Content uploaded by Yican Liu
Author content
All content in this area was uploaded by Yican Liu on Oct 20, 2015
Content may be subject to copyright.
Available via license: CC BY-NC-ND 3.0
Content may be subject to copyright.
GSF REVIEW
Neoarchean (2.5e2.8 Ga) crustal growth of the North
China Craton revealed by zircon Hf isotope: A synthesis
Andong Wang*, Yican Liu
CAS Key Laboratory of Crust-Mantle Materials and Environments, School of Earth and Space Sciences, University of Science and
Technology of China, Hefei 230026, China
Received 31 July 2011; accepted 27 October 2011
Available online 16 December 2011
KEYWORDS
Zircon;
U-Pb dating;
Hf isotope;
Neoarchean crustal
growth;
North China Craton
Abstract The crustal growth of the North China Craton (NCC) during the Neoarchean time (2.5e2.8 Ga)
is a hotly controversial topic, with some proposing that the main crustal growth occurred in the late Neoarch-
ean (2.5e2.6 Ga), in agreement with the time of the magmatism, whereas others suggest that the main crustal
accretion took place during early Neoarchean time (2.7e2.8 Ga), consistent with the time of crustal-
formation of other cratons in the world. Zircon U-Pb ages and Hf isotope compositions can provide rigorous
constraints on the time of crustal growth and the evolution and tectonic division of the NCC. In this contri-
bution, we make a comprehensive review of zircon Hf isotope data in combination with zircon U-Pb geochro-
nology and some geochemistry data from various divisions of the NCC with an aim to constrain the
Neoarchean crustal growth of the NCC. The results suggest that both 2.7e2.8 Ga and 2.5e2.6 Ga crustal
growth are distributed over the NCC and the former is much wider than previously suggested. The Eastern
block is characterized by the main 2.7e2.8 Ga crustal growth with local new crustal-formation at
2.5e2.6 Ga, and the Yinshan block is characterized by w2.7 Ga crustal accretion as revealed by
Hf-isotope data of detrital zircons from the Zhaertai Group. Detrital zircon data of the Khondalite Belt indi-
cate that the main crustal growth period of the Western block is Paleoproterozoic involving some w2.6 Ga
and minor Early- to Middle-Archean crustal components, and the crustal accretion in the Trans-North China
Orogen (TNCO) has a wide age range from 2.5 Ga to 2.9 Ga with a notable regional discrepancy. Zircon Hf
isotope compositions, coupled with zircon ages and other geochemical data suggest that the southern margin
may not be an extension of the TNCO, and the evolution and tectonic division of the NCC is more complex
* Corresponding author. Tel.: þ86 551 3600367.
E-mail address: adw008@mail.ustc.edu.cn (A. Wang).
1674-9871 ª2011, China University of Geosciences (Beijing) and Peking
University. Production and hosting by Elsevier B.V. All rights reserved.
Peer-review under responsibility of China University of Geosciences
(Beijing).
doi:10.1016/j.gsf.2011.10.006
Production and hosting by Elsevier
available at www.sciencedirect.com
China University of Geosciences (Beijing)
GEOSCIENCE FRONTIERS
journal homepage: www.elsevier.com/locate/gsf
GEOSCIENCE FRONTIERS 3(2) (2012) 147e173
than previouslyproposed, probably involvingmulti-stage crustal growth and subduction processes. However,
there is no doubt that 2.7e2.8 Ga magmatism and crustal-formation are more widely distributed than previ-
ously considered, which is further supported by the data of zircons from Precambrian lower crustal rocks,
overlying sedimentary cover, modern river sediments and Late Neoarchean syenogranites.
ª2011, China University of Geosciences (Beijing) and Peking University. Production and hosting by Else-
vier B.V. All rights reserved.
1. Introduction
Up to now, at least three different models have been put forward to
depict the crustal growth and evolution history of the Earth. The
first is that the volume of continental crust has increased linearly
or progressively with time (Hurley and Rand, 1969; Moorbath,
1978), as evidenced by the present continental crust of various
ages. The second argues that most of the mass of present conti-
nents formed in the first billion years of the Earth’s history with
only minor subsequent growth (no growth model) (Armstrong,
1981), implying that the present crust might be remelting or
differentiation of the pre-existing ancient continental crust. In
contrast to these two models, in recent years voluminous in-situ
zircon U-Pb ages and radiogenic isotope model ages of granit-
oids and modern river sediments have shown several striking age-
peaks. This has led many geologists to argue for a third model in
which the continental crust has grown throughout geological time
with several pulses (Condie, 1998, 2000; Rion et al., 2004; Condie
et al., 2009; Condie and Aster, 2010; Iizuka et al., 2010; Kr€
oner,
2010; Safonova et al., 2010).
The North China Craton (NCC) is one of the oldest cratons in the
world and contains ancient crust remnants as old as 3.8 Ga in the
eastern part (Liu et al., 1992, 2007, 2008; Song et al., 1996; Zheng
et al., 2004a; Wu et al., 2005a,b, 2008a; Wilde et al., 2008; Wan
et al., 2009a; Nutman et al., 2009, 2011). In the past two decades,
numerous geochronology studies, especially in-situ zircon U-Pb
ages suggest that the most strongest tectono-thermal event in the
NCC occurred in w2.5 Ga (e.g., Guan et al., 2002; Zhao et al., 2002,
2008; Kr€
oner et al., 1998, 2005a,b; Wilde et al., 2004, 2005; Guo
et al., 2005; Shen et al., 2005; Geng et al., 2006, 2010, 2011; Liu
et al., 2009a,b, 2011a; Wang et al., 2010a, 2011; Zhang et al.,
2011a). Accordingly, some geologists have presumed that an
important continental crustal growth time for the NCC is w2.5 Ga,
which is different from that of the other cratons with a main peak at
w2.7 Ga (Windley, 1995; Gao et al., 2004; Wang et al., 2004; Geng
et al., 2010, 2011). However, published whole-rock Sm-Nd isotopic
data indicate that the major crustal growth in the NCC took place at
2.7e2.8 Ga (Wu et al., 2005b), and the w2.5 Ga crustal growth is
subdominant and may represent the remeling or differentiation of the
older crust formed at 2.7e2.8 Ga. In fact, in many cases whole-rock
Nd model ages cannot reflect the formation ages of extracting
juvenile crust from depleted mantle due to Sm-Nd mobility and
mixing or/and contamination of ancient crustal materials (Liu et al.,
2009b; Iizuka et al., 2010; Kr€
oner, 2010). For instance, in some cases
where mantle melt underplates the overlying continental lithosphere
and interacts with pre-existing older crustal materials before differ-
entiating further, marked decoupling between zircon and Nd model
ages may occur, depending on the age of crustal materials and the
degree of crust-mantle interaction. In this regard, the whole-rock Nd
model age no longer reflects the time of extraction of a melt from the
depleted mantle but merely represents a mean crustal residence age
(Arnde and Goldstein, 1987; Kr€
oner, 2010). In addition, zircon age-
peaks in age spectraare not equal to the periods of continental crustal
growth. Condie et al. (2009) found that the existing Nd and Hf
isotope database do not support widespread production of juvenile
continental crust during the Neoproterozoic (800e600 Ma) and
Greenvillian (1200e1000 Ma), which represent marked age-peaks
in zircon U-Pb age spectra. In contrast to other isotope systems,
the zircon Lu-Hf isotopic system has a relatively high closure
temperature and low Lu/Hf ratios, which makes zircon Lu-Hf
isotopic analyses an ideal and reliable method for investigating
early crustal growth in combination with zircon U-Pb ages and
other geochemical data (Amelin et al., 1999; Zheng et al., 2005; Liu
et al., 2009c; Iizuka et al., 2010; Jiang et al., 2010; Safonova et al.,
2010).
In the past several years, great achievements have been made in
the study of the NCC, one of which is the tectonic subdivision and
evolution of the craton (Zhao et al., 1999, 2000a,b, 2001, 2004,
2005, 2011; Zhai et al., 2000, 2010; Wilde et al., 2002; Kusky
and Li, 2003; Wang et al., 2004, 2010b; Zhai, 2004; Polat et al.,
2005; Faure et al., 2007; Kusky et al., 2007a,b; Li and Kusky,
2007; Trap et al., 2007, 2008, 2009a,b, 2011; Zhao, 2009; Wang,
2009; Santosh, 2010; Santosh et al., 2011; Zhai and Santosh,
2011; Zhang et al., 2011d). In terms of substantive structural,
geological, geochemical, geochronological and p-Tdata, the base-
ment of the NCC can be tectonically divided into two discrete
blocks named the Eastern block (EB, also called Yanliao block by
Santosh, 2010) and Western block (WB) that are separated by the
Paleoproterozoic Trans-North China Orogen (TNCO). Although
numerous investigations about the timing and tectonic processes of
the Paleoproterozoic amalgamation of the NCC have been made,
our knowledge of the pre-collision history of the EB and WB
remains poorly understood and controversial, especially in terms of
their crustal-formation ages and mechanisms (e.g., Wang et al.,
2004; Zhai, 2004; Zhao, 2009; Geng et al., 2010, 2011). Recently,
Wu et al. (2005b) reviewed whole-rock Nd isotopic compositions
and model ages of the EB and WB and TNCO and obtained many
important conclusions about the crustal-formation and tectonic
subdivision. However, at that time, zircon Hf isotope studies have
not been fully carried out (Zheng et al., 2004a, 2004b). From then
on, a large amount of zircon Hf analyses have been published and it
is opportune to review these data with an aim to better trace the
crustal growth and evolution of the NCC.
2. The reason to choose zircons
It is well known that zircon is a ubiquitous accessory mineral in
igneous, sedimentary and metamorphic rocks, and has high
mechanical stability and chemical resistance. Its ability to
concentrate U and exclude Pb provides the basis of U-Pb dating.
More importantly, zircon generally has a relatively high U-Pb
diffusion closure temperature and is an ideal mineral for
geochronology (Lee et al., 1997; Cherniak and Watson, 2000; Wu
and Zheng, 2004). Recently, Gard
es and Montel (2009) have
A. Wang, Y. Liu / Geoscience Frontiers 3(2) (2012) 147e173148
provided a new theoretical model for diffusive isotope loss that
assesses the opening and resetting of radiochronometers during
metamorphism of various minerals. The opening temperature
defines the beginning temperature of daughter isotope loss, and
the temperature at which the daughter isotope is completely lost is
the resetting temperature. Of all the evaluated minerals, zircon has
the highest opening temperature of >900 C depending on its
grain size, and the highest resetting temperature of about 1400 C.
All these merits make zircon an ideal and reliable mineral for
dating various thermal events, even for the extreme metamorphism
like ultrahigh-temperature (UHT) and ultrahigh pressure (UHP)
metamorphism (e.g., M€
oller et al., 2003; Hermann et al., 2001;
Santosh et al., 2009; Liu et al., 2011f). In addition to the
U-Th-Pb isotope system, zircon possesses another radiogenic
Lu-Hf isotope system, which is essential for depicting crustal
growth and evolution (Vervoort and Patchett, 1996; Griffin et al.,
1999; Vervoort and Blichert-Toft, 1999; Zheng et al., 2005, 2006).
The geochemical behavior of Hf is so similar to that of Zr that it is
easily concentrated and bound in the zircon crystal lattice,
whereas the REEs including Lu are far less compatible. Therefore,
zircons generally have very low Lu/Hf ratios (typically <0.001),
so that in-situ radiogenic Hf isotope growth is virtually negligible,
which is favorable for tracing crustal evolution and distinguishing
magmatism from metamorphism.
In addition, zircon also has many other advantageous aspects.
For example, empirical studies have established that oxygen
diffusion in zircon is sufficiently sluggish even through long-term
metamorphism and crustal fusion (King et al., 1998). Zircon has
high capacity to contain trace elements, and the trace elements in
igneous zircon including contents and ratios can be used to indi-
cate the composition and crystallization environment of the
magma from which they crystallized (Belousova et al., 2002).
Thus, both isotopes and trace elements can provide rigorous
constraints on the magmatic zircon evolution from mantle-derived
precursors or from mixed juvenile and recycled sources (Bibikova,
2003; Hawkesworth and Kemp, 2006; Zheng et al., 2006; Wilde
et al., 2008; Liu et al., 2009c).
Regarding the Hf analytical technique, in the past few years
following by pioneering studies by Griffin et al. (1999, 2002),
analysis of Hf isotopes in zircon by laser ablation has become
almost mature, although the technique is still undergoing refine-
ment (Woodhead et al., 2004; Hawkesworth and Kemp, 2006).
The interference correction and ablation effects during zircon Hf
isotope analyses are well understood. Another problem is to
concern the stability and closure temperature of the Lu-Hf isotope
system when using Hf isotope data to explain zircon genesis and
crustal evolution. Voluminous investigations indicate that the
zircon Lu-Hf isotope system has high stability, and it may be
higher than zircon U-Pb isotope system (e.g., Zheng et al., 2005,
2007; Wan et al., 2009b). It has been confirmed by other nature
researches and experimental data. For instance, for granite
samples showing a single magmatic zircon age-group, no rela-
tionship between the Hf isotope composition and the degree of
discordance on U-Pb concordia diagrams is observed, where the
discordance of zircon ages is probably ascribed to radiogenic Pb
loss (Hawkesworth and Kemp, 2006). Experimental measure-
ments on cation diffusivity in zircon also indicate that Hf diffuses
much more slowly than Pb and HREE but a little faster than U and
Th (Cherniak and Watson, 2003). Thus the zircon Hf isotope
composition is more refractory to metamorphic resetting by
diffusion than zircon U-Pb isotope compositions, and meta-
morphically recrystallized zircon is still capable of faithfully
recording its protolith Hf isotope composition (Zheng et al.,
2005). Therefore, although the metamorphic effect on zircon Hf
isotope is complex, especially for metamorphic zircon over-
growths that formed in response to younger metamorphic episodes
due to their very different Hf isotope ratios, the zircon Lu-Hf
isotope system is still an important tool in constraining the nature
and timing of metamorphism and trace crustal growth and
evolution (Vervoort and Patchett, 1996; Vervoort and Blichert-
Toft, 1999; Wu et al., 2008b).
How to define “juvenile crust”, “reworked crust” and “crustal
growth” is difficult (Zheng et al., 2005; Belousova et al., 2010;
Diwu et al., 2010). It is reasonable to define “juvenile crust” is
that magmas forming the crust were generated directly from
depleted mantle, and that “reworked crust” represents the
remelting of ancient crust. However, when the time interval
between the formation and remelting is short (instant reworking),
the model age is most probably regarded as the timing of the
corresponding crustal growth. Thus, the model ages of both
juvenile crust and instant reworked crust can be considered as the
timing of crustal growth. Belousova et al. (2010) defined that
“zircons possessing ε
Hf
0.75 times of the Hf of the depleted
mantle curve, which is equivalent to 75% of the MORB range”,
can be deciphered as “juvenile crust” or “crustal growth”. Thus,
this method is considered to be a reasonable and practical
approach to deal with Hf isotope data when applying zircon Hf
isotope data to trace crustal growth.
In this contribution, we firstly introduce the geological setting
of the NCC, then compile zircon Hf isotope data from the base-
ment rocks, and finally discuss the crustal growth and evolution of
the NCC, and provide some constraints on the tectonic subdivision
of the NCC. Recently, Wan et al. (2011a,b) have compiled a total
of 7586 zircon ages from basement rocks over the entire NCC and
have made a comprehensive review about the zircon ages and
geochemistry of late Neoarchean syenogranites in the NCC.
Zhang et al. (2011a) have comprehensively reviewed U-Pb
geochronology and Hf isotope of zircons from granulite xenoliths
entrained in Phanerozoic magmatic rocks and inherited xenocrysts
from associated lower crust rocks from both the EB and Hannuoba
region in the TNCO. All these data provide us with invaluable
information to better understand the crustal growth and evolution
of the NCC.
3. Geological background
The NCC refers to the Chinese part of the Sino-Korean Craton. It
is the oldest and largest known craton in China and contains
ancient crustal relicts as old as 3.6e3.8 Ga (e.g., Liu et al., 1992;
Song et al., 1996; Zheng et al., 2004a; Wu et al., 2005a,b, 2008a;
Nutman et al., 2009, 2011; Wilde et al., 2008; Wan et al., 2009a)
with an area of about 1,500,000 km
2
. The craton is bounded to the
west and north by Early Paleozoic Qilianshan Orogen and the Late
Paleozoic TianshaneXing’aneMongolian Orogen, respectively,
and is separated from the Yangtze Craton in the south by the
Qinling-Dabie-Su-Lu UHP metamorphic belt.
Traditionally, the NCC was considered as to be composed of
a uniform ArcheanePaleoproterozoic crystalline basement, over-
lain by younger cover (Huang, 1977). However, in the past decade,
extensive lithological, structural, geochronological and geochem-
ical investigations have led to a three-fold tectonic division of the
NCC (Zhao et al., 1998, 1999, 2000a,b, 2001; Kusky and Li, 2003;
Polat et al., 2005; Li and Kusky, 2007; Santosh, 2010; Kusky,
A. Wang, Y. Liu / Geoscience Frontiers 3(2) (2012) 147e173 149
2011; Santosh et al., 2011). Specifically, the NCC can be tecton-
ically divided into two discrete Eastern and Western blocks (EB
and WB) and the intervening Paleoproterozoic Trans-North China
Orogen (TNCO). The Archean basement rocks of the EB and WB
are characterized by anticlockwise p-Tpaths involving isobaric
cooling (IBC) with metamorphism occurring at w2.5 Ga, whereas
the Archean to Paleoproterozoic basement rocks from the TNCO
are characterized by clockwise p-Tpaths involving near-
isothermal decompression (ITD) with metamorphism taking
place at w1.85 Ga. Additional data collected from the whole
craton have led to further tectonic division of the WB into the
Yinshan block in the north and the Ordos block in the south
separated by the Paleoproterozoic Khondalite Belt (also called the
Inner Mongolia Suture Zone (IMSZ) by Santosh, 2010)(Zhao
et al., 2005, 2010a, 2011; Zhao, 2009). The metamorphic evolu-
tion of the Khondalite Belt is also characterized by clockwise p-T
paths involving near-isothermal decompression with the meta-
morphic age of 1.92e1.95 Ga, a little earlier than the timing of
collision between the EB and WB (Zhao et al., 2005, 2010a,
2010b, 2011; Zhao, 2009; Santosh et al., 2006, 2007, 2009,
2011; Yin et al., 2009, 2011; Wan et al., 2006a, 2009b; Li et al.,
2011a; Liu et al., 2011e). Voluminous studies for the Jiao-Liao-
Ji Belt suggest that this belt divides the EB into the Longgang
block in the north and the Nangrim block in the south (Faure et al.,
2004; Luo et al., 2004, 2006, 2008; Lu et al., 2004, 2006; Li et al.,
2005, 2006, 2007, 2011b; Zhou et al., 2008; Tam et al., 2011a,b;
Zhao et al., 2011). Thus, the Archean to Palaeoproterozoic base-
ment of the NCC consists of four micro-continental blocks (Yin-
shan block, Ordos block, Longgang block, Nangrim block) and
three Palaeoproterozoic orogenic belts (Khondalite Belt, Jiao-Liao-
Ji Belt, Trans-North China Orogen) (Fig. 1,Zhao et al., 2005,
2011). It is noteworthy that other models have been put forward
to explain the evolution and tectonic subdivision of the NCC
involving different collisional ages/stages and subduction polarities
(Zhai et al., 2000, 2010; Kusky and Li, 2003; Faure et al., 2004;
Wang et al., 2004, 2010a,b; Zhai, 2004; Polat et al., 2005; Kusky
et al., 2007a,b; Li and Kusky, 2007; Trap et al., 2007, 2008,
2009a,b, 2011; Wang, 2009; Santosh, 2010; Santosh et al., 2011;
Zhai and Santosh, 2011). Following by the w1.85 Ga amalgam-
ation, the NCC underwent a series of extensional and rifting events
in its interior and margins during the time of 1.85e1.6 Ga, forming
aulacogens and marginal rift basins with the emplacement of
mafic-ultramafic dyke swarms, anorthositeegabbroemangeritee
rapakivi granites (AGMR) and A-type granites, and eruption of
super-high potassium volcanic rocks (e.g., Halls et al., 2000; Zhai
et al., 2000; Lu et al., 2002, 2008; Peng et al., 2008; Zhang et al.,
2007; Hou et al., 2008; Wang et al., 2008; He et al., 2009; Zhao
et al., 2009; Peng 2010; Piper et al., 2011; and references therein).
The EB comprises the domains of eastern Hebei, Miyune
Chengde, western Liaoning, AnshaneBenxi, south Liaoning,
Figure 1 Tectonic subdivision of the North China Craton (after Zhao et al., 2005). Abbreviations of metamorphic complexes: CDdChengde;
DFdDengfeng; EHdeastern Hebei; ESdeastern Shandong; GYdGuyang; HAdHuai’an; HLdHelanshan; JNdJining; LLdL€
uliang;
MYdMiyun; NHdnorthern Hebei; NLdnorthern Liaoling; QLdQianlishan; SJdsouthern Jilin; SLdsouthern Liaoning; THdTaihua;
WDdWulashaneDaqingshan; WLdwestern Liaoning; WSdwestern Shandong; WTdWutai; XHdXuanhua; ZHdZanhuang;
ZTdZhongtiao.
