1. No category

Journal of Asian Earth Sciences 103 (2015) 169–183
Contents lists available at ScienceDirect
Journal of Asian Earth Sciences
journal homepage: www.elsevier.com/locate/jseaes
Nd–Hf isotopic mapping of Late Mesozoic granitoids in the East Qinling
orogen, central China: Constraint on the basements of terranes and
distribution of Mo mineralization
Xiaoxia Wang a,⇑, Tao Wang b, Changhui Ke a, Yang Yang c, Jinbao Li d, Yinghong Li a, Qiuju Qi e,
Xingqiu Lv c
a
MLR Key Laboratory of Metallogeny and Mineral Assessment, Institute of Mineral Resources, Chinese Academy of Geological Sciences, Beijing 100037, China
Institute of Geology, Chinese Academy of Geological Sciences, Beijing 100037, China
c
China University of Geosciences, Beijing 100083,China
d
Chang’an University, Xi’an 710054, China
e
Institute of Resource Survey and Assessment, ECE, Nanjing 210007, Chian
b
a r t i c l e
i n f o
Article history:
Received 2 April 2014
Received in revised form 30 June 2014
Accepted 1 July 2014
Available online 12 July 2014
Keywords:
Granitoid
Nd–Hf isotope
Source
Basement
Mo deposit
a b s t r a c t
Voluminous Late Mesozoic granitoids and the world’s largest Mo deposits occur in the East Qinling. This
paper presents the results of Nd–Hf isotopic mapping for the Late Mesozoic granitoids (155–105 Ma) and
demonstrates their constraint on the basements and distribution of the Mo deposits in the East Qinling.
This isotopic map, made by 98 (21 new and 77 published) whole-rock Nd isotopic and 29 (7 new and 22
published) average zircon Hf isotopic data, shows large variations of whole-rock eNd(t) values from 22.1
to 1.5, and the correspondingly Nd model ages (TDM(Nd)) from 2.83 to 0.79 Ga, and zircon eHf(t) values
from 26.3 to +0.1 and two-stage Hf model ages (TDM2(Hf)) from 2.86 to 0.96 Ga. Three regions of variations have been identified from north to south: (a) eNd(t) values range from 22.1 to 10.9 with TDM(Nd) of
2.82–1.47 Ga, and eHf(t) values 26.3 to 13.5 with TDM2(Hf) 2.86–2.04 Ga; (b) eNd(t) values 13.9 to 1.5
with TDM(Nd) 2.02–0.79 Ga, and eHf(t) values 16.2 to +0.1 with TDM2(Hf) 1.96–0.96 Ga; and (c) eNd(t) values
6.3 to 4.5 with TDM(Nd) 1.28–1.12 Ga, and eHf(t) values 1.0 to 0.3 with TDM2(Hf) 1.25–1.22 Ga, respectively. The three regions approximately correspond to the three different terranes, the southern margin of
the North China Block (NCB), the North Qinling Belt (NQB) and the South Qinling Belt (SQB), respectively.
These demonstrate that the granitoids in the different terranes have distinct sources and their sources
change from old to more juvenile from the north (southern margin of the NCB) to the south (SQB). These
also reveal the distinct basements for the terranes in Late Mesozoic. The southern margin of the NCB contains widespread Neoarchaean to Paleoproterozoic basement, the NQB comprises Archaean to Neoproterozic basement and the SQB Mesoproterozic to Neoproterozic basement. All these suggest that
the three terranes underwent different tectonic evolution and the continental crust of the East Qinling
were mainly formed during Archaean to Neoproterozic, different from a typical accretion orogen. The
old sources of the granitoids and basements of the terranes constrain the distribution, scale and number
of the Mo mineralization and deposits. Mo mineralization is closely related to the small granitic bodies
with old continental component sources and Mo deposits are mainly hosted by the terranes with oldest
basement. The scale and number of the Mo mineralization and deposits decreased from the southern
margin of the NCB to SQB.
Ó 2014 Elsevier Ltd. All rights reserved.
1. Introduction
The Qinling orogen, one of the largest orogenic belts in Asia
(Mattauer et al., 1985), underwent multi-stage (e.g., Neoproterozoic,
⇑ Corresponding author. Tel.: +86 10 68999043.
E-mail address: xiaoxiawang@hotmail.com (X. Wang).
http://dx.doi.org/10.1016/j.jseaes.2014.07.002
1367-9120/Ó 2014 Elsevier Ltd. All rights reserved.
Paleozoic, and Early Mesozoic) orogenic processes and finally
formed by collision of the North China Block (NCB) and South China
Block (SCB) during the Early Mesozoic (e.g., Mattauer et al., 1985;
Kröner et al., 1993; Meng and Zhang, 1999; Zhang et al., 2001;
Ratschbacher et al., 2003). Correspondingly, multi-stage magmatisms (e.g., Neoproterozoic, Paleozoic, and Early Mesozoic) occurred
(Wang et al., 2013). Significantly, after final formation of the orogen,
170
X. Wang et al. / Journal of Asian Earth Sciences 103 (2015) 169–183
voluminous Late Mesozoic (Jurassic–Cretaceous) granitoids (e.g., Lu,
1999; Wang et al., 2013) and the world’s largest Late Mesozoic Mo
deposits, including porphyry and porphyry–skarn types (e.g., Li
et al., 2007, 2011, 2012a; Mao et al., 2011), occurred in the East Qinling. Many investigations have been made for these granitoids and
Mo deposits (e.g., Chen et al., 2000; Lu et al., 2002; Zhu et al.,
2008; Bao et al., 2009, 2014; Li et al., 2009a, 2009b, 2012b; Mao
et al., 2008, 2009, 2010, 2011; Wang et al., 2013; and references
therein). However, the sources and origin of the granitoids and Mo
deposits, particularly their relations have not been well understood.
The main debates include: (1) the sources of the Late Mesozoic
granitoids were derived from partial melting of the crystalline basement, such as the Archaean Taihua Group in the southern margin of
the NCB (e.g., Chen et al., 2000), or from the old crust with contribution of the juvenile compositions (e.g., Luo et al., 1993; Sun and
Liu,1987; Zhang et al., 2010; Zhu et al., 2010; Li et al., 2012c;
Wang et al., 2013), or from subducted continental crust of the SCB
(Bao et al., 2009, 2014; Li et al., 2012d). (2) The source of Mo was
mainly derived from the lower crust, or from the Archaean basement
and Paleoproterozoic rocks of the NCB (e.g., Liu et al., 2007; Lu et al.,
2002). Some researchers suggested that the carbonaceous sedimentary rocks may be the main source for the Mo mineralization (e.g., Li
et al., 2012d; Zhang et al., 2010); while few others considered the
upper mantle (Bao et al., 2009; Zhu et al., 2010) or subducted continental crust of the SCB (Bao et al., 2014) as their major sources. The
key problem is the major factor controlling the distribution of the
Mo related granitoids and Mo deposits.
In this paper we present the results of Nd–Hf isotopic mapping
for the Late Mesozoic granitoids in the East Qinling, using 28 new
and 99 published data to study isotopic variations and sources of
the granitoids. The results can help us to better understand the
sources of the granitoids and basement nature of this orogen, as
well as their constraint on the Mo mineralization.
2. Geological setting
The Qinling orogen extends more than 1500 km across central
China and links the Kunlun Orogen in the west and the Dabie Orogen in the east (Fig. 1), and separates the NCB and SCB (e.g., Zhang
et al., 2001; Ratschbacher et al., 2003). This orogen is composed of
four major blocks or terranes, from north to south, i.e., the southern margin of the NCB, North Qinling Belt (NQB), South Qinling Belt
(SQB) and northern margin of the SCB, which are separated by one
fault and two sutures, i.e., the Luonan-Luanchuan fault, and the
Shangdan and Mianlue sutures (Fig. 1, Meng and Zhang, 1999,
2000), respectively. The Shangdan suture is generally considered
to be the result of a Middle Paleozoic collision of the NCB and
SQB (Meng and Zhang, 2000; Dong et al., 2011b) and a multistage
accretion of the SQB to NQB. The Mianlue suture was formed by the
Early Mesozoic (Triassic) collision between the SQB and SCB
(Zhang et al., 2004).
