Wuchuan complex (2545–2507 Ma; Dong

to intermediate rocks (Cullers, 2000). However, two samples et al., 2012) and the orthogneisses of the Hongqiyingzi “Group”

(11HD16-1 and 11HD16-2) from the Sanxiatian Formation have (2535–2484 Ma; Liu et al., 2007) from the Yinshan Block. Available

depleted light REEs and slightly enriched heavy REEs compared to geochemical and geochronological data indicate that the episodic

300 C. Liu et al. / Precambrian Research 254 (2014) 290–305

A subordinate population of detrital zircons from the Huade

Group has an age range between 2150 and 1710 Ma, with a peak

at ∼1900 Ma (Fig. 11). The intermediate to felsic rocks with such

an age range, although volumetrically subordinate, are reported

in the adjacent Hongqiyingzi “Group”, represented by the granitic

mylonite gneisses, amphibole-biotite-quartz dioritic gneisses and

biotite monzonitic granitic gneisses (1871–1810 Ma; Liu et al.,

2007). In addition, in the adjacent Khondalite Belt, a large number of

similar aged Paleoproterozoic detrital zircons have been reported,

which have an age range from 2150 to 1830 Ma, with the peak at

∼1950 Ma (Wan et al., 2006; Xia et al., 2006a, 2006b; Yin et al.,

2011). These detrital zircons from the Khondalite Belt yielded Hf

− ε

values ranging from 7.9 to +9.7, which overlap with the Hf values

of these Paleoproterozoic detrital zircons from the Huade metased-

imentary samples (Fig. 10), suggesting that the subordinate part of

the group was derived from the erosion of the Paleoproterozoic

granites from the Hongqiyingzi “Group” and/or recycled from the

metasedimentary units from the Khondalite Belt.

On the other hand, relatively subordinate zircons with the ages

of 1660–1330 Ma (the peak at ∼1500 Ma; Figs. 9 and 11) from the

Sanxiatian and Hujiertu Formations of the Huade Group most likely

have been transported from exotic sources. As mentioned above, in

the Yan-Liao rift zone to the east, zircon ages of 1.68–1.62 Ga (Lu and

Li, 1991; Li et al., 1995; Lu et al., 2008; Gao et al., 2008a), ∼1.56 Ga

(Li et al., 2010), ∼1.44 Ga and ∼1.37 Ga of volcanic interlayers (Gao

et al., 2007, 2008b; Su et al., 2008, 2010) and 1.35–1.32 Ga diabase

sill (Zhang et al., 2009, 2012a; Li et al., 2009) have been reported

in the Changcheng, Jixian and Qingbaikou Groups. However, these

three groups are composed of dominantly metasedimentary rocks

and detrital zircons from them are characterized by a bimodal age

peaks of ∼2.5 and ∼1.8 Ga (Wan et al., 2003, 2011). Moreover, the

thickness and zircon fertility of the volcanic interlayers and dia-

base sill are both much less than those of the metasedimentary

rocks (Gao et al., 2008b; Zhang et al., 2009; Su et al., 2010). There-

fore, detrital zircons sourced from the Yan-Liao rift zone should

be characterized by two major age peaks of ∼2.5 and ∼1.8 Ga and

minor populations of 1.68–1.32 Ga, but this is not the case for the

upper part of the Huade Group (Figs. 9 and 11). Therefore, felsic

rocks from cratonic blocks connected to the northern margin of

the NCC in the Columbia supercontinent are candidate sources for

these early Mesoproterozoic detrital zircons from the upper Huade

Group. As already mentioned, the suggested adjacent craton to the

NCC ranges from the India (Zhao et al., 2002, 2004), through the

Baltica (Rogers and Santosh, 2009), to the North America (Hou et al.,

2008). In the Indian Craton, the 1480–1262 Ma alkaline complexes

have only been reported from the suture zone between the Bhan-

dara craton and the Eastern Ghats Belt and no lithologies or zircons

with the age of ∼1.5 Ga have been found (Upadhyay, 2008 and refer-

ences therein). Furthermore, detrital zircons from both the Eastern

Ghats Belt and the Chhattisgarh Basin within the Bastar Craton lack

the age peak of ∼1.5 Ga (Upadhyay et al., 2009; Bickford et al., 2011),

suggesting scarce supply of early Mesoproterozoic detritus from

the Indian Craton. Therefore, detrital zircons within the age range in

Fig. 11. Binned frequency histograms of detrital zircon ages from each formation the upper Huade Group were not likely derived from the Indian Cra-

of the Huade Group. Plots are arranged with the oldest unit at the bottom and the ton. On the other hand, the 1.5–1.4 Ga Telemark Group in the NW

youngest unit at the top. The patterned polygons depict the three major age ranges.