A. Wang, Y. Liu / Geoscience Frontiers 3(2) (2012) 147e173150
south Jilin, western Shandong and eastern Shandong (Zhao et al.,
1998). The basement rocks of the EB are mainly dominated by
a Late Archean lithological assemblage, with minor Early- to
Middle-Archean rocks with ages being from 3.3 Ga to 3.8 Ga
(Jahn et al., 1987, 1988; Liu et al., 1992; Song et al., 1996; Wan
et al., 2009a; Nutman et al., 2009, 2011). The Late Archean
basement rocks include 2.6e2.5 Ga TTG gneisses, mafic to
ultramafic igneous intrusives and dykes, and w2.5 Ga syntectonic
charnockites and granites with minor w2.5 Ga supracrustal rocks
(Kr€
oner et al., 1998; Zhao et al., 1998). All of them suffered
greenschist to granulite-facies metamorphism at 2.48e2.50 Ga
with anticlockwise IBC-type p-Tpaths (Wu et al., 2011). The
Palaeoproterozoic Jiao-Liao-Ji Belt is located in the eastern
margin of the EB, and consists of greenschist to lower amphibolite
facies sedimentary and volcanic succession associated with some
granites and mafic intrusions. The Jiao-Liao-Ji Belt is character-
ized by paired metamorphic zones and can be further divided into
the northwestern zone of the North Liaohe, Laoling and Fenzishan
Groups that have undergone medium-pressure-type clockwise p-T
paths and the southeastern zone of the south Liaohe, Ji’an and
Jingshan Groups that is characterized by low-pressure-type anti-
clockwise p-Tpaths (Zhao et al., 2005; 2011; Luo et al., 2008;
Zhao, 2009; Li et al., 2011b). The tectonic nature of the Jiao-
Liao-Ji Belt is controversial and different models have been
proposed including intra-continental rifting, arc-continent or
continentecontinent collision, and rift-and-collision (Faure et al.,
2004; Luo et al., 2004, 2006, 2008; Li et al., 2005, 2006, 2007,
2011b; Lu et al., 2006; Li and Zhao, 2007; Zhou et al., 2008; Tam
et al., 2011a, 2011b; Zhao et al., 2011). More intergraded work is
clearly required in the future.
The TNCO contains the Defeng, Fuping, Hengshan, Huai’an,
L€
uliang, Wutai, Zanhuang, Taihua, north Hebei and Zhongtiao
domains and is separated from the EB and WB by major faults. It is
composed dominantly of Late Archean to Paleoproterozoic base-
ment rocks metamorphosed from greenschist to granulite facies. On
the basis of lithology and metamorphic grade, Zhao et al. (2000a,b)
grouped the basement rocks into low-grade graniteegreenstone
belts containing the Dengfeng, L€
uliang, Zhongtiao, Wutai and
Zanhuang domains and high-grade gneisses including Taihua,
Hengshan, Fuping and Huai’an domains. Emplacement of TTG and
granitic plutons and eruption of mafic to felsic volcanic rocks took
place mainly at 2.5e1.9 Ga with a main age-peak at w2.5 Ga and
a minor age-peak at w2.1 Ga (e.g., Wilde et al., 1997, 2004; Zhao
et al., 2000a,b, 2001, 2002, 2004, 2008; Guo et al., 2005; Kr€
oner
et al., 2005a,b, 2006). Metamorphism of the basement in the
TNCO, regardless of their protolith age, composition and meta-
morphic grade, is characteristically featured by clockwise ITD-type
clockwise p-Tpaths involving collision between the EB and WB
(Zhao et al., 2000a, 2010b; Xiao et al., 2010). Extensive geochro-
nological studies based on zircon SHRIMP U-Pb, mineral Ar-Ar
and Sm-Nd, and monazite U-Pb dating methods show that the
timing of the metamorphism for the TNCO happened at w1.85 Ga
(Guo and Zhai, 2001; Guo et al., 2005; Liu et al., 2006a; Wan et al.,
2006a,b; Wang et al., 2010a; Zhao et al., 2010b, 2011, and refer-
ences therein). It is noteworthy that w2.7 Ga and even older
basement components and zircon ages are more widely distributed
along the southern margin of the TNCO than in the middle and
northern segments of the TNCO (Kr€
oner et al., 1988; Gao et al.,
2005a; Yang, 2008; Liu et al., 2009c; Diwu et al., 2010; Huang
et al., 2010).
The WB is composed of the Ordos block in the south and the
Yinshan block in the north separated by the Palaeoproterozoic
EW-trending Khondalite Belt that extends from Helanshan and
Qianlishan in the west, through Daqingshan and Wulanshan in the
central, to Jining in the east (Zhao et al., 1999, 2005, 2011; Zhao,
2009; Santosh, 2010; Santosh et al., 2011; Li et al., 2011a). The
Ordos block is completely covered by the younger Ordos Basin
(Wu et al., 1986). The Yinshan block is dominated by late
Archean TTG gneisses and minor supracrustal rocks exposed in
the Guyang and Wuchuan domains. All of them were meta-
morphed to greenschist to granulite-facies grade at w2.5 Ga and
exhibit counter-clockwise IBC-type p-Tpaths (Zhao et al., 1999;
and references therein). The Khondalite Belt was formed by
collision between the Ordos and Yinshan blocks at 1.92e1.95 Ga
(Yin et al., 2009, 2011; Zhao, 2009; Zhao et al., 2005, 2011;
Santosh et al., 2006, 2007, 2009; Wan et al., 2006a, 2009a,b,c;
Dong et al., 2007, 2009; Li et al., 2011a), and its metamorphic
evolution is also characterized by clockwise ITD-type p-Tpaths
(Zhao et al., 1999, 2005, 2011). Besides, ultrahigh-temperature
(UHT) metamorphic rocks within the Khondalite Belt (also
named as the Inner Mongolia Suture Zone (IMSZ) by Santosh,
2010) has also been widely investigated by various authors (Guo
et al., 2006; Santosh et al., 2006, 2007, 2008, 2011; Liu et al.,
2010; Jiao and Guo, 2011; Jiao et al., 2011; Tsunogae et al.,
2011).
In recent years, many investigations of zircon U-Pb and Hf
isotope isotope from different blocks/domains have been con-
ducted to unveil the craton’s growth and evolution history. In
this contribution, we compile published data and review the
Neoarchean (2.8e2.5 Ga) crustal growth of the NCC. The
Neoarchean can be further subdivided into Early Neoarchean
(2.7e2.8 Ga) and late Neoarchean (2.5e2.6 Ga). Traditionally,
it has been proposed that the main crustal growth period was at
2.5e2.6 Ga, consistent with the timing of Late Neoarchean
magmatism; whereas another suggestion is that 2.7e2.8 Ga was
also an important time of NCC’s crustal growth. Available
zircon Hf isotope data can provide rigorous constraints on the
timing of crustal growth of the NCC. It is notable that we have
just compiled the data having coupled zircon U-Pb age and Hf
isotope analyses in the present study. At the same time, detrital/
inherited zircons with ages 2.7 Ga (age discordant <10%) and
Hf isotope model ages out the scope of the Neoarchean are also
mentioned.
4. Data sources
The basement of the NCC is mainly dominated by w2.5 Ga rock
series with minor Early- to Middle-Archean and Paleoproterozoic
rocks. Hf and Nd-isotope studies show that minor EB crustal
growth occurred in Early- to Middle-Archean and variable
proportions of Paleoproterozoic crustal growth occurred in both
the EB and WB and the TNCO. As this contribution concentrates
on the Neoarchean (2.8e2.5 Ga) crustal growth of the NCC, pre-
Neoarchean crustal growth is beyond of the scope of this study,
and detailed information about the growth of pre-Neoarchean
crust can be found in the relevant references (e.g., Jahn et al.,
1987, 2008;Liu et al., 1992, 2007, 2008; Song et al., 1996;
Wan et al., 2005, 2009a; Wu et al., 2005a,b, 2008a; Wilde
et al., 2008; Zheng et al., 2004a; Nutman et al., 2009, 2011;
Geng et al., 2010, 2011). In addition, some Nd-isotope data
have also been recently published (e.g., Wan et al., 2005; Wu
et al., 2005b; Chen et al., 2006a; Li et al., 2006, 2008; Liu
et al., 2006b;Jahn et al., 2008;Wang et al., 2009).
A. Wang, Y. Liu / Geoscience Frontiers 3(2) (2012) 147e173 151
Published Hf isotope data of each block are listed in Table 1.
Data for the WB are mainly from Xia et al. (2006a,b, 2008, 2009),
Dong et al. (2007, 2009),Li et al. (2007),Wan et al. (2009b), Yin
et al. (2011); that of the EB from Zheng et al. (2004a,b), Yang
et al. (2005, 2008), Luo et al. (2008); Du et al. (2010a); Jiang
et al. (2010); Li et al. (2010); Wan et al. (2010a, 2011b); Wang
et al. (2011); Zhang et al. (2011a,b); and that of the TNCO
from Chen et al. (2006b);Xia et al. (2006c);Diwu et al. (2007,
2008, 2010, 2011); Guo et al. (2008); Liu et al. (2009b,c,
2011b,c,d);Xu et al. (2009);Zhou et al. (2009a,b, 2011); Huang
et al. (2010); Jiang et al. (2010).
4.1. Western block
4.1.1. Khondalite Belt
Hf isotope data have only been reported from the Khondalite
Belt and from the Zhaertai Group within the Yinshan block. The
main features of the Hf isotope compositions are evaluated as
follows.
Xia et al. (2006a, 2008) have carried out detrital zircon U-Pb
and Hf and whole-rock Sr-Nd isotopic compositions of the
khondalites from the Jining complex in order to trace the crustal
growth of the WB. Detrital zircons were mainly derived from
1.9 Ga to 2.1 Ga Paleoproterozoic rocks. Sr-Nd-Hf isotopic data
suggest that 65%e75% juvenile materials from the depleted
mantle was accreted at 2.1 Ga with 25%e35% pre-existing
w2.6 Ga continental crustal contamination. No w2.7 Ga crustal
materials were found, but only one zircon has Hf model age of
2.71 Ga. The zircon age data are consistent with the new results of
Li et al. (2011a).
In-situ U-Pb and Hf isotopic study for detrital zircons from the
Wulashan khondalites shows that U-Pb ages have a wide range
from 1.84 Ga to 2.32 Ga with some sporadic Late Archean ages
and significant addition of juvenile materials took place
at w2.0 Ga. More importantly, the main crustal growth period was
at w2.6 Ga with a shoulder at w2.7 Ga (Xia et al., 2006b).
Therefore, the w2.6 Ga and w2.7 Ga crustal growths probably
represent two discrete stages rather than a continuous process
based on the following reasons: (1) the frequencies of w2.6 Ga
and w2.7 Ga Hf model ages are different, with the former being
much higher than the later. If they represent a continuous process
they should have the same frequencies; and (2) in zircon age
spectra, some zircon grains have ages of 2.5e2.6 Ga but no ages
of >2.7 Ga (Xia et al., 2006b). It is noted that zircon age and Hf
isotope data between different samples have some notable
differences, some zircon grains give Hf model ages of 2.7 Ga
whereas others do not. Thus, it is possible that the w2.7 Ga Hf
model ages may be underestimated.
Dong et al. (2009) and Wan et al. (2009b) reported zircon
U-Pb ages and Hf isotope data for detrital zircons in the
Daqingshan area of the Khondalite Belt and obtained results
similar to other areas in the Khondalite Belt. Specially, the source
of the detrital zircons was mainly derived from Paleoproterozoic
rocks with abundant 2.56e2.51 Ga rocks, and Hf isotope data
show that the crustal growth occurred in the Paleoproterozoic
with some 2.6e2.5 Ga juvenile mantle-derived materials being
accreted to crust involving minor Early- to Middle-Archean
crustal materials.
U-Pb and Hf isotopic analyses of zircons have been carried out
for the Helanshan complex by Dong et al., (2007) and Yin et al.
(2011). Magmatic-type detrital zircons reveal two distinct age-
groups: 2.85e2.53 Ga and 2.2e2.0 Ga. Corresponding Hf
isotope data indicate that 2.85e2.53 Ga zircons possess negative
ε
Hf
(t) values with depleted mantle model ages of 3.34e3.10 Ga,
whereas nearly all 2.2e2.0 Ga zircons have positive ε
Hf
(t) values
with depleted model ages of 2.45e2.15 Ga. Paleoproterozoic
crustal growth was therefore far more important than that of
PaleoeMesoarchaean (Yin et al., 2011). Dong et al. (2007) also
obtained the same result. Zircon Hf model ages of the nearby
Paleoproterozoic Bayanwula gneissic granite have w2.6 Ga age
peak, consistent with other areas within the Khondalite Belt (Dong
et al., 2007). However, Dan et al. (2011) gave an alternative
explanation.
Xia et al. (2009) proposed that the L€
uliang khondalites within
the L€
uliang complex were deposited along the eastern margin of
the WB, and were subsequently thrusted eastward during the
collision between the EB and WB, so they are different from other
supracrustal assemblage in the TNCO. Zircon U-Pb ages and Hf
isotope data support this conclusion and show that the dominant
provenance for detrital zircons of the khondalites were derived
from 1.9 Ga to 2.1 Ga rocks with minor Archean rocks (one zircon
with a Middle-Archean age and three zircon ages in the range of
2.5e2.6 Ga). Hf isotopic data indicate that w2.1 Ga is the main
crustal growth period with some w2.6 Ga crustal material
involving in the Paleoproterozoic magmatic event. The data from
the L€
uliang khondalites is similar to that of the Jining khondalites
(Fig. 3).
In summary, zircon U-Pb age and Hf isotope data of the
Khondalite Belt suggest that the main crustal growth time is the
Paleoproterozoic involving various degrees of w2.6 Ga crustal
material contamination. At the same time, sporadic w2.7 Ga and
Early- to Middle-Archean crustal materials are also locally found
in the detrital zircons in some regions, which is confirmed by
detrital zircon ages (Darby and Gehrels, 2006). A distinct differ-
ence between different areas of the Khondalite Belt is that they
have various source materials, i.e., some areas are dominated by
Paleoproterozoic crustal rocks with no Early Archean crustal
compositions but others by Paleoproterozoic crustal rocks with
minor Early Archean crustal materials. The amount of 2.5e2.6 Ga
crustal materials in different areas has different proportions. The
main crustal growth time took place in the Paleoproterozoic with
some w2.6 Ga and sporadic w2.7 Ga and Early- to Middle-
Archean crustal material (Fig. 3).
4.1.2. Yinshan block
In the Yinshan block, the published zircon ages and Nd-Hf
isotopic compositions of the Zhaertai Group suggest that Archean
basement rocks underlying this group have detrital zircon age
population of w2500 Ma, and the Hf model ages have a w2.7 Ga
peak with minor 3.8 Ga and 2.5 Ga crustal accretion (Li et al.,
2007). Thus, the main crustal growth in the region most likely
took place at w2.7 Ga (Fig. 3).
Additionally, indirect evidence on crustal growth periods can
be from Late Neoarchean high-Mg diorites. Jian et al. (2005)
proposed that high-Mg diorites at Guyang, Inner Mongolia, in
the Yinshan block have geochemical features similar to Archean
sanukite with SHRIMP zircon U-Pb age of w2.55 Ga. The two-
stage model has been widely used to explain the generation of
sanukitoid magmas (e.g., Smithise and Champion, 2000; Wang
et al., 2009). In the first stage, the mantle was metasomatised by
fluids/melts derived from the subducted slab and then the previ-
ously metasomatised mantle melted to generate the sanukitoid
magmas. Some sanukitoids in the Baltic Shield have Nd-isotope
A. Wang, Y. Liu / Geoscience Frontiers 3(2) (2012) 147e173152
Table 1 Zircon Hf isotope data from the basement and supracrustal rocks of the North China Craton.
Khondalite Belt
Locality Samples Zircon ages Hf isotope composition References
Jining. High-grade Al-rich gneisses
include a medium-grained
sillimanite-garnet-feldspar
gneiss, a sillimanite-garnet-
feldspar gneiss, a sillimanite-
garnet gneiss.
More than 200 detrital zircon
grains show three age
populations of 2060, 1940 and
1890 Ma without ages
>2500 Ma; metamorphic rims
with an age of w1811 Ma.
Hf model ages range from
2.08 Ga to 2.74 Ga with a peak at
2.24e2.40 Ga, most samples
formed by mixing of 65%e75%
2.1 Ga depleted mantle and
25%e35% w2.6 Ga crust.
Xia et al., 2006a;
Xia et al., 2008;
Li et al., 2011a
Wulashan. Two garnet-bearing metapelitic
gneisses, i.e., sillimanite-
garnet-biotite gneiss and
meta-quartzite.
Detrital zircons give U-Pb ages
of 1.84e2.32 Ga with a single
peak at w2.0 Ga.
Significant addition of juvenile
materials at w2.0 Ga with
voluminous w2.6 Ga ancient
crustal material remelting.
Xia et al., 2006b
Helanshan. Six fine- to medium-grained
garnet-sillimanite-cordierite
gneisses, a fine-grained garnet-
bearing quartzite, two S-type
granites.
Magmatic-type detrital zircons
reveal two age populations, one
in Archaean (2.85e2.53 Ga,
minor) and the other in
Paleoproterozoic (2.2e2.0 Ga,
main).
The main crustal growth events
were in the Paleoproterozoic
with contamination of
minor w2.60 Ga and
PaleoeMesoarchaean
(3.34e3.10 Ga) crustal
components.
Yin et al., 2011
Bayan Ul-Helanshan. A gneissic granite and a garnet-
mica two-feldspar gneiss.
Zircons from the gneissic granite
show core-mantle-rim structures
with magmatic core and
metamorphic mantle and rim
yielding ages of 2323, 1923,
1856 Ma. Detrital zircons from
garnet-mica two-feldspar gneiss
have a weighted mean age of
1978 Ma and a few older ages
(2469e2871 Ma).
T
DM1
of Hf isotope for the
gneissic granite have a range of
2455e2655 Ma, half of which
are in Paleoproterozoic and the
other in w2.6 Ga. T
DM1
of Hf
isotope for garnet-mica two-
feldspar gneiss have a wide range
of 1999e3047 Ma, most of
which are in the
Paleoproterozoic.
Dong et al., 2007
Daqingshan. Two samples from Sanggan
Group, five samples from
Wulashan Group and a quartzite
from Meidaizhao Group.
Four episodes of tectono-thermal
events occurred in 2.6e2.5,
2.45e2.37, 2.3e2.0 and
1.95e1.85 Ga.
Three episodes of juvenile,
depleted mantle-derived
materials were accreted to the
crust, i.e., 2.60e2.50, 2.37 and
2.06 Ga involving subtle ancient
crustal components.
Wan et al., 2009b;
Dong et al., 2009
Jiehekou Group in the L€
uliang
complex (Jinzhouyu area).
Three samples comprise a meta-
quartzose sandstone, a
sillimanite-bearing biotite gneiss
and a metamorphosed pebble-
bearing quartzose sandstone.
Detrital zircon ages of the three
samples show a provenance
dominated by 1.9e2.1 Ga rocks
with minor 2.5e2.6 Ga crustal
materials.
Hf isotope compositions suggest
that the main juvenile crustal
growth event took place at
2.1 Ga involving the remelting
of w2.6 Ga old crustal materials.
Xia et al., 2009
(continued on next page)
A. Wang, Y. Liu / Geoscience Frontiers 3(2) (2012) 147e173 153
Table 1 (continued)
Khondalite Belt
Locality Samples Zircon ages Hf isotope composition References
Yinshan block
Zhaertai Group (Inner
Mongolia).
Four sandstones, one migmatitic
granite and one basalt.
Forty-seven zircon grains from
four sandstones give ages
ranging from 2527 Ma to
2403 Ma with an age peak at
2500 Ma. The granite was
formed at 2564 Ma and
experienced migmatization at
2480 Ma. The basalt was
formed w1750 Ma with
xenocrystic zircons being from
2536 Ma to 2134 Ma.
T
DM1
(Hf) of the four sandstone
samples range from 2900 Ma to
2500 Ma, clustering at w2.7 Ga.
Two highly negative initial ε
Hf
values have model ages
of w3800 Ma.
Li et al., 2007
Trans-North China Orogen
Wanzi supracrustals within the
Fuping complex (Taihangshan
region).
Four sillimanite-bearing gneissic
samples.
Inherited igneous zircon cores
yield two age-groups at w2.10
Ga and w2.51 Ga with few ages
scattering between 2.5 and
2.9 Ga.
All w2.51 Ga ages with
positive initial ε
Hf
values
of þ1.4eþ10.9, indicating an
important crustal growth event
at w2.5 Ga with minor 2.8 Ga
ancient crustal components.
w2.1 Ga zircons are featured
by remelting of pre-existing old
crustal materials with minor
juvenile material contribution.
Xia et al., 2006c
Yejishan Group in the L€
uliang
complex in L€
uliangshan.