The southern margin of the NCB, which previously belongs to
the NCB, but was involved in the Qinling orogeny, consists mainly
of an Archaean (2.5 to 2.8 Ga) basement and Proterozoic overlying volcanic and sedimentary sequences (Zhang et al., 2001). The
Archaean basement is composed of the amphibolite- to granulite-facies metamorphic rocks of the Taihua Group. The Proterozoic
volcanic and sedimentary sequences consist of the Paleoproterozoic mafic to felsic volcanic rocks and minor sedimentary rocks of the
Xiong’er Group, Mesoproterozoic quartzite and schist with intercalated dolomitic marble of the Guandaokou Group, and Neoproterozoic meta-sandstone, marble, and schist of the Luanchuan Group.
The NQB is composed predominately of, from north to south,
the Proterozoic Kuanping Group, Paleozoic Erlangping Group, Proterozoic Qinling Complex and Paleozoic Danfeng Group (Zhang
et al., 2001). These groups and complex are composed predominantly of medium-grade metasedimentary and metavolcanic
rocks. The Qinling Complex constitutes the Precambrian basement
in the NQB, which underwent strong Proterozoic and Paleozoic tectonothermal events (e.g., Hu et al., 1993; Wang et al., 2003, 2005;
You et al., 1993).
The SQB, bounded to the north by the Shangdan suture and to
the south by Mianlue suture (Fig. 1), constitutes mainly Proterozoic crystalline basement and a thick pile of Late Proterozoic to
Triassic (e.g., the Paleozoic Liuling group) overlying sedimentary
sequences (Zhang et al., 2001, 2006, Lu et al., 2004). Its Proterozoic basement consists of low to high greenschist facies of volcanic to sedimentary metamorphic rocks such as Wudang and
Yaolinghe groups.
Paleozoic and Mesozoic intrusions occur widely in the Qinling
orogen. The Paleozoic intrusions are regarded as the recording
accretion and collision between the NCB and SQB (Lerch et al.,
1995; Xue et al., 1996; Wang et al., 2009a, 2013). The Early Mesozoic magmatism is interpreted as the result of subduction and/or
collision of the NCB and SCB (Dong et al., 2011a; Wang et al.,
2013; Li et al., 2013). The Late Mesozoic magmatism is response
to an intraplate setting (Zhang et al., 2001; Dong et al., 2011b;
Mao et al., 2010; Wang et al., 2011, 2013).
Late Mesozoic Mo deposits mainly occur in the southern margin
of the NCB, with minor in the NQB and a few in the SQB (Fig. 2).
They are mostly of Late Jurassic to Early Cretaceous in age and
show a close spatial–temporal relationship to the contemporaneous granitoid porphyries (Mao et al., 2008, 2011; Bao et al.,
2014; and reference therein).
Fig. 1. A tectonic sketch map of the Qinling orogen. Modified after Zhang et al. (2001) and Dong et al. (2011a).
X. Wang et al. / Journal of Asian Earth Sciences 103 (2015) 169–183
171
Fig. 2. Distribution of the Mesozoic granitoids and Mo deposits in the East Qinling orogen. The base map after 1/500,000 scale geological map and tectonic map of the Qinling
(Zhang et al., 2001). Mo deposits distribution modified after Mao et al. (2008, 2011).
3. Late Mesozoic granitoids
Late Mesozoic granitoid intrusions are mainly distributed in the
east segment of the Qinling orogen, i.e., East Qinling (Fig. 2), and
they occur generally in forms of both small porphyritic bodies
and large batholiths (Wang et al., 2011; and reference therein).
They all contain microgranular mafic enclaves (MMEs) and occasionally with two pyroxene granulite enclaves (Wang et al.,
1986). The porphyritic bodies and large batholiths were mainly
intruded into the Archaean Taihua, Proterozoic Xiong’er, Luanchuan and Guandaokou groups along the southern margin of the NCB,
the Kuanping Group in the NQB, and the Devonian Liuling Group in
the SQB. The smaller porphyritic bodies occupy areas less than
1 km2 and are closely related to coeval Mo deposits (including
W, Fe, Cu, Au, Pb and Zn mineralization). Some bodies are associated with coeval mantle-derived mafic dikes (Bao et al., 2009,
2014).
We collected almost all available zircon ages for these Late Mesozoic granitoids, and these ages show two peaks, at 155–130 Ma and
120–105 Ma (Figs. 2 and 3a), indicating two major stages of
granitoid magmatisms. The first-stage (155–126 Ma) granitoids
occur along the southern margin of the NCB, NQB and SQB,
whereas the second-stage (120–105 Ma) only in the southern
margin of the NCB and NQB (Fig. 2).
The first-stage granitoids are mainly composed of syenogranites, monzogranites, granodiorites and quartz diorites and they
are I-type, I- to A-type, calc-alkaline to shoshonitic, and metaluminous with A/CNK ratios of 0.9–1.0 (1.1–1.2 for a few granitoids,
Wang et al., 2013). The second-stage consist of syenogranites,
monzogranites and granodiorites and are characterized by I- to
A-type and/or A-type, alkaline, and slightly peraluminous (A/
CNK = 0.96–1.25) (Wang et al., 2013). The granitoids of both
stages in the southern margin of the NCB have large range in
SiO2, K2O and A/CNK than these in the NQB and SQB (Fig. 4a
and b). All the granitoids show LREE-enriched and HREE-flat patterns but the granitoids in the NQB have obvious negative Eu
anomalies than these in the southern margin of the NCB and
SQB (Fig. 5).
Fig. 3. Zircon U–Pb age (a) and Re–Os age (b) histograms of the Late Mesozoic
granitoids and Mo deposits in the East Qinling orogen (zircon U–Pb age histograms
modified after Wang et al., 2011, 2013; Re–Os age histograms modified after Mao
et al., 2011 and some data after Su et al., 2009; Liu et al., 2010; Huang et al., 2010;
Meng et al., 2012).
4. Late Mesozoic Mo deposits
The Qinling, especially the East Qinling, hosts the world’s most
important Mo deposits (Li et al., 2007, 2013; Mao et al., 2008).
Based on molybdenite Re–Os ages, the Late Mesozoic porphyryrelated Mo deposits including porphyry and porphyry–skarn type
172
X. Wang et al. / Journal of Asian Earth Sciences 103 (2015) 169–183
Fig. 4. Major element diagrams for the Late Mesozoic granitoids. Date after Wang
et al. (2011), Qi et al. (2012), Ke et al. (2012, 2013), Yang et al. (2012), Zhu et al.
(2008), Nie and Fan (1989), Guo et al. (2009), Zhao et al. (2010), Ke et al., 2011.
can be divided into two stages, 155–125 Ma and 125–105 Ma
(Fig. 3b).
Most of them are located in the southern margin of the NCB,
some of them in the NQB and a few in the SQB (Fig. 2). They are
closely related to the Late Mesozoic granitoids, especially granite
porphyry, forming the porphyry, porphyry–skarn and skarn type
Mo (including Mo–W, Mo–Fe, Mo–Cu) deposits, except a few
related to the Early Mesozoic magmatism (Mao et al., 2008;
Huang et al., 2009). The large Mo deposits (mainly from 115 to
145 Ma) often occur in the southern margin of the NCB, such as
the Jinduicheng, Sandaozhuang–Nannihu, and Donggou Mo and
Mo–W deposits. The number and scale of Mo deposits are
decreased from the southern margin of the NCB to NQB then to
SQB. And Mo mineralization decreased but Cu mineralization
increased in this direction (Fig. 2).