∼ ε

Baltica craton has a detrital zircon age peak at 1500 Ma, with Hf

values from −0.5 to +7.2 (Lamminen and Köykkä, 2010) and detri-

tal zircons from the Mississippi river in the North American craton

mantle melting and related crustal reworking led to the late are characterized by a 1.6–1.3 Ga age peak with Hf values from

Neoarchean thermotectonic events in the Yinshan Block (Jian et al., 0 to +5 (Iizuka et al., 2010). In addition, 1.65–1.50 Ga convergent

2012). Hf isotopic data of the major population of detrital zircons margin-related magmatism was widespread along the southern

(2690–2450 Ma) from the Huade Group suggest that the magmas and northwestern margins of the North American and Baltica cra-

that form these source rocks resulted from the mixing of a Meso- tons, respectively (Rivers, 1997; Bogdanova et al., 2008). Most early

Neoarchean crust with depleted mantle-derived magmas (Fig. 10), Mesoproterozic detrital zircons from the studied samples have Hf

consistent with a possible mantle plume tectonic setting in the values ranging between −1 and +10, which are broadly consistent

Guyang complex (Jian et al., 2012). with those of the similar-aged detrital zircons found in the North

C. Liu et al. / Precambrian Research 254 (2014) 290–305 301

American and Baltica cratons, suggesting that the minor part of the On the other hand, the Gejiaying and Sanxiatian Formations are cut

upper Huade Group was likely derived from the above two cra- by the A-type granites, which were dated at ∼1320 Ma (Zhang et al.,

tonic blocks connecting to the northern margin of the NCC in the 2012a; Shi et al., 2012). Taken together, the depositional age of the

Columbia supercontinent. upper Huade Group can be constrained in the period between ∼1.34

The chemistry and thermometry of detrital rutiles from and ∼1.32 Ga.

metasedimentary rocks of the Huade Group have also provided For the Maohuqing and Gejiaying Formations, the youngest zir-

important information about their source rocks. Rutile Cr–Nb sys- cons found in the studied samples gave similar ages of ∼1850 Ma.

tematic indicated a single input of metapelitic lithologies in the It is worthy to note that the youngest zircons from the Jixian and

Sanxiatian Formation and a mixed metamaﬁc and metapelitic Qingbaikou Groups in the Yan-Liao rift zone also yielded the similar

lithologies in the Hujiertu Formation (Fig. 7). The calculated youngest ages of ∼1820 Ma (Wan et al., 2003, 2011), whereas the

rutile formation temperatures (TW) range between ca. 640 and two groups were deposited after 1.6 Ga (Gao et al., 2007; Su et al.,

◦ ◦

740 C with a single 890 C rutile in the Sanxiatian Formation. 2008, 2010; Li et al., 2010). Such a phenomenon is consistent with

For the rutiles from the Hujiertu Formation, they gave tempera- the inferred intraplate and divergent plate tectonic setting for these

◦ ◦

tures between 680 and 760 C with two hotter grains at ∼900 C. sedimentary units, which usually lack inputs from contemporane-

Based on the detrital zircon age and Hf isotopic signatures, we ous igneous sources and show an age gap up to 500 Ma between

suggest the North American and/or Baltica cratons as their pos- depositional age and the youngest detrital zircon ages (Cawood

sible sources, so the amphibolite- and eclogite-facies rocks in et al., 2007). Therefore, a conservative constraint on the maximum

the Trans-Hudson Orogen (Hoffman, 1989), the Kola-Karelia Oro- depositional age of the lower Huade Group given by the youngest

gen (Bogdanova, 1999) or their age-equivalent orogens may be detrital zircons is ∼1850 Ma.

their sources. Another potential source could be the Khondalite

Belt, where amphibolite- and eclogites-facies rocks have been 5.3. Evolution of the Huade Group

reported (Zhao et al., 2005) and metamorphic rutiles from ultra-

high-temperature granulites gave similar results (Jiao et al., 2011). Generally, the Paleo-Mesoproterozic successions in the

Zhaertai–Bayan Obo–Huade and Yan-Liao rift zones on the

5.2. Depositional age of the Huade Group northern margin of the NCC were believed to be deposited in

continental rift zones related to the breakup of the Columbia

Depositional age of the Huade Group has not been well supercontinent (Zhai and Liu, 2003; Zhao et al., 2003; Lu et al.,

constrained because of the lack of volcanogenic interlayer and 2008). The continental rift interpretation has been supported by

radioactive diagenetic minerals. Based on the appearance of small the bimodal volcanism (Zhang et al., 2012a) and narrow zones of

shelly fossils in the upper part of the group, some researchers have thick sediment accumulation (Wang et al., 1992a). Depositional

suggested that the Huade Group was formed in early Paleozoic patterns in continental rift basin are affected by local sites of uplift