Four samples consist of a grey
black meta-siltstone, a pale red
feldspar-quartz sandstone, a grey
siltstone, and a feldspar-
quartz sandstone.
Detrital zircons have a wide age
range of 1.81e3.24 Ga with
dominant Paleoproterozoic ages.
Hf model ages have a main age
peak at w2.6 Ga with minor
older crustal components.
Liu et al., 2011d
Hutuo Group in the Wutai
complex in Wutaishan.
Ten samples include greywackes,
arenites, sublitharenites and
litharenites.
Detrital zircons have a wide age
range with two peaks at w2470
and w2150 Ma.
Hf model ages have a large rang
between 2.3 and 3.0 Ga with
age-peaks at w2.6 Ga involving
the remelting of >2.7 Ga older
crustal materials.
Zhang et al., 2006;
Liu et al., 2011c
Songshan Group in the Songshan
region, Henan Province.
Quartzite. Ninety-nine analyses for detrital
zircons yield four age-groups
at w3.40 Ga, 2.77e2.80
Ga, w2.50 Ga and 2.34 Ga.
The w2.50 Ga zircon grains
constitute w85% of the total
grain population.
2.77e2.80 Ga detrital zircons are
minor and their Hf isotope data
indicate they were derived from
coeval depleted mantle; most of
w2.50 Ga detrital zircons have
positive ε
Hf
values, suggesting
that they derived from
2.5 e2.6 Ga depleted mantle
involving remelting of some old
crustal materials.
Diwu et al., 2008
A. Wang, Y. Liu / Geoscience Frontiers 3(2) (2012) 147e173154
Taihua complex exposed in
Yiyang area in Henan
Province.
Two TTG gneisses. The LA-ICPMS zircon U-Pb
analyses give w2.3 Ga
formation ages.
Hf model ages have a wide range
of 2.57e3.01 Ga with a peak
at w2.8 Ga.
Diwu et al., 2007
Zhangjiakou region. A pyroxenite xenolith entrained
in the tertiary Hannuoba alkali
basalts; a tonalitic gneiss, a mafic
granulite and an amphibolite
from the basement of the
Zhangjiakou region.
They give various ages ranging
from w2.7 Ga through w2.5 Ga
to w1.8 Ga.
Nd-Hf isotope data indicate that
all of them were abstracted from
depleted mantle at 2.7e2.8 Ga.
Jiang et al., 2010
ChengdeeLuanping and
ChichengeZhangjiakou areas
in northern Hebei Province.
Monzogranitic gneiss. LA-ICP-MS zircon U-Pb dating
reflects its crystallization age of
w2510 Ma.
Nd-Hf isotope data suggest that
they were abstracted from
depleted mantle at ca. 2.7 Ga.
Liu et al., 2011b
Huai’an. Four TTG gneisses and dioritic
gneisses.
In-situ zircon ages show that they
were formed at w2.5 Ga.
Zircon Hf isotope data show that
they were derived from depleted
mantle at 2.5e2.6 Ga.
Liu et al., 2009b
Wutai complex in Shanxi
Province.
A gneissic K-rich granitic pluton. The gneissic K-rich granitic
pluton was emplaced
at w2509 Ma.
Almost all of the zircons have
positive initial ε
Hf
values,
suggesting that most of them
were abstracted from depleted
mantle at ca. 2.6 Ga involving
the remelting of minor ancient
crustal materials.
Chen et al., 2006b
Sushui complex in the Zhongtiao
mountains.
Three TTG gneiss samples. SHRIMP zircon U-Pb dating
indicate that they were emplaced
during 2.53e2.56 Ga.
Zircon Hf isotope data suggest
that they were extracted from
depleted mantle at w2.6 Ga
involving some older continental
crustal materials.
Guo et al., 2008
Late Archean Taihua complex in
Lushan region, Henan
Province.
Two TTG gneisses and two
amphibolites in the gneisses
series of the Taihua complex.
The TTG gneisses and
amphibolites are dated
at 2794e2752 Ma, some 2.9 and
3.1 Ga xenocrystaic zircons are
found in the amphibolites.
Both the TTG gneisses and
amphibolites were extracted
from depleted mantle
at 2.7e2.8 Ga with reworking of
some older crustal materials.
Diwu et al., 2010
Late Archean Taihua complex in
Lushan region, Henan
Province.
One dark-grey gneiss (TTG-like
gneiss) and one light-grey gneiss
(TTG gneiss).
The TTG-like gneiss gives
emplacement age of 2765 Ma
and the TTG gneiss yields
emplacement age of 2723 Ma.
Nd-Hf isotope gives model age
range of 2.8e3.1 Ga.
Considering that the most
positive ε
Hf
values approach the
coeval depleted mantle and the
model ages are roughly equal to
the formation ages of the
gneisses, an important crustal
accretion may happen
at 2.7e2.8 Ga involving
contamination of some ancient
crustal materials.
Huang et al., 2010
(continued on next page)
A. Wang, Y. Liu / Geoscience Frontiers 3(2) (2012) 147e173 155
Table 1 (continued)
Khondalite Belt
Locality Samples Zircon ages Hf isotope composition References
Taihua complex in Lushan area
in Henan Province.
Two supracrustal rocks include a
banded amphibolite and a
gneissic amphibolite and two
tonalites include a biotite tonalite
and a hornblende tonalite.
In-situ zircon dating indicate that
they were formed during
2.83e2.85 Ga and experienced
at least two stages of
metamorphism at w2.8 Ga
and w2.7 Ga.
Coupled zircon Hf-O isotope
compositions of magmatic
domains show that most of them
were derived from 2995 Ma
depleted mantle source with
some minor crustal
contamination.
Liu et al., 2009c
Dengfeng complex in Junzhao
region.
Two TTG gneisses, an
amphibolite and a metadiorite.
LA-ICPMS zircon U-Pb dating
shows that the Dengfeng
complex was formed during
2504e2547 Ma.
Zircon Hf isotope data show that
2.5e2.6 Ga is a major period of
crustal growth in the southern
NCC.
Diwu et al., 2011
Dengfeng complex in the
Songshan area.
Two TTG gneisses. SHRIMP zircon U-Pb analyses
yield a crystallization age of
2600e2500 Ma.
Nd-Hf isotope data suggest that
they were derived from w2.6 Ga
depleted mantle source.
Zhou et al., 2009a
Xutai and Lujiagou plutons
exposed in the SongshaneJian
area.
One sample from Xutai pluton
and one sample from Lujiagou
pluton.
The crystallization age of Xutai
pluton is 2509 33 Ma and that
of Lujiagou pluton is
2424 24 Ma. Both of them
contain inherited zircons with
age of 2.77 Ga.
The Xutai pluton has zircon Hf
isotope compositions similar to
the coeval depleted mantle
values, suggesting that some
crustal growth occurred
at w2.5 Ga; whereas the
Lujiagou pluton has zircon Hf
isotope composition similar to
the Songshan TTG gneisses with
a range of 2802e2652 Ma.
Zhou et al., 2011
The upper Taihua Group
(complex).
An amphibolite from the
Xiong’ershan terrane and
a biotite gneiss from the
LantianeXiaoqingling terrane.
They were formed during
2.3e2.5 Ga and experienced
metamorphism at 2.1 Ga. Some
zircon grains have ages of
2505e2529 Ma.
Nd-Hf isotope data suggest that a
magmatic episode with juvenile
input at 2.3e2.5 Ga with some
older crustal component being
3.1 Ga old.
Xu et al., 2009
Eastern block
YixianeFuxin greenstone belt in
Liaoning Province.
Three representative samples of
hornblende plagioclase gneisses
were carried out for age and
Lu-Hf isotope analyses.
Magmatic zircon ages of the
YixianeFuxin greenstone belt
indicate that they were formed
at 2534e2589 Ma.
All the magmatic zircons
give positive ε
Hf
values of
þ2.7eþ8.3 with model ages
of 2.76e2.57 Ga. The youngest
model age is close to their
crystallization ages, suggesting
that they were derived from
2.5 Ga to 2.6 Ga depleted
mantle. Therefore, 2.5e2.6 Ga is
an important time of crustal
growth in the western Liaoning
terrane.
Wang et al., 2011
A. Wang, Y. Liu / Geoscience Frontiers 3(2) (2012) 147e173156
The intrusive rocks from eastern
Hebei.
Four samples include a diorite,
two granodiorites, a K-feldspar
granite, a granitic gneiss and a
biotite-plagioclase gneiss.
All the intrusive rocks have
similar crystallization ages of
2515e2526 Ma.
Zircon Hf model ages show that
the main age-peaks cluster at
2.7e2.8 Ga with minor older
model ages.
Yang et al., 2008;
Wan et al., 2011c
Taishan region in western
Shandong Province.
An amphibolite and a tonalitic
gneiss from the basement in
Taishan region.
The amphibolite was formed at
2570 18 Ma, and tonalitic
gneiss was formed at
2691 7 Ma.
Zircon Hf isotope composition
indicates that both samples were
derived from depleted mantle
at w2.7 Ga.
Jiang et al., 2010
The south and north Liaohe
Group in the Jiao-Liao-Ji Belt.
Seven samples, i.e., a biotite
schist, a staurolite mica schist,
three fine-grained biotite
gneisses, a felsic gneiss were
conducted for zircon U-Pb dating
and Hf isotope analyses.
Magmatic-type detrital zircons
from both groups give the same
results with two age populations
at 2.0e2.2 Ga (major) and
w2.5 Ga (minor) plus minor
>2.7 Ga ages.
Hf isotope data show that the
zircons of the two age
populations were abstracted from
depleted during 2.7e2.8 Ga
involving a significant addition
of juvenile materials at
2.0e2.2 Ga.
Luo et al., 2008
Shuichang BIF in eastern Hebei
Province.
A plagioclase-hornblende gneiss
in Shuichang iron deposit.
Zircon cores yield a concordant
age of 2547 7 Ma, interpreted
as the forming age of the
protolith of the plagioclase-
horblende gneiss.
Almost all the zircon ε
Hf
(t)
values are negative with single-
stage Hf model ages being from
2836 Ma to 3249 Ma, suggesting
that the gneiss was mainly
derived from >3.0 Ga ancient
crustal materials with minor
addition of w2.8 Ga depleted
mantle.
Zhang et al., 2011b
Zunhua complex in eastern
Hebei Province.
Two dykes include an olivine
gabbro and a syenite.
The magmatic crystallization age
of the olivine gabbro dyke and
the syenite dyke are
2516 26 Ma and
2504 11 Ma, respectively.
Their zircons have single-stage
Hf model ages of w2.7 Ga.
Li et al., 2010
Taishan-Xintai area, western
Shandong Province.
Three samples of supracrustal
rocks in Taishan association
include a fine-grained
hornblende-biotite gneiss, a
fined-grained biotite gneiss and a
mylonitized fine-grained biotite
gneiss. Five Archean granitoids
of TTG composition include a
quartz diorite, two gneissic
trondhjemites, a gneissic tonalite
and a fine-grained granodiorite.
All the supracrustal and granitic
rocks were formed during early
Neoarchean (2.70e2.75 Ga).
Most of magmatic zircons from
supracrustal and granitoid rocks
show highly positive ε
Hf
values
approaching the values of the
coeval depleted mantle, meaning
that the continental crust was
mainly formed during
2.70e2.80 Ga.
Wan et al., 2010a,
2011b; Du et al., 2010a
A. Wang, Y. Liu / Geoscience Frontiers 3(2) (2012) 147e173 157
characteristics similar to the coeval depleted mantle, whereas
others have lower initial ε
Nd
(t) values (Kovalenko et al., 2005).
The later is widely observed by various authors like Shirey and
Hanson (1984) who first introduced the term sanukitoid to
Archean Shield. The Nd-isotope data indicate that metasomatic
enrichment of the mantle could not have occurred more than
100e200 Ma before melting. Accordingly, it is suggested that the
crustal growth occurred at w2.5 Ga or w2.7 Ga, but w2.7 Ga is
more probably.
Thus, in terms of limited zircon Hf isotope data and the U-Pb
ages of sanukitoid mentioned above, it is inferred that the main
crustal-forming time of the Yinshan block occurred in w2.7 Ga. At
the same time, w2.7 Ga crustal materials supplied local sedimen-
tary sources for the khondalites in the Khondalite Belt (Fig. 3).
Figure 2 Zircon
207
Pb/
206
Pb ages vs. ε
Hf
(t) diagram of the Archean plutonic rocks. Data sources are given in the text and in Table 1. The dashed
gray line represents the 0.75ε
Hf
of the coeval depleted mantle (Belousova et al., 2010; Diwu et al., 2011).
A. Wang, Y. Liu / Geoscience Frontiers 3(2) (2012) 147e173158
4.2. Trans-North China Craton
Extensive zircon geochronology for basement rocks of the TNCO
have contributed our understanding to the evolution of the NCC.
The age data show that the main magmatic events in the TNCO
occurred in w2.5 Ga with subdominant Paleoproterozoic
magmatic events. Minor w2.7 Ga basement components and
zircon age population are also recognized in the TNCO.
Specially, a medium-grained hornblende gneiss enclave within
biotite orthogneiss collected from the Fuping complex yields
a SHRIMP U-Pb zircon age of 2708 8 Ma, which is considered
to be the crystallization age of the tonalitic protolith (Guan et al.,
2002); two samples of foliated grey biotite gneiss and grey
granodioritic gneiss within the Hengshan complex are dated at
2701 6 Ma and 2697 1 Ma, respectively, and are interpreted
as formation ages of the formation age of granitoid plutons
(Kr€
oner et al., 2005a,b). No rocks of similar ages have been
documented in the Wutai complex, but some Wutai granitoid
rocks contain a small number of zircons with ages of w2.7 Ga
(Wilde et al., 2004, 2005). In contrast to the middle segment of
the TNCO, more w2.7 Ga and even older basement components
and zircon ages are recorded from the southern margin of the
TNCO (Kr€
oner et al., 1988; Gao et al., 2005a; Yang, 2008; Liu
et al., 2009c). For example, TTG gneisses and amphibolites of
the Taihua complex are dated at 2.7e2.8 Ga by Diwu et al. (2010)
and Huang et al. (2010), and much older ages of w2830 Ma are
reported by Liu et al. (2009a,b,c). Xeocrystic zircons with ages
of 2.9 Ga and 3.1 Ga were also found in amphibolites from
the Taihua complex (previously the lower Taihua Group, also
named as the Dangzehe complex by Yang, 2008)byDiwu et al.
(2010).
In addition to the basement plutonic rocks (including TTG
gneisses, metadiorite, amphibolite and potassic granite), numerous
SHRIMP zircon U-Pb ages have been also collected from detrital
zircons in the supracrustal rocks. Main age-peaks occur in
w2.5 Ga and w2.1 Ga in the zircon age spectra, but some much
older ages are found in detrital zircons (Du et al., 2010b). For
instance, the Gaofan Group possesses detrital zircon ages of
w2.7 Ga and some older w3.4 Ga detrital zircons (Wan et al.,
2010b). Detrital zircon ages as old as 2.7e2.8 Ga and w3.9 Ga
are also reported from the Hutuo Group by Liu et al. (2011c), and
detrital zircons with ages of w2.8 Ga and w3.24 Ga are docu-
mented in the Yejishan Group within the L€
uliang complex by Liu
et al. (2011d). Paleoproterozoic supracrustal rocks within the
Taihua complex (previously called the upper Taihua Group)
contain detrital zircons as old as 2873 and 2956 Ma (Diwu et al.,
2010). Some detrital zircon grains with ages of 3.26e2.65 Ga
were identified in quartzite within the Paleoproterozoic Songshan
Group (Diwu et al., 2008).
Coupled U-Pb and Hf analyses have been conducted for the
plutonic and supracrustal rocks and the results are discussed
below.
Figure 3 Zircon Hf model ages of the North China Craton. Data sources are given in the text. Data for the Yinshan block are from the
detrital zircons of the Zhaertai Group. Data for the Khondalite Belt are from detrital zircons of khondalites in Jining, Wulashan, Helanshan and
Daqingshan. In the Trans-North China Craton and eastern block subsections, light gray area represents data from detrital zircon from
supracrustal rocks and the Liaohe Group; dark gray area represents data from zircons of TTG gneiss and late Neoarchean granitoids (Archean
plutonic rocks).
A. Wang, Y. Liu / Geoscience Frontiers 3(2) (2012) 147e173 159
4.2.1. Plutonic rocks
The basement complex consists of two main lithological units of
supracrustal and plutonic rocks. The plutonic rocks include TTG
gneisses, metadiorites, amphibolites and potassic granites.
Liu et al. (2009b) carried out zircon U-Pb and Hf isotope
analyses for the Huai’an terrane consisting mainly of TTG
gneisses and dioritic gneisses in combination with whole-rock Nd-
isotope compositions. The results suggested that the protoliths of
these gneisses were emplaced at w2.5 Ga and were extracted
from depleted mantle at 2.5e2.6 Ga. Similar methods have been
used to investigate the gneissic K-rich granitic pluton within the
Wutai complex (Chen et al., 2006b). LA-ICPMS in-situ zircon
U-Pb dating for a gneissic K-rich granite yields an age of
2509 7.4 Ma and almost all of the zircon Hf data show positive
initial ε
Hf
(t) values, suggesting that they were melted from coeval
depleted mantle involving minor ancient crustal components,
which is supported by w2.7 Ga detrital/inherited zircon ages. The
Precambrian Sushui complex of TTG composition in the Zhong-
tiao mountain was taken for SHRIMP zircon U-Pb dating and Hf
isotope analyses with formation age of 2536 8 Ma and positive
initial Hf isotope compositions, indicating that the magmas could
be derived from the partial melting of 2.5e2.6 Ga juvenile crust
material from the depleted mantle (Guo et al., 2008)(Fig. 2b). In
short, these data imply that 2.5e2.6 Ga is an important time of
crustal-formation of the central part of the NCC.
Neoarchean granitoid gneisses in the ChengdeeLuanping and
ChichengeZhangjiakou regions at the northern margin of the
NCC are mainly composed of tonalitic, trondhjemitic, granodio-
ritic and monzogranitic gneisses (TTGM). The dating results
suggest that they were formed at w2510 Ga and low ε
Hf
(t) values
(0.4 to þ1.9) suggest that they were abstracted from w2.7 Ga
depleted mantle, which is in good agreement with whole-rock Nd-
isotope data (Liu et al., 2011b)(Fig. 2a). Four samples, including
a pyroxenite xenolith in the tertiary Hannuoba alkali basalts,
a tonalitic gneiss, a mafic granulite and an amphibolite from the
basement of the Zhangjiakou area were investigated by Jiang et al.
(2010) by applying zircon geochronology, geochemistry and
isotope analyses. Zircon geochronology yields various ages
of w2.7 Ga, w2.5 Ga and w1.8 Ga. Combined Nd-Hf isotope data
suggest that all the target samples were extracted from w2.7 Ga
depleted mantle (Fig. 2e). Consequently, Jiang et al. (2010) presume
that the w2.7 Ga magmatism and crustal growth are probably much
greater in extent than previously suggested.
Plutonic rocks along the southern margin of the NCC have also
been extensively studied. The Taihua complex exposed in the
Yiyang area of the western Henan Province was studied by Diwu
et al. (2007). LA-ICPMS zircon dating indicates that the complex
was formed at w2.3 Ga, and most of the zircon ε
Hf
(t) values
exhibit negative values with minor low positive values. Two-stage
zircon Hf model ages range from 2.57 to 3.01 with a main age
peak at 2.8 Ga, probably indicating that they were derived
from w2.8 Ga depleted mantle with 0.4e0.5 Ga crustal residence
ages. The Taihua complex exposed in the Lushan region has been
investigated by Liu et al. (2009c), Diwu et al. (2010), and Huang
et al. (2010). The age data show that TTG gneisses and amphib-
olites of the complex were emplaced between 2.7 Ga and 2.8 Ga
with inherited zircon ages of 2.9 and 3.1 Ga. The combined zircon
Hf isotope and whole-rock Nd-isotope data indicate that the
Figure 4 Age spectra for zircons from the basement of the North China Craton (after Wan et al., 2011a). A: All data for the North China
Craton; B: Data for eastern block; C: Data for western block; D: Data for Trans-North China Orogen. MA Zmagmatic zircon; D & I Zdetrital
and inherited zircon; ME Zmetamorphic zircon.
A. Wang, Y. Liu / Geoscience Frontiers 3(2) (2012) 147e173160
2.7e2.8 Ga tectono-thermal event represents an important period
of crustal growth in the studied area involving the reworking of
some ancient crustal materials (Fig. 2d). On the basis of integrated
geochronology, geochemistry and isotope data, Huang et al.
(2010) obtained the same conclusion as Diwu et al. (2010). But
two differences are notable, the first is that the gray gneisses can
be divided into TTG and TTG-like gneisses, the latter was formed
slightly earlier than the former, and they each have different
genesis models; the other is that these authors obtained more relic
zircons (2.95e2.80 Ga) with negative ε
Nd
(t) and ε
Hf
(t) values.
However, Liu et al. (2009c) suggested that tonalities and
amphibolites of the Taihua complex in the Lushan region were
formed at w2.84 Ga and subsequently underwent at least two
episodes of metamorphism at w2.78 and w2.67 Ga. Liu et al.