Detailed studies have been done for these Mo deposits in the
Qinling (e.g., Mao et al., 2008, 2011; Bao et al., 2014; and references
therein). The Mo mineralization usually occurred at the contact of
the granitoids with the country rocks such as the Xiong’er, Guandaokou and Kuanping groups. K-feldspar–quartz–sulfide veins
and/or quartz–sulfide veins are the major type of the most significant Mo mineralization. The porphyry and porphyry–skarn type
Mo mineralization are typical stockwork mineralization in both
granitoid porphyries and country rocks, accompanied by pervasive
Fig. 5. Chondrite-normalized (Sun and McDonough, 1989) REE abundance patterns
for the Late Mesozoic granitoids. Date references as same as Fig. 4.
alteration of K-feldspar, quartz, fluorite, and less sericite, zeolite
and calcite. Ore minerals are molybdenite and pyrite, with minor
magnetite, chalcopyrite, galena, sphalerite and cassiterite. Gangue
minerals include quartz, K-feldspar, albite, biotite, muscovite (or
sericite), calcite and fluorite.
5. Sampling, analytical methods and results
5.1. Sampling
Twenty-one samples are collected from 10 plutons for Sm–Nd
isotopic compositions. Among them 12 samples are from 6 intrusions in the southern margin of the NCB and 9 samples from 4
intrusions in the NQB (Table 1). The rocks for Sm–Nd isotopic analyses are granite porphyry, granodiorite porphyry, monzogranite
porphyry, quartz diorite porphyry, granodiorite and monzogranite.
The intrusions and rock types are listed in Table 1.
Seven samples, including granodiorite, granite porphyry and
monzogranite porphyry, from 7 intrusions located in the southern
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X. Wang et al. / Journal of Asian Earth Sciences 103 (2015) 169–183
Table 1
Nd isotopic compositions of the Late Mesozoic granitoids.
Location Pluton
S-NCB
Rock type
Age (Ma)
Sm
(10
Nd
) (10
6
147
Sm/144Nd
143
0.09444
0.09728
0.51168
0.51185
9
4
18.7
15.5
0.52
0.51
17.3 1.88
14.0 1.70
Zhang et al. (2006)
0.08000
0.10000
0.09000
0.08000
0.51166
0.51182
0.51178
0.51182
6
8
3
6
19.1
16.0
16.7
15.9
0.59
0.49
0.54
0.59
17.3
14.5
15.1
14.2
1.69
1.78
1.68
1.51
Dai et al. (2009)
6
)
42.86
42.12
Nd/144Nd 2sm eNd
(0)
fSm/Nd eNd
(t)
TDM
(Ga)
References
Funiushan
Granite
113 (Ar)
6.691
6.774
Donggou
Granite porphyry
117
0.640
0.820
0.890
1.000
Lantian
Monzogranite
133 (Wang et al., 2011)
5.987
6.191
5.165
4.847
5.657
4.866
8.454
5.017
37.30
36.09
32.08
29.75
34.70
29.05
51.75
34.54
0.09709
0.10380
0.09738
0.09857
0.09860
0.10130
0.09877
0.08780
0.51163
0.51166
0.51174
0.51161
0.51163
0.51165
0.51163
0.51194
9
30
48
10
10
11
10
11
19.7
19.2
17.5
20.1
19.7
19.2
19.7
13.7
0.51
0.47
0.50
0.50
0.50
0.49
0.50
0.55
17.9
17.4
15.6
18.3
17.8
17.6
18.0
11.8
1.99
2.06
1.84
2.04
2.01
2.02
2.01
1.47
Zhang et al. (2006)
Zhang et al. (2006)
5.080
5.310
6.210
7.540
This paper
Huashan
Monzogranite
134
4.431
4.626
4.523
28.40
29.67
29.40
0.09439
0.09432
0.09308
0.51159
0.51163
0.51160
30
13
6
20.4
19.6
20.2
0.52
0.52
0.53
18.7 1.99
17.9 1.93
18.4 1.95
Heyu
Monzogranite
135
7.734
5.787
5.194
5.604
4.898
3.840
4.250
2.620
5.580
1.630
3.300
7.410
1.860
55.95
40.36
37.26
39.56
32.97
25.60
28.10
15.20
39.10
9.53
22.10
41.90
11.40
0.08362
0.08674
0.08432
0.08568
0.08986
0.09510
0.09590
0.10920
0.09070
0.10860
0.09480
0.11220
0.10360
0.51171
0.51176
0.51165
0.51174
0.51180
0.51175
0.51172
0.51198
0.51180
0.51184
0.51178
0.51172
0.51172
6
14
8
16
15
7
8
9
11
8
7
7
7
18.2
17.2
19.4
17.6
16.3
17.4
17.9
12.8
16.4
15.7
16.7
18.0
17.9
0.57
0.56
0.57
0.56
0.54
0.52
0.51
0.44
0.54
0.45
0.52
0.43
0.47
16.2
15.3
17.4
15.6
14.4
15.7
17.9
12.8
16.4
15.7
14.8
18.0
17.9
0.09532
0.09629
0.09304
0.51173
0.51179
0.51172
6
13
7
17.8
16.6
17.9
0.52
0.51
0.53
15.9 1.83
14.8 1.76
16.0 1.80
Zhao et al. (2010)
0.11300
0.11920
0.10950
0.11030
0.51180
0.51180
0.51180
0.51170
13
14
15
11
16.3
16.3
16.3
18.3
0.43
0.39
0.44
0.44
14.8
14.9
14.8
16.7
2.04
2.17
1.97
2.13
Li et al. (2012d)
Zhang et al. (2006)
148
Shijiawan
Granite porphyry
141
Jinduicheng Granite porphyry
143
Laoniushan
Monzogranite
146
Nannihu
Granite porphyry
Shangfang
Granite porphyry
Gelaowan
Granite porphyry
146
Shibaogou
Monzogranite
porphyry
148
12.90
14.40
13.20
13.10
353
309
333
385
5.247
5.114
5.303
4.904
5.038
4.689
33.81
33.44
33.70
31.93
33.68
30.93
0.09388
0.09250
0.09518
0.09290
0.09048
0.09169
0.10118
0.51170
0.51170
0.51170
0.51170
0.51172
0.51169
0.51178
7
8
8
7
9
11
16
18.2
18.4
18.3
18.4
17.8
18.5
16.7
0.52
0.53
0.52
0.53
0.54
0.53
0.49
16.3
16.4
16.4
16.4
15.9
16.5
14.8
1.84
1.82
1.86
1.83
1.76
1.82
1.86
145
3.251
1.031
3.417
5.020
22.1
7.20
24.3
34.46
0.08887
0.08659
0.08489
0.08809
0.51178
0.51188
0.51176
0.51174
11
10
8
8
16.8
14.8
17.2
17.6
0.55
0.56
0.57
0.55
14.8
12.7
15.2
15.5
1.68
1.52
1.65
1.71
145
1.211
0.686
8.256 0.08870
5.189 0.07994
0.51181
0.51185
10
10
16.2
15.3
0.55
0.59
14.3 1.64
13.2 1.48
151
Mulonggou
1.69
1.67
1.77
1.68
1.65
1.80
1.84
1.70
1.68
1.90
1.75
2.15
1.97
Bao et al. (2014)
Nie and Fan (1989)
Qi et al. (2012)
Bao et al. (2009)
0.09325
0.51198
10
12.9
0.53
10.9 1.48
This paper
14.79
1.808 0.07392
0.51183
7
15.8
0.62
13.5 1.44
Bao et al. (2014)
18.37
8.959
2.337 0.07693
1.665 0.11238
0.51184
0.51182
7
7
15.5
15.9
0.61
0.43
13.3 1.45
14.4 1.99
0.09120
0.10039
0.51160
0.51160
11
11
20.3
20.3
0.54
0.49
18.3 1.93
18.5 2.08
Granodiorite porphyry 150
This paper
Wanghegou Monzogranite
porphyry
153
0.09014
0.51173
9
17.7
0.54
15.6 1.74
Heishan
154
0.10436
0.51172
11
17.8
0.47
16.0 1.98
0.10324
0.12156
0.51167
0.51144
9
10
19.0
23.4
0.48
0.38
17.1 2.04
21.9 2.82
0.09736
0.09271
0.51179
0.51174
10
11
16.6
17.6
0.51
0.53
14.7 1.78
15.5 1.77
This paper
8.256 0.11435
0.51151
19
22.0
0.42
20.4 2.51
Jiao et al. (2010)
Quartz diorite
porphyry
Yongping
Granodiorite
154
Balipo
Monzogranite
porphyry
155
1.562