(Wang et al., 1992b; Chen, 1993). However, authenticity and geo- and erosion, sediment supply and transport, and accommodation

logical signiﬁcance of the fossils have been doubted or even denied space for deposition (Gawthorpe and Leeder, 2000; Lamminen and

by following studies (Li and Zhang, 1993; Zhang, 1994). Recently, Köykkä, 2010). In this section, a model based on the combination of

Zheng et al. (2004) and Li et al. (2005) suggested that the Huade provenance and lithostratigraphic data is presented to describe the

Group was deposited in the Paleoproterozoic based on their inter- evolution of the basin in which the Huade Group was deposited.

pretation that the 2.1–1.5 Ga monzogranites intrude the group. Evolution of the basin was initiated with syn-rift sedimenta-

However, due to the unclear contact relationship of the monzo- tion of the lower Maohuqing Formation, which was characterized

granites with the group, their suggestions on the depositional ages by coarse-grained delta sediments. Accelerated subsidence was

of the Huade Group may be questionable. recorded by the upper Maohuqing and Gejiaying coastal-shallow

Our U–Pb dating results of detrital zircons from different lithos- marine deposits, such as quartz schists and phyllites (Li et al., 2005).

tratigraphic units of the Huade Group place reliable constraints on Synchronously with rifting, the rift ﬂanks possibly underwent local

the maximum depositional ages of the group. In this study, 459 and transient uplift due to the increased sediment loads (Burov

detrital zircons from the four formations of the Huade Group were and Cloetingh, 1997), leading to the basal pebbly quartzite deposits

dated. The low greenschist-facies metamorphism of the group, rel- in the Gejiaying Formation. Detrital zircon data suggest that sed-

atively high Th/U ratios (0.1–3.5) and oscillatory zoning structures iments of the Maohuqing and Gejiaying Formations were derived

(Fig. 8) of the analyzed zircons suggests that their U–Th–Pb systems from the Neoarchean to Paleoproterozoic granitic rocks in the Yin-

remained closed after their deposition and the youngest detrital shan Block and recycled from the metasedimentary rocks of the

zircons ages could be used to constrain the maximum depositional Khondalite Belt close to the basin. This is also supported by the

times. whole-rock geochemistry because most samples from the lower

For the Sanxiatian Formation, the youngest group of detrital zir- Huade Group were plotted in or near to the passive margin area,

cons from Samples 11HD06-1 and 11HD16-1 yielded the weighted indicating craton-interior provenance (Fig. 12; Bhatia and Crook,

average ages of 1333 ± 17 Ma and 1368 ± 31 Ma, respectively, 1986).

which are consistent within analytical errors. For the overlying Subsequent deposition of the Sanxiatian schists, phyllites and

Hujiertu Formation, the youngest group of detrital zircons in Sam- minor slates suggests that the subsidence rate of the rift had

ple 11HD31-1 deﬁne a weighted average age of 1337 ± 7 Ma, older decreased, with the comeback of a coastal environment (Li et al.,

than the single-grained youngest age of 1222 ± 13 Ma. We favor 2005). Thermal subsidence became obvious again lately and

the age of ∼1337 Ma as a more reliable constraint on the maximum resulted in marine transgression and shallow-marine carbonate

depositional age of the Hujiertu Formation based on the following deposition in the Hujiertu Formation (Fig. 3). In this stage, asso-

considerations: (1) the youngest age peak of ∼1337 Ma was deﬁned ciated with extension leading to continental breakup and sea

by nine grains, which is in accordance with the criterion that the opening, drainage was established from other cratonic blocks (the

reliable youngest zircon age must belong to a signiﬁcant population Baltica or/and North American cratons), therefore extrabasinal or

composed of three or more grains (Andersen, 2005; Gehrels et al., long-traveled sediments were allowed to enter the basin. This

2006); (2) detrital zircons with the U–Pb age of ∼1220 Ma do not process is readily apparent from the zircon age pattern from the

occur in other studied samples, whereas ∼1337 Ma detrital zircons Sanxiatian and Hujiertu Formations, which are different from that

have also been found in the samples from the Sanxiatian Formation. of the underlying Maohuqing and Gejiaying Formations (Fig. 11).

302 C. Liu et al. / Precambrian Research 254 (2014) 290–305

Fig. 12. Tectonic discrimination diagrams for the studied samples of the Huade Group: (a) Th–Sc–Zr/10 diagram of Bhatia and Crook (1986) and (b) Ti/Zr vs. La/Sc tectonic

discrimination plots (Bhatia and Crook, 1986). OIA, oceanic island arc; CIA, continental island arc; ACM, active continental margin; PM, passvie continental margin.