(2009a,b,c) also found that the Hf and O isotopic features of the
magmatic zircons are characterized by mostly positive ε
Hf
(t)
values and mantle-like d
18
O values, suggesting that the main
period of crustal growth is between 2.8 Ga and 2.9 Ga with minor
contamination of ancient crustal materials (Fig. 2d). No w1.85 Ga
zircon metamorphic ages are documented as previously reported
by Wan et al. (2006b). All the available data suggest that the
geology of Lushan is more complex than previously suggested
(Liu et al., 2009c).
The Dengfeng complex exposed in the Songshan region of
Henan Province is an important part of the ancient crystalline
basement in the southern segment of the NCC. In recent years,
a large number of studies have been carried out (Wan et al., 2009c;
Zhou et al., 2009a,b, 2011; Diwu et al., 2011). The plutonic rocks
of the Dengfeng complex are composed of TTG gneisses, meta-
diorite, amphibolite and granite. The dating results suggest that all
of them were formed at 2.5e2.6 Ga with minor older inherited
zircons except the Lujiakou pluton and the Shichen monzosyenite
with formation ages of w2.4 and w1.78 Ga, respectively. The Hf
data of 2.5e2.6 Ga magmatic zircons have positive ε
Hf
(t) values,
where the highest values approach that of the contemporaneous
depleted mantle. These results suggest that the rocks in the
Dengfeng complex represent 2.5e2.6 Ga juvenile crust (Fig. 2c).
In combination with other geochemical data, Diwu et al. (2011)
and Zhou et al. (2009a,b) proposed that modern-style plate
tectonics processes were probably initiated in the southern margin
of the NCC during late Archean.
4.2.2. Supracrustal rocks and basin sediments
Voluminous highly metamorphosed supracrustal rocks deposited
upon the basement of the TNCO, some of which were considered
to be originally formed at the foreland basins (Li and Kusky,
2007). Li and Kusky (2007) suggest that the Qinglong foreland
basin extending N to NE up to 1600 km exists in the eastern side
of the TNCO. This basin can be further divided into the northern
Qinglong Group in the eastern Hebei Province, the middle Gaofan
and Hutou Groups in the Wutaishan region and the Wanzi Group
in the Taihangshan area, and the southern Songshan Group in the
Songshan area. U-Th-Pb and Lu-Hf isotopic compositions of
detrital zircons from the basin sediments can provide rigorous
constraints on the crustal growth and evolution of the NCC
(Krabbendam et al., 2008). As mentioned above, the main detrital
zircon age populations concentrate at w2.1 Ga and w2.5 Ga,
consistent with ages of Archean TTG gneiss and Paleoproterozoic
magmatic rocks. It is different from the age features of the
khondalites in the WB characterized by main 2.1e2.0 Ga age-
group with minor Archean zircon ages. There is also a marked
source age difference between the southern margin and middle
sector basin sediments, implying that the southern margin is more
complex than previously suggested. For instance, the Songshan
Group lack w2.1 Ga detrital zircon ages, which widely occur in
the Hutuo Wanzi Groups in the middle segment of the TNCO.
Xia et al. (2006c) firstly reported U-Pb age and Hf isotope data
of detrital zircons from the Wanzi supracrustal rocks within the
Fuping complex in order to constrain on the tectonic setting and
evolution of the TNCO. The igneous zircon ages show two age-
groups at w2.1 Ga and w2.5 Ga with some inherited zircons as
old as w2.9 Ga. The w2.5 Ga ages have positive ε
Hf
(t) values of
þ1.4 to þ10.9, close to the values of the coeval depleted mantle,
implying that 2.5e2.6 Ga is an important time of crustal growth.
In addition, rare relict zircons show 2.8 Ga zircon Hf model ages.
The w2.1 Ga zircons have both negative and positive initial Hf
isotope ratios, interpreted as mixing of ancient crust materials with
minor juvenile materials at w2.1 Ga.
U-Pb and Hf isotope data of detrital zircons from the Hutou
Group within the Wutai complex have been investigated by Liu
et al. (2011c). The zircons have a wide age range from 1.88 Ga
to 3.88 Ga with main Neoarchean to Paleoproterozoic ages,
similar to the Wanzi Group. Most of the zircons exhibit positive
ε
Hf
(t) values and have model age-peaks at w2.6 Ga involving
remelting of minor older crustal components. Similar researches
are also carried out for detrital zircons from the Yejishan Group of
the L€
uliang complex (Liu et al., 2011d). The detrital zircons have
a wide range from w1.8 Ga to w3.24 Ga with two age-peaks at
w2.5 Ga and 2.1e2.2 Ga. Zircon Hf model ages show w2.6 Ga
age-peaks with some ancient crustal materials.
All the above authors supposed that the older zircons or rocks
are remnants of an older continental crust on which an Andean-
type continental margin arc developed and then was incorporated
into the TNCO during the collision between the WB and EB, and
all of them may have formed in the same large foreland basin in
the middle sector of the TNCO during the L€
uliang movement.
Amphibolites from supracrustal rocks within the Dengfeng
complex have been studied by Zhou et al. (2009a) and Diwu et al.
(2011). Zircon dating results suggest that the protolith age of the
amphibolite is 2547 Ma, and intergraded Nd-Hf isotope data
indicate that they were extracted from depleted mantle during
2.5e2.6 Ga. U-Pb ages and Hf isotopes for detrital zircons from
quartzite within the Paleoproterozoic Songshan Group are studied
by Diwu et al. (2008). Ninety-nine detrital zircon ages have a large
age range with several peaks clustering at w3.40, 2.77e2.80,
w2.50 and w2.34 Ga. Of these, w2.50 Ga ages constitute about
85% of the total grain population and high and positive ε
Hf
(t)
values are close to the ratios of coeval depleted mantle, implying
that major growth of juvenile crust took place at w2.50 Ga
involving minor reworking of ancient crust. Furthermore,
2.77e2.80 Ga zircons make up a small proportion of the total
zircon age population and have high ε
Hf
(t) values approaching that
of coeval depleted mantle, implying that minor w2.8 Ga crustal
growth also occurred.
Many studies suggest that the traditional Taihua Group can be
further divided into the early Neoarchean (2.7e2.8 Ga) Dangzehe
complex (previously known as the lower Taihua Subgroup) and
the Paleoproterozoic Taihua complex (previously known as the
upper Taihua Subgroup) (Yang, 2008; Diwu et al., 2010). The
Paleoproterozoic upper Taihua Group (supracrustal rocks) consists
of graphite-bearing gneisses, biotite gneisses, marbles, banded
iron formations (BIF), amphibolites and quartzites. Coupled in-
situ U-Pb dating and Hf isotope analysis of zircons from a bio-
tite gneiss (from the LantianeXiaoqinling terrane) and an
A. Wang, Y. Liu / Geoscience Frontiers 3(2) (2012) 147e173 161
amphibolite (from the Xiong’ershan terrane) suggest that the
upper Taihua Group formed in the Paleoproterozoic (2.3e2.5 Ga).
Nd-Hf isotope data indicate that 2.3e2.5 Ga magmas were derived
from the depleted mantle source with some assimilation of ancient
crustal material as old as 3.1e3.2 Ga (Xu et al., 2009). Xu et al.
(2009) have proposed that the Taihua Group underwent strong
metamorphism and deformation, and the terrains of Taihua Group
were not formed by the collision between the EB and WB of the
NCC. The Taihua Group may now represent an integral part of the
Qinling Orogen terranes rather than simply being the southern
extension of the Central Zone of the NCC.
In short, the obtained zircon U-Pb ages and Hf isotope
compositions of the TNCO basement rocks suggest that some
areas like Huai’an, Wutai, Dengfeng and Zhongtiaoshan are
characterized by dominant 2.5e2.6 Ga crustal growth and other
areas such as Lushan, Zhangjiakou, and northern Hebei Province
are characterized by the main 2.7e2.8 Ga crustal growth. The
southern margin of the TNCO is more complex than previously as
evidenced by the presence of more 2.7 Ga and even older rocks
and zircon ages (Fig. 3). Geochemical features also show marked
differences as discussed below.
4.3. Eastern block
The EB has a long research history and is famous for the occurrence
of Early Archean rocks (e.g., Liu et al., 1992). Except for 3800 Ma
continental crust remnants, some rocks with ages ranging from
3600 Ma to 2800 Ma include ultramafic, mafic, and felsic volcanic
rocks and pre-tectonic gneisses. About 80% of the Precambrian
basement is composed of TTG gneisses, charnockites, granites,
amphibolites, mafic granulites with ages of 2600e2500 Ma. The
Paleoproterozoic Jiao-Liao-Ji Belt is located in the eastern part of
the EB and divides the EB into the north Longgang block and the
south Nangrim block (Luo et al., 2008; Li et al., 2011b; Zhao et al.,
2011). The belt comprises metamorphosed sedimentary and
volcanic successions metamorphosed to greenschist and amphibo-
lite facies grade and voluminous granitic and mafic rocks. The
metamorphic rock series includes the Jingshan and Fenzishan
Groups in eastern Shandong, the south and north Liaohe Groups in
eastern Liaoning, the Ji’an and Laoling Groups in southern Jilin, and
possibly the Macheonyeong Group in North Korea. Strati-
graphically, the Fenzishan Group is well correlated with the north
Liaohe and Laoling Groups, and the Jingshan Group is well
correlated with the south Liaohe and Ji’an Groups, representing the
northern and southern belt of the Jiao-Liao-Ji Belt, respectively
(Luo et al., 2008). The Liaohe Group occurs associated with volu-
minous Paleoproterozoic granitoids and mafic intrusions. Mafic
intrusions consist of dolerites and gabbros, most of which experi-
enced greenschist to amphibolites facies metamorphism. The
granitoids, also called the Liaoji granitoids, comprise pre-tectonic
A-type monzongranitic gneisses and post-tectonic undeformed
porphyritic monzogranites, granites and alkali syenites. Zircon
SHRIMP dating has been carried out for the granitoids by Lu et al.
(2004) and Li and Zhao (2007). Although numerous structural,
geochemical and geochronological investigations have been
undertaken on the Jiao-Liao-Ji Belt (Faure et al., 2004; Li et al.,
2005, 2006, 2007,2010, 2011b; Lu et al., 2006; Luo et al., 2004,
2006, 2008; Zhou et al., 2008; Tam et al., 2011a,b; Zhao et al.,
2011), yet no consensus has been reached on the tectonic nature
of the Jiao-Liao-Ji Belt. Different models, such as rifting, arc-
continent/continent-continent collision, rifting-and-collision, have
been proposed. Luo et al. (2008) initially carried out U-Pb and Hf
isotopic analysis of detrital zircons from the south and north Liaohe
Groups, and many investigations have also been undertaken on the
basement rocks. The most significant difference between the EB
and WB and the TNCO is that the wide occurence of 3.8 Ga
zircons and Early Archean crustal materials. Numerous geochro-
nological and Nd-Hf isotopic data have been reported to elucidate
the early stage evolution of the eastern NCC (Wu et al., 2005a,
2008a; Wilde et al., 2008; Zhang et al., 2011a). Crustal growth
with age-peaks at w3.4, w3.6 and w3.9 Ga are documented based
on geochronology and Nd-Hf isotope data, no detailed information
is given in this contribution and the readers can refer to the following
papers (Wu et al., 2005a,b, 2008b; Wilde et al., 2008;Jahn et al.,
2008;Wan et al., 2005, 2009a; Zheng et al., 2004a; Nutman et al.,
2009, 2011; Geng et al., 2010, 2011; Zhang et al., 2011a).
4.3.1. North and south Liaohe Groups
Numerous detrital zircons extracted from the south and north Liaohe
Groups have been used for U-Pb age and Hf isotope composition
determination, in combination with previous Nd-isotope data and
geochronology, Luo et al. (2008) gave some important conclusions
on the crustal growth history of the eastern margin of the EB. Detrital
zircons show two age-groups at w2.50 Ga (minor) and w2.10 Ga
(major), consistent with the ages of the basement gneisses and Liaoji
granitoids. Hf isotope compositions of w2.5 Ga zircons suggest that
the main mantle extraction event in the EB occurred in w2.8 Ga
involving the remelting of minor ancient crustal materials, those of
the w2.10 Ga detrital zircons suggest that the precursor magmas
were mostly abstracted from depleted mantle at w2.7 Ga with minor
addition of w2.10 Ga mantle-derived materials (Fig. 3).
The crustal growth period of the EB revealed by the detrital
zircons from the south and north Liaohe Groups is distinct from the
results of detrital zircons from both khondalites in the WB and
supracrustal rocks/basin sediments in the TNCO. The supracrustal
rocks/basin sediments in the TNCO show that major crustal growth at
2.5e2.6 Ga with minor crustal growth at 2.8 Ga and in the Paleo-
proterozoic, detrital zircons from Khondalite Belt exhibit the main
crustal growth in the Paleoproterozoic involving some w2.6 Ga and
minor early Archean crustal accretion.
4.3.2. Basement rocks
Extensive studies have been undertaken for the western Shandong
Province in recent years by using methods of zircon dating,
geochemistry and Nd-Hf isotope analyses (Du et al., 2010a; Wan
et al., 2010a, 2011b). The age data suggest that the basement
rocks consisting of TTG and supracrustal assemblages were formed
in the Neoarchean (2.75e2.58 Ga) and were intruded by volumi-
nous Late Archean quartz diorite, monzodiorite and granodiorite.
Wan et al. (2011b) suggested that thewestern Shandong Province is
a greenstone-granite terrain and is characterized by both w2.7 Ga
and w2.5 Ga magmatic events, and that the Neoarchean basement
can be divided into three belts: a late Neoarchean (2525e2490 Ma)
crustally-derived granite belt (Belt A) in the northeast; an early
Neoarchean (2.75e2.60 Ga) belt of TTG and supracrustal rocks in
the central (Belt B); and a late Neoarchean (2550e2500 Ma) belt of
juvenile rocks in the southwest southwestern (Belt C). Hf isotope
data indicate that the widely distributed crustally-derived w2.5 Ga
granites and 2.75e2.70 Ga supracrustal and TTG rocks were
extracted from the depleted mantle at 2.7e2.75 Ga, and Late
Neoarchean (2550e2500 Ma) juvenile rocks are also widely
occurred. Thus, both 2.75e2.70 Ga and 2.55e2.50 Ga crust-
forming events are widely developed in the western Shandong
A. Wang, Y. Liu / Geoscience Frontiers 3(2) (2012) 147e173162
Province, and the former may be much more widespread than the
latter (Fig. 2g). Wan et al. (2011b) believed that the largest differ-
ence between the NCC and the other cratons in the world is not the
weak development of tectono-thermal events in w2.7 Ga, but the
strong overprinting of w2.5 Ga tectono-thermal events in the NCC.
Jiang et al. (2010) also conducted combined U-Pb and Lu-Hf
isotope analyses of zircons separated from an amphibolite and
a tonalitic gneiss from the basement of the western Shandong
Province in the Taishan region. The results suggest that the
amphibolite and the tonalitic gneiss were formed at 2570 18 Ma
and 2691 7 Ma, respectively, and both were derived from
depleted mantle at w2.7 Ga. The 2.8e2.7 Ga crustal accretion is
also confirmed by Polat et al. (2006) in the Taishan region.
The YixianeFuxin greenstone belt is located along the
northern termination of the eastern NCC. In terms of geochem-
istry, metavolcanic rocks in the greenstone belt can be grouped
into four groups: normal-mid-ocean ridge basalts (N-MORBs),
boninite-like rocks, adakite-like rocks and high magnesium
andesites (HMAs), suggesting that they formed in an active
continental margin setting related to oceanic slab subduction,
similar to the southern margin of the NCC (Diwu et al., 2011;
Zhou et al., 2011). Magmatic zircons suggest that the meta-
volcanic rocks were emplaced at 2534e2589 Ma and have highly
positive ε
Hf
(t) values approaching to the coeval depleted mantle
values. These data indicate that 2.5e2.6 Ga is an important
episode of crustal growth in the western Liaoning metamorphic
terrane (Wang et al., 2011)(Fig. 2f).
In contrast to the western Liaoning Province, the eastern Hebei
region provides a different scenario (Yang et al., 2008; Li et al.,
2010; Zhang et al., 2011b). Here, a rare coeval mafic-ultramafic
and syenitic dykes intruding the 3.8e2.55 Ga Caozhuang
complex have been dated by in-situ zircon U-Pb and Hf isotope
analyses and the results suggest that they crystallized between
2504 Ma and 2516 Ma and were derived from depleted mantle
at w2.7 Ga. In combination with Sr-Nd isotopic and whole-rock
geochemical data, these authors thought that these intrusions
derived from an enriched mantle which was metasomatised by
fluids/melt from a subducted slab and represent the latest stage of
Archean magma activity (Li et al., 2010). Thus, w2.7 Ga is an
important crustal growth period for the eastern Hebei region. SIMS
U-Pb dating and in-situ Lu-Hf analysis of zircons from plagioclase-
hornblende gneiss associated with the Shuichang BIF in the eastern
Hebei Province have been made by Zhang et al. (2011b). The results
indicate that the gneiss formed at w2547 Ma, but almost all the
ε
Hf
(t) values are negative with single-stage Hf model ages being
2836e3249 Ma. This suggests that the gneiss was mainly derived
from >3.0 Ga ancient crust with minor addition of w2.8 Ga
depleted mantle. Yang et al. (2008) also carried out LA-ICPMS and
Lu-Hf isotopic analysis of zircons from Late Archean hornblenditc,
tonalitc, dioritic, granodioritc and granitc plutons in the eastern
Hebei Province. Magmatic zircons record emplacement age of
2526e2515 Ma and corresponding Hf isotopic data suggest that
these rocks originated from partial melting of a juvenile lower crust
at shallow crustal depths. Hf model ages indicate that they were
derived from depleted mantle at 2.7e2.8 Ga with minor compo-
nents of remelted ancient crustal materials.
Yang et al. (2005) also conducted zircon U-Pb and Hf isotope
analyses of gneiss which hosts Paleoproterozoic Miyun rapakivi
granite in Beijing. The results suggest that the gneiss was formed
at w2521 Ma and derived from depleted mantle at 2.5e2.6 Ga
(Fig. 2f). This conclusion is further confirmed by Ren et al.
(2011).
Until now, no zircon Hf isotopic data have been reported for
the Jiaodong Terrane in eastern Shandong Province. However,
Jahn et al. (2008) conducted an intergrated study of zircon
geochronology, bulk-rock elemental and Nd-isotope geochemistry
on gneisses and granodiorites from the Jiaodong Terrane, in
combination with a previous study by Tang et al. (2007), found
that except for one TTG gneiss with age of w2.9 Ga, the others
yield ages of 2.71e2.73 Ga. Jahn et al. (2008) proposed that the
most significant crust-forming episode in the Jiaodong Terrane is
2.71e2.73 Ga, similar to the western Shandong Province terrane.
A potential region of 2.7e2.8 Ga crustal growth could be the
Houqiu area in the southeastern margin of the NCC. Basement
rocks and detrital zircons with ages of 2.75e2.7 Ga are identified
(Wan et al., 2010c), although are not confirmed by the Hf isotope
data. Zircon xenocrysts from early Fuxian and Mengyin dia-
moniferous kimberlites in the EB also show 2.7e2.8 Ga crustal
accretion (Zheng et al., 2009). U-Pb geochronology and Hf
isotopes of zircons separated from granulite xenoliths in Phaner-
ozoic magmatic rocks and inherited xenocrysts from the associ-
ated lower crust rocks in the eastern domains of the NCC, also
suggest that the main crustal growth occurred at w2.7 Ga,
although involving significant contribution of w2.5 Ga juvenile
materials. Recently, Geng et al. (2010, 2011) suggested that major
crustal accretion of the EB and TNCO took place at 2.7 Ga and
essential cratonization of the NCC took place at the end of
Archean related to mantle plume activity.
In summary, the crustal growth period in the EB is complex.
The main crustal growth period in eastern and western Shandong
Province, and eastern Hebei Province occurred in w2.7 Ga,
whereas that of the western Liaoning Province and Miyun in
Beijing happened at 2.5e2.6 Ga. The crustal accretion at w2.7 Ga
may be an underestimate due to the extensive overprint
of w2.5 Ga tectonthermal events or insufficient data (Fig. 3).
4.4. Detrital zircon from modern river sediments
One of the best ways to elucidate crustal growth and terrane
evolution history is to determine U-Pb age and Lu-Hf isotopic
composition of detrital zircons from modern river sediments (Rion
et al., 2004; Iizuka et al., 2010; Safonova et al., 2010). Four
hundred and seventy-nine concordant detrital zircons in three sand
samples from the Yellow River and two sand samples from the
Yongding and Luan Rivers were determined by Yang et al. (2009).
Several age-peaks occur in the zircon age spectra with one peak at
2.2e2.6 Ga, and one of the dominant groups of Hf crust model
ages occur between 2.4 Ga and 2.9 Ga with a peak at 2.7e2.8 Ga.
The 2.7e2.8 Ga age-peak in all the river sand samples agrees well
with the coeval major peak for global crustal growth.