(continued on next page)
174
X. Wang et al. / Journal of Asian Earth Sciences 103 (2015) 169–183
Table 1 (continued)
Location Pluton
NQB
SQB
Rock type
Age (Ma)
Sm
(10
Nd
) (10
6
147
Sm/144Nd
6
)
143
Nd/144Nd 2sm eNd
(0)
fSm/Nd eNd
(t)
2.980
4.032
18.46
24.33
0.09760
0.10020
0.51150
0.51141
10
11
22.2
24.1
0.50
0.49
TDM
(Ga)
22.2 2.16
24.1 2.33
Fengyu
Granite
116 (Ar)
4.322
6.958
3.376
2.393
2.561
0.461
31.17
73.57
20.26
13.97
16.82
1.972
0.08388
0.05721
0.10080
0.10360
0.09210
0.14150
0.51247
0.51233
0.51233
0.51242
0.51244
0.51238
70
7
5
5
8
10
3.2
6.1
6.0
4.3
3.8
5.1
0.57
0.71
0.49
0.47
0.53
0.28
1.5
4.0
4.6
2.9
2.3
4.3
0.79
0.80
1.11
1.01
0.89
1.63
Laojunshan
Monzogranite
111 (Meng et al., 2012)
5.412
4.263
5.158
4.967
6.980
30.43
22.13
28.90
27.48
33.73
0.10760
0.11650
0.10790
0.10930
0.12520
0.51230
0.51231
0.51234
0.51236
0.51222
7
12
11
9
9
6.6
6.4
5.8
5.5
8.2
0.45
0.41
0.45
0.44
0.36
5.3
5.2
4.5
4.2
7.1
1.22
1.31
1.17
1.16
1.60
Muhuguan
Monzogranite
150
2.373
2.616
1.657
7.419
3.493
2.216
2.901
14.57
15.08
11.25
44.25
21.79
13.92
17.69
0.09855
0.10490
0.08908
0.10140
0.09697
0.09623
0.09915
0.51196
0.51195
0.51201
0.51216
0.51197
0.51200
0.51200
8
7
7
26
8
11
11
13.2
13.4
12.3
9.4
13.0
12.5
12.5
0.50
0.47
0.55
0.48
0.51
0.51
0.50
11.4
11.7
10.2
7.6
11.2
10.5
10.6
1.57
1.68
1.39
1.35
1.54
1.49
1.53
1.46
1.42
1.46
1.52
Mangling
Monzogranite
150 (Wang et al., 2011)
0.09508
0.09539
0.09585
0.09286
0.51201
0.51205
0.51202
0.51195
10
9
10
11
12.2
11.5
12.0
13.5
0.52
0.52
0.51
0.53
10.2
9.6
10.1
11.5
Xigou
Monzogranite
porphyry
153 (Ke et al., 2012)
0.08693
0.51200
11
12.5
0.56
10.4 1.38
0.08335
0.51199
10
12.2
0.52
10.2 1.46
157 (Ke et al., 2012)
0.11537
0.51184
10
15.5
0.41
13.9 2.02
145
0.09900
0.10700
0.10500
0.10300
0.10800
0.09700
0.10900
0.10400
0.51231
0.51233
0.51226
0.51230
0.51226
0.51222
0.51224
0.51225
12
4
8
8
7
25
12
12
6.4
6.1
7.5
6.7
7.4
8.1
7.7
7.5
0.50
0.46
0.47
0.48
0.45
0.51
0.45
0.47
Taoguanping Monzogranite
porphyry
Chigou
Granite porphyry
Diorite
Quartz diorite
References
4.6
6.1
7.5
6.7
7.4
8.1
7.7
7.5
1.12
1.18
1.25
1.17
1.28
1.21
1.32
1.25
Zhang et al. (2006)
This paper
This paper
Xie et al. (2012)
Note: eNd = ((143Nd/144Nd)s/(143Nd/144Nd)CHUR 1) 10,000, fSm/Nd = (147Sm/144Nd)s/(147Sm/144Nd)CHUR 1, where s = sample, (143Nd/144Nd)CHUR = 0.512638, and
(147Sm/144Nd)CHUR = 0.1967. The model ages (TDM) were calculated using a linear isotopic ratio growth equation: TDM = 1/k ln(1 + ((143Nd/144Nd)s 0.51315)/
((147Sm/144Nd)s 0.2137)). S-NCB: Southern margin o the North China Block; NQB: North Qinling Belt; SQB: South Qinling Belt.
margin of the NCB, were analyzed for zircon Lu–Hf isotopic compositions. The intrusions and rock types are listed in Table 2.
5.2. Analytical methods
5.2.1. Whole-rock Sm–Nd isotopic analyses
Sm–Nd isotopic analyses were carried out at the Department of
Earth and Environmental Sciences, Ludwig-Maximilians-University
of Munich (LMU) following the methods described by Hegner et al.
(1995). Isotope analyses were performed on an upgraded MAT 261
multi-collector mass spectrometer. Nd were measured using a
dynamic triple-collector routine, monitoring interfering 144Sm.
143
Nd/144Nd ratio is normalized to 146Nd/144Nd = 0.7219, applying
an exponential fractionation law. During this study the La Jolla
Nd reference material 143Nd/144Nd = 0.511847 ± 0.000008 (2 SD
of population, N = 10). The long-term external precision for
143
Nd/144Nd measured is estimated at 1.1 10 5 (2 SD).
5.2.2. Zircon Lu–Hf isotopic analyses
In situ zircon Hf isotopic analyses were conducted using a Neptune multi-collector ICP-MS coupled to a New Wave UP213 laser
ablation microprobe at the Institute of Mineral Resources, Chinese
Academy of Geological Sciences, Beijing, China. Instrumental conditions and data acquisition methods are described in detail by Hou
et al. (2007) and Wu et al. (2006). A stationary spot was used for
the analyses, with a beam diameter of 40 or 55 lm. Helium was used
as a carrier gas to transport the ablated sample from the laser ablation cell to the ICP-MS torch via a mixing chamber, where the helium
was mixed with argon. In order to correct for isobaric interferences
of 176Lu and 176Yb on 176Hf, 176Lu/175Lu = 0.02658, and
176
Yb/173Yb = 0.796218 ratios were used (Chu et al., 2002). Yb isotope ratios were normalized to a 172Yb/173Yb ratio of 1.35274 (Chu
et al., 2002) and Hf isotope ratios to a 179Hf/177Hf ratio of 0.7325
using an exponential law in order to correct for instrumental mass
bias. The instrumental mass bias behavior of Lu was assumed to follow that of Yb, and the mass bias correction is described by Wu et al.
(2006) and Hou et al. (2007). Zircon GJ1 was used as the reference
standard, and yielded a weighted mean 176Hf/177Hf ratio of
0.282000 ± 0.00006 (2r; n = 11) or 0.282000 ± 0.000019 (2r;
n = 11) during the course of the analyses. These values are indistinguishable from a weighted mean 176Hf/177Hf ratio of 0.282013 ± 19
(2r) obtained by Elhlou et al. (2006).
5.3. Results
5.3.1. Whole-rock Sm–Nd isotopes
Sm–Nd concentrations and 143Nd/144Nd ratios for the granitoids
are listed in Table 1. All the rocks have relatively uniform
147
Sm/144Nd (0.0834–0.1216; fSm/Nd
0.38 to
0.56) and
X. Wang et al. / Journal of Asian Earth Sciences 103 (2015) 169–183
143
Nd/144Nd (0.51144–0.51205) ratios. Age-corrected eNd(t) values
of the granitoids range from 21.6 to 9.6 and yield depleted mantle
model ages (TDM(Nd)) from 2.82 to 1.38 Ga (ages for calculation are
zircon U–Pb ages, except two Ar–Ar ages. The ages with their references are in Table 1). eNd(t) values from 21.9 to 10.9 are for the
granitoids in the southern margin of the NCB and from 13.9 to
9.6 for these in the NQB. eNd(t) values for each intrusion show a
small range, most of them within 5 eNd(t) units.