This is also supported by the whole-rock geochemistry because probably sourced from the granitic rocks in the Yinshan Block.

most samples from the upper Huade Group were plotted into the The subordinate 2150–1710 Ma detrital zircons were probably

continental island arc or active continental margin areas, indicating derived from the erosion of the Paleoproterozoic granites of the

more inputs of magmatic arc products (Fig. 12; Bhatia and Crook, Honqiyingzi “Group” and/or recycled from the metasedimen-

1986). tary units from the Khondalite Belt. The youngest detrital zircon

age peak of ∼1850 Ma in the lower Huade Group indicates that

5.4. Implications for the breakup of the Columbia supercontinent it was deposited after this time.

(2) The metasedimentary rocks from the upper Huade Group have

As mentioned in the introduction, controversies still remain continental island arc or active continental margin geochem-

about the role of the NCC in the Columbia supercontinent. Firstly, ical signatures. Besides the age population of 2690–2450 and

position of the NCC varies in the different conﬁgurations of the 2150–1710 Ma, minor amounts of 1660–1330 Ma detrital zir-

Columbia supercontinent. Rogers and Santosh (2009) correlated cons in the upper Huade Group were likely derived from

the North Hebei Orogen with the Volhyn belt of Baltica, whereas the North American and/or Baltica cratons connecting to the

Hou et al. (2008) suggested the North Hebei Orogen as an Andean- northern margin of the NCC in the Columbia supercontinent.

type continental margin similar to the Wopmay Orogen of western The youngest age peak of ∼1337 Ma, in combination with the

Canada. On the other way, Zhao et al. (2002, 2004) correlated ∼1320 Ma granitoids intruding the Huade Group, indicates that

the 1.9–1.8 Ga active Trans-North China Orogen with the Central the depositional ages of the upper Huade Group can be con-

Indian Tectonic Zone. Secondly, it is generally believed that the NCC strained in the period between ∼1.34 and ∼1.32 Ga.

was not involved in the 1.3–1.2 Ga ﬁnal fragment of the Columbia (3) Detrital rutiles from the Huade Group are suggestive of dom-

supercontinent because middle Mesoproterozoic rift-related tec- inantly metapelitic rocks and peak metamorphic temperature

◦

tonic events were scarce (Rogers and Santosh, 2002; Hou et al., of 700–750 C.

2008). (4) Our new geochronological and geochemical data suggest that

Determination of depositional ages and provenance of the continental rift basin deposits represented by the upper Huade

Huade Group in this study places a rigorous constraint on the timing Group on the northern margin of the NCC developed between

∼

of the breakup of the NCC from the Columbia supercontinent and 1.34 and ∼1.32 Ga and received detritus from the North Amer-

its reconstruction. The existence of 1.35–1.31 Ga bimodal magmatic ica and/or Baltica, which indicate that the ﬁnal breakup of the

associations caused by continental rift in the northern NCC (Zhang NCC from the Columbia supercontinent happened in the middle

et al., 2009, 2012a; Shi et al., 2012), combined with the 1.34–1.32 Ga Mesoproterozoic.

upper Huade Group indicate that the breakup of the NCC from the

Columbia supercontinent was at middle Mesoproterozoic. These

ages are nearly synchronous with those of rift-related activities in Acknowledgments

other cratonic blocks such as North America and Baltica (Karlstrom

et al., 2001; Bogdanova et al., 2008), Greenland (Pearce and Leng, This research was ﬁnancially funded by the NSFC grants

1996; Upton et al., 2003) and Australia (Wingate et al., 2005). Fur- (41372195 and 41190075), Hong Kong RGC GRF grants (7060/12P

thermore, our data also suggest that the northern margin of the and 7063/13P), the Basic Outlay of Scientiﬁc Research Work from

NCC has received sediments from the North America and/or Baltica the Ministry of Science and Technology (No. J1218), and HKU Seed

in the middle Mesoproterozoic, which are also supported by the Funding Programme for Basic Research (201210159022). We thank

similar paleomagnetic poles of the NCC with the North America, Kejun Hou and Chunli Guo for their laboratory assistance. We are

Siberia and Baltica (Pei et al., 2006; Zhang et al., 2012b) during late also grateful for thoughtful and constructive reviews that signiﬁ-

Paleoproterozoic to early Mesoproterozoic, suggesting that these cantly improved the quality of this paper.

cratonic blocks joined together at ∼1.8 Ga and did not fragment until ∼1.38 Ga. References

6. Conclusions

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source rocks are felsic, displaying passive margin signa-

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