4.5. Detrital zircon from sedimentary cover rocks
Following the L€
uliang movement at w1.8 Ga, the NCC was
subjected to an extensional regime and voluminous thick-layered
clastic rocks and carbonates were deposited in the margins or
interior of the craton (Lu et al., 2008). The Meso- to Neo-
proterozoic sedimentary succession can be divided into the
Changcheng, Jixian and Qingbaikou Groups. U-Pb geochronology
and Hf isotopic compositions for detrital zircons from the Meso-
to Neoproterozoic cover succession of the NCC in the Ming
Tombs area in Beijing have been measured by Wan et al. (2003,
2011a). Detrital zircon age spectra agree well with that of early
A. Wang, Y. Liu / Geoscience Frontiers 3(2) (2012) 147e173 163
Precambrian basement of the NCC, both display age-peaks at
w2.5 Ga and w1.85 Ga. While the age spectra has a notable
change through different groups, the lower Changcheng Group is
predominated by detrital zircons of late Neoarchean age, and the
overlying Jixian and Qinbaikou Groups are dominated by late
Paleoproterozoic zircons. More importantly, the w2.5 Ga detrital
zircons have various initial Hf isotopic values and Hf model ages
of 2.7e2.8 Ga (Wan et al., 2011a; Ren et al., 2011).
4.6. Zircon in Precambrian lower crustal rocks
Recently, Zhang et al. (2011a) have made a comprehensive review
of U-Pb geochronology and Hf isotopes of zircons collected from
granulite xenoliths entrained in Phanerozoic magmatic rocks and
zircons from inherited xenocrysts from associated lower crust rocks
from various regions of the NCC, most of which concentrates on the
EB except some granulite xenoliths in the Cenozoic Hannuoba
basalts on the TNCO. These data provide important insights into
understanding the growth and evolution of the lower crust and
suggest that several episodic stages of growth of Precambrian lower
crust beneath the NCC. These authors proposed that the oldest lower
crust was indeed formed in the Eo-Archean with ages as old as
4.0e4.1 Ga. In addition to an important crustal growth period
during 2.8e3.0 Ga and the Paleoproterozoic reworking of the
Archean lower crust with some addition of juvenile materials, The
Hf T
DM
ages show a main age peak at w2.7 Ga, consistent with the
data of xenocrystic zircons from both the Fuxian and Mengyin
kimberlites (Zheng et al., 2009). These results suggest that
2.7e2.8 Ga is an important time of crustal accretion for the EB,
corresponding to a major episode of global crustal-formation. It is
interesting to note that the w2.5 Ga tectono-thermal event involved
both the remelting of pre-existing old crustal materials and input of
juvenile materials, probably in association with mantle-derived
magma underplating in mantle plume setting (Geng et al., 2010).
This thermal event marks cratonization of the EB of the NCC. Thus,
with respect to lower crustal evolution, both 2.7e2.8 Ga and
2.5e2.6 Ga crustal growth events occurred in the EB. The
2.7e2.8 Ga thermal event may be more widely distributed than that
presently exposed, which may be due to the strong resetting and
destruction of 2.5e2.6 Ga thermal event or insufficient data as
suggested by Diwu et al. (2010); Jiang et al. (2010) and Wan et al.
(2011a,b,c).
4.7. Zircon from Neoarchean syenogranites
At the end of the Neoarchean, voluminous syenogranites and K-rich
granites were emplace in the NCC (e.g., Grant et al., 2009; Zhang
et al., 2011c; Wan et al., 2011c). Such rocks are widely distrib-
uted in the EB including in the regions of AnshaneBenxi, Qin-
huangdao, western Shandong, northern Liaoning, southern Jilin and
northern Hebei, in the southern margin of the TNCO of central
Henan and in the northern segment of the TNCO of the Huai’an
area. Wan et al. (2011c) reviewed the zircon ages and geochemistry
of these late Neoarchean syenogranites, and found that they were
formed between 2.53 Ga and 2.50 Ga and generated by melting of
continental crust with different mean crustal residence ages. Most of
the w2.5 Ga granites including syenogranites have whole-rock Nd
and zircon Hf model ages of 2.7e2.8 Ga, indicating an important
time of crustal growth of the NCC. The zircon Hf data is also
consistent with the results of Li et al. (2010) and Zhang et al. (2011c)
for the areas of eastern Hebei and Huai’an.
5. Discussion
5.1. Mantle extraction ages in the NCC
From the zircon Hf isotopic data described above (Figs. 2 and 3),
there are some significant differences in crustal-formation ages
between different divisions of the NCC. Combined with previous
zircon U-Pb age and Hf isotope and whole-rock Nd-isotope data,
some key points are obtained as follows. The EB is characterized
by crustal growth episodes at w3.4, w3.6 and w3.9 Ga. The
main crustal growth time in the Neoarchean is at 2.7e2.8 Ga in
the eastern and western Shandong Province, eastern Hebei Prov-
ince, with local crustal-formation at 2.5e2.6 Ga in western
Liaoning Province and at Miyun near Beijing. The main crustal
growth time in the Yinshan block of the WB occurred mainly
in w2.7 Ga, as indicated by detrital zircon Hf isotope composi-
tions from the Zhaertai Group. Detrital zircon Hf model ages of
the Khondalite Belt within the WB are very complex, the main
feature is that they are mainly characterized by Paleoproterozoic
crustal growth involving some w2.6 Ga crustal materials and
minor w2.7 Ga, Early- and Middle-Archean and even older
crustal compositions, in good agreement with the ages of detrital
zircon from upper Proterozoic to Ordovician strata from the
Zhuozi Shan in north-central China (Darby and Gehrels, 2006).
The TNCO’s crustal growth has a wide age range from 2.5 Ga to
2.9 Ga but marked differences exist in different localities. The
Wutai, Huai’an, Dengfeng and Zhongtiaoshan complexes display
2.5e2.6 Ga crustal growth, while the basement in the Zhangjia-
kou, Lushan and northern Hebei regions is characterized by
2.7e2.8 Ga crustal growth. The supracrustal rocks/basin sedi-
ments within the L€
uliang, Fuping and Wutai complexes are also
characterized by 2.5e2.6 Ga zircon Hf model age-peaks involving
minor 2.7e2.8 Ga and even older crustal materials. It is notable
that the southern margin of the TNCO is featured by a greater
proportion of 2.7e2.8 Ga and even older basement rocks and
zircon ages and lacks evidence of w1.85 Ga metamorphism in the
Dengfeng complex, indicating that its evolution is more complex
than previously considered.
In summary, the time of NCC’s crustal growth is more complex
involving both 2.7e2.8 Ga and 2.5e2.6 Ga. The 2.7e2.8 Ga
magmatic events and crustal growth are more widely distributed
than previously thought, which is confirmed by zircon Hf isotope
data of modern river sediments, overlying sedimentary cover,
Precambrian lower crustal rocks and Neoarchean syenogranites.
Crustal growth and magmatism at 2.7e2.8 Ga may be under-
estimated due to the overprint of strong 2.5e2.6 Ga thermal
tectonism, poor exposure and insufficient data.
It should be noted that the tectonic setting of w2.5 Ga mag-
matism and crustal growth is hotly controversial in that it
considered to be the result of mantle plume activity or arc mag-
matism, or both (Chen, 2007; Liu et al., 2007; Yang et al., 2008;
Grant et al., 2009; Zhao, 2009; Geng et al., 2010, 2011; Wang
et al., 2011).
5.2. Constraints on evolution and tectonic division of the
NCC
Regarding the evolution and tectonic division of the Precambrian
basement of the NCC, researchers have different opinions. Some
suggest that the NCC can be tectonically divided into three parts,
the EB (Yanliao block), the WB consisting of the Ordos and
A. Wang, Y. Liu / Geoscience Frontiers 3(2) (2012) 147e173164
Yinshan blocks, and the TNCO. There is controversy over the
timing and tectonic process of amalgamation of the two blocks.
One proposal is eastward-directed subduction of an old ocean,
with final collision of the two blocks at w1.85 Ga; another is
westward-directed subduction with final collision between the two
blocks at w2.5 Ga. In recent time, a two-stage subduction model
involving different Paleoproterozoic ages has been suggested (e.g.,
Wang et al., 2010b). In contrast, Zhai et al. (2000, 2010) proposed
that the NCC can be divided into six micro-blocks; Ji’ning,
Qianhuai, Fuping, Xuchang, Jiaoliao and Alashan blocks. They
suggested that Precambrian crustal growth and stabilization of the
NCC can be related to four major geological events: (1) a major
phase of continental growth for the NCC at 2.7e2.9 Ga, which is
in accordance other cratons worldwide; (2) the amalgamation of
the micro-blocks and formation of the NCC were completed
by w2.5 Ga, with a tectonic constitution defined by greenstone
belts and high-grade metamorphic regions; (3) Paleoproterozoic
rifting-subduction-accretion-collision tectonics and subsequent
high-grade granulite-facies metamorphism and granitoid magma-
tism at 1950e1830 Ma, suggesting that the NCC is an important
part of the Columbia supercontinent; (4) the major subsequent
Paleoproterozoic extension is considered to be plume-related,
which finally resulted in the break-up of the NCC from the
Columbia supercontinent at w1.8 Ga. However, Geng et al. (2010,
2011) suggested that the widely distributed magmatism
at w2.5 Ga was likely related to the mantle plume activity that
caused partial melting and reworking of w2.7 Ga crustal mate-
rials, and that essential cratonization of the NCC took place
at w2.5 Ga.
One of the major reasons resulted in the difference in under-
standing of the evolution and tectonic subdivision of the NCC is
mainly due to the different interpretations on the zircon ages.
There is a marked zircon age difference between the EB and WB
and the TNCO. Recently, Wan et al. (2011a) have compiled a total
of 7586 zircon ages from the entire NCC that comprise 3905
magmatic, 1511 metamorphic and 2170 detrital zircons (Fig. 4).
Although there is an uneven geographic distribution of the data,
some notable features are evident. The entire NCC is character-
ized by w2.5 Ga and w1.8 Ga tectonthermal events. Firstly,
a series of rocks and zircons dated at >2.8 Ga are documented in
the EB, i.e., in the Anshan region of Liaoning Province, Caoz-
huang region of eastern Hebei Province, and Xinyang region of
Henan Province. The w2.8 Ga TTGs and supracrustal rocks are
distributed in the Lushan region of central Henan Province.
However, 2.8 Ga inherited and detrital zircons are widely
discovered in the TNCO, e.g., the Wutai, Fuping, Jiaozuo and
Dengfeng areas, and in the EB, e.g., Huoqiu, western and eastern
Shandong Province. Secondly, w2.7 Ga old rocks are identified in
eastern and western Shandong Province and other areas of Huo-
qiu, Zhangjiakou, Fuping, Hengshan, Lushan and Guyang, and
detrital and inherited zircons of this age occur over almost the
whole NCC. Thirdly, the strongest tectono-thermal event for the
NCC occurred in w2.5 Ga, which is different from other world-
wide cratons with w2.7 Ga being predominant. There is contro-
versy over the w2.5 Ga age involving juvenile crustal accretion or
reworking of ancient crust or both. Finally, middle Paleoproter-
ozoic 2.3e2.0 Ga rocks and inherited/detrital zircons are widely
reported in the whole NCC, but from the statistical diagrams, the
proportion of 2.3e2.0 Ga zircons in the WB is much higher than
those in the EB and TNCO (Fig. 4). It is also supported by ages of
detrital zircons from the supracrustal rocks. For instance, the
majority of detrital zircons from the Khondalite Belt are
characterized by 2.3e2.0 Ga ages with a few yielding Archean
ages, while detrital zircons from supracrustal rocks within the
TNCO exhibit both w2.1 Ga and w2.5 Ga age-peaks.
Therefore, there is a marked difference in zircon age spectra
between the EB,WB and the TNCO. It is reasonable to divide into the
NCC into three main parts. The EB is characterized by ancient crustal
relicts as old as 3.8 Ga and wide occurrence of 2.7e2.8 Ga mag-
matism with minor w2.1 Ga and w1.85 Ga magmatism. The WB is
characterized by strong w1.95 Ga, 2.1e2.0 Ga and w2.5 Ga mag-
matism with minor ancient crustal materials as revealed by detrital
zircons. The TNCO is characterized by main w2.5 Ga magmatism
and some 2.3e2.1 Ga magmatism and widespread w1.8 Ga meta-
morphism. However, there is a notable age difference between the
middle and northern parts and southern margin of the TNCO. The
southern margin is featured by widespread occurence of 2.7e2.8 Ga
and even older rocks. and detrital/inherited zircons Conversely,
detrital zircons of quartzite in the Paleoproterozoic Songshan Group
lack w2.1 Ga ages, as documented widely in the Wanzi, Hutou and
Yejishan Groups in the central part of the TNCO.
Zircon Hf isotope data provide another constraint on the
evolution of the NCC. The strongest magmatic event in the NCC
took place at w2.5 Ga, and many geologists consider that the
main crustal-formation occurred at 2.5e2.6 Ga, probably in rela-
tion to mantle plume activity (e.g., Geng et al., 2010). While
zircon Hf isotope data exhibit some notable differences between
different parts of the NCC as mentioned above.
The combined zircon U-Pb ages and Hf isotope compositionscan
provide some constraints on the evolution and tectonic division of
the NCC. Zhao et al. (2007) proposed that the TNCO was an
Andean-type magmatic arc along the western margin of the EB and
separated from the WB by a major ocean, with subduction of the
oceanic lithosphere beneath the western margin of the EB. These
authors suggested that the TNCO is a w700 Ma long-lived accre-
tionary magmatic arc and the closure of the ocean between the EB
and WB at 1880e1820 Ma led to continent-arc-continent collision.
At the same time they also proposed that Neoarchean evolution of
eastern part of the NCC was related to mantle plume activity (Zhao,
2009). This model can reasonably explain the sporadic occurrence
of w2.7 Ga and even older inherited/detrital zircons in the TNCO
and the difference between the ages of detrital zircons in the
Khondalite Belt and supracrustal rocks in the TNCO. The U-Pb and
Hf isotope data of detrital zircons from basin sediments lend support
to collision between the EB and WB during the Paleoproterozoic,
rather than the Archean. However, some geologists propose a two-
stage subduction model involving two collisional events, with the
earlier one leading to the amalgamation of the Fuping and the
eastern (Yanliao) blocks at about 2.1 Ga, and the younger one
leading to final collision and suturing of the western and eastern
blocks at 1.9e1.8 Ga. The main evidence supporting the two-stage
subduction model is the w2.3 Ga mafic-ultramafic intrusion with
positive ε
Nd
(t) values and nearly the same Nd model ages (ranging
from 2643 Ma to 2200 Ma with the majority between 2350 Ma and
2200 Ma) (Liu et al., 2002; Wang et al., 2010a,b). The compiled Hf
isotope data in this study are probably more supportive of the two-
stage model because a weak w2.4 Ga Hf model age peak of
detrital zircons from supracrustal rocks/basin sediments probably
implying the addition of w2.3 Ga depleted mantle material mixed
with some older crustal materials, similar to the Nd-isotope data.
However, because Hf isotope data is sparse and no corresponding Hf
isotope analyses have been carried out for the mafic-ultramafic
rocks, this view is inconclusive and more data are needed to
confirm it or not.
A. Wang, Y. Liu / Geoscience Frontiers 3(2) (2012) 147e173 165
However, Xu et al. (2009) have proposed that the rocks in the
Taihua complex (upper Taihua Group) did not experience w1.85 Ga
metamorphism and the terranes that make up the Taihua Group
(complex) are not the southern extension of the Central zone of the
NCC. In fact, in many aspects the southern margin of the TNCO is
not the same as the middle and northern parts of the TNCO. For
example, 2.7e2.8 Ga and even older rocks are more widely
distributed along the southern margin (Gao et al., 2005a; Liu et al.,
2009b; Diwu et al., 2010), the Dengfeng complex has no evidence
of w1.85 Ga metamorphism and detrital zircons from quartzite
within the Songshan Group lack 2.1e2.0 Ga ages. In addition, the
geochemistry of volcanic rocks of the Angou Group along the
southern margin suggests that the Angou Group formed in a conti-
nental rift setting, rather than in a magmatic arc setting as previously
suggested (Gao et al., 2005b). Wan et al. (2010a,b,c) consider that
there may be a Paleoproterozoic Southern North China Craton
Orogen (SNCCO) extending in a NWWeSEE direction from
Xiaoqinling, through Lushan, Wuyang and Huoqiu, to Bengbu,
finally truncated by the Tanlu Fault in the east, with a total length of
>800 km. Indeed, extensive Paleoproterozoic metamorphism along
the southeastern margin and the southern segment of the Jiao-Liao-Ji
Belt (Zhou et al., 2008; Guo and Li, 2009; Liu et al., 2009a; Tam
et al., 2011a,b), probably supports the existence of the SNCCO.
Thus the Paleoproterozoic evolution of the NCC is more complex
than previously thought.
More and more lines of evidence suggest that the 2.7e2.8 Ga
is an important crustal growth period in the NCC, which is
compatible with the growth of other cratons worldwide. Numerous
investigations also indicate that w2.5 Ga subduction, active
continental margin arc activity and crustal accretion are wide-
spread in the NCC, indicating that the w2.5 Ga crustal growth
occurs in arc setting (Liu et al., 2007; Diwu et al., 2011; Wang
et al., 2011; Zhou et al., 2011). However, it is notable that volu-
minous w2.5 Ga crustal growth occurred in mantle plume setting
(Yang et al., 2008; Grant et al., 2009; Geng et al., 2010; Zhang
et al., 2011a). More work is needed to further constrain the
evolution and tectonic division of the NCC, but there is little doubt
that the 2.7e2.8 Ga crustal-formation is much wider than that
previously considered.
6. Conclusions
From the above zircon Hf isotope data in combination with the age
and geochemistry data, some important conclusions can be drawn
in the following:
(1) Different divisions of the NCC have different zircon Hf
isotope compositions. The Eastern block (EB) is character-
ized by minor crustal growth at w3.4, w3.6 and w3.9 Ga
and the main crustal growth at 2.7e2.8 Ga with local crustal
accretion at 2.5e2.6 Ga; the TNCO is characterized by
2.5e2.8 Ga crustal growth, with some areas being mainly at
2.5e2.6 Ga and other areas at 2.7e2.8 Ga with minor early-
to middle-Archean crustal materials; the Yinshan block is
mainly characterized by w2.7 Ga crustal growth as revealed
by detrital zircons from the Zhaertai Group and supports
source material to the Khondalites; detrital zircons of khon-
dalites in the Khondalite Belt reveal the main crustal-forma-
tion of the Western block (WB) in Paleoproterozoic with
remelting of some 2.6 Ga and minor 2.7 Ga crustal mate-
rials; Paleoproterozoic crustal growth is minor in the eastern
block and TNCO. The crustal growth at w2.5 Ga involve
both arc and mantle plume settings,
(2) The 2.7e2.8 Ga magmatism and crustal growth most prob-
ably occurred widely in the NCC, which is further supported
by the zircon Hf isotope data of modern river sediments,
overlying sedimentary cover, Precambrian lower crustal rocks
and Neoarchean syenogranites. Thus, 2.7e2.8 Ga crustal
growth and magmatism may be underestimated due to strong
2.5e2.6 Ga tectono-thermal events, poor exposure and
insufficient data,
(3) The evolution and tectonic subdivision of the NCC are more
complex than previously suggested, involving multi-stage
crustal growth and multiple tectono-thermal events.
Acknowledgments
This study was supported by the National Natural Science Foun-
dation of China (Grant Nos. 90814008, 40634023 and 40973043)
and the National Basic Research Program of China (Grant No.
2009CB825002). Critical reviews and many useful suggestions by
Prof. M. Santosh, Prof. Guochun Zhao (University of Hong Kong)
and an anonymous reviewer have greatly improved the final
version of the manuscript.
References
Amelin, Y., Lee, D.C., Halliday, A.N., Pidgeon, R.T., 1999. Nature of the
Earth’s earliest crust from hafnium isotopes in single detrital zircons.
Nature 399, 252e255.
Armstrong, R.L., 1981. Radiogenic isotopes: the case for crustal recycling
on a near-steady state no-continental-growth Earth. Philosophical
Transactions of the Royal Society of London. Series A, Mathematical
and Physical Sciences 301, 443e472.
Arnde, N.T., Goldstein, S.L., 1987. Use and abuse of crust-formation ages.
Geology 15, 893e895.
Belousova, E.A., Griffin, W.L., O’Reily, S.Y., Fisher, N.L., 2002. Igneous
zircon: trace element composition as an indicator of source rock type.
Contributions to Mineralogy and Petrology 143, 602e622.
Belousova, E.A., Kobayashi, K.L., Griffin, W.L., Begg, G.S., O’Reilly, S.Y.,
Pearson, D.G., 2010. The growth of the continental crust: constraints
from zircon Hf-isotope data. Lithos 119 (3e4), 457e466.
Bibikova, E., 2003. Isotope-geochemical Characteristics of the Archaean
Sanukitoids: A Review. EGS eAGU eEUG Joint Assembly, Abstracts
from the meeting held in Nice, France, 6e11 April. abstract #1275.