5.3.2. Zircon Lu–Hf isotopes
Lu–Hf isotopic compositions were analyzed on domains of the
same dating grains. More than ten spots were analyzed for each
sample except one sample from the Yongping body. Age-corrected
176
Hf/177Hf(t) ratios and eHf(t) values of the zircons were calculated
using their U–Pb ages (Table 2).
The analyzed spots have 206Pb/238U ages varying from 158 to
129 Ma, and 176Hf/177Hf(t) ratios of 0.28145–0.28256. They yield
negative eHf(t) values of 30.2 to 4.4 and two-stage Hf model
ages (TDM2(Hf)) of 3.09–1.47 Ga. Most samples show large variations
in eHf(t) values, more than 10 eHf(t) units, except sample from the
Daping porphyritic body less than 10 eHf(t) units.
6. Nd–Hf isotope mapping
6.1. Nd–Hf isotopic data base
The data for Nd–Hf isotope mapping include the above newly
acquired and published Nd–Hf isotopic data.
Seventy-seven published Sm–Nd isotopic data from 16 plutons
and their references are listed in Table 1 and given in Fig. 6. Fiftynine Sm–Nd isotopic data of 13 intrusions are from the southern
margin of the NCB, 10 data of 2 intrusions from the NQB and 8 data
of 1 intrusion from the SQB. All the published data were recalculated using the precise zircon U–Pb ages.
The published zircon Lu–Hf isotopic data are from 22 intrusions.
Twelve samples are from 12 intrusions in the southern margin of
the NCB, 6 samples from 6 intrusions in the NQB and 4 samples
from 3 intrusions in the SQB. The ranges of eHf(t) values and
TDM2(Hf) and their reference Nos. are given in Fig. 7.
6.2. Nd isotope mapping
All above 98 Nd isotopic data are used to mapping for the Late
Mesozoic granitoids in the East Qinling (Fig. 6). This map shows
that, from north to south, the eNd(t) values of the granitoids
increase from 22.1 to 1.5 and TDM(Nd) decrease from 2.82 to
0.79 Ga, and three distinct isotopic regions are identified, approximately corresponding to the southern margin of the NCB, NQB and
SQB, respectively (Fig. 6).
In the southern margin of the NCB, the eNd(t) values are 22.1 to
10.9 and TDM(Nd) 2.82–1.47 Ga (Table 1 and Fig. 6). In the NQB, the
eNd(t) values range from 13.9 to 1.5 with TDM(Nd) 2.02–0.79 Ga.
In the SQB, eNd(t) values are between 6.3 and 4.5 with TDM(Nd)
1.28 and 1.12 Ga (Table 1, Fig. 6), respectively. These clearly indicate that the eNd(t) values increase and TDM(Nd) decrease from the
north (southern margin of the NCB) to south (SQB; Fig. 8). Even
within the same terrane, such as the southern margin of the NCB,
the eNd(t) values increase and TDM(Nd) decrease in this direction
(Fig. 8).
Temporally, the first-stage granitoids in the southern margin of
the NCB display larger variation in eNd(t) values than the second
one (Fig. 9). And in the NQB the first-stage granitoids have lower
negative eNd(t) values than the second-stage (Fig. 9). These suggest
that the temporal variations of eNd(t) values of the granitoids are
different in the two terranes.
175
6.3. Hf isotope mapping
All above 29 average zircon Hf isotopic data are used to mapping for the Late Mesozoic granitoids. As this map shown (Fig. 7),
the eHf(t) values and TDM2(Hf) of the granitoids are from 26.3 to
0.3 and 2.86 to 1.22 Ga, respectively, indicating their Hf isotopic
variations are larger than their Nd isotopic compositions.
In the southern margin of the NCB, the eHf(t) values range from
26.3 to 13.5 and TDM2(Hf) from 2.86 to 2.04 Ga. These large variations are also within one porphyritic body, for instance, granites
from the Jinduicheng body with eHf(t) values from 24.6 to 7.1
and the Niangniangmiao 29.7 to 8.1. But the majority of eHf(t)
values and TDM2(Hf) is from
25 to 10 and 2.6 to 1.6 Ga,
respectively,
In the NQB, the eHf(t) values and TDM2(Hf) of the granitoids also
show a larger range, from 16.2 to +0.1 and 1.96 to 0.96 Ga,
respectively (Fig. 7), except the Taoguanping pluton with lower
eHf(t) values ( 23.2) and older TDM2(Hf) (2.67 Ga) (Fig. 7).
In the SQB, the granitoids have higher eHf(t) values and younger
TDM2(Hf), from 1.1 to 0.3 and 1.25 to 1.22 Ga, respectively, than
these in the southern margin of the NCB and NQB (Fig. 7).
Spatially, similar to the Nd compositions, the eHf(t) values also
increase and TDM2(Hf) decrease from north to south, approximately
corresponding to the southern margin of the NCB, NQB and SQB
(Fig. 7).
Temporally, the variations of Hf isotopic compositions display
the same features as those of the Nd isotope. The first-stage granitoids in the southern margin of the NCB have larger variations in
eHf(t) values than the second one and the first-stage granitoids in
the NQB are lower than the second one (Fig. 10). These also indicate the temporal variations of eHf(t) values related to the terranes.
7. Discussion
7.1. Sources of the granitoids
Sm–Nd and Lu–Hf isotopic characteristics indicate heterogeneous sources for the Late Mesozoic granitoids in the East Qinling
and the granitoids in different terranes have different sources.
The granitoids in the southern margin of the NCB are I-type, I-to
A-type and A-type (Wang et al., 2013; and reference therein). All
the granitoids including from both large batholiths and small porphyritic bodies have the similar whole-rock eNd(t) values ( 22.1 to
10.9) and TDM(Nd) (2.82–1.47 Ga) (Table 1, Fig. 6), indicating their
derivation from partial melting of old crustal components (Fig. 9).
The first- and second-stage granitoids in this terrane also show
similar eNd(t) values, implying the similar sources for them. However, all these granitoids, even from a batholith or a small porphyritic body, show large variations in zircon eHf(t) values ( 30.9 to
6.1) and TDM2(Hf) (3.10–1.47 Ga) (Fig. 7), suggesting multiple
sources for the granitoids. One interpretation for wide ranges in
zircon eHf(t) values, but similar whole-rock Nd isotopes is mixing
or interaction of two distinct magma systems or sources (e.g.,
Cherniak et al., 1995; Kemp et al., 2005; Yang et al., 2007;
Gagnevin et al., 2011). Thus, the sources of the granitoids at least
include two parts, dominant old crust and juvenile component
contribution. The inherited zircon U–Pb ages of the granitoids, such
as monzogranites from the Lantian batholith (2.1–2.3 Ga, Wang
et al., 2011), are similar to the metamorphic ages of the Archaean
Taihua Group (2.2–2.3 Ga, Ni et al., 2003). Consequently, the old
crust components are similar to the Archaean Taihua Group
(Fig. 9; e.g., Wang et al., 1986, 2011, 2013; Guo et al., 2009), and
the juvenile components may come from partial melting of new
growth crust or coeval mantle-derived mafic magmas or subducted
continental crust of the SCB. The occurrence of MMEs in these
176
X. Wang et al. / Journal of Asian Earth Sciences 103 (2015) 169–183
Table 2
New Hf isotopic compositions of the Late Mesozoic granitoids.
Location
Pluton
Rock type
Age
(Ma)
176
Yb/177Hf
176
Lu/177Hf
176
Hf/177Hf
S-NCB
Yongping
Grano-diorite
155
143
155
154
155
154
155
0.052529
0.043957
0.050672
0.054660
0.115273
0.038233
0.104144
0.000755
0.000664
0.000698
0.000811
0.001730
0.000574
0.001639
0.282316
0.282356
0.282215
0.282336
0.282126
0.282165
0.282052
Quli
Granite porphyry
154
150
147
155
148
149
154
152
152
152
152
152
153
152
155
152
0.084437
0.103986
0.137487
0.070302
0.068753
0.078639
0.090710
0.045273
0.099950
0.083324
0.167652
0.112196
0.127272
0.134975
0.120216
0.079630
0.001686
0.001896
0.002940
0.001463
0.001309
0.001511
0.001686
0.000821
0.001812
0.001508
0.003522
0.001853
0.002243
0.002183
0.002252
0.001432
Babaoshan
Granite porphyry
157
156
157
157
154
157
158
158
158
157
157
157
0.153454
0.110540
0.172631
0.177750
0.065567
0.092108
0.142493
0.223505
0.144434
0.171625
0.168086
0.130475
Gelaowan
Granite porphyry
146
143
146
146
146
146
145
146
145
146
148
147
147
147
Houyaoyu
Granite porphyry
Houyaoyu
Shibaogou
eHf (t)
TDM1
(Ga)
TDM2
(Ga)
0.000018
0.000019
0.000019
0.000018
0.000024
0.000018
0.000022
12.8
11.6
16.4
12.1
19.6
18.1
22.3
1.31
1.25
1.45
1.29
1.62
1.51
1.72
2.02
1.94
2.24
1.98
2.45
2.35
2.61
0.282507
0.282453
0.282403
0.282324
0.282511
0.282418
0.282436
0.282485
0.282432
0.282465
0.282355
0.282548
0.282464
0.282446
0.282351
0.282464
0.000019
0.000018
0.000029
0.000025
0.000015
0.000017
0.000017
0.000014
0.000017
0.000018
0.000032
0.000020
0.000019
0.000021
0.000021
0.000016
6.2
8.2
10.1
12.6
6.1
9.4
8.7
6.9
8.9
7.7
11.8
4.8
7.8
8.4
11.7
7.7
1.07
1.16
1.27
1.33
1.06
1.20
1.17
1.08
1.19
1.13
1.36
1.02
1.15
1.18
1.32
1.13
1.59
1.68
1.91
2.01
1.58
1.79
1.79
1.60
1.78
1.61
2.03
1.49
1.70
1.73
1.99
1.75
0.002141
0.001654
0.002479
0.003186
0.001104
0.001890
0.002432
0.004475
0.002459
0.003335
0.003069
0.002360
0.282099
0.282468
0.282010
0.282068
0.282386
0.282392
0.282129
0.282211
0.282093
0.282043
0.282111
0.282103
0.000023
0.000025
0.000030
0.000025
0.000024
0.000024
0.000029
0.000028
0.000022
0.000027
0.000020
0.000016
20.6
7.5
23.8
21.8
10.3
10.2
19.5
16.8
20.8
22.7
20.2
20.5
1.67
1.13
1.82
1.77
1.23
1.25
1.64
1.62
1.70
1.81
1.70
1.68
2.51
1.68
2.71
2.58
1.86
1.85
2.44
2.27
2.52
2.64
2.49
2.50
0.099425
0.065762
0.083724
0.062158
0.093520
0.053514
0.061823
0.053511
0.054669
0.044978
0.070171
0.161588
0.059056
0.075310
0.002299
0.001063
0.001277
0.001094
0.002113
0.001082
0.001550
0.001136
0.001235
0.001001
0.001608
0.003151
0.001136
0.001321
0.282253
0.282282
0.282276
0.282318
0.282159
0.282256
0.282225
0.282284
0.282318
0.282181
0.282342
0.282411
0.282308
0.282276
0.000021
0.000018
0.000022
0.000020
0.000030
0.000018
0.000023
0.000020
0.000020
0.000023
0.000018
0.000033
0.000017
0.000021
15.4
14.3
14.4
13.0
18.7
15.1
16.3
14.2
13.0
17.8
12.1
9.9
13.3
14.4
1.46
1.37
1.39
1.32
1.59
1.41
1.47
1.37
1.33
1.51
1.31
1.26
1.34
1.39
2.17
2.10
2.11
2.02
2.38
2.16
2.23
2.10
2.02
2.33
2.97
1.82
2.04
2.11
129
131
137
134
0.066520
0.094632
0.032843
0.035777
0.001455
0.001782
0.000619
0.000614
0.282226
0.281990
0.281912
0.282276
0.000023
0.000028
0.000021
0.000018
16.6
24.9
27.5
14.6
1.46
1.81
1.86
1.36
2.24
2.76
2.93
2.12
Granite porphyry
137
136
137
141
137
137
137
137
137
137
0.025744
0.061924
0.033503
0.182838
0.075606
0.058318
0.076707
0.154578
0.042159
0.081976
0.000441
0.000982
0.000497
0.003058
0.001451
0.000987
0.001518
0.002324
0.000629
0.001229
0.282439
0.282239
0.282143
0.282042
0.282005
0.282384
0.281838
0.282002
0.282232
0.282566
0.000021
0.000026
0.000019
0.000023
0.000020
0.000026
0.000019
0.000027
0.000020
0.000016
8.8
16.0
19.3
23.0
24.3
10.8
30.2
24.4
16.1
4.4
1.13
1.43
1.54
1.80
1.78
1.23
2.01
1.82
1.42
0.98
1.75
2.20
2.41
2.65
2.72
2.88
3.09
2.73
2.22
1.47
Monzo-granite porphyry
151
156
156
156
156
156
157
0.032921
0.028786
0.044238
0.040254
0.047748
0.033855
0.037931
0.001124
0.000952
0.001426
0.001342
0.001438
0.001113
0.001237
0.282280
0.282241
0.282295
0.282228
0.282286
0.282256
0.282276
0.000011
0.000009
0.000009
0.000008
0.000011
0.000011
0.000011
14.2
15.5
13.6
15.9
13.9
15.0
14.2
1.38
1.43
1.37
1.46
1.38
1.41
1.39
2.10
2.19
2.07
2.22
2.09
2.15
2.11
2r
177
X. Wang et al. / Journal of Asian Earth Sciences 103 (2015) 169–183
Table 2 (continued)
Location
Pluton
Daping
Rock type
Granite porphyry
Age
(Ma)
176
Yb/177Hf
176
Lu/177Hf
176
Hf/177Hf
157
155
150
156
156
156
155
157
156
153
156
156
0.031981
0.023638
0.024599
0.044911
0.041059
0.035012
0.089929
0.046070
0.024879
0.053709
0.029038
0.057086
0.001010
0.000756
0.000623
0.001629
0.001357
0.001056
0.003317
0.001668
0.000816
0.002110
0.001020
0.002439
0.282283
0.282163
0.282446
0.282271
0.282274
0.282298
0.282249
0.282219
0.282038
0.282243
0.282273
0.282302
145
145
145
142
145
145
145
145
144
145
153
145
153
145
144
144
144
0.026909
0.029755
0.039980
0.049936
0.016131
0.033249
0.031661
0.035571
0.030468
0.057443
0.057400
0.041001
0.042494
0.052127
0.043570
0.043344
0.052430
0.000998
0.001080
0.001412
0.001638
0.000466
0.001359
0.001131
0.001189
0.001071
0.001872
0.002148
0.001219
0.001712
0.001649
0.001585
0.001438
0.002101
0.282331
0.282350
0.282351
0.282302
0.282182
0.282311
0.282316
0.282271
0.282348
0.282332
0.282371
0.282429
0.282365
0.282378
0.282331
0.282347
0.282366
eHf (t)
TDM1
(Ga)
TDM2
(Ga)
0.000012
0.000010
0.000011
0.000009
0.000009
0.000015
0.000020
0.000010
0.000017
0.000018
0.000008
0.000021
14.0
18.2
8.3
14.5
14.3
13.4
15.5
16.3
22.6
15.6
14.3
13.5
1.37
1.53
1.13
1.41
1.39
1.35
1.51
1.48
1.70
1.47
1.38
1.39
2.09
2.36
1.73
2.12
2.11
2.06
2.18
2.24
2.64
2.19
2.11
2.06
0.000011
0.000011
0.000010
0.000010
0.000009
0.000018
0.000010
0.000010
0.000011
0.000010
0.000016
0.000012
0.000017
0.000012
0.000013
0.000012
0.000016
12.5
11.9
11.8
13.7
17.7
13.2
13.0
14.7
11.9
12.7
11.1
9.1
11.2
10.9
12.6
12.0
11.4
1.30
1.28
1.29
1.36
1.49
1.34
1.33
1.39
1.28
1.33
1.28
1.17
1.28
1.26
1.32
1.29
1.29
1.99
1.93
1.94
2.11
2.27
2.05
2.02
2.13
1.92
1.98
1.95
1.75
1.92
1.89
2.00
1.93
2.01
2r
eHf(t) = {[(176Hf/177Hf)S–(176Lu/177Hf)S (ekt–1)]/[(176Hf/177Hf)CHUR,0 (176Lu/177Hf)CHUR (ekt 1)] 1}10,000
TDM = 1/k ln{1 + [(176Hf/177Hf)S–(176Hf/177Hf)DM]/
[(176Lu/177Hf)S (176Lu/177Hf)DM]}
TDMC = 1/k ln{1 + [(176Hf/177Hf)S,t (176Hf/177Hf)DM,t]/[(176Lu/177Hf)C (176Lu/177Hf)DM]} + t,
where,
s = sample,
(176Hf/177Hf)CHUR,0 = 0.282772, (176Lu/177Hf)CHUR = 0.0332, (176Hf/177Hf)DM = 0.28325, (176Lu/177Hf)DM = 0.0384 (Blichert-Toft and Albarede, 1997: Griffin et al. 2000).