Chen, B., Liu, S.W., Wang, R., Chen, Z.C., Liu, C.Q., 2006a. NdeSr
isotopic geochemistry of the late ArcheanePaleoproterozoic granitoids
in the L€
uliangeWutai Terrain, North China Craton and implications
for petrogenesis. Acta Geologica Sinica 80 (6), 834e843.
Chen, B., Liu, S.W., Geng, Y.S., Liu, C.Q., 2006b. Zircon U-Pb ages, Hf
isotopes and significance of the late ArcheanePaleoproterozoic gran-
itoids from the WutaieL€
uliang terrain, North China. Acta Petrologica
Sinica 22 (2), 269e304 (in Chinese with English abstract).
Chen, L., 2007. Geochronology and Geochemistry of the Guyang Green-
stone Belt. Post-Doctorate Report. Institute of Geology and Geophysics,
Chinese Academy of Sciences, Beijing, pp. 1e40 (in Chinese with
English abstract).
Cherniak, D.J., Watson, E.B., 2000. Pb diffusion in zircon. Chemical
Geology 172, 5e24.
Cherniak, D.J., Watson, E.B., 2003. Diffusion in zircon. Reviews in
Mineralogy and Geochemistry 53, 113e143.
Condie, K.C., 1998. Episodic continental growth and supercontinents:
a mantle avalanche connection? Earth and Planetary Science Letters
163, 97e108.
A. Wang, Y. Liu / Geoscience Frontiers 3(2) (2012) 147e173166
Condie, K.C., 2000. Episodic continental growth models: afterthoughts
and extensions. Tectonphysics 322, 153e162.
Condie, K.C., Belousova, E., Griffin, W.L., Sircombe, K.N., 2009. Gran-
itoid events in space and time: constraints from igneous and detrital
zircon age spectra. Gondwana Research 15, 228e242.
Condie, K.C., Aster, R.C., 2010. Episodic zircon age spectra of orogenic
granitoids: the supercontinent connection and continental growth.
Precambrian Research 180, 227e236.
Dan, W., Li, X.H., Guo, J.H., Liu, Y., Wang, X.C., 2011. Paleoproterozoic
evolution of the eastern Alax block, westernmost North China:
evidence from in situ zircon U-Pb and Hf-O isotopes. Gondwana
Research. doi:10.1016/j.gr.2011.09.004.
Darby, B.J., Gehrels, G., 2006. Detrital zircon reference for the North
China block. Journal of Asian Earth Sciences 26, 637e648.
Diwu, C.R., Sun, Y., Lin, C.L., Liu, X.M., Wang, H.L., 2007. Zricon U-Pb
ages and Hf isotopes and their geological significance of Yiyang TTG
gneisses from Henan Province, China. Acta Petrologica Sinica 23 (2),
253e262 (in Chinese with English abstract).
Diwu, C.R., Sun, Y., Yuan, H.L., Wang, H.L., Zhong, X.P., Liu, X.M.,
2008. U-Pb ages and Hf isotopes for detrital zircons from quartzite in
the Paleoproterozoic Songshan Group on the southwestern margin of
the North China Craton. Chinese Science Bulletin 53 (18), 2828e2839.
Diwu, C.R., Sun, Y., Lin, C.L., Wang, H.L., 2010. LA-(MC)-ICPMS U-Pb
zircon geochronology and Lu-Hf isotope compositions of the Taihua
complex on the southern margin of the North China Craton. Chinese
Science Bulletin 55 (23), 2557e2571.
Diwu, C.R., Sun, Y., Guo, A.L., Wang, H.L., Liu, X.M., 2011. Crustal
growth in the North China Craton at w2.5 Ga: evidence from in situ
zircon U-Pb ages, Hf isotopes and whole-rock geochemistry of the
Deng complex. Gondwana Research 20, 149e170.
Dong, C.Y., Liu, D.Y., Li, J.J., Wan, Y.S., Zhou, H.Y., Li, C.D., Yang, Y.H.,
Xie, L.W., 2007. Paleoproterozoic Khondalite Belt in the western
North China Craton: new evidence from SHRIMP dating and Hf
isotope composition of zircons from metamorphic rocks in the Bayan
U-Helan mountain area. Chinese Science Bulletin 52, 2984e2994.
Dong, C.Y., Liu, D.Y., Wan, Y.S., Xu, Z.Y., Wang, W., Xie, H.Q., 2009. Hf
isotope composition and REE pattern of zircons from early Precam-
brian metamorphic rocks in the Daqing mountains, Inner Mongolia.
Geological Review 55 (4), 509e520 (in Chinese with English abstract).
Du, L.L., Yang, C.H., Zhuang, Y.X., Wei, R.Z., Wan, Y.S., Ren, L.D.,
Hou, K.J., 2010a. Hf isotopic composition of zircons from 2.7 Ga
metasedimentary rocks and biotiteeplagioclase gneiss in the
Mengjiatun formation complex, western Shandong Province.
Acta Geologica Sinica 84 (7), 991e1001 (in Chinese with English
abstract).
Du, L.L., Yang, C.H., Guo, J.H., Wang, W., Ren, L.D., Wan, Y.S.,
Geng, Y.S., 2010b. The age of the base of the Paleoproterozoic Hutuo
Group in the Wutai mountains area, North China Craton: SHRIMP
zircon U-Pb dating of basaltic andesite. Chinese Science Bulletin 55
(3), 246e254.
Faure, M., Lin, W., Moni
e, P., Bruguier, O., 2004. Palaeoproterozoic arc
magmatism and collision in Liaodong Peninsula (north-east China).
Terra Nova 16, 75e80.
Faure, M., Trap, P., Lin, W., Moni
e, P., Bruguier, O., 2007. Polyorogenic
evolution of the Paleoproterozoic Trans-North China Belt, new insights
from the L€
uliangshaneHengshaneWutaishan and Fuping massifs.
Episodes 30, 1e12.
Gao, S., Rudnick, R.L., Yuan, H.L., Liu, X.M., Liu, Y.S., Xu, W.L.,
Ling, W.L., Ayers, J., Wang, X.C., Wang, Q.H., 2004. Recycling lower
continental crust in the North China Craton. Nature 2432, 892e897.
Gao, L.Z., Zhao, T., Wan, Y.S., Zhao, X., Ma, Y.S., Yang, S.Z., 2005a.
Zircon SHRIMP U-Pb age of the Yuntaishan Precambrian meta-
morphic basement, Jiaozuo, Henan, China. Geological Bulletin of
China 24 (12), 1089e1093 (in Chinese with English abstract).
Gao, S., Zhou, L., Ling, W.L., Liu, Y.S., Zhou, D.W., 2005b. Age and
geochemistry of volcanic rocks of Angou Group at the Archeane
Proterozoic boundary. Earth Science-Journal of China University of
Geosciences 30 (3), 259e263 (in Chinese with English abstract).
Gard
es, E., Montel, J.M., 2009. Opening and resetting temperatures in
heating geochronological systems. Contributions to Mineralogy and
Petrology 158, 185e195.
Geng, Y.S., Liu, F.L., Yang, C.H., 2006. Magmatic event at the end of the
Archean in eastern Hebei Province and its geological implication. Acta
Geologica Sinica 80 (6), 819e833.
Geng, Y.S., Shen, Q.H., Ren, L.D., 2010. Late Neoarchean to early Pale-
oproterozoic magmatic events and tectonothermal systems in the North
China Craton. Acta Petrologica Sinica 26 (7), 1945e1966 (in Chinese
with English abstract).
Geng, Y.S., Du, L.L., Ren, L.D., 2011. Growth and reworking of the early
Precambriancontinental crust in the North China Craton: constraints from
zircon Hf isotopes. Gondwana Research. doi:10.1018/j.gr.2011.07.006.
Grant, M.L., Wilde, S.A., Wu, F.Y., Yang, J.H., 2009. The application of
zircon cathodoluminescence imaging Th-U-Pb chemistry and U-Pb
ages in interpreting discrete magmatic and high-grade metamorphic
events in the North China Craton at the Archean/Proterozoic boundary.
Chemical Geology 261, 155e171.
Griffin, W.L., Pearson, N.J., Belousova, E., Jachson, S.E.,
Achterbergh, E.V., O’Reilly, Y., Shee, S.R., 1999. The Hf isotope
composition of cratonic mantle: LAM-MC-ICPMS analysis of zircon
megacrysts in kimberlites. Geochimica et Cosmochimica Acta 64 (1),
133e147.
Griffin, W.L., Wang, X., Jackson, S.E., Pearson, N.J., O’Reilly, S.Y.,
Xu, W., Zhou, X., 2002. Zircon chemistry and magma mixing, SE
China: in-situ analysis of Hf isotopes, Tonglu and Pingtan igneous
complexes. Lithos 51, 237e269.
Guan, H., Sun, M., Wilde, S.A., Zhou, X.H., Zhai, M.G., 2002. SHRIMP
U-Pb zircon geochronology of the Fuping complex: implications for
formation and assembly of the North China Craton. Precambrian
Research 113, 1e18.
Guo, J.H., Zhai, M.G., 2001. Sm-Nd age dating of high-pressure granulites
and amphibolites from the Sanggan area, North China Craton. Chinese
Science Bulletin 46, 106e110.
Guo, J.H., Sun, M., Chen, F.K., Zhai, M.G., 2005. Sm-Nd and SHRIMP
U-Pb zircon geochronology of high-pressure granulites in the Sanggan
area, North China Craton: timing of Paleoproterozoic continental
collision. Journal of Asian Earth Sciences 24, 629e642.
Guo, J.H., Chen, Y., Peng, P., Liu, F., Chen, L., Zhang, L.Q., 2006.
Sapphirine granulite from Daqingshan area, inner Modolia-1.85 Ga
ultrahigh temperature (UHT) metamorphism. In: Proceedings of
National Conference on Petrology and Geodynamics in China (Nanj-
ing), pp. 215e218 (in Chinese).
Guo, L.S., Liu, S.W., Liu, Y.L., Tian, W., Yu, S.Q., L€
u, Y.J., 2008. Zircon
Hf isotopic features of TTG gneisses and formation environment of
Precambrian Sushui complex in Zhongtiao mountains. Acta Petrolog-
ica Sinica 24 (1), 139e148 (in Chinese with English abstract).
Guo, S.S., Li, S.G., 2009. SHRIMP zircon U-Pb ages for the Paleo-
proterozoic metamorphicemagmatic events in the southeastern margin
of the North China. Science China Series D-Earth Science 52 (8),
1039e1045.
Halls, H.C., Li, J.H., Davis, D., Hou, G.T., Zhang, B.X., Qian, X.L., 2000.
A precisely dated Proterozoic palaeomagnetic pole from the North
China Craton, and its relevance to palaeocontinental reconstruction.
Geophysics Journal of International 143, 185e203.
Hawkesworth, C.J., Kemp, A.I.S., 2006. Using hafnium and oxygen
isotopes in zircons to unravel the record of crustal evolution. Chemical
Geology 226, 144e162.
He, Y., Zhao, G., Sun, M., Xia, X., 2009. SHRIMP and LA-ICP-MS zircon
geochronology of the Xiong’er volcanic rocks: implications for the
PaleoeMesoproterozoic evolution of the southern margin of the North
China Craton. Precambrian Research 168, 213e222.
Hermann, J., Rubatto, D., Korsakov, A., 2001. Multiple zircon growth
during fast exhumation of diamond-iferous, deeply subducted conti-
nental crust (Kokchetav massif, Kazakhstan). Contributions to Miner-
alogy and Petrology 141, 66e82.
Huang, J.Q., 1977. The basic outline of China tectonics. Acta Geologica
Sinica 52, 117e135 (in Chinese).
A. Wang, Y. Liu / Geoscience Frontiers 3(2) (2012) 147e173 167
Huang, X.L., Niu, Y.L., Xu, Y.G., Yang, Q.J., Zhong, J.W., 2010.
Geochemistry of TTG and TTG-like gneisses from LushaneTaihua
complex in the southern North China Craton: implications for late
Archean crustal accretion. Precambrian Research 182, 43e56.
Hurley, P.M., Rand, J.R., 1969. Pre-drift continental nuclei. Science 164,
1229e1242.
Moorbath, S., 1978. Age and isotope evidence for evolution of continental
crust. Philosophical Transactions of the Royal Society of London.
Series A, Mathematical and Physical Sciences 288, 401e412.
Hou, G.T., Li, J.H., Yang, M.H., Yao, W.H., Wang, C.C., Wang, Y.X.,
2008. Geochemical constraints on the tectonic environment of the late
Paleoproterozoic mafic dyke swarms in the North China Craton.
Gondwana Research 13, 103e116.
Iizuka, T., Komiya, T., Rino, S., Maruyama, S., Hirata, T., 2010. Detrital
zircon evidence for Hf isotopic evolution of granitoid crust and
continental growth. Geochimica et Cosmochimica Acta 74,
2450e2472.
Jahn, B.M., Auvray, B., Cornichet, J., Bai, Y.L., Shen, Q.H., Liu, D.Y.,
1987. 3.5 Ga old amphibolites from eastern Hebei Province, China:
field occurrence, petrography, Sm-Nd isochron age and REE
geochemistry. Precambrian Research 34, 311e346.
Jahn, B.M., Auvray, B., Shen, Q.H., Liu, D.Y., Zhang, Z.Q., Dong, Y.J.,
Ye, X.J., Zhang, Q.Z., Cornichet, J., Mace, J., 1988. Archean crustal
evolution in China: the Taishan complex, and evidence for juvenile
crustal addition from long-term depleted mantle. Precambrian
Research 38, 381e403.
Jahn, B.M., Liu, D., Wan, Y., Song, B., Wu, J., 2008. Archean crustal
evolution of the Jiadong Peninsula, China, as revealed by zircon
SHRIMP geochronology, elemental and Nd-isotope geochemistry.
American Journal of Science 308, 232e269.
Jiang, N., Guo, J.H., Zhai, M.G., Zhang, S.Q., 2010. ～2. Ga crust growth
in the North China Craton. Precambrian Research 179, 37e49.
Jian, P., Zhang, Q., Liu, D.Y., Jin, W.J., Jia, X.Q., Qian, Q., 2005. SHRIMP
dating and geological significance of late Archaean high-Mg diorite
(sanukite) and hornblende-granite at Guyang of Inner Mongolia. Acta
Petrologica Sinica 21 (1), 151e157 (in Chinese with English abstract).
Jiao, S.J., Guo, J.H., 2011. Application of the two-feldspar geo-
thermometer to ultrahigh-temperature (UHT) rocks in the Khondalite
Belt, North China Craton and its implications. American Mineralogist
96, 250e260.
Jiao, S.J., Guo, J.H., Mao, Q., Zhao, R., 2011. Application of the Zr-in-
rutile thermometry: a case study from ultrahigh temperature granu-
lites of the Khondalite Belt, North China Craton. Contributions to
Mineralogy and Petrology 162, 379e393.
King, E.W., Valley, J.W., Davis, D.W., Edwards, G.R., 1998. Oxygen
isotope ratios of Archaean plutonic zircons from graniteegreenstone
belts of the Superior Province: indicator of magmatic source.
Precambrian Research 92, 47e67.
Kovalenko, A., Clemens, J.D., Savatenkov, V., 2005. Petrogenetic
constraints for the genesis of Archaean sanukitoid suites: geochemistry
and isotopic evidence from Karelia, Baltic Shield. Lithos 79, 147e160.
Krabbendam, M., Prave, T., Cheer, D., 2008. A fluvial origin for the
Neoproterozoic Morar Group, NW Scotland: implications for Torrid-
oneMorar Group correlation and the Grenville Orogen foreland basin.
Journal of the Geological Society 165, 379e394.
Kr€
oner, A., Compston, W., Zhang, G.W., Guo, A.L., Todt, W., 1988. Age
and tectonic setting of late Archean greenstoneegneiss terrain in
Henan Province, China, as revealed by single-grain zircon dating.
Geology 16, 211e215.
Kr€
oner, A., Cui, W.Y., Wang, S.Q., Wang, C.Q., Nemchin, A.A., 1998.
Single zircon ages from high-grade rocks of the Jianping complex,
Liaoning Province, NE China. Journal of Asian Earth Sciences 16,
519e532.
Kr€
oner, A., Wilde, S.A., O’Brien, P.J., Li, J.H., Passchier, C.W.,
Walte, N.P., Liu, D.Y., 2005a. Field relationships, geochemistry, zircon
ages and evolution of a late Archaean to Palaeoproterozoic lower
crustal section in the Hengshan Terrain of North China. Acta Geo-
logica Sinica 79 (5), 605e629.
Kr€
oner, A., Wilde, S.A., Li, J.H., Wang, K.Y., 2005b. Age and evolution of
a late Archean to Paleoproterozoic upper to lower crustal section in the
Wutaishan/Hengshan/Fuping terrain of northern China. Journal of
Asian Earth Sciences 24, 577e595.
Kr€
oner, A., Wilde, S.A., Zhao, G.C., O’Brien, P.J., Sun, M., Liu, D.Y.,
Wan, Y.S., Liu, S.W., Guo, J.H., 2006. Zircon geochronology and
metamorphic evolution of mafic dykes in the Hengshan complex of
northern China: evidence for late Paleoproterozoic extension and
subsequent high-pressure metamorphism in the North China Craton.
Precambrian Research 146, 45e67.
Kr€
oner, A., 2010. The Role of Geochronology in Understanding Conti-
nental Evolution, vol. 338. Geological Society of London, Special
Publications. 179e196.
Kusky, T.M., Li, J.H., 2003. Paleoproterozoic tectonic evolution of the
North China Craton. Journal of Asian Earth Sciences 22, 383e397.
Kusky, T.M., Windley, B.F., Zhai, M.G., 2007a. Tectonic Evolution of the
North China Block: From Orogen to Craton to Orogen. Geological
Society of London, Special Publications. vol. 280, 1e34.
Kusky, T.M., Li, J.H., Santosh, M., 2007b. The Paleoproterozoic north
Hebei Orogen: North China Craton’s collisional suture with the
Columbia supercontinent. Gondwana Research 12, 4e28.
Kusky, T.M., 2011. Geophysical and geological tests of tectonic models of
the North China Craton. Gondwana Research 20 (1), 26e35.
Lee, J., Williams, I., Eillis, D., 1997. Pb, U and Th diffusion in nature
zircon. Nature 390, 159e162.
Li, S.Z., Zhao, G.C., Sun, M., Han, Z.Z., Luo, Y., Hao, D.F., Xia, X.P.,
2005. Deformation history of the Paleoproterozoic Liaohe assemblage
in the eastern block of the North China Craton. Journal of Asian Earth
Sciences 24, 659e674.
Li, S.Z., Zhao, G.C., Sun, M., Han, Z.Z., Zhao, G.T., Hao, D.F., 2006. Are the
south and north Liaohe Groups of North China Craton different exotic
terranes? Nd isotope constraints. Gondwana Research 9, 198e208.
Li, J.H., Kusky, T., 2007. A late Archean foreland fold and thrust belt in
the North China Craton: implications for early collisional tectonics.
Gondwana Research 12, 47e66.
Li, S.Z., Zhao, G.C., 2007. SHRIMP U-Pb zircon geochronology of the
Liaoji granitoids: constraints on the evolution of the Paleoproterozoic
Jiao-Liao-Ji Belt in the eastern block of the North China Craton.
Precambrian Research 158, 1e16.
Li, Q.L., Chen, F., Guo, J., Li, X.H., Yang, Y.H., Siebel, W., 2007. Zricon
ages and Nd-Hf isotopic composition of the Zhaertai Group (Inner
Mongolia): evidence for early Proterozoic evolution of the northern
North China Craton. Journal of Asian Earth Sciences 30, 573e590.
Li, Q.G., Liu, S.W., Wang, Z.Q., Chu, Z.Y., Song, B., Wang, Y.B.,
Wang, T., 2008. Contrasting provenance of late Archean metasedi-
mentary rocks from the Wutai complex, North China Craton: detrital
zircon U-Pb, whole-rock Sm-Nd isotopic, and geochemical data.
International Joural of Earth Science 97, 443e458.
Li, T.S., Zhai, M.G., Peng, P., Chen, L., Guo, J.H., 2010. Ca.2.5 billion
year old coeval ultramafic-mafic and syenitic dykes in eastern Hebei:
implications for cratonization of the North China Craton. Precambrian
Research 180, 143e155.
Li, X.P., Yang, Z.Y., Zhao, G.C., Grapes, R., Guo, J.H., 2011a. Geochro-
nology of khondalite-series rocks of the Jining complex: confirmation
of depositional age and tectonometamorphic evolution of the North
China Craton. International Geology Review 53 (10), 1194e1211.
Li, S.Z., Zhao, G.C., Santosh, M., Liu, X., Dai, L.M., 2011b. Palae-
oproterozoic tectonothermal evolution and deep crustal processes in
the Jiao-Liao-Ji Belt, North China Carton: a review. Geological Jour-
nal. doi:10.1002/gj.1282.
Liu, D.Y., Nutman, A.P., Compston, W., Wu, J.S., Shen, Q.H., 1992.