11
1
176
177
t = crystallization age of zircon. k = 1.867 10
a (Soderlund et al. 2004). ( Lu/ Hf)C = 0.015. S-NCB: Southern margin of the North China Block.
Note: If readers want to reference the original published Hf data please consult the relative reference or contact with the corresponding author of this paper.
granitoids indicates that mixing/mingling has happened in these
intrusions (see Baxter and Feely, 2002; Rajaieh et al., 2010). Therefore, the sources of these granitoids are more reasonable old crust
and coeval mantle-derived magma contribution instead of the
older crust only (e.g., Chen et al., 2000) or subducted continental
crust of the SCB (Bao et al., 2009, 2014; Li et al., 2012d).
The granitoids in the NQB are I-type, I-to A-type (Wang et al.,
2013; and reference therein) and have higher whole-rock eNd(t)
values ( 13.9 to 1.5) and younger TDM(Nd) (2.02–0.79 Ga) than
those in the southern margin of the NCB. These suggest that they
were derived from slightly younger (juvenile) crust components
than the granitoids in the southern margin of the NCB. The eNd(t)
Fig. 6. Nd isotope map (whole-rock eNd(t) values and TDM(Nd)) for Late Mesozoic granitoids in the East Qinling. Date references see Table 1.
178
X. Wang et al. / Journal of Asian Earth Sciences 103 (2015) 169–183
Fig. 7. Hf isotope map (zircon eHf(t) values and TDM2(Hf)) for the Late Mesozoic granitoids in the East Qinling. eHf(t) value and TDM2(Hf) from Table 2 and after (1) – Guo et al.
(2009); (2) – Qi et al. (2012); (3) – Wang et al. (2011); (4) – Li et al. (2012e); (5) – Zhao et al. (2011); (6) – Ke et al. (2013); (7) – Yang et al. (2012); (8) – Yang (2014); (9) – Ke
et al. (2013); (10) – Ke et al. (2012); (11) – Gao et al. (2012); (12) – Meng (2010); (13) – Dai et al. (2009); (14) – Ke et al. (2014); (15) – Wu et al. (2014); and (16) – Nie et al.
(2014).
values and TDM(Nd) for the first-stage are from 13.9 to 7.6 and
2.02 to 1.35 Ga and second-stage 7.1 to 1.5 and 1.60–0.79 Ga
(Table 1, Figs. 6 and 7), respectively, implying more juvenile
sources for the second-stage granitoids.
The zircon eHf(t) values and TDM2(Hf) for the granitoids in the
NQB show large variations, even within one intrusion such as
granitoids from the Nantai body with eHf(t) = 28.8 to 7.9 and
TDM2(Hf) = 2.65–1.5 Ga, also indicating multiple sources of old crust
and juvenile components. The crust sources for the granitoids of
the second-stage are more juvenile than the first-stage, as suggested by higher eHf(t) values for second-stage granitoids. It
implies that the crust of the NQB is more complex, which is
consistent with the results by zircon U–Pb ages of the Qinling
Group (Yang et al., 2010) and detrital zircon U–Pb ages and Hf isotopic compositions of the NQB (Zhu et al., 2011). The old crust
component for the first-stage granitoid source is similar to the Qinling Group (Complex) (Fig. 9) and for the second-stage is younger
than this group. The juvenile component is also coeval mantlederived magmas supported by the occurrence of MMEs in these
granitoid intrusions.
The granitoids in the SQB are mainly I-type (Xie et al., 2012; Wu
et al., 2014) and have small range in isotopic compositions, wholerock eNd(t) = 8.1 to 4.5, TDM(Nd) = 1.28–1.12 Ga (Table 1, Fig. 6)
and zircon eHf(t) = 1.0 to 0.3, TDM2(Hf) = 1.25–1.22 Ga (Fig. 7).
The slightly negative eNd(t) and eHf(t) values of the granitoids suggest that their source is more juvenile than these in the southern
margin of the NCB and NQB. The juvenile components could be
mantle-derived component supported by strong mantle-derived
Neoproterozoic magmatism in the SQB (Xia et al., 2008; Zhu
et al., 2014) and the occurrence of MMEs in the granitoids (see
Wu et al., 2014).
The above whole-rock eNd(t) and zircon eHf(t) values of the
granitoids increase and whole-rock TDM(Nd) and zircon TDM2(Hf)
decrease from the north of the southern margin of the NCB to
the SQB (Fig. 8), indicating the sources becoming younger in this
direction. This scenario can be interpreted by more mantle-derived
magmas southward in the granitoids or more juvenile crust component southward or both. The petrography and geochemistry,
such as the amount of MMEs, Mg# and content of compatible elements of the granitoids, show no obvious change southward. Thus,
the first possibility can be excluded and the second one is more
possible. Additionally, although the granitoid intrusions display
Fig. 8. Nd isotopic section from the southern margin of the NCB to SQB. The grey
arrow in Fig. 2 showed the location of the section.
X. Wang et al. / Journal of Asian Earth Sciences 103 (2015) 169–183
Fig. 9. eNd(t) value vs. age diagram for the granitoids (date from Table 1).
magma mixing/mingling the lower zircon eHf(t) values and older
TDM2(Hf) can represent the nature of the old component. These
lower zircon eHf(t) values of the granitoids increase and older
TDM2(Hf) decrease from the southern margin of the NCB to SQB
(Fig. 10). Accordingly, this suggests that the crust component
become juvenile southward.
The isotopic tracer reveals that the sources of the Late Mesozoic
granitoids in the East Qinling are closely related to the nature of
the terranes into which they intruded and their source components
become more juvenile from north to south (the southern margin of
the NCB to SQB), even in the same terrane (Figs. 6–9).
7.2. Nature of basements in the East Qinling
The Sm–Nd and Lu–Hf isotope tracer technique has played an
important role in studying basement nature and crustal growth
in Precambrian terranes (e.g., Milisenda et al., 1988; Chen and
Jahn, 1998; DePaolo et al., 1991; Dickin and McNutt, 1989, 2003;
Sanislava et al., 2014), and distinguishing different terranes within
a orogen (e.g., Thorogood, 1990; Kovalenko et al., 1996, 2004;
Dickin and McNut, 2003; Wang et al., 2009b; Guo et al., 2010).
Here, we use Nd–Hf isotope characteristics to approach the basement nature of the East Qinling.
7.2.1. Basement characteristics of the different terranes
The present isotopic mapping shows that granitoids in the
southern margin of the NCB have old model ages, TDM(Nd) = 2.82–
179
1.47 Ga and TDM2(Hf) = 2.86–2.04 Ga. These suggest an old basement, which is similar to the ages of Precambrian metamorphic
rocks in this region. The Archaean Taihua Group with ages from
2.8 to 2.5 Ga is considered to be the basement of the southern margin of the NCB (Kröner et al., 1993; Xue et al., 1995; Zhou et al.,
1998; Diwu et al., 2010) and its Proterozoic overlying volcanic
rocks with ages of 1.95–1.75 Ga (Zhao et al., 2001). Consequently,
considering probable magmatic mixing, the age of the basement
may be slightly older than the model ages.
The granitoids in the NQB have TDM(Nd) and TDM2(Hf) from 2.02 to
0.79 Ga and 1.96 to 0.96 Ga, respectively. The granitoids in the
eastern part of this terrane have younger model ages (Figs. 6 and
7). The majority model ages are similar to the main ages of the Qinling Complex (2.27–1.1 Ga, see Zhang et al., 1996a, 2001, 2006), the
basement in this terrane. Therefore, these model ages suggest that
the major basement of this region could be Paleoproterozoic to
Mesoproterozoic. The older model ages of the granitoids in the
western party of this terrane may reveal that the basement could
involve some older components.
The TDM(Nd) and TDM2(Hf) for the granitoids in the SQB have a
small range, from 1.28 to 1.12 Ga and 1.25 to 1.22 Ga, respectively,
indicating Mesoproterozoic to Neoproterozoic basement in this
terrane. These model ages are probably close to the ages of main
Precambrian metamorphic rocks in the SQB, such as the Wudang
Group (1.92 Ga, 1.17–0.87 Ga; Zhang et al., 2002) and the Yaolinhe
Group (0.92–0.70 Ga; Xia et al., 2008; Zhu et al., 2014).
It should be mentioned that there are generally large error in Nd
and Hf model ages, and probable magmatic mixing/mingling and
crustal contamination could make model ages younger. Thus, here
the model ages are only used approximately to trace the nature of
the basement. On the other hand, the old components shown by
zircon Hf isotope are more close to the nature of the basement.
Anyway, the above available Nd–Hf isotopes indicate that: (1) different terranes in the East Qinling have different basements; (2)
their major basements are older than Mesoproterozoic, confirming
that continental growth mainly occurred during the Proterozoic
and there was insignificant Phanerozoic crustal growth in the East
Qinling; and (3) the Qinling orogen is a typical one of continental
(or arcs) collision orogens, rather than a typical accretion orogen,
such as Central Asian Orogenic Belt that has voluminous granitoids
with positive eNd(t) values and younger TDM(Nd) (Jahn et al., 2000a,
2000b; Wang et al., 2009b).
7.2.2. Constraint on attribution of the NQB
It is still controversial for the attribution of the NQB, i.e., it was
derived from the NCB (e.g., Zhang et al., 2001, 2006), or from the
SCB (e.g., Yang et al., 2010; Zhu et al., 2011), or an independent terrane (Zhang et al., 1996b). Our present isotopic mapping shows
that granitoids in the NQB have distinct Nd–Hf isotopic signatures
different from these in the southern margin of the NCB and the
SQB. Consequently, these suggest that the NQB could not be affinity with the SQB. Although the granitoids in the NQB and the
southern margin of the NCB have similar trend in eNd(t) values
and TDM(Nd) variations, eNd(t) values of the granitoids in the NQB
are obvious higher and TDM(Nd) younger, suggesting that the two
terranes are not the same. It is consistent with detrital zircon U–
Pb ages and Hf isotopic composition of the NQB (Zhu et al.,
2011). Therefore, the isotopic mapping suggests that the NQB not
only belong previously to the NCB, but also not to the SCB, and it
may be an independent terrane.
7.3. Correlations of Nd–Hf isotopic variations with Mo mineralization
Fig. 10. eHd(t) value vs. age diagram for the granitoids (data references as Fig. 7).
Mo mineralization is closely related to the Late Mesozoic granitoids in the East Qinling orogen. Re–Os dating indicates two-stage
Mo mineralization, 155–125 Ma and 125–105 Ma (Fig. 3b), coev-
180
X. Wang et al. / Journal of Asian Earth Sciences 103 (2015) 169–183
Fig. 11. Basements of the different terranes in Late Mesozoic and their hosted Mo deposits.
ally with the two-stage granitoids, 155–130 Ma and 120–105 Ma
(Fig. 3a), respectively. The locations of the Mo deposits are consistent with small granitoid porphyritic bodies, especially the bodies
closed to the large batholiths. Similar to the other granitoids, the
Mo-bearing granites also display different isotopic composition
in different terranes. In the southern margin of the NCB, where
the majority of the Mo deposits hosted, Mo-bearing granitoids
show eNd(t) values of 22.4 to 10.9 and TDM(Nd) of 2.51–1.48 Ga,
in the NQB eNd(t) of 13.9 to 10.2 and TDM(Nd) of 2.02–1.38 Ga,
and in the SQB eNd(t) of
6.30 to
4.50 and TDM(Nd) of
1.32–1.12 Ga. These characteristics are also documented by Hf
isotope compositions.
In the southern margin of the NCB, eHf(t) values and TDM2(Hf) for
the Mo-bearing bodies are 26.3 to 14.9 and 2.86–1.7 Ga, respectively. In the NQB eHf(t) values are 23.2 to +0.1 and TDM2(Hf)
2.67–0.96 Ga. While in the SQB eHf(t) values are from 1.0 to
0.3 and TDM2(Hf) 1.25–1.22 Ga.
It seems that the Mo-bearing granitoids have larger variation in
isotopic compositions than those of Mo-barren ones, such as the
Mo-bearing granitoid bodies (Jinduicheng, Shijiawan, Baliponear,
Taoguanping, Xigou, Nantai and Yingchenggou) near the Mo-barren Laoniushan and Mangling batholiths (Figs. 6 and 7).
The scale and number of Mo deposits have positive correlation
with whole-rock TDM(Nd) and zircon TDM2(Hf) (Fig. 11), suggesting
that the sources of the granitoids and basement features of the
terranes are responsible for Mo mineralization and Mo deposits.
The terrane with very old basement is propitious to the development of large and numerous Mo deposits, such as the southern
margin of the NCB, while the terrane with juvenile basement hosts
less and small Mo deposits, accompanied by Cu, and Fe mineralization, for instance the NQB and SQB (Fig. 11). Therefore, the terrane
which is more favorable for the formation of Mo deposits is the
southern margin of the NCB rather than the NQB and SQB. This
study also provides evidence for old continental sources constraint
on Mo deposits.
8. Conclusions
(1) The Nd–Hf isotopic compositions of the Late Mesozoic granitoids in the East Qinling shows large variations from north to
south: (a) lowest e(t) values (eNd(t) = 22.1 to
10.9;
eHf(t) = 26.3 to
13.5) with oldest model ages (TDM(Nd) =
2.82–1.47 Ga; TDM2(Hf) = 2.86–2.04 Ga); (b) lower e(t) values
(eNd(t) = 13.9 to 1.5; eHf(t) = 16.2 to +0.1) with older
model
ages
(TDM(Nd) = 2.02–0.79 Ga,
TDM2(Hf) = 1.96–
0.96 Ga); and (c) slightly higher e(t) values (eNd(t) = 6.3 to
4.5; eHf(t) = 1.0 to 0.3) with slightly younger model ages
(TDM(Nd) = 1.28–1.12 Ga; TDM2(Hf) = 1.25–1.22 Ga), approximately corresponding to the southern margin of the NCB,
NQB and SQB, respectively.
(2) All the granitoids in different terranes were mainly derived
by partial melting of old crust with some juvenile component contribution. But the granitoids in different terranes
have different old crust component. Their source components become juvenile from the north of the southern margin of the NCB to NQB and SQB. The southern margin of the
NCB has an oldest basement, the SQB a slightly younger, and
the NQB a complex basement. It may imply that the three
terranes could experience different geological processes.
(3) The distribution, scale and number of Mo deposits in the
East Qinling are obviously restricted by the granitoid sources
and basements of the terranes. The southern margin of the
NCB with the oldest basement is favorable for Mo mineralization and hosts large scale and numerous Mo deposits.
Acknowledgements
This work is supported by the China Geological Survey (Nos.
1212010012012 and 1212010811033), Geological Commonweal
Program (No. 200911007-9) and the National Natural Science
Foundation of China (NSFC Grants 41172062 and 40872054).
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