Remnants of 3800 Ma crust in the Chinese part of the Sino-Korean
craton. Geology 20, 339e342.
Liu, S.W., Pan, Y.M., Li, J.H., Li, Q.G., Zhang, J., 2002. Geological and
isotopic geochemical constraints on the evolution of the Fuping
complex, North China Craton. Precambrian Research 117, 41e56.
Liu, S.W., Zhao, G.C., Wilde, S.A., Shu, G.M., Sun, M., Li, Q.G.,
Tian, W., Zhang, J., 2006a. Th-U-Pb monazite geochronology of the
A. Wang, Y. Liu / Geoscience Frontiers 3(2) (2012) 147e173168
L€
uliang and Wutai complex: constraints on the tectonothermal evolu-
tion of the Trans-North China Orogen. Precambrian Research 148,
205e224.
Liu, C.H., Liu, S.W., Li, Q.G., L€
u, Y.J., Park, K.H., Song, Y.S., 2006b.
Petrogenesis of the Paleoproterozoic Guandishan Granitoids in Shanxi
Province: constraints from geochemistry and Nd isotopes. Acta Geo-
logica Sinica 80 (6), 925e935.
Liu, D.Y., Wan, Y.S., Wu, J.S., Wilde, S.A., Zhou, H.Y., Dong, C.Y.,
Yin, X.Y., 2007. Eoarchean rocks and zircons in the North China
Craton. In: Van Kranendonk, M.J., Smithies, R.H., Bennett., V. (Eds.),
Earth’s Oldest Rocks, pp. 251e273.
Liu, D.Y., Wilde, S.A., Wan, Y.S., Wu, J.S., Zhou, H.Y., Dong, C.Y.,
Yin, X.Y., 2008. New U-Pb and Hf isotopic data confirm Anshan as the
oldest preserved segment of the North China Craton. American Journal
of Science 308, 200e231.
Liu, Y.C., Wang, A.D., Rolfo, F., Groppo, C., Gu, X.F., Song, B., 2009a.
Geochronological and petrological constraints on Paleoproterozoic
granulite facies metamorphism in southeastern margin of the North
China Craton. Journal of Metamorphic Geology 27, 125e138.
Liu, F., Guo, J.H., Lu, X.P., Diwu, C.R., 2009b. Crustal growth at w2.5 Ga
in the North China Craton: evidence from whole-rock Nd and zircon
Hf isotopes in the Huai’an gneiss terrane. Chinese Science Bulletin 54,
4704e4713.
Liu, D.Y., Wilde, S.A., Wan, Y.S., Guo, A.L., Wang, H.L., Liu, X.M.,
2009c. Combined U-Pb, hafnium and oxygen isotope analysis of
zircons from meta-igneous rocks in the southern North China Craton
reveal multiple events in the late Mesoarcheaneearly Neoarchean.
Chemical Geology 261, 139e153.
Liu, S.J., Li, J.H., Santosh, M., 2010. First application of the revised Ti-in-
zircon geothermometer to Paleoproterozoic ultrahigh-temperature
granulites of Tuguiwala, Inner Mongolia, North China Craton.
Contributions to Mineralogy and Petrology 159, 225e235.
Liu, S.W., Santosh, M., Wang, B.W., Bai, X., Yang, P.T., 2011a. Zircon
U-Pb chronology of the Jianping complex: implications fro the
Precambrian crustal evolution history of the northern margin of North
China Craton. Gondwana Research 20, 48e63.
Liu, S.W., L€
u, Y.J., Wang, W., Yang, P.T., Bai, X., Feng, Y.G., 2011b.
Petrogenesis of the Neoarhean granitoid gneisses in northern Hebei
Province. Acta Petrologica Sinica 27 (4), 909e921 (in Chinese with
English abstract).
Liu, C.H., Zhao, G.C., Sun, M., Zhang, J., He, Y.H., Yin, C.Q., Wu, F.Y.,
Yang, J.H., 2011c. U-Pb and Hf isotopic study of detrital zircons from
the Hutuo Group in the Trans-North China Orogen and its tectonic
implications. Gondwana Research 20, 106e121.
Liu, C.H., Zhao, G.C., Sun, M., Wu, F.Y., Yang, J.H., Yin, C.Q.,
Leung, W.H., 2011d. U-Pb and Hf isotopic study of detrital zircons
from the Yejishan Group of the L€
uliang complex: constraints on the
timing of collision between the eastern and western blocks, North
China Craton. Sedimentary Geology 236, 129e140.
Liu, C.H., Zhao, G.C., Sun, M., Zhang, J., Yin, C.Q., 2011e. U-Pb
geochronology and Hf isotope geochemistry of detrital zircons from the
Zhongtiao complex: constraints on the tectonic evolution of the
Trans-North China Orogen. Precambrian Research. doi:10.1016/
j.precamres.2011.08.007.
Liu, Y.-C., Gu, X., Li, S., Hou, Z.H., Song, B., 2011f. Multistage meta-
morphic events in granulitized eclogites from the north Dabie complex
zone, central China: evidence from zircon U-Pb age, trace element and
mineral inclusion. Lithos 122, 107e121.
Lu, S.N., Yang, C.L., Li, H.K., Li, H.M., 2002. A group of rifting events in
the terminal Paleoproterozoic in the North China Craton. Gondwana
Research 5 (1), 123e131.
Lu, X.P., Wu, F.Y., Lin, J.Q., Sun, D.Y., Zhang, Y.W., Guo, G.L., 2004.
Geochronological successions of the early Precambrian granitic mag-
matism in southern Liaodong Peninsula and its constraints on tectonic
evolution of the North China Craton. Chinese Journal of Geology 39
(1), 123e138 (in Chinese with English abstract).
Lu, X.P., Wu, F.Y., Guo, J.H., Wilde, S.A., Yang, J.H., Liu, X.M.,
Zhang, X.O., 2006. Zircon U-Pb geochronological constraints on the
Paleoproterozoic crustal evolution of the eastern block in the North
China Craton. Precambrian Research 146, 138e164.
Lu, S.N., Zhao, G.C., Wang, H.C., Hao, G.J., 2008. Precambrian meta-
morphic basement and sedimentary cover of the North China Craton:
a review. Precambrian Research 160, 77e93.
Luo, Y., Sun, M., Zhao, G.C., Li, S.Z., Xu, P., Ye, K., Xia, X.P., 2004. LA-
ICP-MS U-Pb zircon ages of the Liaohe Group in the eastern block of
the North China Craton: constraints on the evolution of the Jiao-Liao-Ji
Belt. Precambrian Research 134, 349e371.
Luo, Y., Sun, M., Zhao, G.C., Li, S.Z., Xia, X.P., 2006. La-ICP-MS U-Pb
zircon geochronology of the Yushulazi Group in the eastern block,
North China Craton. International Geology Review 48, 828e840.
Luo, Y., Sun, M., Zhao, G.C., Ayers, J.C., Li, S.Z., Xia, X.P., Zhang, J.H.,
2008. A comparison of U-Pb and Hf isotopic composition of detrital
zircons from the north and south Liaohe Group: constraints on the
evolution of the Jiao-Liao-Ji Belt, North China Craton. Precambrian
Research 163, 279e306.
M€
oller, A., O’Broen, P.J., Kennedy, A., Kr€
oner, A., 2003. Linking Growth
Episodes of Zircon and Metamorphic Textures to Zircon Chemistry:
An Example from the Ultrahigh-temperature Granulites of Rogaland
(SW Norway), vol. 220. Geological Society of London, Special
Publications. 65e81.
Nutman, A.P., Wan, Y.S., Liu, D.Y., 2009. Integrated field geological and
zircon morphology evidence for ca.3.8 Ga rocks at Anshan: comment
on “zircon U-Pb and Hf isotopic constraints of the early Archean
crustal evolution in Anshan of the North China Craton” by Wu et al.
Precambrian Research 167 (2008), 339e362. Precambrian Research
172, 357e360.
Nutman, A.P., Wan, Y.S., Du, L.L., Friend, C.R.L., Dong, C.Y., Xie, H.Q.,
Wang, W., Sun, H.Y., Liu, D.Y., 2011. Multistage late Neoarchaean
crustal evolution of the North China Craton, eastern Hebei. Precam-
brian Research 189 (1e2), 43e65.
Peng, P., Zhai, M.G., Ernst, R.E., Guo, J.H., Liu, F., Hu, B., 2008. A 1.78 Ga
large igneous province in the North China Craton: the Xiong’er Volcanic
Province and the North China dyke swarm. Lithos 101, 260e280.
Peng, P., 2010. Reconstruction and Interpretation of Giant Mafic Dyke
Swarms: A Case Study of 1.78 Ga Magmatism in the North China
Craton, vol. 338. Geological Society of London, Special Publications.
163e178.
Piper, J.D.A., Zhang, J.S., Huang, B.C., Roberts, A.P., 2011. Palae-
omagnetism of Precambrian dyke swarms in the North China shield:
the ～1.8 Ga LIP event and crustal consolidation in late Palae-
oproterozoic times. Journal of Asian Earth Sciences 41, 504e524.
Polat, A., Kusky, T., Li, J.H., Fryer, B., Kerrich, R., Patrick, K., 2005.
Geochemistry of Neoarchean (ca. 2.55e2.50 Ga) volcanic and
ophiolitic rocks in the Wutaishan greenstone belt, central orogenic belt,
North China Craton: implications for geodynamic setting and conti-
nental growth. GSA Bulletin 117 (11e12), 1387e1399.
Polat, A., Li, J., Fryer, B., Kusky, T., Gagnon, J., Zhang, S., 2006.
Geochemical characteristics of the Neoarchean (2800e2700 Ma)
Taishan greenstone belt, North China Craton: evidence for plumee
craton interaction. Chemical Geology 230, 60e87.
Ren, R., Han, B.F., Zhang, Z.C., Li, J.F., Yang, Y.H., Zhang, Y.B., 2011.
Zircon U-Pb and Hf isotopic studies of basement gneiss and overlying
MesoeNeoproterozoic sedimentary rocks from the Changping area,
Beijing, and their geological implications. Acta Petrologica Sinica 27
(6), 1721e1745 (in Chinese with English abstract).
Rion, S.,Komiya, T., Windley, B.F., Katayama,I., Motoki, A.,Hirata, T.,2004.
Major episodic increase of continental crustal growth determined from
zircon ages of river sands: implications for mantle overturns in the early
Precambrian. Physics of the Earth and Planetary Interiors 146, 369e394.
Safonova, I., Maruyama, S., Hirata, T., Kon, Y., Rino, S., 2010. LA ICP
MS U-Pb ages of detrital zircons from Russia largest rivers: implica-
tions for major granitoid events in Eurasia and global episodes of
supercontinent formation. Journal of Geodynamics 50, 134e153.
Santosh, M., Sajeev, K., Li, J.H., 2006. Extreme crustal metamorphism
during Colombia supercontinent assembly: evidence from North China
Craton. Gondwana Research 10, 256e266.
A. Wang, Y. Liu / Geoscience Frontiers 3(2) (2012) 147e173 169
Santosh, M., Wilde, S.A., Li, J.H., 2007. Timing of Paleoproterozoic
ultrahigh-temperature metamorphism in the North China Craton:
evidence from SHRIMP U-Pb zircon geochronology. Precambrian
Research 159, 178e196.
Santosh, M., Tsunogae, T., Ohyama, H., Sato, K., Li, J.H., Liu, S.J., 2008.
Carbonic metamorphism at ultrahigh-temperatures: evidence from
North China Craton. Earth and Planetary Science Letters 266,
149e165.
Santosh, M., Wan, Y.S., Liu, D.Y., Dong, C.Y., Li, J.H., 2009. Anatomy of
zircons from an ultra-hot Orogen: suturing the North China Craton
within Columbia supercontinent. Journal of Geology 117, 429e443.
Santosh, M., 2010. Assembling North China Craton within the Columbia
supercontinent: the role of double-sided subduction. Precambrian
Research 178, 149e167.
Santosh, M., Liu, S.J., Tsunogae, T., Li, J.H., 2011. Paleoproterozoic
ultrahigh-temperature granulites in the North China Craton: implica-
tions for tectonic models on extreme crustal metamorphism. Precam-
brian Research. doi:10.1016/j.precamres.2011.05.003.
Shen, Q.H., Geng, Y.S., Song, B., Wan, Y.S., 2005. New information from
the surface outcrops and deep crust of Archaean rocks of the North
China and Yangtze blocks, and Qinling-Dabie Orogen Belt. Acta
Geologica Sinica 79, 616e627 (in Chinese).
Shirey, S.B., Hanson, G.N., 1984. Mantle-derived Archaean monzodiorites
and trachyandesites. Nature 310, 222e224.
Smithise, R.H., Champion, D.C., 2000. The Archaean high-Mg diorite
suite: links to tonaliteetrondhjemiteegranodiorite magmatism and
implications for early Archaean crustal growth. Journal of Petrology 41
(12), 1653e1671.
Song, B., Nutman, A.P., Liu, D.Y., Wu, J.S., 1996. 3800 to 2500 Ma crustal
evolution in Anshan area of Liaoning Province, northeastern China.
Precambrian Research 78, 79e94.
Tam, P.Y., Zhao, G.C., Liu, F.L., Zhou, X.W., Liu, X.M., Sun, M., Li, S.Z.,
2011a. Timing of metamorphism in the Paleoproterozoic Jiao-Liao-Ji
Belt: new SHRIMP U-Pb zircon dating of granulites, gneisses and
marbles of the Jiaobei massif in the North China Craton. Gondwana
Research 19, 150e162.
Tam, P.Y., Zhao, G.C., Zhou, X.W., Sun, M., Guo, J.H., Li, S.Z., Yin, C.Q.,
Wu, M.L., He, Y.H., 2011b. Metamorphic PeT path and implications
of high-pressure politic granulites from the Jiaobei massif in the Jiao-
Liao-Ji Belt, North China Craton. Gondwana Research. doi:10.1016/
j.gr.2011.09.006.
Tang, J., Zheng, Y.F., Wu, Y.B., Gong, B., Liu, X.M., 2007. Geochro-
nology and geochemistry of metamorphic rocks in the Jiaobei terrane:
constraints on its tectonic affinity in the Sulu Orogen. Precambrian
Research 152, 48e82.
Trap, P., Faure, M., Lin, W., Moni
e, P., 2007. Late Paleoproterozoic
(1900e1800 Ma) nappe-stacking and polyphase deformation in the
HengshaneWutaishan area: implications for the understanding of the
Trans-North-China Belt, north China Craton. Precambrian Research
156, 85e106.
Trap, P., Faure, M., Lin, W., Bruguier, O., Moni
e, P., 2008. Contrasted
tectonic styles for the Paleoproterozoic evolution of the North China
Craton. Evidence for a 2.1 Ga thermal and tectonic events in the
Fuping massif. Journal of Structural Geology 30, 1109e1125.
Trap, P., Faure, M., Lin, W., Moni
e, P., Meffre, S., Melleton, J., 2009a. The
Zanhuang massif, the second and eastern suture zone of the Paleoproter-
ozoic Trans-North China Orogen. Precambrian Research 172, 80e98.
Trap, P., Faure, M., Lin, W., Moni
e, P., Meffre, S., 2009b. The L€
uliang
Massif: A Key Area for the Understanding of the Palaeoproterozoic.
Geological Society of London, Special Publications, vol, 323. 99e125.
Trap, P., Fuare, M., Lin, W., Augier, R., Fouassier, A., 2011. Syn-colli-
sional channel flow and exhumation of Paleoproterozoic high pressure
rocks in the Trans-North China Orogen: the critical role of partial-
melting and orogenic bending. Gondwana Research 20 (2e3),
498e515.
Tsunogae, T., Liu, S.J., Santosh, M., Shimizu, H., Li, J.H., 2011. Ultra-
high-temperature metamorphism in Daqingshan, inner Mongolia suture
zone, North China Craton. Gondwana Research 20 (1), 36e47.
Vervoort, J.D., Patchett, P.J., 1996. Behaviour of hafnium and neodymium
isotope in the crust: constraints from Precambrian crustally-derived
granites. Geochimica et Cosmochimica Acta 60, 3717e3733.
Vervoort, J.D., Blichert-Toft, J., 1999. Evolution of the depleted mantle: Hf
isotope evidence from juvenile rocks through time. Geochimica et
Cosmochimica Acta 63, 533e566.
Wan, Y.S., Zhang, Q.D., Song, T.R., 2003. SHRIMP ages of detrital
zircons from the Changcheng System in the Ming Tombs area, Beijing:
constraints on the protolith nature and maximum depositional age of
the Mesoproterozoic cover of the North China Craton. Chinese Science
Bulletin 48 (22), 2500e2506.
Wan, Y.S., Liu, D.Y., Song, B., Wu, J.S., Yang, C.H., Zhang, Z.Q.,
Geng, Y.S., 2005. Geochemical and Nd isotopic compositions of 3.8
Ga meta-quartz dioritic and trondhjemitic rocks from the Anshan area
and their geological significance. Journal of Asian Earth Sciences 24,
563e575.
Wan, Y.S., Song, B., Liu, D.Y., Wilde, S.A., Wu, J.S., Shi, Y.R., Yin, X.Y.,
Zhou, H.Y., 2006a. SHRIMP U-Pb zircon geochronology of Palae-
oproterozoic metasedimentary rocks in the North China Craton:
evidence for major late Palaeoproterozoic tectonothermal event.
Precambrian Research 149, 249e271.
Wan, Y.S., Wilde, S.A., Liu, D.Y., Yang, C.X., Song, B., Yin, X.Y., 2006b.
Further evidence for w1.85 Ga metamorphism in the central zone of
the North China Craton: SHRIMP U-Pb dating of zircon from meta-
morphic rocks in the Lushan area, Henan Province. Gondwana
Research 9, 189e197.
Wan, Y.S., Liu, D.Y., Dong, C.Y., Nutman, A., Wilde, S.A., Wang, W.,
Xie, H.Q., Yin, X.Y., Zhou, H.Y., 2009a. The oldest rocks and zircons
in China. Acta Petrologica Sinica 25, 1793e1807 (in Chinese with
English abstract).
Wan, Y.S., Liu, D.Y., Dong, C.Y., Xu, Z.Y., Wang, Z.J., Wilde, S.A.,
Yang, Y.H., Liu, Z.H., Zhou, H.Y., 2009b. The Precambrian Khondalite
Belt in the Daqingshan area, North China Craton: evidence for multiple
metamorphic events in the Palaeoproterozoic era. Journal of the Lon-
don Geological Society, Special Publications 323, 73e97.
Wan, Y.S., Liu, D.Y., Wang, S.Y., Zhao, X., Dong, C.Y., 2009c. Early
Precambrian crustal evolution in the Dengfeng area, Henan Province
(eastern China): constraints from geochemistry and SHRIMP U-Pb
zircon dating. Acta Geologica Sinica 83 (7), 982e999 (in Chinese with
English abstract).
Wan, Y.S., Liu, D.Y., Wang, S.J., Dong, C.Y., Yang, E.X., Wang, W.,
Zhou, H.Y., Ning, Z.G., Du, L.L., Yin, X.Y., Xie, H.Q., Ma, M.Z.,
2010a. Juvenile magmatism and crustal recycling at the end of the
Neoarchean in western Shandong Province, North China Craton:
evidence from SHRIMP zircon dating. American Journal of Science
210, 1503e1552.
Wan, Y.S., Miao, P.S., Liu, D.Y., Yang, C.H., Wang, W., Wang, H.C.,
Wang, Z.J., Dong, C.Y., Du, L.L., Zhou, H.Y., 2010b. Formation ages
and source regions of the Paleoproterozoic Gaofan, Hutuo and Dong-
jiao groups in the Wutai and Dongjiao areas of the North China Craton
from SHRIMP U-Pb dating of detrital zircons: resolution of debates
over their straigraphic relationships. Chinese Science Bulletin 55 (7),
572e578.
Wan, Y.S., Dong, C.Y., Wang, W., Xie, H.Q., Liu, D.Y., 2010c. Archean
basement and a Paleoproterozoic collision Orogen in the Huoqiu are at
the southeastern margin of North China Craton: evidence from sensi-
tive high resolution ion micro-probe U-Pb zircon geochronology. Acta
Geologica Sinica 84 (1), 91e104.
Wan, Y.S., Liu, D.Y., Wang, W., Song, T.R., Kr€
oner, A., Dong, C.Y.,
Zhou, H.Y., Yin, X.Y., 2011a. Provenance of Meso- to Neoproterozoic
cover sediments at the Ming Tombs, Beijing, North China Craton: an
integrated study of U-Pb dating and Hf isotopic measurement of
detrital zircons and whole-rock geochemistry. Gondwana Research 20,
219e242.
Wan, Y.S., Liu, D.Y., Wang, S.J., Yang, E.X., Wang, W., Dong, C.Y.,
Zhou, H.Y., Du, L.L., Yang, Y.H., Diwu, C.R., 2011b. w2.7 Ga
juvenile crust formation in the North China Craton (TaishaneXintai
area, western Shandong Province): further evidence of an understated
A. Wang, Y. Liu / Geoscience Frontiers 3(2) (2012) 147e173170
event from U-Pb dating and Hf isotopic composition of zircon.
Precambrian Research 186 (1e4), 169e180.
Wan, Y.S., Dong, C.Y., Liu, D.Y., Kr€
oner, A., Yang, C.H., Wang, W.,
Du, L.L., Xie, H.Q., Ma, M.Z., 2011c. Zircon ages and geochemistry
of late Neoarchean syenogranites in the North China Craton: a review.
Precambrian Research. doi:10.1016/j.precamres.2011.05.001.
Wang, Z.H., Wilde, S.A., Wang, K.Y., 2004. A MORB-arc basalteadakite
association in the 2.5 Ga Wutai greenstone belt: late Archean mag-
matism and crustal growth in the North China Craton. Precambrian
Research 131, 323e343.
Wang, Y.J., Zhao, G.C., Cawood, P.A., Fan, W.M., Peng, T.P., Sun, L.H.,
2008. Geochemistry of Paleoproterozoic (w1770 Ma) mafic dikes
from the Trans-North China Orogen and tectonic implications. Journal
of Asian Sciences 33, 61e77.
Wang, Y.J., Zhang, Y.Z., Zhao, G.C., Fan, W.M., Xia, X.P., Zhang, F.F.,
Zhang, A.M., 2009. Zircon U-Pb geochronological and geochemical
constraints on the petrogenesis of the Taishan sanukitoids (Shandong):
implications for Neoarchean subduction in the east block, North China
Craton. Precambrian Research 174, 273e286.
Wang, Z.H., 2009. Tectonic evolution of the HengshaneWutaieFuping
complexes and its implication for the Trans-North China Orogen.
Precambrian Research 170, 73e87.
Wang, J., Wu, Y., Gao, S., Peng, M., Liu, X.C., Zhao, L.S., Zhou, L.,
Hu, Z.C., Gong, H.J., Liu, Y.S., 2010a. Zircon U-Pb and trace element
data from rocks of the Huai’an complex: new insights into the late
Paleoproterzoic collision between the eastern and western blocks of the
North China Craton. Precambrian Research 178, 59e71.
Wang, Z.H., Wilde, S.A., Wang, J.L., 2010b. Tectonic setting and signif-
icance of 2.3e2.1 Ga magmatic events in the Trans-North China
Orogen: new constraints from the Yanmenguan mafic-ultramafic
intrusion in the HengshaneWutaieFuping area. Precambrian
Research 178, 27e42.
Wang, W., Liu, S., Bai, X., Yang, P., Li, Q., Zhang, L., 2011. Geochemistry
and zircon U-Pb-Hf isotopic systematics of the Neoarchean Yix-
ianeFuxin greenstone belt, northern margin of the North China Craton:
implications for petrogenesis and tectonic setting. Gondwana Research
20 (1), 64e81.
Wilde, S.A., Cawood, P.A., Wang, K.Y., 1997. The Relationship and
Timing of Granitoid Evolution with Respect to Felsic Volcanism in the
Wutai Complex, North China Craton. Proceeding of the 30th Interna-
tional Geological Science Publishers, Amsterdam, pp. 75e87.
Wilde, S.A., Zhao, G.C., Sun, M., 2002. Development of the North China
Craton during the late Archean and its final amalgamation at 1.8 Ga:
some speculations on its positions within a global Palaeoproterozoci
supercontinent. Gondwana Research 55 (1), 85e94.
Wilde, S.A., Cawood, P.A., Wang, K.Y., Nemchin, A., Zhao, G.C., 2004.
Determining Precambrian Crustal Evolution in China: A Case-study
from Wutaishan, Shanxi Province, Demonstrating the Application of
Precise SHRIMP UePb Geochronology. Geological Society of Lon-
don, Special Publications, vol. 226, 5e25.
Wilde, S.A., Cawood, P.A., Wang, K.Y., Nemchin, A.A., 2005. Granitoid
evolution in the late Archean Wutai complex, North China Craton.
Journal of Asian Earth Sciences 24, 597e613.
Wilde, S.A., Valley, J.W., Kita, N.T., Cavosie, A.J., Liu, D.Y., 2008.
SHRIMP U-Pb and CAMECA 1280 oxygen isotope results from
ancient detrital zircons in the Caozhuang quartzite, eastern Hebei,
North China Craton: evidence for crustal reworking 3.8 Ga age.
American Journal of Science 308, 185e199.
Windley, B.F., 1995. The Evolving Continents, third ed. John Wiley and
Sons, Chichester, pp. 1e526.
Wu, C.H., Li, S.X., Gao, J.F., 1986. Archean and Paleoproterozoic meta-
morphic regions in the North China Craton. In: Dong, S.B. (Ed.),
Metamorphism and Crustal Evolution of China. Geological Publishing
House, Beijing, pp. 53e89 (in Chinese).
Wu, Y.B., Zheng, Y.F., 2004. Genesis of zircon and its constraints on
interpretation of U-Pb age. Chinese Science Bulletin 49, 1554e1569.
Wu, F.Y., Yang, J.H., Liu, X.M., Li, T.S., Xie, L.W., Yang, Y.H., 2005a. Hf
isotopes of the 3.8 Ga zircons in eastern Hebei Province, China:
implications for early crustal evolution of the North China Craton.
Chinese Science Bulletin 50 (21), 2473e2480.
Wu, F., Zhao, G., Wilde, S.A., Sun, D.Y., 2005b. Nd isotopic constraints on
crustal formation in the North China Craton. Journal of Asian Earth
Sciences 24, 523e545.
Wu, F.Y., Zhang, Y.B., Yang, J.H., Xie, L.W., Yang, Y.H., 2008a. Zircon
U-Pb and Hf isotopic constraints on the early Archean crustal evolution
in Anshan of the North China Craton. Precambrian Research 167,
339e362.
Wu, Y.B., Gao, S., Zhang, H.F., Yang, S.H., Jiao, W.F., Liu, Y.S.,
Yuan, H.L., 2008b. Timing of UHP metamorphism in the Hong’an
area, western Dabie mountains, China: evidence from zircon U-Pb age,
trace element and Hf isotope composition. Contributions to Mineralogy
and Petrology 155, 123e133.
Wu, M., Zhao, G., Sun, M., Yin, C., Li, S., Tam, P.Y., 2011. Petrology and
peTpath of the Yishui mafic granulites: implications for tectono-
thermal evolution of the western Shandong complex in the eastern
block of the North China Craton. Precambrian Research. doi:10.1016/
j.precamres.2011.08.008.
Woodhead, J., Hergt, T., Shelley, M., 2004. Zircon Hf-isotope analysis
with an excimer laser, depth profiling, ablation of complex geometries,
and concomitant age estimation. Chemical Geology 209, 121e135.
Xia, X.P., Sun, M., Zhao, G.C., Luo, Y., 2006a. LA-ICP-MS U-Pb
geochronology of detrital zircons from the Jining complex, North
China Craton and its tectonic significance. Precambrian Research 144,
199e212.
Xia, X.P., Sun, M., Zhao, G.C., Wu, F.Y., Xu, P., Zhang, J.H., Luo, Y.,
2006b. U-Pb and Hf isotopic study of detrital zircons from the Wula-
shan khondalites: constraints on the evolution of the Ordos Terrane,
western block of the North China Craton. Earth and Planetary of
Science Letters 241, 581e593.
Xia, X.P., Sun, M., Zhao, G.C., Wu, F.Y., Xu, P., Zhang, J., He, Y.H.,
Zhang, J.H., 2006c. U-Pb and Hf isotope study of detrital zircons from
the Wanzi Supercrustals: constraints on the tectonic setting and
evolution of the Fuping Complex, Trans-North China Orogen. Acta
Geologica Sinica 80, 844e863.
Xia, X.P., Sun, M., Zhao, G.C., Wu, F.Y., Xu, P., Zhang, J., He, Y.H., 2008.
Paleoproterozoic crustal growth in the western block of the North
China Craton: evidence from detrital zircon Hf and whole rock Sr-Nd
isotopic compositions of the khondalites from the Jining complex.
American Journal of Science 308, 304e327.
Xia, X.P., Sun, M., Zhao, G.C., Wu, F.Y., Xie, L.W., 2009. U-Pb and Hf
isotopic study of detrital zircons from the L€
uliang khondalite, North
China Craton, and their tectonic implications. Geological Magazine
146 (5), 701e716.
Xiao, L.L., Wu, C.M., Zhao, G.C., Guo, J.H., Ren, L.D., 2010. Meta-
morphic peTpaths of the Zanhuang amphibolites and metapelites:
constraints on the tectonic evolution of the Paleoproterozoic Trans-
North China Orogen. International Journal of Earth Sciences 100,
717e739.
Xu, S., Griffin, W.L., Ma, X., O’Reilly, S.Y., He, Z., Zhang, C., 2009. The
Taihua group on the southern margin of the North China craton: further
insights from U-Pb ages and Hf isotope compositions of zircons.
Mineralogy and Petrology 97, 43e59.
Yang, J.H., Wu, F.Y., Liu, X.M., Xie, L.W., 2005. Zircon U-Pb ages and Hf
isotopes and their geological significances of the Miyun rapakivi
granites from Beijing, China. Acta Petrologica Sinica 21 (6),
1633e1644 (in Chinese with English abstract).
Yang, C.X., 2008. Zircon SHRIMP U-Pb ages, geochemical characteristics
and environmental evolution of the early Precambrian metamorphic
series in the Lushan area, Henan, China. Geological Bulletin of China
27 (4), 517e533 (in Chinese with English abstract).
Yang, J.H., Wu, F.Y., Wilde, S.A., Zhao, G.C., 2008. Petrogenesis and
geodynamics of late Archean magmatism in the eastern Hebei, eastern
North China Craton: geochronological, geochemical and Nd-Hf
isotopic evidence. Precambrian Research 167, 125e149.
Yang, J., Gao, S., Chen, C., Tang, Y., Yuan, H.L., Gong, H., Xie, S.,
Wang, J., 2009. Episodic crustal growth of North China as revealed by
A. Wang, Y. Liu / Geoscience Frontiers 3(2) (2012) 147e173 171
U-Pb age and Hf isotopes of detrital zircons from modern rivers.
Geochimica et Cosmochimica Acta 73, 2660e2673.
Yin, C.Q., Zhao, G.C., Sun, M., Xia, X.P., Wei, C.J., Zhou, X.W.,
Leung, W.H., 2009. LA-ICP-MS U-Pb zircon ages of the Qianlishan
complex: constrains on the evolution of the Khondalite Belt in the western
block of the North China Craton. Precambrian Research 174, 78e94.
Yin, C.Q., Zhao, G.C., Guo, J.H., Sun, M., Xia, X.P., Zhou, X.W., Liu, C.H.,
2011. U-Pb and Hf isotopic study of zircons of the Helanshan complex:
constraints on the evolution of the Khondalite Belt in the western block
of the North China Craton. Lithos 122, 25e38.
Zhai, M.G., Bian, A.G., Zhao, T.P., 2000. The amalgamation of the
supercontinent of North China Craton ate the end of Neo-Archaean and
its breakup during late Palaeoproterozoic and MesoeProterozoic.
Science in China (Series D) 43 (Suppl.), 219e232.
Zhai, M.G., 2004. Precambrian Geological Events in the North China
Craton, vol. 226. Geological Society of London, Special Publications.
57e72.
Zhai, M.G., Li, T.S., Peng, P., Hu, B., Liu, F., Zhang, Y.B., 2010.
Precambrian Key Tectonic Events and Evolution of the North China
Craton, vol. 388. Geological Society of London, Special Publications.
235e262.
Zhai, M.G., Santosh, M., 2011. The early Precambrian odyssey of the North
China Craton: a synoptic overview. Gondwana Research 20, 6e25.
Zhang, J., Zhao, G.C., Li, S.Z., Sun, M., Liu, S.W., Xia, X.P., He, Y.H.,
2006. U-Pb zircon dating of the granitic conglomerates of the Hutuo
Group: affinities of the Wutai granitoids and significance to the
tectonic evolution of the Trans-North China Orogen. Acta Geologica
Sinica 80 (6), 886e898.
Zhang, S.H., Liu, S.W., Zhao, Y., Yang, J.H., Song, B., Liu, X.M., 2007.
The 1.75e1.68 Ga anorthositeemangeriteealkali granitoiderapakivi
granite suite from the northern North China Craton: magmatism related
to a Paleoproterozoic Orogen. Precambrian Research 155, 287e312.
Zhang, H.F., Ying, J.F., Santosh, M., Zhao, G.C., 2011a. Episodic growth of
Precambrian lower crust beneath the North China Craton: a synthesis.
Precambrian Research. doi:10.1016/j.precamres.2011.04.006.
Zhang, S.J., Zhang, L.C., Xiang, P., Wan, B., Pirajno, F., 2011b. Zircon U-
Pb age, Hf isotopes and geochemistry of Shuichang Algoma-type
banded iron-formation, North China Craton: constraints on the ore-
forming age and tectonic setting. Gondwana Research 20, 137e148.
Zhang, H.F., Zhai, M.G., Santosh, M., Diwu, C.R., Li, S.R., 2011c.
Geochronology and petrogenesis of Neoarchean potassic meta-granites
from Huai’an complex: implications for the evolution of the North
China Craton. Gondwana Research 20, 171e183.
Zhang, J., Zhao, G., Li, S., Sun, M., Chan, L.S., Shen, W., Liu, S.W.,
2011d. Structural pattern of the Wutai complex and its constraints on
the tectonic framework of the Trans-North China Orogen. Precambrian
Research. doi:10.1016/j.precamres.2011.08.009.
Zhao, G.C., Wilde, S.A., Cawood, P.A., Lu, L.Z., 1998. Thermal evolution
of the Archaean basement rocks from the eastern part of the North
China Craton and its bearing on tectonic setting. International Geology
Review 40, 706e721.
Zhao, G.C., Wilde, S.A., Cawood, P.A., Lu, L.Z., 1999. Tectonothermal
history of the basement rocks in the western zone of the North China
Craton and its tectonic implications. Tectonophysics 310, 37e53.
Zhao, G.C., Cawood, P.A., Wilde, S.A., Sun, M., Lu, L.Z., 2000a. Meta-
morphism of basement rocks in the central zone of the North China
Craton: implications for Paleoproterozoic tectonic evolution. Precam-
brian Research 103, 55e88.
Zhao, G.C., Wilde, S.A., Cawood, P.A., Lu, L.Z., 2000b. Petrology and Pe
T path of the Fuping mafic granulites: implications for tectonic
evolution of the central zone of the North China Craton. Journal of
Metamorphic Geology 18, 375e391.
Zhao, G.C., Wilde, S.A., Cawood, P.A., Sun, M., 2001. Archean blocks
and their boundaries in the North China Craton: lithological,
geochemical, structural and PeTpath constraints and tectonic evolu-
tion. Precambrian Research 107, 45e73.
Zhao, G.C., Wilde, S.A., Cawood, P.A., Sun, M., 2002. SHRIMP U-Pb
zircon ages of the Fuping complex: implications for late Archean to
Paleoproterozoic accretion and assembly of the North China Craton.
America Journal of Science 302, 191e226.
Zhao,G.C.,Sun,M.,Wilde,S.A.,Guo,J.H.,2004.LateArchaeantoPalae-
oproterozoic Evolution of the Trans-North China Orogen: Insights from
Synthesis of Existing Data from the HengshaneWut aieFuping Belt, vol.
226. Geological Society of London, Special Publications. 27e55.
Zhao, G.C., Sun, M., Wilde, S.A., Li, S.Z., 2005. Late Archean to Pale-
oproterozoic evolution of the North China Craton: key issues revisited.
Precambrian Research 136, 177e202.
Zhao, G.C., Kr€
oner, A., Wilde, S.A., Sun, M., Li, S.Z., Li, X.P., Zhang, J.,
Xia, X.P., He, Y.H., 2007. Lithotectonic elements and geological events
in the HengshaneWutaieFuping Belt: a synthesis and implications for
the evolution of the Trans-North China Orogen. Geological Magazine
144 (5), 753e775.
Zhao, G., Wilde, S.A., Sun, M., Guo, J.H., Kr€
oner, A., Li, S.Z., Li, X.P.,
Zhang, J., 2008. SHRIMP U-Pb zircon geochronology of the Huai’an
complex: constraints on late Archean to Paleoproterozoic magmatic
and metamorphic events in the Trans-North China Orogen. American
Journal of Science 308, 270e303.
Zhao, G.C., 2009. Metamorphic evolution of major tectonic units in the
basement of the North China Craton: key issues and discussion. Acta
Petrologica Sinica 25 (8), 1772e1792 (in Chinese with English abstract).
Zhao, T.P., Chen, W., Zhou, M.F., 2009. Geochemical and Nd-Hf isotopic
constraints on the origin of the ～1.74 Ga anorthosite complex, North
China Craton. Lithos 113 (3e4), 673e690.
Zhao, G.C., Wilde, S.A., Guo, J.H., Cawood, P.A., Sun, M., Li, X.P., 2010a.
Single zircon grains record two Paleoproterozoic collisional events in
the North China Craton. Precambrian Research 177, 266e276.
Zhao, G.C., Yin, C.Q., Guo, J.H., Sun, M., Li, S.Z., Li, X.P., Wu, C.M.,
Liu, C.H., 2010b. Metamorphism of the L€
uliang amphibolite: impli-
cations for the tectonic evolution of the North China Craton. American
Journal of Science 310, 1480e1502.
Zhao, G., Li, S., Sun, M., Wilde, S.A., 2011. Assembly, accretion, and
break-up of the PaleoeMesoproterozoic Columbia supercontinent:
record in the North China Craton revisited. International Geology
Review 53 (11e12), 1331e1356.
Zheng, J.P., Griffin, W.L., O’Reilly, S.Y., Lu, F.X., Wang, C.Y., Zhang, M.,
Wang, F.Z., Li, H.M., 2004a. 3.6 Ga lower crust in central China: new
evidence on the assembly of the North China Craton. Geology 32 (3),
229e232.
Zheng, J.P., Lu, F.X., Yu, T.M., Tan, H.Y., 2004b. A study on Hf isotope,
U-Pb dating and trace elements of granulite enclaves in the Hannuoba
basalts: record of early evolution of the lower crust of the North China
Craton. Chinese Science Bulletin 49, 375e383.
Zheng, Y.F., Wu, Y.B., Zhao, Z.F., Zhang, S.B., Xu, P., Wu, F.Y., 2005.
Metamorphic effect on zircon Lu-Hf and U-Pb isotope systems in
ultrahigh-pressure eclogite-facies metagranite and metabasite. Earth
and Planetary Science Letters 240, 378e400.
Zheng, Y.F., Zhao, Z.F., Wu, Y.B., Zhang, S.B., Liu, X.M., Wu, F.Y., 2006.
Zircon U-Pb age, Hf and O isotope constraints on protolith origin of
ultrahigh-pressure eclogite and gneiss in the Dabie Orogen. Chemical
Geology 231, 135e158.
Zheng, Y.F., Chen, R.X., Zhang, S.B., Tang, J., Zhao, Z.F., Wu, Y.B., 2007.
Zircon LueHf isotope study of ultrahigh-pressure eclogite and granitic
gneiss in the Dabie Orogen. Acta Petrologica Sinica 23 (2), 317e330
(in Chinese with English abstract).
Zheng, J.P., Griffin, W.L., O’Reilly, S.Y., Zhao, J.H., Wu, Y.B., Liu, G.L.,
Pearson, N., Zhang, M., Ma, C.Q., Zhang, Z.H., Yu, C.M., Su, Y.P.,
Tang, H.Y., 2009. Neoarchean (2.7e2.8 Ga) accretion beneath the
North China Craton: U-Pb age, trace elements and Hf isotopes of
zircons in diamondiferous kimberlites. Lithos 112, 188e202.
Zhou, X.W., Zhao, G.C., Wei, C.J., Geng, Y.S., Sun, M., 2008. EPMA
U-Th-Pb monazite and SHRIMP U-Pb zircon geochronology of high-
pressure pelitic granulites in the Jiaobei massif of the North China
Craton. America Journal of Science 308, 328e350.
Zhou, Y.Y., Zhao, T.P., Xue, L.W., Wang, S.Y., Gao, J.F., 2009a. Petro-
logical, geochemical and chronological constraints for the origin and
geological significance of Neoarchean TTG gneiss in the Songshan
A. Wang, Y. Liu / Geoscience Frontiers 3(2) (2012) 147e173172
area, North China Craton. Acta Petrologica Sinica 25 (2), 331e347 (in
Chinese with English abstract).
Zhou, Y.Y., Zhao, T.P., Xue, L.W., Wang, S.Y., 2009b. Geochemistry and
origin of Neoarchean amphibolites in Songshan, Henan Province. Acta
Petrologica Sinica 25(11), 3043e3056 (inChinese with English abstract).
Zhou, Y.Y., Zhao, T.P., Wang, S.Y., Hu, G.H., 2011. Geochronology and
geochemistry of 2.5 to 2.4 Ga granitic plutons from the southern
margin of the North China Craton: implications for a tectonic tran-
sition from arc to post-collisional setting. Gondwana Research 20,
171e183.
A. Wang, Y. Liu / Geoscience Frontiers 3(2) (2012) 147e173 173
